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Al H THE

QUARTERLY JOURNAL

GEOLOGICAL SOCIETY OF LONDON.

EDITED BY

THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.

VOLUME THE TWELFTH.

1856.

PART THE FIRST.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

LONDON: pails
LONGMAN, BROWN, 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.

MDCCCLVI.

List

OF THE

OFFICERS

OF THE

GEOLOGICAL SOCIETY OF LONDON.

Elected February and June 1856.

PresiVent.
Col. Portlock, R.E., F.R.S.

Gice-PrestVents.

Sir P. De M. G. Egerton, Bart., M.P., F.R.S.
R. A. Godwin-Austen, Esq., B.A., F.R.S.
Sir Charles Lyell, F.R.S. and L.S.

Secretaries.

Robert W. Mylne, Esq.
Warington W. Smyth, Esq., M.A.

Foreign Secretary.
Samuel Peace Pratt, Esq., F.R.S. and L.S.

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

COUNGCIL.
Prof. Thomas Bell, F.R.S. and L.S. John Morris, Esq.
Col. P. T. Cautley, K.C.B., F.R.S. and L.S.| Sir R. I. Murchison, G.C.St.S., F.R.S. &
Earl of Ducie. L.S.
Sir P. De M. G. Egerton, Bart., M.P., F.R.S.| R. W. Mylne, Esq.
H. Falconer, M.D., F.R.S. S. R. Pattison, Esq.

Thomas F. Gibson, Esq.

Prof. John Phillips, F.R.S.

R. A. Godwin-Austen, Esq., B.A., F.R.S. Col. Portlock, R.E., F.R.S.

William John Hamilton, Esq., F.R.S. Joseph Prestwich, Esq., F.R.S.
William Hopkins, Esq., M.A., F.R.S. Samuel Peace Pratt, Esq., F.R.S. & L.S.
Leonard Horner, Esq., F.R.S.L. & E. Prof. A. C. Ramsay, F.R.S.

Sir Charles Lyell, F.R.S

John C. Moore, Esq., M.A.

Gy say) BESS Warington W. Smyth, Esq., M.A.

Henry Clifton Sorby, Esq.

Assistant-Decretary, Curator, and Librarian.

T. Rupert Jones, Esq.

TABLE OF CONTENTS.

PART I.—ORIGINAL COMMUNICATIONS.

Page
ANSTED, Prof. D.T. Description of remarkable Mineral Veins: The
Copper Lodeiof Santiago de Cuba i720 o.22 220408. Wr. a. 144

BABBAGE, C., Esq. On the Action of Ocean-Currents in the forma-
tion of the Strata of the Earth. [Abstract.] ...............- 366

Banks, R.W., Esq. On the Tilestones, or Downton Sandstones, in
the neighbourhood of Kington, and their Contents. (With a
aE ALE) OOTY. PPOs LEIS A RIMES axe heidi sept theyecrenwtes

Beck Es, 8. H., Esq. On the Lowest Strata of the Cliffs at Hastings. 288
Breprorp, E. J., Commander R.N. Notice of some Raised Beaches

HUME NEOUS ULC eee fe oe ere t tee we Ace Aetee oan wee od 167
BInNEY, E.W., Esq. On the Permian Character of some of the

Red Sandstones and Breceias of the South of Scotland ........ 138
——. On some Footmarks in the Millstone Grit of Tintwistle,

COL ESIETIS. GG Pe CIS Ot Cesc RESET 7 Ey ae oa 350
Bout, M. Ami. On the Probable Origin of the English Channel by

imennstotarlissure.. .\Albstract.|psitaseciele astro J» sects} esol» 325

Bowen, H. G., Esq. On the Geology of Trinidad. [Abstract.] .. 389
Bunsury, C. J. F., Esq. Notice of some Appearances observed on

draining a Mere near Wretham Hall, Norfolk................ 355
CHARTERS, Major S. Ona Section near Mont Blanc............ 385
CosBo.Lp, Rev. R. H. On the Occurrence of Coal near the City of

OETUTHIN CITT AM Borg Go e, REO Geet Oey Aes Bs ocean ae a 358
Croker, Dr. J. G. On the Lignite-Deposits of Bovey Tracey,

Weyonsiire: | | Abstracts] 1.2, -,.22)-,0ye01-,s.<.0,000(0,5 sie Sincindh oaeeiele 354
DEGOUSEE and LAuRENT, MM. On the Valenciennes Coal-Basin.

AONE ok cramer yee wc cre atta te cn on be getce she agoryec oy whch Sle. Siemon Bienen 252

Dennis, Rev. J. B. P. On some Organic Remains from the Bone-
bed at the base of the Lias at Lyme Regis. [Abstract.] ...... 252

1V TABLE OF CONTENTS.

Page
Dick, A., Esq. Analysis of the Cleveland Iron-Ore from Eston .. 357

Gopwin-AusTEN, R., Esq. On the Newer Tertiary Deposits of the

Bresex Const: (Abstracte).. 6.05 00:.0 odie bile omen 4
——. On the Possible Extension of the Coal-Measures beneath the

South-Eastern part of England. (With a Plate.) ........ 38, 46*
HARKNESS, Prof. R. On the Lowest Sedimentary Rocks of the

OUCH OL SeOtlAMG: «occas cae. + sicle wleiena wale ole is.0 eae opeieiaesl se 238
——. On the Sandstones and Breccias of the South of Scotland of

an Age subsequent to the Carboniferous Period.............. 254
HavucutTon, Rev. Prof. SamurL. Experimental Researches on the

Graumites of Ireland.» 0). 2.70.6 «0 acto cone ale ol apne ere ee 171
Huxtey, Prof. T. H. On the Structure and Affinities of Himan-

RO PECIWS os os 6 a's « eyeisnrd waelejaia es wiebee St sree eines ee 34
Ippetson, L. L. B., Esq. On the Possible Origin of Veins of Gold

in Quartz and other Rocks. { Abstract.|.......:..:-....eeen 384
Martin, P. J., Esq. . On some Geological Features of the Country

between the South Downs and the Sussex Coast ............ 134
Miter, W., Esq. Notice of the recent Eruption of Mauna Loa in

Hawaii, Sandwich Islands. [Abstract.]...............-..-6 IZ]
-—. Further Notice of the Recent Eruption from the Volcano of

Mauna Loa in Hawaii (Owhyhee). [Abstract.].............- 386
MocertipeGs, M., Esq. On the Section exposed in the Excavation

of the Swansea Doelss sis pac ed: 5.5 Gi sl “laid ooh as pole cd 169
Moors, J. C., Esq. On the Silurian Rocks of Wigtownshire. ..... 359

Murcuison, Sir Ropericx I. On the Discovery by Mr. Robert
Shimon of Fossils in the Uppermost Silurian Rocks near Lesma-
hago in Scotland, with Observations on the Relations of the Pa- -
leozoic Strata in that part of Lanarkshire .................. 15

Owen, Prof. R. Description of a Fossil Cranium of the Musk-Buf-
falo [Bubalus moschatus, Owen; Bos moschatus (Zimm. and
Gmel.), Pallas; Bos Pailasii, De Kay; Ovibos Pallasu, H. Smith
and Bl.| from the Lower-Level Drift at Maidenhead, Berkshire.
(Watt! Mioures.) 2s) aac Oo. vd? oe peo eS aoe 124

——. On the Affinities of the large Extinct Bird (Gastornis Parisi-
ensis, Hébert), indicated by a Fossil Femur and Tibia discovered
in the Lowest Eocene Formation near Paris. (With a Plate.).. 204

——. Description of some Mammalian Fossils from the Red Crag

on Suitolk.. (Wath, Higures.).... 0%. jj 26 smb safe ole 0 )s cre pl
Pant, JAMES, Esq. Onthe Upper Keuper Sandstone (included in
the New Red Marls) and its Fossils at Leicester.............. 369

Poots, H., Esq. Notice of a Visit to the Dead Sea. [Abstract.].. 203
——, On the Coal of the North-Western Districts of Asia Minor.. ]
PrestwicH, J., Esq. On the Boring through the Chalk at Kentish
Powra; LOmie se’ e's terorn ioc tom ters nee a ees Cv wea nes oe ale ee
——. Note on the Gravel near Maidenhead, in which the Skull of
the: Mrusk-~ Biritalo: Was fOUMNGs.: bse vce vc eevee ed ele Selene 131
——. Onthe Correlation of the Middle Eocene Tertiaries of England,
France, and Belgium. [Abstract.] ........ 60s se ee eee e eens 390

TABLE OF CONTENTS. Vv

Page
RusipGE, Dr. R.N. Notes on the Geology of some parts of South
iiniedy Abstract, lacey ere ictens\ elope loycte seid apes cove 2a cles sein se 237

SALTER, J. W., Esq. On some new Crustacea from the Uppermost
Silurian Rocks. With a Note on the Structure and Affinities of
imantopterus, by UT. He Huxumy, Wsq. ..0.252. 6.60.8. 2. 26

——. On Fossil Remains in the Cambrian Rocks of the Longmynd
and: Northo Wales: . (With a: Plates )acitajee. << ote etter tls o's ao 246

——. Ona New Genus of Cephalopoda, Diploceras (Orthoceras bi-
siphonatum of Sowerby) ; and on the Occurrence of Ascoceras in

Esnibatiaes) (Abstracha| . 2. datremerrere 6 +0 vied 4 sic ela vnie'e ae OO
—. On the Fossils found in the Chalk-Flints and Greensand of
mibertecnshire. = | Alostract. | afte Bae oc 0 «!c)aj eel aie ole opr lae 06.06 390
SAWKINS, JAMES Gay, Esq. On the Movement of Land in the
SMM Sea tSIARGS 4 cade tateeye le, «sialoieueTeleyspesavers elec a0 383
Scrops, G. PouLett, Esq. On the Formation of iGsakers, and the
Nature of the: Liquidity of Mavas’.... 73% (sec selene oo 0s <0 0 oie 326

SHARPE, DANIEL, Esq. On the Last Elevation of the Alps; with
Notices of the Heights at which the Sea has left Traces of its

PAG HOLY OME ACMA SIGS esi 555 5 «9:5 12 “Laie ay y's Seaphf + hy! Megan ghee 9 0 8-e) won ee 102
Sorsy, H.C., Esq. On the Physical Geography of the Tertiary

Estuary of the Isle of NWitomtte me PADSUEREL S| (A cet tee epee cele gies 137
Spratt, T., Capt. R.N. On the Geology of Varna and its Vicinity,

and of other parts of Bulearia, “ [ Abstract. |. j.i04 oi) once es 387
Symonps, Rev. W.S. On Trap-dykes intersecting Syenite in the

Malvern. Fills... Woreestershire ....,.. <0 +s secomacceebece sels 382

TAYLER, J. W., Esq. On the Cryolite of Evigtok, Greenland .... 140
Witson, J. 8., Esq. Notes on the Geology of the Neighbourhood

of Sydney, Newcastle, and Brisbane, Australia ............6% 283
Woopward, S. P., Esq. On an Orthoceras from China. (With a
Plate.) Pence tere cet e rene t eee n eee te cere ee tnne ee terete 378

Wrieut, Dr. THomas. On the Paleontological and Stratigraphical
Relations of the so-called “ Sands of the Inferior Oolite” .... 292

PauMMaWepOTt. = cscs scans ea eee esse eee ence a betes ee re i
Anniversary Address ......0.00 esse cece cece crt e cere rece teeees XXV1

Donations'to the Library -. 2... 2. <5 2.6.2.0 pages 74, 154, 268, 293

ERRATA.

Part I. p. vi, line 6 from bottom, for L. L. Dillwyn read L. W. Dillwyn.

Ixx., line 9 from top, for o Alet read d’Alet.

239, in description of woodcut, read 6. Anthracite-schist (*), and grey
and purple, &c.

243, line 10 from bottom, for ¢ read 3.

244, line 7 from top and the following lines, read In the lower or first
group there are six pairs of large imprints, gradually coming
nearer to the central line, and somewhat closer also to each
other, as far as c, which may have been a point of rest, and is
nearer to the groove than any of the others.

244, add to the note after central line; the wider track would then
indicate a relaxation, and not an increase, of effort.

247, line 8 from bottom, read Church Stretton; and W. of.

254, line 16 from top, for Marguise read Marquise.

Part II. p.14, lines 5, 16, and 20 from bottom, for pianzite read piauzite.
15, line 22 from top, for phodadiformis read pholadiformis.
20, line 13 from bottom, for Sau-alps read Sau-alp.

Directions to the Binder.

The Binder is directed to place opposite page 46 the page numbered 46*; and
at page 350 the loose slip relating to Prof. Naumann’s paper on gneiss, &c.

a

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.

RippLeE-MARKS.

Ripple-Marks. Pl. iv. f. 5 & 6, and| Cambrian...... Longmynd......... 250
Woodcut, p. 251.
Marks of al Ee eas: La soo. -=| CAMMOTIAN . 1350 Longmynd......... 250
PLANTA.
Chondrites, Sp. ....ssceeees spaitnebawscnaes | Cambrian ... | Bangor............ | 246
ANNELIDES.
Annelide Tubes. Pl. iv. f.2 ......... Cambrian ...... Longmynd ......... 249
Arenicola didyma. Pl. iv. f. 1......006 Cambrian ......| Longmynd ......... 248
Crustacea. (12.)
Ceratiocaris. Woodcut, f. 8, p. 33...| } Lanarkshire ...... 33
Eurypterus pygmeus. P\.ii.f.4...... = LAGS eee 99
Himantopterus acuminatus. Wood- 3 Lanarkshire ...... 29
cut, f. 4, p. 28. ®
Banksii. Pl. ii. £.5 & 6 wc... B Kington. 32
bilobus. Woodcut, f.1, p.28...| > a Lanarkshire ...... 30
lanceolatus. Woodcut, f. 5, p.28 D Lanarkshire ...... 32
—— maximus. Woodcut, f. 3, p. 28 = Lanarkshire ...... 29
perornatus. Woodcut, f. 6, p. 28 a Lanarkshire ...... 31
Piteraspis Banksii. Pl. ii. £. 2.000... e IM e tO 25 < .ecisecsee 100
trumeatus. PVs £1 cc. .c0sss0c3 Deg Kine honilinieey seca, 100
Paleopyge Ramsayi. Pl.iv. f.3...... Cambrian ...... Longmynd......... 249
Protichnites Scoticus. Woodcut. ...| Cambrian? ...| Binks ....... “Sanne 243
Motuusca. (11.)
(Lamellibranchiata.)
Cardin FUME «, 0.000500 paeeieteeaa cies Upper Lias ...| Frocester............ 324
GAPEN Tit nerioncocaeanhepse’vcctesisa5 Upper Lias ...| Nailsworth.........| 325
Cypricardia brevis ....c1...sssceceeeess Upper Lias ...| Gloucestershire & | 324
Dorsetshire.
OEE COVDIALUS jonas ss(evcsiasiiseetnl votes’ Upper Lias ...| Frocester............ 324
Trigonia Ramsayii, Wright .....:.....- Upper Lias ...| Frocester............ 323
( Cephalopoda.)
Actinoceras Lyonii. Pl. vi. f.3 ......| Black River | New York State...| 379
Limestone.
Ammonites Dorsetensis, Wright ......| Upper Lias ...| Somersetshire and| 321
Dorsetshire.
Orthoceras conicum? PI. vi. f.2 ...| Silurian? ...... fh SPB cenone cciashoc. 381
—— striatum. Pl. vi. f. 4 ............ Carboniferous | Ireland ..... Reb eos 379
Limestone.
trigonalessy Elvis f. Decrees: Devonian ...... Gerolstein ......... 380

atm mea | sp. Pl. Vie fe Dea eee soes Devonian ? eee China @0eFSoeetesecon 378

Name of Species. | Formation. | Locality.

Vill

REPTILE.
Chelichnus ingens ..... ARC eee | Millstone-grit. | Tintwistle.........
Aves. (5).
mptorms. Plat. 1) occas. Danae Pleistocene ...| New Zealand......
Cygnus ferus. Pl. iii. f. 13 ........0005 Pliocene ...... Grays, Essex .......
Dinornis casuarinus. PI, iii. f. 2......| Pleistocene ...| New Zealand......
Gastornis Parisiensis. Pl. iii. f.] ...| Eocene......... Near Paris, 2...
Pleistocene ...}| New Zealand ......

Mortars, Plo £..10..ncccaseonsmeees

MamMALIA. (15.)

Bubalus moschatus. Woodcuts, p. 127.

Canis, sp. Woodcut, f. 21, p. 235...

—,sp. Woodcut, f. 22, p. 236 ...

Carnivore allied to Hyznodon and
Pterodon. Woodcut, f. 20, p. 235.

Cervus dicranocerus. Woodcuts, f. 14,
p. 234.

— —? Woodcut, f. 15, p. 234.

— —. Woodcut, f. 16, p. 234.

? Woodcuts, f.17, p. 235.

Equus (Hipparion?), sp. Woodcuts,
f Wups2o0.

— plicidens? Woodcut, f. 12,
p- 233.

Felis pardoides. Woodcut, f. 19,
p- 235.

Megaceros Hibernicus. Woodcut,f. 18,
p- 235.

Phocena, sp. Woodcut, f. 23, p. 236.

Rhinoceros Schleiermacheri? Wood-
cuts, f. 1-7, p. 231-232.

Sus antiquus. Woodcut, f. 11, p. 233.

paleocherus. Woodcut, f. 10,
p- 233.

Tapirus priscus. Woodcuts, f. 8, 8a,
9) pi 200:

Pleistocene ...| Berkshire .........
Red Crag......| Woodbridge, Suff.
Red Crag ...... Woodbridge, Suff.
Red Crag ...... Woodbridge, Suff.
Red Crag ...... Sutton, Suffolk ...
hed Crags: «ct; Sutton, Suffolk ...
Red Crag ...... Near Ipswich, Suff.
Red Crag ...... NearIpswich, Suff.
Norwich Crag.) Norfolk ..........

Red Crag ...... Bawdsey, Suffolk..
Red Crag ...... Newbourn, Suffolk
Red Crag ...:..| Felixstow, Suffolk
Red Crag...... Bawdsey, Suffolk..
Red Crag ......) Wolverton, Felix-

stow, & Sutton.
Red Crag ...... Ramsholt, Suifolk
Red Crag...... Sutton, Suffolk ...

Red Crag ...... Sutton, Suffolk ...

Ziphius (Dioplodon, Gervais), sp.| Red Crag...... Felixstow, Suffolk

Woodcut, f. 24, p. 236.

Page.

354

EXPLANATION OF THE PLATES.

PLATE

1.—Map, to illustrate Mr. R. Godwin-Austen’s paper on the possible
Extension of the Coal-Measures ........0......0+06 Balle de/ciasreaiaists To face p. 46*

2.—Fossit CrusTacEAN Remains, to illustrate Mr. Banks’s paper on the
Tilestones or Downton Sandstones in the Neighbourhood of Kington,
SPHCMARe ITC OTELENUS |): alas singlet 4a aia sis\weisweiieisamnieive's necisiaisisnie alate «alsiciuieew aciois se 101

3.—T1B1 oF Birps, to illustrate Prof. Owen’s paper on the Affinities of
the large extinct Bird (Gastornis Parisiensis, Hébert), indicated by a

. Fossil Femur and Tibia discovered in the Lowest Eocene Formation
MEME R ARIST sacs), cage voweeaslseicsesdssiodeaccccaGtes SeeatebcinSastoareddsscetenesohes 217

4.—ANNELID Markines, &c., to illustrate Mr. Salter’s paper on Fossil
Remains in the Cambrian Rocks of the Longmynd and North Wales 250

5.—Map or THe Franco-Beteran CoaL-pistRicr, to illustrate the paper
by MM. Degousée and Laurent on the Valenciennes Coal-basin...... 254

6.—ORTHOCERAS AND ACTINOCERAS, to illustrate Mr. cant paper
on an Orthoceras from China

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GEOLOGICAL SOCIETY OF LONDON.

ANNUAL GENERAL MEETING, FEBRUARY 15, 1856.

REPORT OF THE COUNCIL.

Tue Council, in laying their annual statement of the affairs of the
Society before its Members, beg to express their opinion that it
evinces a continuance of the same satisfactory state to which, on
former occasions, they have directed attention. The number of
Fellows, it is true, has suffered a diminution of nine; but this is

mainly to be attributed to the numerous deaths which have occurred.
since the last anniversary. The Society from this cause has lost
twenty-six ordinary Fellows, and seven have resigned during the
same period, making a loss of thirty-three. Twenty new Fellows
have been elected in the past year, and four elected in the previous
year have paid their subscriptions in this ; making, in all, 24, which,
deducted from 33, leaves a loss to the Society of 9, as before stated.
One Foreign Member has died, and one has been elected during the
year. The total number of the Society at the close of 1854 was
884, and 875 at the close of 1855.

The expenditure during 1855 has exceeded the income by
£97 12s. 4d.: but in the income is included £191 12s. 9d., the
balance at the beginning of the year. The actual excess of
expenditure is, therefore, £289 5s. 1d., which has principally been
occasioned by increased expenditure on the Quarterly Journal and

VOL. XII. a

ll ANNIVERSARY MEETING.

the forthcoming Volume of the Transactions. The Council con-
fidently hope that the Fellows will not regret an outlay, whose pur-
pose is to further those objects for which they are associated. At
the same time they would remark that the expenditure on this head
would be materially lightened, were it met by a greater disposition
on the part of the Fellows to purchase the Society’s publications.
Were this the case, the Council would have it in its power to do
justice to the Memoirs read before the Society by more liberal illus-
tration.

Among those whose loss the Society has to deplore during the
past year is George Bellas Greenough, the first President of this

' Society, and ever its liberal patron. At his death, which occurred

in April 1855, he bequeathed to the Society all his title to the
Geological Map of England which bears his name, and which will
ever be a monument of his extensive knowledge and untiring perse-
verance ; he also bequeathed all his Books, Maps, Charts, Sections,
and Engravings relating to Geology. He further bequeathed to the
Society the sum of £500 to defray the expense of finding accommo-
dation for the Collections. This sum of £500 has been for the
present invested in the Funds; so that the amount of the Funded
Property of the Society, which at the close of 1854 was£4014 15s.84d.,
is now £4578 19s. 2d. In addition to this the Society holds two
Exchequer bills of £100 each.

Amongst the many Donations received since the last anniversary,
the Council would call especial notice to the “Natural History of
Deeside,”’ by the late Dr. M°Gillivray, printed at the expense of Her
Majesty, and presented by His Royal Highness Prince Albert, Fellow
of this Society. Many other copies of this beautifully executed work
have been liberally distributed among the Fellows by His Royal
Highness.

The Council have to report that the 11th volume of the Quarterly
Journal has been completed; and that the Ist part of volume 12th
will very shortly appear, although its publication from unavoidable
circumstances has been retarded.

The Council have also to state that the 4th part of the 7th volume
of the Transactions is in the press, and will shortly appear. The
Supplement to the Catalogue of the Library, of which six sheets are
now printed, will also soon be ready for publication.

In conclusion the Council beg to state, that they have unani-
mously awarded the Wollaston Palladium Medal to Sir William E.
Logan, Director of the Geological Survey of Canada, for his yalu-
able contributions to geological knowledge in his elaborate papers on
the origin and structure of the Coal-beds in England, and for his
subsequent labours in Canada, in carrying out the Geological Survey
of that country ; and particularly for the admirable Geological Map
of Canada, constructed by himself from materials of his own collect-
ing, and exhibited at the Universal Exhibition in Paris, last year.

They have also awarded the balance of the proceeds of the Fund
to M, G, Deshayes, for his great exertions in the extension of our
knowledge of Tertiary Geology, and for his Palzontological works

ANNUAL REPORT. li

illustrative of the Tertiary Basin of Paris, and to assist him in the
publication of the forthcoming continuation of his Work ‘Sur les
Coquilles fossiles du Bassin de Paris.”’

Report of the Library and Museum Committee.
Inbrary,

During the past year the principal addition to the Library has
been the magnificent bequest of Mr. Greenough of the whole of his
collection of Geological Books and Maps: these haye not yet been
arranged in our Library, but, as the Council has appointed a special
Committee to consider of the best plan for the arrangement of .that
collection, it is not necessary for us to enter into the consideration of
this important matter.

The other additions which have been made to the Library during
the year haye all been worked into their places both in the shelves
and the Catalogue ; among these we call attention to the large number
of parts of the Journals of various Scientific Societies, both English
and Foreign, which have been obtained by application to those So-
cieties, or by exchange of our own publications for them, and the
Geological and Mineralogical contents of which will be found under
the list of the Donations published in our Journal by the Assistant-
Secretary. The system of exchanging publications with other Societies
has answered so well, that we strongly recommend its continuance and
extension as opportunities occur.

The additional shelves ordered by the Council have been placed in
the Assistant-Secretary’s room, and have served to receive the addi-
tions constantly reaching the Society ; they will probably be sufficient
to hold the usual additions of the next two years, if another recep-
tacle be prepared for Mr. Greenough’s books: the re-arrangement
of the serials brought on by the moving part from the old to the new
shelves has taken up a good deal of Mr. Jones’s time.

The mounting of such Maps as are likely to be often referred to,
including all those lately received from the Ordnance Geological
Survey, has been continued, and two new Map-Cases have been added
to hold them; and a Stand has been added to hold large Portfolios.

The printing of the Supplemental Catalogue has been proceeded
with ; six sheets are already printed, containing nearly all the books,
and the printers are at work on the part containing the rest of the
Books and the Maps; and the MS, Catalogue of the Charts is already
prepared. This, when completed, will include all the additions to the
Library during the ten years ending with 1853.

As the MS. additions to the yolume of the Catalogue of reference
in the Library, which contains the Periodicals, are now included in
the printed Supplement, it is desirable that a portion of that volume
should be re-arranged for greater convenience of reference.

In the Lower Museum a Case has been added to receive Maps and
Charts, and is already partly occupied.

Application was made to the Board of Ordnance for the revised
sheets of the Survey of England, and for the Block-Plan of London,
which application has been refused by letter of 4th June 1855,

a 2

iv ANNIVERSARY MEETING.

Museum.

The additions to the British Collection include a large collection of
specimens from Bovey Tracey, presented by Dr. J. G. Croker, which
have just been received, and are not yet placed; also a set of Fossil
Plants from Studland, presented by Mr. W. R. Brodie; and a very
interesting series of Ferns, &c., from the Yellow Sandstone of Ire-
land, presented by the Rev. Prof. Haughton, F.G.S.; also specimens
of Allophane from the chalk-pit of Charlton, Kent, presented by
Dr. Krantz.

During M. E. Renevier’s stay in London he examined all the
specimens from the Gault in our collection, and compared their
names with those in use on the Continent, especially with those of
Pictet and Roux, in their “ Mollusques fossiles des Grés Verts de
Geneve.”

Agreeably to the order of the Council, an interleaved copy of
Mr. Morris’s Catalogue of British Fossils has been placed in the
Museum, to serve as a means of cataloguing our collection; and a
beginning has been made in it by Mr. S. V. Wood, in the Tertiary
series, and by Mr. D. Sharpe in the Cretaceous series. It is to be
hoped. that other Fellows of the Society will lend their assistance
towards carrying out this most desirable object.

Mr. Gawan has been employed during the year assisting Mr. Jones,
both in the necessary attention to the Museum and in the arranging
the Library and preparing a catalogue of Mr. Greenough’s books;
and Mr. Jones reports most favourably of the assistance which he
has received from him.

The following interesting additions of foreign specimens have been
received. :-—

Cryolite, Tantalite, and Eudiatite-rock, from Evigtok, Greenland ;
presented by J. W. Tayler, Esq. The specimens of Tantalite are
particularly fine.

The Rev. Mr. Hislop, of Nagpoor, has continued to send us valuable
collections of Fossil Plants and other Organic Remains, from the
Nagpoor Territory, and which we hope will soon be examined by
several Fellows of the Society, who have promised their assistance
towards their publication in the Society’s Journal.

Mr. J. W. Mudge has presented an interesting collection of Tertiary
Fossils from Prome, which, added to those which the Society has
before received from Col. Turton and Mr. Crawfurd, make up a
most interesting series from that locality.

Danie SHARPE.
S. P. Pratt.
January 30, 1856.

ANNUAL REPORT. +V

Comparative Statement of the Number of the sseotaty at the close of
the years 1854 and 1855.

Dec. 31, 1854. Deer si rsos.

Wompounders:....... 50.52% SMR Ed. Meni 131
EPIL E MSs isla s.> s,s Ses oe 7: apes bad 201
Won-residents. 3.6%... 05. 2 Aira tare Sethi 474

815 806
Honorary Members...... Toa Lene alee, 15
Foreign Members........ 50 eae oO)
Personages of Royal Blood Oe es aie so at 4—69

884 879

General Statement explanatory of the Alteration in the Number of
Fellows, Honorary Members, yc. at the close of the years 1854
and 1855.

‘Number of Compounders, Residents, and Non-residents,

Mecentmers Oa ee eb es we AO erete dex 815
Add, Fellows elected during former) Resident.... 2
years, and paid in 1855...... Non-resident 2
— 4
Fellows elected, and pa oe Resident. . 13
1855 : Non-resident 7
—20
— 24
839
Deduct, Compounders deceased .............. 7
BRESHACMES 1 chieh oe we ee eee ce cio 6. - 7
Womerestdlenise ei.) ee ook tn 3 12
Resigned. ... . 7
— 33
Total number of Fellows, 3lst Dec. 1855, as above. . 806
Number of Honorary Members, Foreign Members, and 69
Personages of Royal Blood, December 31, 1854 .
Add, Foreign Member elected during 1855 . aerate 1
70
Deduct, Foreign Member deceased .............+++-- 1

As above 69

vl ANNIVERSARY MEETING.

Number of Fellows liable to Annual Contribution at the close of
1855, with the Alterations during the year.

Wunmiberat the close of 1854.5 ...:...... [See ee ce 203
Add, Elected in former years, and paid in 1855 ........ 2
Elected and! paid m L655. ... 4... wage eee ak 13
Non-residents who became Resident ............ 4
222
Medubty Deceased... 050%. 425 Bee ee ee ee 7
BUESIONEO (i. 02 = 2 sie SURO eee ee a: eae 6
Compounded .34.24.2.04 fds g tits ee cee 1
Became Non-resident ..........1.......- 7
en

As above 201

DECEASED FELLOWS:
Compounders (7).

Rt. Hon. Sir W. Molesworth.
E. W. W. Pendarves, Esq.
Rey. Richard Sheepshanks.
John Ward, Esq.

John Brogden, Jun., Esq.
C. Colclough, Esq.
G. B. Greenough, Esq.

Residents (7).

Sir H. T. De la Beche. Philip Pusey, Esq.
Lord de Mauley. W. D. Saull, Esq.
Rt. Hon. Sir T. F. Lewis, Bt. J. H. Vivian, Esq.

Thos. Weaver, Esq.

Non-residents (12).

W. A. Cadell, Esq. Rev. E. James.

J. E. Cliffe, Esq. Prof. J. F. W. Johnston.
L. L. Dillwyn, Esq. Josias Lambert, Esq.

Rt: Hon. Sir H. Ellis. Christopher Rawson, Esq.
J. D. Gilbert, Esq. George Stephenson, Esq.
Rev. J. P. Higman. Alfred Thomas, Esq:

Foreign Member (1).
M. G. Fischer de Waldheim.

ANNUAL REPORT. Vii

The following Persons were elected Fellows during the year 1855.

January 3rd.—Alexander Halley, M.D., Queen Anne Street.

: 3lst.—Rev. Thos. J. Prout, A.M., Christ Church, Oxford.

February 21st.—Edward Hull, Esq., A.B., Geological Survey of
Great Britain.

April 4th.—K. Ward Jackson, Esq., Bayswater ; James E. Saunders,
jun., Esq.; Finsbury Circus; Edward L. J. Ridsdale, Esq., Ton-
bridge ; and G. Henry Wathen, Esq., Clifton, Bristol.

—— 18th.—John George Blackburn, Esq., Oldham ; and Rev. Wm.
.Charles Kendall, Newmarket-upon-Trent.

May 2nd.—William Foster White, Hsq., St. Bartholomew’s Hos-
pital; C. S. Mann, Esq., Eltham; Lucas Barrett, Esq., Totten-
ham Court Road ; and John D’ Urban, Esq., Gordon Street.

16th.—Edward H. Hargraves, Esq.,; Upper Spring Street.

— 30th.—Rev. John Knowles, Croydon; and James M‘Cann,
Esq., Liverpool.

June 13th.—George D. Gibb, M.D., Guildford Street.

Nov. 7th.—William Harrison, Esq:, Blackburn, Lancashire.

—— 2|st.—James G. Sawkins, Esq., Swanage.

Dec. 5th.—John Lubbock, Esq., High Elms, Farnborough ; Henry

' Conybeare, Esq., Abingdon Street; and Richard Hayter Jarvis,
Esq., Dorset Square.

The following Person was elected a Foreign Member.

June 13th.—Dr. Carl Friedrich Naumann, Leipsic.

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

British Specimens.

Tron Ore from Waltham on the Wolds; presented by J. A. Kuipe,

Esq.

Spetinens of Allophane from the Charlton Chalk Pit; presented by
Dr. Krantz.

Fossil Freshwater Shells from Fisherton, near Salisbury ; presented
by J. Brown, Esgq., F.G.S.

Specimens of Ferns, &c., in the Yellow Sandstones of Ireland; pre-
sented by the Rev. Prof. S. Haughton, F.G.S.

Specimens of Fossil Leaves from Studland, Dorset; presented by
W. R. Brodie, Esq. |

Lignite and Rock-specimens from Bovey Tracey, Devon; presented
by Dr. Croker.

Vill ANNIVERSARY MEETING.

Foreign Specimens.

Fossils from Algoa Bay; presented by J. S. Bowerbank, Esq., F.G.S.
Fessil Plants from the Pachmadi Hills; presented by the Rev.
Messrs. Hislop and Hunter. 2

Suite of Fossils from Prome ; presented by J. W. Mudge, Esq.

Ss iotad from Mokattam, Egypt; presented by L. Horner, Esq.,

Specimens from the Nummulitic formation of Switzerland ; presented
by M. E. Renevier.

Specimens from Silurian Rocks of Beechy Island; presented by Dr.
Armstrong.

Specimens of Scandinavian Limestones with Beyrichie; presented
by T. R. Jones, Esq., F.G.S.

Specimens of Cryolite, Tantalite, and Eudiatitie rock, from Evigtok,
Greenland ; presented by J. W. Tayler, Esq.

Vegetable-remains and other Fossils from the Nagpur Territory ;
presented by the Rev. Mr. Hislop.

CHARTS AND Maps.

The Charts, &c., published by the Admiralty during the past year ;
presented by John Washington, Esq., by direction of the Lords
Commissioners of the Admiralty.

Twenty-six Charts published by the Depdt de la Marine; presented
by the Director-General of the “ Depot de la Marine.”

Geognostische Karte des Thiirmger-Waldes, von H. Credner; 4 sheets
and Memoir ; presented by Herr Justus Perthes.

Golpe de vista da America do Sul, by J. D. Sturz; presented by the
Author.

Section of the Greensand at Hast Compton, Dorset, by J. Hicks,
Esq. ; presented by the Author.

Topographical Map of London and its Environs, by R. W. Mylne,
Esq., F.G.S.; presented by the Author.

Geologische Ubersichts-Karte der Schweiz, von B. Studer und A.
Escher ; presented by M. S. M. Ziegler.

Deux Vues Géologiques pour servir a la Description Géologique du
Danemark représentant les Falaises de Stevens-Klint et de Méens-
Klint, par C. Piggaard ; presented by the Author.

Map of the Vestiges of Assyria, in 3 sheets ; presented by the Asiatic
Society of Great Britain.

Map of St. Thomas, with MS. Index of Geological Features, by
H. B. Hornbeck, M.D.; presented by the Author.

Tableau Synoptique des Terrains et des principales Couches Minérales
qui constituent le Sol du Bassin Parisien, par M. Chas. d’Orbigny ;
presented by the Author.

Geological Map of Wisconsin, by J. A. Lapham; presented by the
Author.

A Leptometer, invented by M. le Dr. Guido Sandberger; presented
by Dr. Sandberger,

ANNUAL REPORT. ix

The following List contains the Names of the Persons and Public
Bodies from whom Donations to the Library and Museum were

received during the past year.

Admiralty, Lords Commission-
ers of the.

Albert, His Royal Highness
Prince, F.G.S.

American Academy of Arts and
Sciences.

American Philosophical Society.

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

Armstrong, Dr.

Arnott, N., M.D., F.G.S.

Art-Union of London.

Ashley, J. M., Esq.

Ashmolean Society.

Asiatic Society of Bengal.

Asiatic Society of Great Britain.

Athenzeum Journal, Editor of the.

Baker, J. G., Esq.

Barlow, P. W., Esq., F.G.S.

_Barrande, M. J., For. M.G.S.

Basel Natural History Society.

Belcher, Captain Sir Edward,
R.N., C.B., F.G.S.

Belgium, Royal Academy of
Sciences of.

Berlin, German Geological So-
ciety at.

Berlin, Royal Academy of Sci-
ences at.

Berwickshire Naturalists’ Club.

Bianconi, Signor J. J.

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

Boston Natural History Society.

Bowerbank, J. S., Esq., F.G.S.

Breslau Academy.

British Museum, Trustees of the.

Brodie, W. R., Esq.

Brown, J., Esq., F.G.S.

Calcutta Public Library.

Canadian Journal, Editor of the.

Candolle, M. A. de.

Catullo, Prof. T. A.

Caus and Co., Messrs.

Cautley, Col. Sir P. T., K.C.B.,
F.G.S.

Chapman, E. J., Esq.

Chemical Society of London.

Civil Engineers’ Journal, Editor
of the.

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

Copenhagen, Royal Society of.

Critic, Editor of the.

Croker, Dr.

D’Archiac, M. le Vicomte A.,
For. M.G.S.

Darwin, C., Esq., F.G.S.

Davidson, Thomas, Esq., F.G.S.

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

Delesse, M. A.

Deslongchamps, M. E.

Dijon, Academy of Sciences of.

Dilke, C. W., Esq., F.G.S.

D’Orbigny, M. C.

Dublin Geological Society.

East India Company, The Hon.

Edinburgh, Royal Society of.

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

Everest, Rev. Robert, F.G.S.

Fairbairn, Wm., Esq., F.G.S.

Faraday, M., D.C.L., F.G.S.

Favre, M. A.

Forbes, D., Esq., F.G.S.

Forchhammer, Dr. J. G., For. M.
G.S.

Forrester, J. J., Esq.

France, Geological Society of.

Frankfort Society of Sciences.

Franklin Institute of Pennsyl-
vania.

Geinitz, Dr. Hans Bruno.

Geographical and Commercial
Gazette, Editors of the.

Gillis, Lieut. J. M., A.M.

Glasgow Philosophical Society.

Goebel, Herr von A.

Graty, M.A. M. du.

x ANNIVERSARY MEETING.

Greenough, G.B., Esq., V.P.G.S.
Greg, R. P. jun., Esq., F.G.S.
Griffin and Co., Messrs.

Halle Society of Natural Science.
Hamilton, W. J.,; Esq:, Pres.G.S.
Harkness, Prof., F.G.S.

Hauer, Herr F. R. v.
Haughton, Rev. Prof. S., F.G.S.
Hébert, M: E.

Hewitt, H. jun., Esq.

Hicks, J., Esq.

Hislop, Rev. S.

Holmes, Prof. F. S.
Hombres-Firmas, M. le Baron de.
Hooker, J. D., M:D., F.G.S.
Hornbeck, H: B., M.D.
Horner, L., Esq.; F.G.S.
Hornes; Dr. M.

Horticultural Society.

Hunter, Rev. R.

Indian Archipelago Journal;
Editor of the.
Institute of Actuaries.
James, Lieut.-Col. H., R.E.,
5

Jennings, F. M., Esq., F.G.S.
Jones, T. R., Esq., F.G.S.

Knipe; J. A., Esq.
Krantz, Dr.

Lancashire and Cheshire Historic
Society.

Langel, M. A.

Lapham, J. A., Esq.

Lea, J., LL.D.

Leeds Philosophical Society.

Leidy; J., M.D.

Linnean Society.

Literary Gazette, Editor of the.

Liverpool Literary and Philoso-
phical Society.

Logan, Sir W. E., F.G.S.

Lombardy, Imperial and Royal
Institute of:

Longman and Co., Messrs.

Lyell, Sir Charles, F:G.S.

Lyon, Commission Hydromé-
trique de.

Madrid Royal
Sciences.

Manchester PhilosophicalSociety.

Mantell, R. N., Esq.

Marcou, M. Tuleh.

Martins, M. Ch.

Meyer, Herr Hermann von, For.
M.G.S.

Montagna, M. C.

Moore, J. C., Esq., F:G.S.

Mortillet, M. G. de.

Moscow Imperial Society of Na-
turalists.

Mudge, J. W., Esq.

Munich, Bavarian Academy of
Sciences of.

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

Museum of Practical Geology.

Mylne, R. W., Esq., F.G.S.

Academy of

New York Lyceum of Natural
History.

New York, University of the
State of.

Orleans Academy of Sciences.

Palzeontographical Society. _

Paris, Academy of Sciences of.

Paris, Ecole des Mines de.

Paris, M. le Directeur-Général du
Depot de la Marine de.

Paris, Muséum d’Histoire Na-
turelle de.

Perrey, M. A.

Perthes, Herr Justus.

Petermann, Dr. A. ’

Peters, Herr K. F.

Philadelphia Academy of Natural
Sciences.

Photographie Society.

Pictet, Prof. F. J.

Prossian Government.

Puggaard, M. C.

Reeve, L., Esq., F.G.S.
Renevier, M. E.

|

ANNUAL REPORT. xl

Roemer, Dr. Ferd.

Royal Agricultural Society.

Royal Astronomical Society.

Royal College of Surgeons.

Royal Geographical Society.

Royal Institution of Great Bri-
tain.

Royal Irish Academy.

Royal Society of London.

Ryckholt, M. le Baron de:

Sandberger, Dr. F.

Sandberger, Dr. G.

Scarborough Philosophical and
Archeological Society.

Schmidt; Dr. Carl.

Scottish Meteorological Associa-
tion.

Sedgwick, Rev. Prof., F.G.S.

Sheffield Literary and Philoso-
phical Society.

Sherz, M. T. D.

Siena, Accademia del Fisiocritici

de.
Silliman, Prof., M.D., F.G.S.
Smithsonian Institution.
Society of Arts.
Statistical Society.

Stockholm Royal Academy of
Sciences.
Suess, M. Edouard.

Tayler, J. W., Esq.

Taylor, R., Esq., F.G.S:
Thomson, T., M.D:

Trask, J. B., Esq.

Trimmer; J., Esq.; F.G.S.
Turin Royal Academy of Sciences.

Vaud Society of Natural Sciences.

Verneuil, M. E: de, For. M.G.S.

Vienna Geological Institute.

Vienna Imperial Academy of
Sciences:

United States Patent Office.

Wailes, B. L. C:, Esq.
Wathen, G. H., Esq:; F.G.S.
Wetterau Society.

Wright, Dr. T.

Yorkshire Philosophical Society.

Ziegler, M.S. M.
Zeisezner, Herr C.

List of Pavers read since the last Anniversary Meeting,
February 16¢h, 1855.

1855.

Feb. 21st. —Evidences of the Occurrence of Glaciers and Icebergs in
the Permian Period, by Prof. A. C. Ramsay, F.G.S.

March 7th.—On the Geology of the Ballarat, Eureka, and Creswick
Creek Gold-fields, Victoria, by M. H. Resales. communicated by

W. W. Smyth, Esq., F.G.S.

On the Geology of Part of the Peel River District,

Australia, by M. F. Odernheimer ;

Murchison, V.P.G.S.

communicated by Sir R. I.

On the Occurrence of Obsidian Bombs in the Auri-

ferous Alluvium of Australia, by the Rev. W. B. Clarke, F.G.S.

On the Oceutrence of Fossil Mammalian Bones in

the Auriferous Alluvium of Australia, by the Rev. W. B. Clarke,

E.G. S.

Notes on the Geology of New South Wales, by the

Rev. W. B. Clarke, F.G:S.; in a Letter to Sir R. I. Murchison,

V.P.G.S.

Xll ANNIVERSARY MEETING.

1855.

April 4th.—On the Paleeozoic Rocks of the Thiiringerwald and the
Hartz, by Sir R. I. Murchison, V.P.G.S., and Prof. J. Morris,
F.G.S.

April 18th.—On the St. Cassian Beds between the Keuper and the
Lias in the Vorarlberg, by Prof. Merian; in a Letter to Sir R. I.
Murchison, V.P.G.S.

On Fossils from the Keuper at Pendock, near the
Malverns, by the Rev. W. S. Symonds, F.G.S.

—_—___—_—. On Cretaceeous Rocks near Natal, South Africa, by
Capt. Garden; with a Notice of the Fossils, by W. H. Baily,
Esq. ; communicated by R. Godwin-Austen, Esq., F.G.S.

——_———— On the Geology of Natal, by P. C. Sutherland, M.D.;
in Letters to Sir R. I. Murchison, V.P.G.S.

May 2nd.—On the Physical Geography and the Pleistocene Phee-
nomena of the Cotteswold Hills, by E. Hull, Esq., F.G.S.

—— Notice of the Occurrence of Coal near the Gulf of
Nicomedia, by D. Sandison, Esq., Her Majesty’s Consul at Brussa;
forwarded by the Foreign Office.

——— On the Anthracitic Schists and Fucoidal Shales of
the Lower Silurians in the South of Scotland, by Prof. R. Hark-
ness, F.G.S. |

May 16th.—Geological Notes on the British Possessions in North
America, accompanied by a Geological Map, by A. K. Isbister,
Esq. ; communicated by Sir R. I. Murchison, V.P.G.S.

wo Notes on the Geology of Georgia, U.S., by W. Bray,

Esq. ; communicated by the President.

On the Geology and the Coal-bearing Rocks of New
Zealand, by C. Forbes, Esq. ; communicated by Sir H. T. De la
Beche, F.G.S.

———————. Notes on the Geology of New Zealand, by J. C.
Crawford, Esq. ; communicated by the President.

Description of the Skull of the Dicynodon tigriceps,
by Prof. Owen, F.G.S.

May 30th.—Notice of the Occurrence of a Bore at Port Lloyd,
Bonin Islands, by P. W. Graves, Esq., H.M. Consul-General for
the Sandwich Islands; forwarded by the Foreign Office.

On the probable Extension of the Coal-Measures be-
neath the South-eastern Parts of England, by R. Godwin-Austen,
Esq., F.G.S.

June 13th.—On the Remains of the Dicynodon from South Africa,
by Prof. Owen, F.G.S.

———— On a Fossil Sirenoid Mammal from Jamaica, by
Prof. Owen, F.G.S.

On the Brown-Coal Formation of Germany, by

Prof. Beyrich; with Observations by W. J. Hamilton, Esq.,

Pres. G.S.

bee

———_—— On the Section of the Metamorphic and Devonian
Rocks at the Eastern end of the Grampians, by Prof. Nicol,
F.G.S.,

ANNUAL REPORT. xill

1855.

June 13th.—On Fossils and Drift-wood collected in the Arctic
Archipelago by Capt. M‘Clure and Lieut. Pimm, by Sir R. I. Mur-
chison, V.P.G.S.

——_-—— On the Raised Beaches of Argyllshire, by Capt. E. J.
Bedford ; communicated by Sir R. I, Murchison, V.P.G.S.

On Sand-worn Granite, by R. W. Fox, Hsq.; com-

municated by Sir R. I. Murchison, V.P.G.S.

On the Red Soil of India, by Dr. W. Gilchrist ; com-
municated by Sir R. I. Murchison, V.P.G.S.

see On the Umret and other Coal-fields of India, by the
Rev. Stephen Hislop; communicated by J. C. Moore, Ksq., Sec.
G.S.

—_—_——__——- On the Earthquakes at Brussa, by D. Sandison,

Esq., H.M. Consul at Brussa; forwarded by the Foreign Office.
—_—_— ——. Onsome Fossil Seeds from Lewisham, by J. D. Hooker,

M.D., F.G.S.

—_——— On some Fossil Seeds from the Bovey Lignite, by

J.D. Hooker, M.D., F.G.S.

November 7th.—On the Newer Tertiary Deposits of the Sussex

Coast, by R. Godwin-Austen, Esq., F.G.S. |
—_——_ Report on the Coal of the North-Western Districts of

Asia Minor, by H. Poole, Esq. ; communicated by Sir R. I. Mur-

chison, V.P.G.S.

November 21st.—Notice of the Boring at Kentish Town, by Joseph

Prestwich, Esq., Sec. G.S.

—— Notice of the Upper Silurian Rocks of Lesmahago, in
the South of Scotland (an which Mr. Slimon has discovered
Fossil Crustaceans), by Sir R. I. Murchison, V.P.G.S.

—— Description of some Fossil Crustaceans from Lesma-
hago, in the South of Scotland, by J. W. Salter, Esq., F.G.S.
December 5th.—On the Tilestones, or Downton Sandstone, in the

neighbourhood of Kington, and their fossil contents, by R. W.

Banks, Esq. ; communicated by Sir R. I. Murchison, V.P.G.S.
——_—~— On the last Elevation of the Alps, with Notices of

the Heights at which the Sea has left Traces of its Action on their

Sides, by Daniel Sharpe, Esq., Treas. G.S.

December 19th.—On the Remains of the Musk-Buffalo from the

Gravel near Maidenhead, by Prof. Owen, F.G.S.

Note on some Gravel Beds near Maidenhead, by
Joseph Prestwich, Esq., Sec. G.S. ,

On some of the Geological Features of the Country
alg the South-Down and the Sea, by P. J. Martin, Esq.,
F.G.S.

1856.
January 9th.—On the Physical Geography of the Tertiary Estuary
of the Isle of Wight, by H. C. Sorby, Esq., F.G.S.
——— On the probable Permian Character of the Red Sand-
stones of the South of Scotland, by E. W. Binney, Hsq., F.G.S.

xiv ANNIVERSARY MEETING.

1856.
January 23rd.—On the Cryolite of Evigtok in Greenland, by
J. W. Tayler, Esq.; communicated by Prof. Tennant, F.G.S.
On remarkable Mineral Veins, with a Notice of Cobre
Copper Lode, near Santiago de Cuba, by D. 'T. Ansted, Esq.,
F.G.8,

February 6th,—Experimental Researches on the Granites of Ireland,
by the Rev. Prof. Haughton, F.G.S.

On the Raised Beaches of the Western Isles of Scot-

land, by Capt. J. E. Bedford ; communicated by Sir R. I. Mur-

chison, V.P.G.S.
———— On the Section exposed in the Excavation of the
Docks at Swansea, by M. Mogeridge, Esq. ; communicated by
Sir R. I. Murchison, V.P.G.8.

-— : On the late Eruption of Mauna Loa, Hawaii, by
W. Miller, Esq., H.M. Consul at the Sandwich Isles; forwarded
by the Foreign Office.

After the Reports had been read, it was resolved,—

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

It was afterwards resolved,—

1. That the thanks of the Society be given to Sir R. I. Murchi-
son and Professor Phillips, retiring from the office of Vice-President.

2. That the thanks of the Society be given to J. C. Moore, Esq,,
and Joseph Prestwich, Esq., retiring from the office of Secretary,

3. That the thanks of the Society be given to Daniel Sharpe,
Esq., retiring from the office of Treasurer. ae

4, That the thanks of the Society be given to Dr. Bigsby, the
Earl of Enniskillen, Dr. Hooker, Dr. Percy, and J. W. Salter, Esq.,
retirmg from the Council.

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

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 Officers and Council for the ensuing
year :—

——

ANNUAL REPORT.

OFFICERS.

———

PRESIDENT.
Daniel Sharpe, Esq., F.R.S. and L.S.

VICE-PRESIDENTS.

Sir P. G. Egerton, Bart., M.P., F.R.S
R. A. Godwin-Austen, Esq., B.A., F.

B.S.

Sir Charles Lyell, F.R.S. and LS.
Col. Portlock, R.E., F.R.S.

SECRETARIES.

Robert W. Mylne, Esq.
Warington W. Smyth, Esq., M.A.

FOREIGN SECRETARY.
Samuel Peace Pratt, Esq., F.R.S. and L.S.

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

COUNCIL.

Prof. Thomas Bell, F.R.S. and
L.S

Col. Sir P. T. Cautley, K.C.B.,
F.R.S. and L.S.

Earl of Ducie.

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

Thomas F. Gibson, Esq.

R.A. Godwin-Austen, Esq., B.A.,
F.R.S.

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

William Hopkins, Esq., M.A.,
E:B.S.

Leonard Horner, Esq., F.R.S.L.
and E.

Sir Charles Lyell, F.R.S.and L.S.

John C. Moore, Esq., M.A.

Prof. John Morris.

Sir R. I. Murchison, G.C.St.S.,
F.R.S. and L.S.

Robert W. Mylne, Esq.

S. R. Pattison, Esq.

Prof. John Phillips, F.R.S.

Col. Portlock, R.E., F.R.S.

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

Samuel Peace Pratt, Esq., F.R.S.
and L.S.

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

D. Sharpe, Esq., F.R.S. and L.S.

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

Henry Clifton Sorby, Esq.

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Income and Expenditure during the

INCOME.
SS a8. ae eS
Balance at Banker’s, January 1, 1855 .... 383 4 3
Balance in Clerk’s hands ....... epee 22 16.6
— 406
iueeary (Greenough). oii i alc kee oi bce bale, Giese
COMPUSIIGN.FECeIVEd: — 6. ci wecs.o o & vin Gs ee ec ol
Arrears of Admission Fees .......2.. .. ‘Sa 22090
Arrears of Annual Contributions ...... cs ot Ts oo
eee oe
Admission Fees of 1855 ........02.. ee a are ee ar le
Annual Contributions of 1855). 23g ce ee cee 636
Dividends ou.3 per cent.\Consolaa sme. oj. sete ee 112
Dividends'on Exchequer Bonds. .ecg. - . rl oe 6

Publications :
Longman & Co. for Sale of Journal in 1854 . 59 18 10

g. inde
0 9
0 O
10 O

m— CO o> OC Or
wOhOC SO

Sale of Transactions ........... Bs olen Rint Os cltat ares 15 4 9
Sale of Proceedings) 2.0.22 n0e--css-eermeraenn ak a 0h 1
Sale of Journal, Vol. dcto' Vikiw..:sskeetauos. vse 1419 0
Sale of Journal} Val. WANG <.5.0: ore nceeens.seeeay 5 0 6
Sale.of Journal; Viol: VU. jctess cox cocn se castes 8 14 0
Sale of Journal, ViolMdexs yactecacssceaneesececes on 16 .o6
Sale of Journal, Vole XGpeeccs-ceseacsshraressalne 89 19 0
Sale:of Journal, Vol: 2M4% orcs. eter nee cea 160 13 2
—— o7 bk soe
male-of Library Catalosues . vn peels + - oe yeeteee eae 0 17.46
Sale of Geological Map of England (Greenough) . 7.108
We have compared the Books and
Vouchers presented to us with these
Statements, and find them correct. !
THOS. F. GIBSON, Audit
Feb. 2, 1856: ALFRED TYLOR, ( “"®"°T%- 00906. gay

* Due from Messrs. Longman and Co., in

addition to the above, on Journal, Vol. XI... £57 7 6
Due from Authors for Corrections ............ 811 0
Due from Fellows for Subscriptions ......... 44 6 0

Year ending December 31st, 1855.

EXPENDITURE.
aoe oS,
favested im Consols: (Legacy) 2.3.) 22-..-25...-4 22.500 0
General Expenditure : Bane Se A
FEMS ce detac coca cie car's sanseaseisadeencnsqancnesiccs 64 12 10
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Re MAIO NS. 0565, 199. cabcieps si ciceiaan a ces eistodaannacmene 230
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Salaries and Wages:

Assistant Secretary and Curator ....+.-++...08. 200 0 0
NOE an oe he nat Pes civ ccicee shsohcde vote co eos ceow een we 120 0.0
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Publications :
PETAHSACHIOUNS © cocci snaceccceecsweb as vvcieebaaesacec Outs: 2
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754 9
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Balance in Clerk’s hands ............ Adit 228
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PROCEEDINGS
AT THE

ANNUAL GENERAL MEBRTING,

15tH FEBRUARY, 1856.

AWARD OF THE WoLLAsSTON MEDAL AND Donation FunD.

Arter the Reports of the Council had been read, the President,
W. J. Hamilton, Esq., on delivermg to Sir Roderick I. Murchison
the Wollaston Medal, awarded to Sir William Edmond Logan,
addressed him as follows :—

Str Roperick Murcuison,—lIt has already been announced
this day that the Council of the Geological Society have awarded the
Wollaston Palladium Medal for this year to Sir William Logan for
his valuable contributions to geological knowledge in his paper on
the origin and structure of the coal-beds in England, and his subse-
quent labours in Canada in carrying out the geological survey of
. that country, and more particularly for the admirable geological
map of Canada constructed by himself from materials of his own
collecting, and exhibited at the great exposition at Paris last year.
The Council hope that Sir William Logan will continue the further
progress of this survey with the same energy which he has hitherto
shown, and that the Canadian legislature will not be slow in pro-
viding him with the necessary means to enable him to complete an
undertaking which reflects no less credit on the Government which
has so liberally supported him than on himself.

In requesting you, Sir, to forward to Sir William Logan this
mark of their appreciation of his exertions, 1 may be permitted to
allude more fully to his merits and to some of the circumstances con-
nected with his survey of the Canadian provinces. Previous to the
year 1842, when Mr. Logan first commenced the geological survey
of Canada, he had already distinguished himself in this country by
several valuable papers communicated to this Society. In 1840*
he read an interesting paper ‘‘ On the character of the beds of clay
lying immediately below the coal-seams of South Wales, and on the
occurrence of coal-boulders in the Pennant grit of that district.’
In this paper Mr. Logan pointed out the great importance of this
underclay varying from six inches to more than ten feet in thick-
ness, and considered such an essential accompaniment of the coal.
He also pointed out the important fact of the inumerable specimens
of Stigmaria ficoides, by which these underclay beds are so strongly
marked. He was, I believe, the first to remark that, from the fact

* Proceedings of the Geol. Soc. of London, vol. iii. p. 275.

VOL. XII. c

XXi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

that over the vast area of the coal field of South Wales not a seam
had been discovered without an underclay abounding in Stigmaria,
it was impossible to avoid the inference that there must be some
essential and necessary connexion between the existence of Stigmaria
and the production of the coal. He thought there were reasonable
grounds for supposing that in some way or other the Stgmaria
ficoides was the plant to which may be mainly ascribed the vast
stores of fossil fuel.

In 1842 he communicated another important paper, ‘On the
Coal-fields of Pennsylvania and Nova Scotia*,” im which he described
some interesting particulars connected with the extent and character
of the carboniferous deposits of Pennsylvania; he also pointed out
the extension to the coal-fields of America of those facts bearing on
the origin of coal which I have alluded to in noticing his former
paper on the coal-seams of South Wales. The presence of the
underclay, or Stigmaria fire-clay as it is sometimes called, was almost
universal. The second portion of this paper refers to the coal-fields
of Nova Scotia, which he also examined in the autumn of 1841.
Here also he observes, that under every bed of coal which he had
examined, amounting to more than twelve, he had detected the
Stigmaria fire-clay, and he was informed by Mr. Poole, the super-
intendent of the Albion Mines, that similar strata occupy the same
position in the coal-field of Cape Breton.

In the same year Mr. Logan communicated another paper to this
Society, in which he described the phenomena accompanying the
packing of ice in the river St. Lawrence. In the same paper he
has described a remarkable landslip which took place in the valley
of the St. Lawrence in 1840, and has also given an account of the
occurrence of marine shells on Montreal Mountain, where they are
found on a sort of raised beach, 430 feet above Montreal Harbour,
or about 460 feet above the Atlantic.

Since that period, with the exception of two papers on the fossil
tracks in the Potsdam sandstone and on the stratigraphical relations
of that rock, Mr. Logan’s communications to this Society have
ceased. Appointed in 1842 to superintend the geological survey
of Canada his whole time and energies have ever since been devoted
to that important work. We have watched his progress with m-
terest, and now witness the result. And in congratulating him upon
it we must not forget that before this period no systematic exa-
mination of the geology of Canada had been undertaken. Up to
that time some partial attempts only had been made by a few
enlightened individuals to form a commission with the view to
examine the country, both geologically and mineralogically ; but it
was only in 1841 that the Chambers allotted a sum of £1200, or
30,000 francs, for the geological examination of the province, and
Sir William Logan was appointed to carry out the work with Mr.
Alexander Murray as an assistant. The examination having been
thus commenced, it was continued under the government of Lord
Metcalfe by a second vote of 40,000 francs per annum, for five

* Proceedings of the Geol. Soc. of London, vol. iii. p. 707.

ANNIVERSARY MEETING.—WOLLASTON MEDAL. XXilj

years from 1845. In 1850 the grant was again renewed under
the government of Lord Elgin for a similar period.

When we consider the circumstances connected with carrying
out a geological investigation in a new country like Canada, where
the progress of civilization has not yet cleared the ground of its
primeeval forests, where the geographer has not yet prepared the
way for the geologist by the construction of correct and trustworthy
maps, and where commerce and social intercourse have not yet pre-
pared the means of communication, we may form some idea of the
vast difficulties with which Sir William Logan has had to contend,
and which he has so successfully overcome. A considerable portion
of the Canadian territory has already been geologically surveyed by
Sir William Logan and Mr. Murray, assisted by Mr. Richardson.
It appears that up to 1854 the explorations embraced the shores of
Lakes Superior and Huron, as well as the great western basin of
Canada, the valley of the St. Lawrence, as far as the Gulf, to-
gether with numerous other valleys, as the Richelieu, Yamaska,
Saint Francois, and Chaudiére, together with a large portion of Lower
Canada south of the St. Lawrence, including the district of Gaspé.

Having placed himself m communication with Mr. James Hall of
New York, who is about to publish a geological map of the United
States on the same scale as that of Canada, Sir William Logan has
adopted the same subdivision of formations as that already em-
ployed by Mr. Hall in the paleeozoic district of the United States ; we
shall thus have the advantage of seeig these two maps constructed ~
on the same plan, an arrangement of great importance for the future
examination of the American continent; and Sir William Logan
deserves great praise for thus adopting a nomenclature already in-
troduced, instead of endeavouring to establish a new one of his own.

I can give no better evidence of the value of this survey and
of the manner in which it has been carried on by Sir William Logan
than by quoting the testimony of an American writer in Silliman’s
Journal*. It is there stated: ‘No geological survey on this conti-
nent has been carried on with more thoroughness and with results
of higher importance to the science than those of Canada under the
direction of Mr. W. E. Logan. There is great precision in his
observations and exactness in his statements... .. All the observa-
tions bear directly on the geology of the United States, and they
have already solved several doubtful points as to the age of American
rocks.”

When the Canadian Government determined to send to the Paris
Exhibition a series of the economic minerals of the country, Sir
William Logan was charged with the arrangement of the collection,
the whole of which, with scarcely an exception, had been procured by
the personal exertions of the geological commission. In order to
point out the geological relations of the specimens thus collected, he

exhibited at the same time a map on the scale of ae on which

he laid down, for the first time, all the details of his geological

* Silliman, vol. xix. N.S. p. 438.
e2

XX1V PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

labours ; I consider this map to be one of the special grounds which
entitle Sir William Logan to the medal which has this day been
awarded to him. I am sure that every one who saw it in the Paris
Exposition, or subsequently in this country, must have been struck
with its execution, and the clear idea it conveyed of the geological
structure of the country.

It only remains for me to request you to convey this token of our
appreciation of his exertions to Sir William Logan and to assure him
of our good wishes for his future success, and for the continued
progress of the Geological Survey of Canada under his auspices.

Str Ropericx Murcuisovy, having received the Wollaston Medal
from the President, replied :—

Srr,—As Sir William Logan was, in the earlier part of his scien-
tific career, a distinguished contributor to the British Geological
Survey, and as my lamented predecessor, Sir Henry De la Beche,
had formed the highest opinion of his capacity, it naturally gives me
sincere pleasure to be the medium of transmitting to him this Wol-
laston Medal.

Although the Atlantic has subsequently separated us from our
medallist during most of the period in which he has been occupied in
successfully advancing geological science in his native country, Canada,
it has been a source of true gratification to me to observe the very
able manner in which he has elaborated the full and accurate succes-
sion of the most ancient rocks of the vast regions he has surveyed ;
and to see how clearly he has separated the great series of funda-
mental sedimentary unfossiliferous rocks, termed ‘‘ Lawrentian,” or
“Cambrian,” from those Silurian Rocks which, in common with all
geologists of the United States until the present moment, he has
placed in parallel with the Lower as well as the Upper Silurian of
Britain and the continent of Europe.

The skilful manner in which he has followed out the course of
these ancient Silurian deposits, from their undisturbed and unbroken
sequence over vast tracts on the West to the sea-board or Eastern
region of North America, where they have been contorted, broken up,
metamorphosed, and mineralized, will doubtless be considered among
the most remarkable labours of our honoured associate.

Whilst in his younger days he established, by the close and
repeated observations to which you, Sir, have well adverted, that
natural history constant which has enabled us to read off the true
history of the greater number of coal-fields, his maps. and sections
illustrating the structure of the Canadas, prepared in the vast wilds
of that country amidst hardships and privations unknown to Euro-
pean explorers, will be the imperishable records of his fame as a
practical geologist.

The devotion and untiring energy with which he arranged and
explained the natural productions of Canada, first at the Great
British Exhibition of 1851, and recently at the grand Exposition
of France, have obtained for him honours both from his own

ANNIVERSARY MEETING.—WOLLASTON MEDAL. XXV

gracious Sovereign and from the Emperor of the French; and I
have now only to assure you that no one of his well-merited honours
will be more highly estimated by him, than the marked approba-
tion of his brother geologists in bestowing upon him their highest
distinction, the Wollaston Medal.

On delivering to the Secretary the Balance of the Proceeds of the
Wollaston Fund, the President addressed him as follows :—

Mr. Prestwicu,—I have great pleasure in placing in your hands
the proceeds of the Wollaston Fund for this year, awarded by the
Council of the Geological Society of London to M. Deshayes; and
im requesting you to transmit them to that gentleman, I must beg
you to inform him that the Council have came to this decision, not
only in recognition of the great services he has already rendered to
palzontology, and especially to that of the tertiary epoch by the
exertions he has bestowed on the development of the molluscous
Fauna of the Paris basin, but more especially with the view of
assisting him in the further completion of his great work, ‘ Description
des Coquilles Fossiles des Environs de Paris.’ Those who like yourself
have laboured at the investigation of the different beds of the Paris
basin can best appreciate the merits of M. Deshayes. We all know
that for many years he has regularly spent a considerable por-
tion of each year in examining the different localities in the neigh-
bourhood of Paris, for the purpose of making himself acquainted
with their fossil molluscous fauna, and of verifying im situ the occur-
rence of specimens collected by others, and that each successive year
has greatly added to the number of new species.

It is also well known that since the publication of that great work
(from 1824 to 1836), the attention of many new labourers in the
field of tertiary geology has been directed to this subject. , They have
not only settled satisfactorily the order of succession of the beds, but
have collected their organic remains in large numbers, and these
have in most cases heen brought under the notice of M. Deshayes in
addition to those collected by himself. Thus finding the number of
new species rapidly increasing, and that his own collection contained
many hitherto unpublished specimens, he resolved to publish a sup-
plement to his original work, now become doubly necessary, since
without a knowledge of these new forms the true correlation of the
Paris beds with those of England, Belgium, and Germany is impos-
sible. Such is the accumulated mass of materials, that he has now
about six hundred new species to figure and describe, requiring from
sixty to seventy plates, in the preparation of which considerable pro-
gress is already made. At the same time he proposes to re-examine
the species described in his former work, and to class them all
according to the present position of geology and conchology, thus
bringing up the materials of his old work to the standard of the
new one.

_ The Council would also wish by this award to testify their appre-
ciation of M. Deshayes’ talents as a conchologist, and of the manner
in which he has made the study of recent Mollusca subservient to

XXV1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the elucidation of fossil species ; and with reference to this subject,
they cannot speak too highly of the assistance M. Deshayes has
rendered to the British Museum in arranging and correcting the no-
menclature of a considerable portion of the Bivalves in that collection,
and by preparing a catalogue which has been already partly pub-
lished. I have only now to request you to inform M. Deshayes that
while the Council regret that the sum which they are enabled to
place at his disposal is not of larger amount, they yet trust that he will
find in it an assurance of the high estimation in which they hold his
labours and his talents, and of the sincere interest they take in his
future welfare and prosperity.

Mr. Prestwicu replied as follows :—

Srr,—It will give me great pleasure to convey, as I am sure it
will my friend M. Deshayes to receive, the mark of distinction with
which the Society has to-day honoured him. I have long known
and highly appreciated the deep research and extensive comparisons
which M. Deshayes has brought to bear on the study of Tertiary
shells, and can bear willmg testimony to the kindness with which
he is always ready to assist others engaged in similar or collateral
inquiries.

I trust that this evidence of the sympathy with which the Society
views M. Deshayes’s labours will mduce him to persevere in those
labours, and to lay before us with as little delay as possible the
further results of his extended researches into the fossil Testacea of
the Paris Tertiary strata.

THE ANNIVERSARY ADDRESS OF THE PRESIDENT.

GEeNTLEmMEN,—I now come in the fulfilment of my duty to that
part of my task which, necessary as it is, must always be one of the
most painful services which your President has to perform. I mean
the recalling to your notice the most distinguished Members of the
Society whom we have had the misfortune to lose during the pre-
ceding year. And I deeply regret that I have to state that our losses
during the past year have been unusually great; great, not only as
regards the members we have lost, but more particularly so with
reference to the high position, both in the world of science as well as in
this Society, held by many of those who have ceased to move among us.
It is no small matter to have to record in one year the loss of such
men as George Bellas Greenough and Henry De la Beche, the one
remarkable for his zealous and faithful attention to the interests of
this Society from the very first day of its existence, and the other
for his success in founding and permanently establishing what has
been justly called the first palace ever raised from the ground in
Great Britain which is entirely devoted to the advancement of science.

GrorGe BevLuas GREENOUGH was born in 1778, and had con-
sequently attained his seventy-seventh year when he died. His

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXVI

father, who was a proctor in the ecclesiastical courts, died when the
son was but two years old, nor did his mother, who was the daughter
of Mr. Greenough, an eminent surgeon-apothecary, long survive her
husband, leaving her only son to the care of his grandfather, an
accomplished classical scholar. To his care and instruction Mr.
Greenough was wont in after years to attribute much of his success
in life, and that taste for laborious study which he began to manifest
at a very early period. He was sent to school at an early age, and
when nine years old went to Eton. His grandfather died while
George Bellas was still at school, leaving him a considerable fortune,
under the guardianship of Mr. Hunt, and desiring him to add to his
paternal name that of Greenough.

In 1795 he entered Pembroke College, Cambridge, and resided
there for nine terms consecutively, but he never took his degree, and
in 1811 he removed his name from the college books. In 1798 he
proceeded to Géttingen for the purpose of prosecuting his legal
studies. Here, however, it would appear that the study of natural
science, under the celebrated Blumenbach, had more attractions for
his inquiring mind than the Pandects and Institutes of Justinian.
Having been advised to attend the lectures of this distinguished
naturalist, to the attractions of which I can myself bear witness, he
determined to abandon the law and to devote himself thenceforth
to the pursuit of natural history and its cognate sciences. An inter-
leaved copy of Blumenbach’s ‘ Institutiones Physiologice’ contains
copious notes by Mr. Greenough, showing with what zeal and in-
dustry he followed his instructor’s lectures. He afterwards studied
mineralogy at Freiberg under Werner, and adopted his views on
geology, which he continued to hold for many years. From thence
he visited the Hartz Mountains and other mining districts of Ger-
many, and, after spending some time in Germany, Italy, and Sicily,
he returned to England in 1801, when he visited Cornwall and the
Scilly Islands.

From that time until 1807 he was actively employed as a Member
of the Royal Institution, attending lectures on chemistry, working in
the laboratory, and with Chenevix, Wollaston, Davy, Babington, and
others, endeavourmg to promote the progress of science in all its
branches. In 1806 he visited Ireland in company with Mr. R. Hutton,
and although principally occupied with geological investigations, he
took a deep interest in the political state of that country, and in
making himself acquainted with those important social questions
which were then agitatmg men’s minds. In 1807 he was returned
to parliament for the borough of Gatton, for which he continued
to sit until the dissolution in 1812. But the pursuits of science
were more congenial to his tastes than politics, and in the very year
when he was first returned to Parliament we find him actively en-
gaged in promoting the study of geology. In that year he succeeded
in associating with himself several active and able advocates of the
then infant science, the result of which was a proposal to found a
new society for the furtherance of geological and mineralogical
science. A printed list of geological queries was issued, and

XXVill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

regulations for the management of a new society were discussed and
arranged.

For some time before the period to which I am now alluding, a
warm interest for the sciences of Mineralogy and Mining had sprung
up among some of the leading men of science in England, which had
led to the formation of several valuable mineralogical collections.
Availing himself of this growing feeling, Mr. Greenough exerted him-
self to give a practical direction to the efforts of scientific men by the
establishment of a new Society for the cultivation of mineralogical
and geological science in a more special manner than that in which
it was entertained at the Royal Society.

But Mr. Greenough could hardly have anticipated the difficulties
of the task he had undertaken. During this and the two following
years the opposition of Sir Joseph Banks, the President of the Royal
Society, seconded by that of other influential members, threatened
the existence of the new Society. They opposed the formation of a
Society which they imagined would encroach on the province and
impair the dignity of their own, and no means were omitted for the
purpose of endeavouring to crush it. Several of the Fellows who
had originally joied withdrew their names, Davy amongst the num-
ber. Mr. Greenough calmly but fearlessly resisted their efforts.
He endeavoured to conciliate matters by every means in his power.
He pointed out to Sir J. Banks the true objects of their intended
action; with his own hands he drew up a list of the subjects which
it was intended to make the objects of inquiry, and promised that any
papers he desired should be freely placed at the disposal of the Royal
Society. But all in vain; the hostile feeling could not be overcome.
Still Mr. Greenough was unshaken, and when the Royal Society
endeavoured to compromise matters by offering to make the Geo-
logical a branch of the Royal, and proposed that the papers read in
the Geological Society should be subject to their control and be pub-
lished in the Transactions of the Royal, Mr. Greenough and his
friends who acted with him calmly but steadily stood their ground,
and finally succeeded in asserting the complete independence of the
Geological Society.

Nor should it be forgotten that, although much warmth was eli-
cited in these discussions, Mr. Greenough never lost a friend. At
length, all obstacles having been overcome, the Geological Society
(first established in 1807) became regularly constituted in 1811, and
Mr. Greenough was elected the first President, an honour justly
merited by his strenuous exertions for its formation, and one which
he held for a period of six years*. In the same year the first volume
of our Transactions was published, and I may here mention that of
the first list of Council and Officers of the Society, Mr. Leonard

-Horner is now the only survivor. I need not remind you that

during the long lapse of intervening years Mr. Horner has ever been
the steady friend of this Society. May he long be spared to us, and
long continue to be the connecting link between the present genera-
tion of geologists and the first founders of the Society.

* Dr. Bostock’s Address; Mareh 1826.

ANNIVERSARY ADDRESS OF THE PRESIDENT. Xx1X

From this period to the last hour of his life Mr. Greenough was
actively employed in forwarding the interests of this Society, and in
advancing the progress of geology and physical geography. He was
unceasingly occupied in increasing his valuable collection of maps,
and in entering on them and in his numerous note-books all the
geological data which he could obtain either from books or from the
communications of scientific travellers. But notwithstanding his
vast collections and his numerous and elaborate notes on every sub-
ject connected with mineralogy, geology or physical geography, Mr.
Greenough was not a great writer. No memoir from his pen, except
his presidential addresses, has been published Py any of the learned
Societies to which he belonged.

About this period, also, Mr. Greenough was made an Honorary
Member of most of the scientific societies of the United Kingdom ;
and, notwithstanding the war with France, he received in 1809 the
diploma of Honorary Member of the Agricultural Society of Bou-
logne. During the next succeeding year he was actively employed
in pursuing his geological explorations in various parts of Great
Britam and Ireland, preparing for that great work which he was
already contemplating, the Geological Map of England. In 1814
he started for Paris the very day after the Treaty of Peace was
signed. Soon afterwards the state of his health, brought on probably
by severe mental and bodily exertions, compelled him to take up his
residence at Cheltenham ; but in 1818 he was again elected President
of this Society.

In 1819, after years of labour in the collection of the materials
and the arrangement and construction of his work, he published his
Geological Map of England and Wales, in six sheets, with an accom-
panying memoir, compiled from an extensive collection of maps and
surveys. In order to render this work as perfect as possible, Mr.
Greenough spared no efforts, and was equally willing to avail himself
of the information collected by his numerous geological friends as by
himself. He ever retained a grateful sense of the. pecuniary assist-
ance given him by Mr. Warburton, who had at one time contributed
as much as a thousand pounds towards the work, a great portion of
which, if not the whole, was subsequently repaid.

In the same year Mr. Greenough published the only work on
geology which issued from the press under his own name, and when
we consider the talent shown in this work, the ingenuity displayed in
controverting those geological theories which he considered injurious
to the science, and at the same time recollect the mass of information
he had collected, and the systematic way in which it was arranged in
those many MS. volumes which must be well known to all who had
the good fortune to be intimately connected with him, we cannot
but regret that Mr. Greenough should not have made more use
of his materials, and have devoted some portion of his time to the
publication of Principles of geology better adapted to the progress of
the science within the last ten years than the work to which I am
now alluding. Under the title of ‘ A Critical Examination of the
First Principles of Geology,’ in a series of essays, Mr. Greenough

XXX PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

proposed to refute many of the popular theories of the day, and
appears to have directed the great weight of his logical argument
against the followers of the Plutonian theory.

At the same time it must be admitted that, notwithstanding the
shrewdness and success with which many of the crude notions of
former days are disproved in these essays, Mr. Greenough has not
unfrequently brought forward statements-and advanced arguments
which could hardly have been expected from one who had studied
his ‘“collegium logicum” at the University of Gottingen. Take
for instance that passage in allusion to the great extent of time re-
quired by the Plutonists for the performance of many operations,
and which to modern geologists does not appear to be an unreason-
able request :—

“Ye gods, perpetuate Time! says the Plutonist, and thinks his
reasoning will be incontrovertible. But suppose the prayer granted ;
suppose the Plutonist to have at command whatever time he desires ;
Time graduating into Eternity ; nay Eternity itself; what use could
he make of it? What profit can a man expect from putting zeros
out to interest? What increase of weight from a Fast sufficiently
prolonged? If seas and rivers do not tend to produce within the
period of human experience any such effect as that which we are
endeavouring to account for, they will evidently produce no such
effect in a million of centuries. Time may complete that which is
im progress, it will never complete that which can never be begun.”
As a general remark too, it may be stated that this work of Mr.
Greenough’s was intended to refute what he considered objectionable
theories, rather than to lay down what aYED to be the principles of
geological investigations.

An excellent review of this work will be found in the pages of the
Edinburgh Review (vol. xxxiii. p. 90), where it is stated, “'The work
before us contams an admirable digest and collation of the most
authoritative statements and opinions on a great variety of important
questions, but is eminently calculated by the contradictions which it
everywhere exhibits to abate the confidence of narrow observers and
rash theorists, and to inculcate the necessity of that patient industry
and modest scepticism by which alone the pursuits of geology can
ever obtain the dignity of a science.”

Excursions at home and on the Continent continued to occupy his
active mind in the relaxation from those periods of hard labour
which are demanded at the hands of a man of science. Mr. Green-
ough for some time occupied u house in Parliament Street, but in
the year 1822 or 1823 the expiration of his lease compelled him to
seek another residence, and he took from Government a lease of
ground in the Regent’s Park, and commenced building that house
which he knew so well how to fill and to adorn, and where we all
enjoyed his hospitality and kindness. In this employment he had
an opportunity of indulging his taste for architecture, to which he
had paid great attention for many years. In 1826 he took a great
interest in, and was one of the most active agents in obtaining for the
Geological Society, that Charter of which “he was one of the first

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXX1

trustees ; and in 1831 he was interested, with Sir R. Murchison and
others, in the establishment of the British Association for the Ad-
vancement of Science, and took. an active share in all the scientific
institutions of the metropolis. In fact he was ever busy, ever occu-
pied in promoting, both by his own exertions and by liberal pecuniary
assistance, whatever measures were necessary for the advancement of
science. Many individuals, as well as our own Society, can bear
witness to Mr. Greenough’s liberality. From 1833 to 1835 he was
again for the third time President of this Society, and, as usual,
most active in promoting its prosperity, as well as harmony and good
fellowship amongst its members.

One of his most favourite pursuits, and on which his fame will
mainly rest, was his skill in the construction of important physical
and geological maps. In consequence of the great progress made
in the investigation of English geology during the last twenty
years, a second and greatly improved edition of his Geological Map
of England and Wales was engraved in 1839, the copyright of
which has, with Mr. Greenough’s accustomed liberality, been pre-
sented to this Society. But Mr. Greenough was not only a man of
science, he also possessed a remarkable taste, and a good eye and
feeling for colour, and it is generally admitted that the harmony
with which he has contrived to blend together the various colours
by which the different geological formations are distinguished is
not the least of the many merits of this Map. In 1852 he was
enabled, from the vast stores of information he had accumulated, to
lay before the Asiatic Society, in illustration of a memoir by himself,
a series of maps of Hindostan defining all the important elements of
the ten water-basins of that peninsula ; and in 1854 he exhibited be-
fore the Asiatic Society and at the last meeting of the British Associa-
tion at Liverpool his geological map of India on a large scale, which
has since been published under the title of ‘ General Sketch of the
Physical Features of British India.’ With regard to this last pro-
duction, the gigantic effort of his declining years, I cannot better
do justice to the subject than by quoting to you a passage from one
of the Addresses of our former President, Sir R. I. Murchison, when
addressing the Royal Geographical Society as their President in
1853*, previously to the publication of this map :—

“Let me now direct your attention to the last year’s labours of
the veteran geographer and founder of the Geological Society of
London, my valued friend Mr. Greenough. Whenever the day
shall come—(and may it be far off!)—when the person occupying
this chair shall be called upon to treat of the labours of this distin-
guished man, then will there be poured forth an enumeration of his
works which will satisfy mankind that in this generation no indi-
vidual among us has accumulated greater stores of geographical and
geological knowledge ; and that no one has made greater efforts to
generalize detached data, and group them together for the benefit of
our race. On this occasion it only behoves me to speak of one of

* Journal of the Royal Geographical Society, vol. xxiii. pp. cvil. and cvili.

XXXil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

his last efforts, or that of the illustration of Hindostan, as put forth
in maps exhibited before the Royal Asiatic Society. Defining on
one of these, each of the ten water-basins of the peninsula, and
noting all their affluents, and the number of square miles drained by
each, he read a valuable memoir to the Asiatic Society. Another
work, and that to which I now particularly advert, is a grand original
physical and geological Map of all India, about 7 feet long and 53 feet
wide, which he has prepared himself, directing the insertion of every
stream and hill, and sedulously consulting every authority for the
geological attributes of each district between the plateaux N. of the
Himalaya and Cape Comorin. On this Map the spectator sees the
delineation of coal-tracts, the larger portion of which are unques-
tionably of tertiary age, and not like the old coal of Europe and
America; the range of the diamond-deposits ; the vast territories
occupied by granitic and eruptive rocks ; the demarcation of masses
of secondary age, in which the cretaceous deposits of the age of our
chalk play so subordinate a part, whilst the nummulitic formation,
or oldest tertiary, has so grand a development, particularly in the
north ; the Silurian and other palzeozoic rocks also being only known
in the north-western extremity of the Punjaub and im the Himalaya
mountains.

‘Such a labour of love as this on the part of such a man seems to
me to call not only for the special acknowledgments of all geogra-
phers and geologists, but also for the approbation of the Board of
Control and Directors of the East India Company, who would do
real service by publishing this great map, and thus render the name
of Greenough as well known in our Eastern Empire as it is in
Europe.” 7

It is, perhaps, hardly possible to estimate the difficulties with which
Mr. Greenough had to contend in preparing this map. It was com-
menced in 1843. Information came in but slowly, and had mostly
to be sought for in the archives of the India House. Frequently when
obtained its application was next to impossible from the nature and
imperfection of the maps, or it was valueless from the ignorance of the
observer. In 1849 Mr. Greenough almost despaired of carrying out
his object, and felt tempted to give up the work which had cost him
so much labour. He was, however, urged to persevere by the accom-
plished lady who had assisted him in his work, and who took the
greatest interest in its completion*. Fresh information at length
poured in, chiefly through the assistance of Col. Sykes, and in 1854
the work was completed.

After the publication of this map, with an energy almost unparal-
leled, Mr. Greenough, at the age of 76, started for Italy and the
East with the view of making further researches, and of connecting
his Eastern labours with the geology of Europe. But the complica-

* His niece, Miss Colthurst (now Mrs. Greer), had lived for many years in his
house during the latter part of his life, and rendered him important services. In
testimony of his regard and affection for her, Mr. Greenough bequeathed to her
care all his MSS., and I am indebted to her for much of the information con-
tained in this memoir.

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXIl1

tion of disease which had for years been undermining his constitution
again developed itself in Italy, and compelled him to remain at Naples,
where an attack of dropsy terminated his long and laborious life on
the 2nd of April, 1855.

But his services to this Society did not cease with his life. By his
will he has bequeathed to the Geological Society of London his valuable
geological library and that portion of his collection of maps on which
he had recorded his geological observations. ‘The number of books and
pamphlets comprised in this bequest considerably exceed a thousand
volumes, and the maps are contained in upwards of 60 cases.
Amongst these are many important works connected with our science
which will greatly enhance the value of our library. He liberally
accompanied this bequest by a sum of £500 to enable us to arrange
the books and maps in such a manner as to render them most useful
and easy of access.

Let me conclude this imperfect notice with a few additional remarks.
No one who has been in the habit of attending our Evening Meetings,
in the discussions. at which Mr. Greenough ever took an active and
important share, can have left this room without admiring the multi-
tudinous and varied mass of information which he was enabled to
bring to bear on every subject brought under our notice. And, al-
though we are here specially called upon to do honour to his memory
as a geologist, it must also be borne in mind that Mr. Greenough was
a distinguished Fellow of the Royal Society, and one of the most
active supporters of the Royal Geographical and Ethnological
Societies. The occupations connected with these two Societies
naturally brought him imto direct contact and acquaintance with
every corner of our globe which had been reached by the inquiries
of science or by the pursuits of commerce and of civilization. At
the same time, as a member of other important scientific societies,
Mr. Greenough had amply availed himself of every opportunity
of storing his mind and of enriching his retentive memory with a
vast mass of varied information, which he was ever ready to pour
forth, in private or in public, on any necessary occasion. And.
if at times his arguments appeared paradoxical, and he himself dis-
posed to be sceptical with regard to newly propounded views and
theories, let it never be forgotten that all was done through a sincere
desire of truth. Mr. Greenough’s turn of mind was eminently prac-
tical, and he was ever reluctant to believe anything that was not
capable of being proved. But when once convinced of truth no one
was more ready to yield to its conviction. Although long refusing
to adopt the new principles of geology founded on palexontological
evidence as distinguished from the mineralogical evidence of the older
school, he was among the first to form a collection of fossils, and
fully admitted the importance and the truth of the geological theories
as deduced from the study of fossils and the investigations of palzeon-
tology.

Nor can I omit, in enumerating the merits of Mr. Greenough, to
mention that to him we are mainly indebted for the great progress
made recently in the science of physical geography, a branch of

XXXIV PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

science singularly neglected until a very recent period, and which
forms the lnk between geology and geography. Mr. Greenough
was one of the first to recognize the necessity of an accurate delinea-
tion of the physical features of a country before we can attempt to
lay down with any certainty the results of our geological investiga-
tions. It was in carrying out these views that he endeavoured to
give a more scientific character to the proceedings of the Royal Geo-
graphical Society, and to enlist in its favour the suffrages of the
geologist and the mineralogist, as well as those of the politician and
the traveller. |

And since we no longer enjoy the benefit of his presence, let us
look with a higher degree of admiration and respect on that bust of
him by Westmacott which we possess in these rooms, and, while thus
contemplating the features of our first President and the Founder of
our Society, endeavour, in our scientific exertions, to emulate his
energy no less than that singleness of purpose, which was one of his
greatest characteristics.

A short twelvemonth has scarcely passed away since I had occa-
sion to announce from this Chair the award of the Wollaston Palla-
dium Medal to the late Director-General of the Museum of Practical
Geology. It is now my duty to allude to him as one of our associates
whose loss we have to deplore. On that occasion I noticed some of
the passages in his scientific career which had established his claim to
the honour then conferred on him; at the risk of repetition I must now
again allude to some of the same circumstances.

Henry Tuomas De ta Becue was born in 1796. After losing
his father at a very early age, he resided for several years with his
mother in Devonshire, then at Charmouth, and afterwards at Lyme
Regis, where the cliffs teeming with the remains of former life appear
to have first drawn his attention to those pursuits which he subse-
quently so successfully and zealously cultivated. We have thus
another instance of the influence of early associations in directing the
mind to those studies by which so many scientific men have after-
wards distinguished themselves. ‘The southern shores of England
soon became classic ground for the geological student; and, with
hammer and note-book in his hand, Henry De la Beche was one of the
first to unfold the mysteries of that portion of the primeval history
of our globe which was written in such indelible characters on the
coasts of Dorsetshire and Devon.

Followmg the profession of his father he entered the Military
School of Great Marlowe in 1810. Here he first exhibited those
powers of the pencil and that facility of sketching the physical
features of ground which so materially favoured his success in his
subsequent pursuits and occupations. But his military career was
short, and, notwithstanding the charms of society, to which he was
by no means insensible, his active and inquiring mind eagerly
sought for a more energetic and independent sphere of action than a
military career could then afford, when the general peace of Europe
condemned our armies to comparative inaction.

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXV

At the early age of twenty-one Mr. De la Beche entered the
Geological Society in 1817. But far different was the position
of the Society at that time from that which it has acquired in these
palmy days. Scarcely ten years in existence it was still struggling
against the attacks of two opposite parties, and was still in danger of
collapsing from the rude efforts of two opposing forces. Churchmen
on the one hand, with a short-sightedness which we can now scarcely
credit, dreaded the effects of the unanswerable truths it put forth,
while philosophers on the other hand looked down upon the young
but energetic band as deserters from the parent body, settmmg a dan-
gerous example to those inquirmg minds who dared to believe that
science required an ampler field than the apartments of the Royal
Society. But time wore on, and Henry De la Beche was one of
the most ardent promoters of the rising Society, which has shown
that true religion has nothing to fear from the investigation of truth,
and that science can best prosper by the establishment of new
institutions specially devoted to the pursuit of separate branches of
scientific Inquiry.

From this period Mr. De la Beche was a constant frequenter of
the Meetings of this Society, taking an active share in its discussions
and visiting with advantage and observation different portions of the
continent of Europe. He resided for some time in Switzerland and
parts of France, cultivating the acquaintance of the most distin-
guished scientific men of those countries, and sedulously applying
himself to the study of the natural phenomena so grandly exhibited
in the Alps. Some of his observations on the depth and tempera-
ture of the Lake of Geneva were published in the “ Bibliotheque
Universelle’’ for 1819, and in the “ Edinburgh Philosophical
Journal”’ for 1820, together with much valuable information respect-
ing the transport and deposit of detritus in seas and lakes. In 1824
he visited his paternal estate in Jamaica, and while attending with
exemplary zeal to the management and improvement of his property
he neglected no opportunity of collecting geological information, the
result of which was the publication in our ‘‘ Transactions” of that
able memoir containing the first information we had received respect-
ing the geological structure and formations of that island. Nor
must it be forgotten that while cultivatmg Geology in its more
attractive forms Mr. De la Beche was one of the few geologists of
our country who pursued with equal zeal the study of Mineralogy.
He was a first-rate mineralogist, and owed no doubt in a great mea-
‘sure to this circumstance much of that success which, in another
sphere, distinguished his subsequent career.

Having already alluded on a former occasion to the valuable con-
tributions to our “Transactions” from the pen of Sir Henry De la
Beche, I will now only briefly recapitulate the titles of those memoirs.
1. “On the Geology of Southern Pembrokeshire.” 2. “On the
Lias of the Coast in the vicinity of Lyme Regis, Dorsetshire.
3. “On the Chalk and Greensand in the vicinity of Lyme Regis,
Dorsetshire, and Beer, Devonshire.” 4. ‘‘ Remarks on the Geology
of Jamaica.” 5. “On the Geology of Tor and Babbacombe Bays,

XXXV1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Devonshire.” 6. “On the Geology of the Environs of Nice and the
Coast thence to Ventimiglia.”” And 7., in conjunction with Dr.
Buckland, ‘On the Geology of the neighbourhood of Weymouth
and the adjacent parts of the Coast of Dorset.”? But while thus
engaged in collecting and describing the facts which came under his
observation, he did not neglect the more abstruse and speculative
branches of the science. From his numerous observations in differ-
ent regions, he arrived, by a sound and energetic system of induction, |
at many of those theoretical views which give a charm to his subse-
quent writings, and may in fact be said to have laid the foundation
of the present school of geological philosophy.

But besides these numerous memoirs in the “ Transactions” of
our Society and others in the ‘ Philosophical Magazine,’’ the
“Annals of Philosophy,’ and other scientific journals, his first
distinct volume appears to haye been a translation, with notes, of
a selection of Geological Memoirs from the ‘‘ Annales des Mines.”
In 1829 he published in 8vo. ‘A Notice on the Excavation of
Valleys,’ ‘Sketch of a Classification of European Rocks,’ and ‘ Geo-
logical Notes;’ and in 4to a valuable series of forty ‘ Sections
and Views Illustrative of Geological Phenomena,’ which has long
been out of print.

In 1831 he published the first, and in 1832 the second edition of
‘The Manual of Geology,’ a work of which it is not too much to
say that it not only offers to the geological student the most perfect
view of the then state of geology, but that, with the exception of
some slight modifications rendered necessary by the subsequent rapid
progress of palzeontology, it is one of the most philosophical intro-
ductions to the science ever published.

But Mr. De la Beche did not stop here. In 1834 he published a
still more valuable and important work. The ‘ Researches in Theo-
retical Geology’ is a work of the highest order of merit, and, indicat-
ing as it does a thorough knowledge of several branches of science,
was the admiration of all his associates; it also exhibits those
powers of mind and sound reasoning which enabled him soon after-
wards to rise to that station which he filled with so much advantage
to his country and with such credit to himself. It is impossible to
read a single page of this interesting volume without being struck
with the internal evidence it affords of the intimate acquaintance of
the author with the various branches of physical science. Chemistry,
Physics, Mineralogy, Zoology, and Mathematics are all brought
forward at the proper moment and in due proportion in elucida-
tion of the author’s views; and we hardly know which is most
deserving of our admiration, the clear and comprehensive form
in which the various topics are brought forward, or the keen and
sagacious judgment with which they are sifted and considered,
and conclusions are drawn from the varied and well-described
pheenomena.

But a new epoch in his career was now commencing, and his own
exertions were to lay the foundation of a great national institution.
During his many visits to the mining districts of Cornwall he con-

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXViI

ceived the idea of a geological map of that interesting region, and
carried out the bold suggestion by commencing, single-handed, at the
Land’s End, this undertaking, which he contemplated extending by
degrees over the entire country. Backed by the support of scientific
friends, the Government of the day wisely resolved that this mineral
delineation should form a part of the Ordnance Survey under Colonel
Colby, to which Mr. De la Beche was consequently attached.

I need not here stop to narrate all the gradual steps by which,
from this small beginning, the plan of Mr. De la Beche ripened into
that flourishing institution, which is now one of the chief scientific
ornaments of this metropolis. With but few assistants in the first
instance, and traversing many thousand miles with hammer in hand,
he produced maps which have been the admiration of all who have
had occasion to consult them, and laid the foundation of that geolo-
gical survey of the United Kingdom, which is destined not only to
enhance the value of our science, but to unfold the vast mineral
riches which lie concealed beneath the surface of our country. By
degrees the rapid accumulation of materials, minerals, rock speci-
mens, and organic remains rendered necessary the establishment of a
museum where they might be placed, preserved, and consulted ; and
then arose the idea of forming a complete Geological Museum of
the British Isles, at the head of which could be placed no more
worthy individual than he from whom the first idea had originated,
and the appointment of Mr. De la Beche as Director of the Museum
of Economic Geology was universally hailed with approbation. And
when the small building in Craig’s Court could no longer contain
the treasures which had been collected, the voice of the nation
liberally responded to the appeal of science, and then, to use the
expressive words of Sir Roderick Murchison, ‘ arose, and very much
after the design of the accomplished director himself, that well-
adapted edifice in Jermyn Street, which, to the imperishable credit
of its author, stands forth as the first palace ever raised from the
ground in Britain which is entirely devoted to the advancement of
science.” 3

These are words which, in speaking of Sir H. De la Beche, ought

never to be forgotten, and I am sure I need make no apology for
repeating them on this occasion. In fact I would willingly have
repeated every word used by Sir R. Murchison on that memorable
occasion, but I can only refer you to them. We all know the success
which attended the establishment of this Institution; the School of
Mines which was attached to it; the able band of scientific men,
naturalists, geologists, palzeontologists, chemists, and mineralogists,
~whom he collected around him, and who assisted him in this great
national work ; and finally, after the close of the Great Exhibition in
1851, to which he also devoted his attention as the chairman of a
jury, the realization of his long-cherished scheme of making the
Museum of Practical Geology, as it was then to be called, available
for educational purposes. This was done by the establishment of
courses of: lectures, with the main object of teaching to the miner
and the smelter those applications of science which they required,
VOL. XII. ee

XXXVIIl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

while at the same time they should be sufficiently general in their
nature to suit persons not interested in mining or metallurgical
pursuits.

In his maugural discourse on the opening of the School of Mines
and of Science applied to the Arts, Sir Henry De la Beche explained
the history and the objects of the Institution, which had for twenty
years been his constant thought, but few who heard him on that
occasion could form any adequate idea of the difficulties with which
he had had to contend, and which he had so successfully overcome.
But during this busy period of his life, his exertions were not con-
fined to the Museum of Practical Geology. In 1847, Sir Henry De
la Beche was elected President of this Society, and I need only appeal
to the recollection of those who were then Members of it, for a con-
firmation of the statement, that, in his discharge of his presidential
duties, he fully realized the anticipations which had been held out
to us.

In 1853 he published the second edition of his work, called the
‘Geological Observer,’ in which the materials of all his former
writings are worked up into a definite shape. Originally founded on
a smaller work called ‘How to observe in Geology,’ the object of
this new publication was to afford a general view of the chief points
of the science, to assist beginners, and to show how the correctness
of observations may be detected, and to sketch the direction in which
they may apparently be extended. |

But success had scarcely crowned his efforts at the period of the close
of the Great Exhibition in 1851, ere the first symptoms of that disease,
which removed him from the scene of his labours, began to be deve-
loped. Before the end of that year, partial paralysis attacked him,
producing at first only a slight lameness, yet gradually and slowly

undermining his strength. During the three following years, the

gradual progress of disease was too painfully evident to his friends.
His strength was slowly wearing away, but his healthy tone of mind
and keen penetration remained unimpaired. For the last few months,
although his limbs refused their proper work, he was daily carried to
his office, the business of which he superitended with the same
energy and vivacity as before, and was actually engaged upon it only
thirty-six hours before his death, which took place on the 13th of
April, 1855.

That the great merits of Sir Henry De la Beche were fully appre-

ciated both at home and abroad, the many honours conferred on

him are a most convincing proof. Knighted by his Sovereign, he was

also a Knight Commander of the Danish Order of Dannebrog, and

of the Belgian Order of Leopold; he was a Correspondent of the In-
stitute of France, and a Member of various Foreign Academies, and
of numerous scientific bodies at home and abroad..

Tuomas WEAVER was born in 1773. He was long a distin-
guished and active Member of this Society, particularly in its earlier
days. He was also one of that band of scientific men, who, with
Jameson, Humboldt, and Von Buch, learnt the first rudiments of

le

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXIX

mineralogy and geology under the tuition of Werner at Freiberg,
where he commenced his studies in 1790. Although he had for
many years retired from the active field of science, the ‘‘Transactions”’
both of the Royal and of our own Society bear witness to the labours
of his early life. Amongst his communications to this Society, I
must particularly mention the Memoir published in the First Volume
of the Second Series of our ‘“‘ Transactions,” entitled ‘‘ Geological Ob-
servations on part of Gloucestershire and Somersetshire;’’ and
another “On the Geological Relations of the South of Ireland.” He
died at his residence in Pimlico on the 2nd of July, 1855.

The Rigut Hon. Sir H. Exxis, K.C.B., was brother to the late
‘Charles Ellis, Esq., formerly consul at Tangiers. At an early period
of his life he embraced the diplomatic profession. He accompanied
the Earl of Amherst to China in 1792, and published ‘an account
of the Embassy. Having been wrecked on his return with the
ambassador, they escaped to Java in an open boat, after a perilous
voyage of several hundred miles. In 1814 he was appointed Minister
Plenipotentiary to Persia, from whence he returned with a treaty of
peace. In 1835 he again went to Persia in the same capacity, but
having returned in the following year, he was soon afterwards sent
on an extraordinary and secret mission to the Brazils in 1842. It
was during his stay in this last country that he forwarded to this
Society the interesting collection of fossil bones which were subse-
quently described by Professor Owen.

Amongst the distinguished statesmen who have been Members of
this Society, the name of Str Witt1am MoLeswortH must not be
forgotten. Chiefly remarkable for his literary and political acquire-
ments, to which, highly as we appreciate them, I have at present no
occasion to allude, Sir William Molesworth, after an honourable
career in the House of Commons, was, on the formation of Lord
Aberdeen’s administration in 1853, appointed to the office of First
“Commissioner of Public Works. In this capacity Sir W. Moles-
worth had to consider the important question of the juxtaposition of
the Scientific Societies in one building. What the scheme would
have ended in, had it not been for the breaking out of the war, it is
difficult to say ; but this I am bound to mention, that the accommo-
dation of the Geological Society in a central position, m a building
suited to its wants, and in close proximity to other scientific societies,
would have found in Sir W. Molesworth, so far at least as the space
or means at his disposal would have permitted, a warm and zealous
advocate. |

As Colonial Minister again, a post to which he subsequently suc-
ceeded, the career of Sir W. Molesworth would not have been indif-
ferent to the Geological Society. Our investigations now extend
over most of the British Colonies, in many of which geological in-
quiries have been set on foot, and are carried on by the Home or
Colonial Governments. From many of these, in Canada, in Austra-
lia, in Ceylon, and in Africa, we have received during past years

2

et |

xl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

much valuable information, and we consequently look with a more
than common interest to the past career and qualifications of the
minister who holds the seals of the Colonial Office. Unfortunately
Sir William Molesworth’s tenure of office was too short to enable him
to carry out his long-matured plan of colonial government, which,
while developing the resources of the Colonies, would at the same
time, we trust, have laid open their productions in natural history,
and their mineral and geological wealth.

Lewis Weston Dituwyn was another of that band of natu-
ralists whose loss we have to deplore, and who was one of the oldest
Members of this Society. Born at Ipswich in 1778, he was placed
by his father in 1801 at the head of the celebrated manufactory of
Cambrian Pottery at Swansea. Under the influence of Mr. Dillwyn’s
taste for natural history, this establishment soon became remark-
able for its beautiful and no less faithful paintings of birds, butter-
flies, shells, and flowers. About the year 1814, this manufactory
became known for the high character of its porcelain ware, under the
name of Swansea China. This high degree of excellence was in a
great measure owing to the introduction of a Kaolin of a superior
quality, brought from the beds of decomposed granite in Cornwall,
remarkable for its great abundance of felspar.

But natural history in its various branches was ever the chief
pursuit of Mr. Dillwyn. In 1802 he published the first part of his
work on the British Confervze, and in 1804 he was elected a Fellow
of the Royal Society. In 1805 he published, with the assistance of
Mr. Dawson Turner of Yarmouth, ‘The Botanist’s Guide.’ In 1817
he printed in two thick volumes a Descriptive Catalogue of Recent
Shells, arranged according to the Linnzan method. Nor did Mr.
Dillwyn confine his attention to the zoology of recent times. An
enthusiastic admirer of the then rapidly developing views of geology,
he communicated to the Royal Society, in the form of a letter
addressed to Sir Humphry Davy, a paper on Fossil Shells, which
was printed in the Philosophical Transactions ; and in the same year,
he presented to the University of Oxford an Index to Lister’s * Hi-
storia Conchyliorum,’ which was printed at the Clarendon Press.
In 1824 he addressed a second letter to Sir Humphry Davy on Fossil
Shells, in which he already pointed out that the gradual approxima-
tion in form to recent shells first observed in the secondary strata, is
also carried on through the tertiary formations, but that it is only in
the upper crag beds that any fossil can be completely identified with
a living species.

For many years Mr. Dillwyn held an influential position both as
a politician and man of science in his adopted borough and county ;
and when, in 1848, the British Association for the Advancement of
Science held its Meeting at Swansea, Mr. Dillwyn, as one of its Vice-
Presidents, and as President of the Section of Zoology and Natural
History, was one of the first to weleome its most distinguished mem-
bers with a genuine and hearty hospitality.

ANNIVERSARY ADDRESS OF THE PRESIDENT. xli

Proressor F. W. JouHnston was born at Paisley in 1796. When
he entered the University of Glasgow, he supported himself for some
time by private tuition, having learnt thus early to maintain himself
by those talents for which he was afterwards conspicuous. Having
at a subsequent period resolved to gratify his taste for chemistry, he
proceeded to Sweden for the purpose of pursuing his favourite studies
under the able teaching of Berzelius. When the Durham University
was founded in 1833, Mr. Johnston was appointed Reader in Che-
mistry and Mineralogy, an appointment which he retained until the
period of his decease. In 1843 he was elected Chemist to the Agri-
cultural Society of Scotland.

Most of his literary productions relate to the chemistry of agricul-
ture. Amongst the most important are his lectures on Agricultural
Chemistry and Geology, and the Catechism on the same science. But
his last work was the most attractive. The ‘Chemistry of Common
Life’ will be a standard work on the subjects it treats of. He was
a great traveller, and his notes on North America are well deserving
of notice. In his application of chemistry to geology, he was pecu-
liarly fortunate, and those geologists who attended the Meeting of
the British Association in Glasgow in 1842, must remember with
delight the lucid and engaging manner in which he described the
chemical change which the vegetable matter had gradually undergone
during the successive processes of transmutation, from the youngest
turf and brown coal, through various stages, down to the anthracitic
coal of the earliest beds.

He died at Durham on the 18th of September 1855, of a rapid
decline, from a neglected cold after his return from the Continent.

I regret that amongst the many Associates whom we have lost, I
can only mention the names of such distinguished men as Mr. J. H.
Vivian, Sir T. Frankland Lewis, Lord de Mauley, Mr. W. D. Saull,
Mr. E. W. Pendarves, Mr. J. Davis Gilbert, Mr. Pusey, and Mr. G.
Stephenson, many of whom were frequent attendants in these rooms ;
and, although not all active geologists themselves, they were fully
capable of appreciating the merits of our science, and took a lively
interest in the welfare of our Society.

Amongst our foreign Associates we have to regret the loss of M.
JEAN DE CHARPENTIER, Director of the Salt-works of Bex. He
was born at Freiberg in Saxony in1787. His father was Director-
General of the Mines of Saxony, and his brother, Toussaint de Char-
pentier, died three years ago, Director of Mines in Prussia. From
an early age he appears to have devoted his energies to the same
pursuits, and became a Member of the Council of Mines in Silesia.
He subsequently became Director of the Copper Mines of Baygorry,
in the Pyrenees, and in 1813, when only 26 years of age, was
appointed Director of the Salt-works of Bex. In this year he pub-
lished his first work in the French ‘ Journal des Mines,’ entitled
“Mémoire sur le Terrain Granitique des Pyrénées.’ In this work,
remarkable for its clear and methodical style, M. de Charpentier de-

xii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

scribes the various characteristic forms assumed by the granitic rocks
of the district, as well as the distribution of the primitive rocks
throughout the mountain chain.

In 1818 he read at the meeting of the Helvetic Society of Natural
Sciences at Lausanne a memoir on the observations which he had made
on the nature and position of the gypsum of Bex. This work, pub-
lished in the following year*, led to a lively discussion between him-
self and Prof. Struve, then Inspector-General of the Mines and Salt-
works of the Canton de Vaud. This discussion led the way to a
more complete examination and knowledge of the other mineral for-
mations of the country and their relations to each other, followed up
by the discovery in 1822 of an enormous mass of rock-salt, thereby
securing the permanent existence of the salt-works of Bex, the value
and produce of which were greatly increased by the intelligent manage-
ment of M. de Charpentier. He gradually abolished the desultory
and imperfect mode of working which prevailed before his appoint-
ment, introducing a system of order and regularity in the employment
of the workmen, and developing. the resources of the works in a
manner unknown to his predecessors. In 1823 he published his
‘Essai sur la Constitution. Géognostique des Pyrénées,’ a work at
which he had been laboriously employed during his residence in those
mountains ; it is accompanied by a large geological map and a view
of the Pyrenees. At the same time he had prepared another im-
portant work entitled ‘La Description des divers Procédés pour
traiter le Minerai de Fer, confondus sous le nom de méthode a la
Catalane.’

But the work which has principally served to raise the character
of M. de Charpentier as a geologist and scientific observer, is his
researches respecting the older and more recent glaciers. As early
as 1815 the attention of M. de Charpentier and M. Venetz was
directed to the glacial question, and to the possibility of glaciers having
at a former period had a far greater extension down the Swiss valleys
than at present. M. de Charpentier became gradually convinced of
the truth of these views, and in 1835 he published in the ‘Annales des
Mines’ his ‘‘ Notice sur la cause probable du Transport des Bloes
Erratiques de la Suisse,’ in which the glacial agency is admitted.
Subsequently, the discoveries of his nephew, M. Blanchet, and the
investigations of Prof. Agassiz on the scratched and polished rocks
of the Jura determined M. de Charpentier to undertake a com-
plete investigation of the whole question. The result of this inquiry
was his work entitled ‘Essai sur les Glaciers, et sur le Terrain Erratique
du bassin du Rhone,’ published in 1841.

In these and other works M. de Charpentier first called attention
to the important phenomena connected with glacial action; and,
although the discoveries of subsequent observers have thrown doubt
on some of his conclusions, and led to modifications of others, geo-
logists are deeply indebted to him for pointing out many important
facts connected with the former extension of glaciers, for his ex-
planation of their effects in wearing down and polishing the rocks

* See Meisner’s Naturhistorischer Anzeiger, Berne.

ANNIVERSARY ADDRESS OF THE PRESIDENT. xii

with which they come in contact, and for his suggestive theories
respecting the causes of the motion of glaciers. On this latter ques-
tion, rejecting, as an insufficient explanation, the gravitation theory
of De Saussure, he brought forward in conjunction with Prof. Agassiz
that theory which has been called by Prof. James Forbes the dilata-
tion theory, and which has been frequently discussed in these rooms.
And although the researches of Prof. Forbes, who gives the preference
to the so-called gravitation theory, have shown that some of M. de
Charpentier’s data are untenable, and that his theory will not account
for all the phenomena connected with glacier motion, yet when
we consider the internal structure of the glacier-ice and the granular
form it assumes, there seems some reason to believe that an expand-
ing force is produced by the tendency of the granules to enlargement,
however it may be occasioned, as evidenced by their increasing size
according to the age and duration of the ice.

In addition to these claims to our notice, I must not omit to
mention that M. de Charpentier was long known as one of the first
conchologists of the Continent. In 1837 he published in the Memoirs
of the Helvetic Society a catalogue of the land and freshwater mollusca
of Switzerland. He possessed a valuable collection of shells which
has been given to the Museum of the Canton de Vaud. He was
elected a Foreign Member of this Society in 1824, and died on the
12th September, 1855.

GENTLEMEN,—I propose in the following remarks to adhere to
the plan which I adopted when I had last the honour of addressing
you on a similar occasion, and I shall endeavour to lay before you a
general view of the progress of our science during the past year, at
the same time pointing out as well as I may be able, some of the
principal features by which that progress has been marked. I con-
ceive that such a plan will be more generally acceptable, and I am
sure that it is one in which I am less likely to fail, than if I
attempted to enter into a minute examination and criticism of some:
individual feature of geological investigation. At the same time I
feel that the task before me is one of no ordinary character. It is
beset with difficulties of the most opposite kind. On the one hand,
if we look at the various publications of Geological Societies and In-
stitutions both at home and abroad, the mass of matter to be examined
and epitomized into an address might well appal a greater literary
gourmand than myself; whilst on the other hand, however great have
been the labours of geologists during the past year, I am not aware
of any discovery of an unusual character, or of such an engrossing
nature as necessarily to attract and rivet your attention, and to
induce you to overlook the imperfections or the short-comings of this
Address. :

Our own proceedings and those of the Museum of Practical Geo-
logy and of the Geological Survey necessarily occupy our first atten-
tion ; and having mentioned that great National Institution, you will,
I trust, allow me to make one allusion in reference thereto. I have
already had occasion to mention, that but a short time had intervened

xliv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

after we had conferred on Sir Henry De la Beche the highest mark
of approbation in our power, before death deprived that institution of
its talented Director. I know that the Noble Lord, in whom the
appointment of a successor was vested, determined that he would
recommend no one to that office whose appomtment would not be
satisfactory, not only to the public, but also to the members of that
scientific corps which the late Director had collected round him.
We all know who was appointed to that vacant office. A more
popular appointment than that of Sir Roderick Murchison could not
have been made, and I am confident that you will all agree with me
when I say, that whoever else might have been a candidate for this
office, if such there were, a better Director-General than Sir R.
Murchison could not have been found. I think, too, we may fairly
congratulate ourselves, that one of the most distinguished members of
this Society, one who has so often and so ably filled this chair, has
been chosen with the unanimous approbation of his countrymen to
fill this important post. Intimately associated with Sir H. De la
Beche and conversant with all his plans, Sir Roderick Murchison is
admirably qualified to carry out and to complete those comprehensive
views and systems of arrangement which the late Director had laid
down. We may, I trust, also hope that those bonds of cordiality
and alliance which have long united these two Institutions will be
drawn closer together by this appointment, and that the Museum of
Practical Geology will ever continue to work hand im hand with the
Geological Society of London in developing the mineral resources of
the country, and in carrying out the details of those branches of geo-
logical aud paleeontographical science in which they both delight.

The publication of the third fasciculus of the work entitled “A
Synopsis of the Classification of the British Paleozoic Rocks,” by
the Rev. Adam Sedgwick, with “ A Systematic Description of the
British Paleeozoic Fossils in the Geological Museum of the Uni-
versity of Cambridge,” by Professor M‘Coy, enables me at last to
congratulate geologists, no less than Professor Sedgwick himself, on
the completion of his long protracted labours, in the appearance of a
work which adds so much to our knowledge of the Paleontology ot
the ancient rocks, while it reflects the greatest credit on its accom-
plished author.

This fasciculus contains the Carboniferous and Permian Mollusca
in the Cambridge Collection, several of which, as we are informed by
Prof. Sedgwick in the introduction, are so well preserved (especially
in the Series of Carboniferous Fossils from Lowick), that the internal
characters of the genera could be described more accurately than was
possible before on less perfect evidence.

Prof. Sedgwick explains in the Introduction the reasons why,
instead of giving the synopsis alluded to in the title-page and contem-
plated when that title-page was struck off, he has been compelled to
publish the work, with little more by way of introduction than a cor-
rected and enlarged tabular view,—resembling that which was prefixed
to the second fasciculus of the Cambridge Paleeozoic fossils. Hopes,
however, are held out that this synopsis will be completed without

ANNIVERSARY ADDRESS OF THE PRESIDENT. xiv

any unnecessary delay. The author then enters into a full and
detailed historical statement of the reasons which have delayed the
publication of the work, adding a well-merited eulogium of Prof.
M‘Coy’s merits, and of the manner in which he has carried out the
task allotted to him.

_ In the tabular view above alluded to, Prof. Sedgwick gives what
he believes to be a true geographical nomenclature of the Oldest
British Paleeozoic groups. These he separates into the three follow-
ing Divisions :—
_ I. Lower Paleozoic Division, representing the Cambrian and Silu-
rian Series in ascending groups. ‘To this is added a statement of the
same division as developed in the Cumbrian Mountains of the north
of England, giving—1, the equivalent of the Cambrian Series, and
2, the equivalent of the Silurian Series.

II. Middle Palzeozoic Division, representing the Devonian Series
or Old Red Sandstone, as developed—1, in Herefordshire and South
Wales ; 2, in Devonshire and Cornwall ; and 3, in Scotland.

Ill. Upper Paleozoic Division, mcluding the Carboniferous and
Permian rocks. |

It will hardly be necessary for me to observe, that in the first or
lowest of these divisions, Prof. Sedgwick altogether ignores the Lower
Silurian Series, and refers everything below his May Hill Sandstone
to the Cambrian Series, which he again subdivides into three groups:
first, the Longmynd and Bangor group called Lower Cambrian ;
second, the Festiniog group called Middle Cambrian ; and third, the
Bala group or Upper Cambrian. In the course of the long and

_ elaborate Introduction, with its accompanying Supplement and Post-
script, the author enters fully mto the arguments by which he
endeavours to justify this nomenclature, and which he has already

brought before this Society. I deeply regret the tone in which this

is done; nor can I believe that any amount of difference of opinion
on scientific nomenclature, even admitting that his prior claims had
been invaded by the author of ‘ Siluria,’ could justify the use of such
language as the author has employed with regard to Sir Roderick Mur-
chison and others. But Iam not called upon to discuss the question,
further than to observe, that altogether to ignore the existence of the

Lower Silurian System, adopted by the Ordnance Survey and by the
first geologists of the continent, seems to me to be doing violence to
an established nomenclature, and destroying those claims to priority
which have been so generally conceded to the author of the ‘ Silurian
System.’ It must not be forgotten, that so early as 1833 Sir R.
Murchison pointed out in the western parts of Shropshire and
Herefordshire the existence of those formations to which the term
Lower Silurian was applied inthe year 1835, and that this term of
Lower Silurian has since been unhesitatingly applied by the Ordnance
Surveyors to the vast development of the same formations which
extend through the greater portion of the regions of North Wales,
while they reserve the term of Cambrian as applicable only to the
lowest members of the series. It would be a strange abuse of
nomenclature to attempt to change the name of a formation because

xlvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the beds of which it consists are found to extend over a much larger
tract of country than was originally supposed, merely because another
name had been applied to the latter, when they were supposed to be
different from those first described and named.

I am also of opinion that Prof. Sedgwick in the course of the
whole argument has laid far too great a stress on what he calls the
natural break below the May Hill Sandstone ; this break appears to
be a mere local phenomenon, unknown in other parts of the forma-
tion, and not differing either in character or degree from similar
breaks in other countries to which such importance has never been
assigned, as e. g. in the Carboniferous Series of the Thiringer Wald.

There are, however, statements in this Introduction affecting the
character of the Council of this Society, which, in the position I now
occupy, I should not be justified in passing over in silence, however
willingly I should have preferred adopting such a course; and I trust
therefore that you will bear with me while I endeavour to refute
the unjust charge which Prof. Sedgwick has brought against your
Council *. I omit as irrelevant all notice of such vague assertions
as that “there is not one Member of the Council who, so far as
English evidence is concerned, has sifted the question to the bottom
and examined it in all its bearings... ....Some of them have dog-
matized very broadly on very narrow and erroneous knowledge,”
&c. But when Prof. Sedgwick accuses the Society of being less
truth-loving in its spirit than formerly, and states that in order to
prevent the risk of mischief, the Council seem now resolved to wage
war upon all discussions and canvassing of opinions on poits which
they themselves wish to regard as settled, 1 am bound to tell him as
temperately but as decidedly as I can, that he is altogether mistaken
as to the spirit by which the Council of this Society has been
animated. If Prof. Sedgwick during the last three or four years had
more frequently been able to come among us, and for this reason I
the more regret the state of his health which has prevented it, he
would have found on numerous occasions the same lively animation
of discussion, and the same independence of tone and spirit which he
affects to miss amongst us; and he would have found the same zeal
in the cause of truth as ever existed in former days. He would have
found that the Council had no fear of running counter to the sup-
posed interests of some scientific bodies ; that they did not wish to
suppress discussion on points which they themselves wished to regard
as settled. With regard to himself, he would have found a feeling of
respect and veneration as due to one of the fathers of the science,
and he would now perhaps recollect what he appears to have for-
gotten, that with reference to the suppression of any matter contained
in his own papers, the Council were only acting in a spirit of self-
defence, and for the interest of the readers of the Journal, when they
determined, after the controversy between himself and the author of
the ‘Silurian System’ had been carried on for some time, and the views
of both on the question of disputed nomenclature had been fully and
freely discussed, that they would not allow any more merely contro-

* See the Supplement to the Introduction. .

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlvii

versial matter to be inserted in the respective papers of either party.
This measure was directed against both authors, and not, as Prof.
Sedgwick seems to imagine, solely against himself. The only differ-
ence was, that one submitted to the wishes of the Council without a
murmur, while the other introduced into all his papers matter of a
merely controversial nature. This is the true origin of what is called
anzgnorant and bitter insult. Does Prof. Sedgwick really believe that
there ever sat at the Council Board a single Member who wished to
insult him? But I must in a few words explain what really hap-
pened. When the paper of 1852, alluded to in the Supplement
(p. xci.), was printed, it was found that matter of a highly controversial
nature, which in compliance with the resolution recently come to,
ought not to have been printed, had unintentionally been inserted.
Sir R. Murchison immediately claimed a right to reply, and gave
notice of a paper to that effect. The Council at once saw the con-
sequences which would ensue from such a course, and, wishing to
adhere to what they believed to be a wise and prudent line of conduct,
they resolved, as the least of two evils, to recal or cancel that portion of
the paper which had been printed in contravention of the rule they
had laid down. Surely no man should have looked upon such a pro-
ceeding as an ignorant and bitter insult.

I must also correct Prof. Sedgwick’s memory when he says in the
next page, that the Council refused to publish his next paper in
1853. It is true he makes no complaint. He admits that part of
it was in a controversial form. But I must remind Prof. Sedgwick
that it was only the conclusion, viz. the controversial portion, which
the Council objected to publish; the body of the paper would have
- been duly printed ; and when I wrote to inform him of this decision,
and to request his sanction to the suppression of the latter portion, the
reply which I received was to the effect that he could give no answer
until he had seen the paper again, and judged of the effect of the in-
tended omission. I directed the paper to be forwarded to him, and
after waiting many months for a reply, the only intimation I received.
of his intention was finding it already printed in another journal.
Such a proceeding was in the highest degree irregular. The paper
was the property of the Society, and Prof. Sedgwick, an old President
of the Society, must have known that he had no right to make such
use of it without having first obtained the sanction of the Council to
its withdrawal. I omit all further allusion to the matter contained
in the Introduction and its Supplement. I deeply regret that I have
been compelled to say so much in justification of the proceedings of
your Council. I will only add, with regard to the work itself, that
it is impossible to speak too highly of its arrangement, or of the
scientific description of the fossils themselves, or of the beautiful
plates by which it is illustrated.

At the last meeting of the British Association at Glasgow, Sir
Roderick Murchison read an interesting paper ‘‘On the Relations of
the Crystalline Rocks of the North Highlands to the Old Red Sand-
stone of that Region, and on the recent fossil discoveries of Mr. C.
Peach.” Availing himself of his leisure hours during the last summer

xlvill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

in re-examining the northernmost counties of Scotland, on which
twenty-eight years ago he and his companion Prof. Sedgwick had shed
much light, Sir Roderick Murchison has endeavoured to determine
the true relations of the crystalline rocks in the Highlands in which
organic remains had been discovered by Mr. Peach, to the great
deposit of the Old Red Sandstone. i

After poimting out the general characters of the crystalline rocks
of Sutherlandshire, and showing how they consist of regularly strati-
fied masses of siliceous, calcareous, and schistose bands, which are very
slightly affected by any-slaty cleavage, he affirms that the limestones
containing the fossils are really part and parcel of those ancient
masses. But whilst the organic remains seem to belong to Euom-
phali, Lituites?, and Orthoceratites, their state of preservation is too
imperfect to admit of their specific determination.

In reference, however, to their relations, he declares it to be his
belief, that they are of a date certainly anterior to the Old Red Sand-
stones, the basement conglomerates of wuich wrap round the crystal-
line rocks, are made up in great measure of their fragments, and are
seen to overlap their edges in discordant positions at several localities
in the western part of Ross-shire. The flagstones and schists of Caith-
ness, with their ichthyolites and fossil plants, are, as indicated long ago
by himself and Prof. Sedgwick, im a still higher position,

Adverting to the vast dimensions and varied composition of the.

Old Red of the northern Highland counties, Sir R. Murchison re-
asserts what he put forth prominently in his work ‘ Siluria,’ that the
great tripartite group of the Old Red Sandstone, as developed in the
north of Scotland, is a full and entire equivalent of the Devonian
rocks of other parts of Europe. :

Another interesting paper was communicated to the Geological
Section of the British Association at Glasgow, by Mr. Salter, “On the
recent discovery of Fossils in the Cambrian Rocks of the Longmynd.”
These rocks, of which the author of this paper has given a mineralo-
gical description, were hitherto considered to be azoic, and to mark
that geological period when, before the introduction of organic life,
sedimentary rocks were first deposited in the ancient seas on the
hardened surface of the earth. It would now appear, from Mr.
Salter’s discoveries, that in these most ancient beds, some small but
unequivocal traces of organic life are to be found. These traces
consist partly of numerous double oval impressions on the surface of
the ripple-marked sandy beds. They are not above a line in length,
are always placed in pairs, and parallel to one another in direction,
although scattered over the stone. As they are not placed in regular
series, they cannot indicate the track of a crustacean; they are sup-
posed to offer the best analogy with the double holes of sand-burrow-
ing worms (4renicola), and have therefore been called by the author
Arenicola didyma. Besides these, there are many distinct traces of
the presence of worms in long sinuous tracks, such as are usually
made by these animals.

But by far the most interesting fossils are several specimens of
portions of the tail, and perhaps the head, ofa new genus of Olenoid

i a ae

> ee

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlix

Trilobites, closely allied to some of the forms already known in the
lowest fossiliferous beds of America. To these fossils Mr. Salter has
given the name of Paleopyge Ramsayi. Mr. Salter then proceeds
to describe the other beds in the series which underlie the fossilife-
rous beds, consisting of shales and sandstones, in some of the lowest
of which are beds of ,conglomerate of considerable thickness (one
is 120 feet thick). These conglomerates are chiefly composed of
ae and indicate the proximity of older and perhaps volcanic
ands.

The discovery of these traces of organic life in these eld rocks, how-
ever interesting in a paleontological point of view, does not justify us
in looking on them as representing a new system or group. They do
not indicate the existence of new or unknown forms, and can there-
fore only.be considered as a further extension downwards of the
Lower Silurian formation of Sir R. Murchison. They appear to
point, however, more directly to the very commencement of organic
life, which reached a considerable development in the succeeding
strata, whatever may have been the lapse of time occupied in their
gradual deposition. It is unfortunate that they are not in a more
perfect state of preservation, since, although there can be no doubt of
their organic origin, they are in far too imperfect a condition to per-
mit any exact conclusion as to their true affinities and connexions.

An interesting communication has also been recently read at one
of our Evening Meetings, from Sir R. Murchison, ‘On the discovery
of Upper Silurian rocks and fossils near Lesmahago, in the south
- of Scotland, by Mr. Robert Slimon.” This discovery is the more
important, as, notwithstanding the extensive development of the
Lower Silurian rocks in the S.W. parts of Scotland and in Ayrshire,
the existence of these upper beds was previously unknown in Scot-
land. The descending order of the strata is well seen on the banks
of the Nethaw River, Logan Water, and other tributaries of the
Clyde. Here the lower carboniferous rocks, in which the coal-field
of Lesmahago occurs, are underlaid by the Old Red Sandstone for-
mation, which is well exposed between Lanark and Lesmahago.
Towards its base the Old Red is here marked by a powerful band of
pebbly conglomerate, while the base itself is made up of alternating
red and light greenish grey flagstones and schists. These are again
underlaid by dark grey, slightly micaceous, flag-like schists contain-
ing large crustaceans and other fossils. Considering the nature of
the organic remains, and the evident position of the beds below the
lowest Old Red, Sir R. Murchison unhesitatingly considers these
Lanarkshire strata as the equivalents of the uppermost Ludlow
rocks or the Tilestones of England*. Amongst the principal fossils
found in this uppermost Silurian rock of Lanarkshire, is a species
of Pterygotus not to be distinguished from the species so abun-
dantly found in the Upper Ludlow rock of Shropshire and of Here-
fordshire, as well as Lingula cornea and Trochus helicites. The
same deposit contains numerous crustaceans of the group of Eury-
pteride (Burmeister), which were described by Mr. Salter under the

* See Lyell’s Manual of Elementary Geology, 5th edit. 1855, p. 420.

l PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

name of Himantopterus. There are five or six species of this genus,
all of which are new, and one of which, judging from the head, which
is alone preserved, must have been 3 feet in length.

With reference to this subject, I must also notice a paper by
Mr. R. W. Banks, communicated to us by Sir R. Murchison, ‘ On
the Tilestones or Downton Sandstones in the neighbourhood of King-
ton, and their contents.”’ Besides describing the geological sequence
of these beds, and noticing the fossil contents by which they are
principally characterized, and which are remarkable for the abun-
dance of crustacean remains, the author exhibited some highly-
finished drawings of the organic remains. These, together with his
descriptive notes, indicated the existence of one or more hitherto
unknown or little understood forms of crustacean life, probably of
the Eurypteride group. Without going further into the question of
other forms of organic life contained in these beds, there appears to
be every reason for concluding that this Tilestone formation is, as
was stated by Sir Roderick Murchison, the equivalent of the fossili-
ferous band which underlies the coal-field of Lesmahago. In con-
cluding his paper, Mr. Banks says,—‘‘ From the absence of the nu-
merous Mollusca characteristic of the Ludlow rocks, and from the
presence of Crustacea that have not been found in the Ludlow beds,
and especially from the abundance of the Pterygotus, so characteristic
of the middle Old Red of Scotland, I am inclined to separate these
Downton or Tilestone beds from the Upper Ludlow rocks, and class
them (as Sir R. Murchison originally arranged them) as the bottom
beds of the Old Red Sandstone.” |

Here we have a remarkable instance of that difficulty to which I
alluded in my Address last year,—a difficulty which increases as our
knowledge of geological formations increases.’ With each advancing
step it becomes more difficult to draw precise limits between suc-
cessive formations. The following words would almost seem to have
been written in anticipation of the question under consideration :—
“It has been found that between these respective limits, as at first
laid down, certain fossils of the lower bed extend higher up into
those above; while some of those hitherto supposed to be charac-
teristic of the overlying formation are found extending downwards
into beds of an older age.” The same idea has been more fully
and more clearly expressed by Sir Charles Lyell, in his last edition
of the ‘ Manual of Elementary Geology.’ He says (chap. x. p. 112),
“The difficulty of assigning clear lines of separation must unavoid-
ably increase in proportion as chasms in the past history of the globe
are filled up.” |

Now, in the case before us, while on the one hand Sir Roderick
Murchison is prepared to regard these Lesmahago flag-like schists,
chiefly on the evidence of their fossil contents, as separate from the
Old Red Sandstone series, and to class them with the Upper Ludlow
beds, Mr. Banks, on the other hand, equally arguing on fossil evi-
dences, proposes to remove the equivalent Tilestones or Downton
Sandstones from the Upper Ludlow rocks, and to class them as the
bottom beds of the Old Red Sandstone. Under such circumstances,

ANNIVERSARY ADDRESS OF THE PRESIDENT. ah

are we not necessarily forced to the conclusion that the strata in
question represent the true passage-bed from the one formation to
the other? Must we not consider them as pointing out the gradual
steps by which Creative power advanced from one formation to an-
other? And, in observing how these and similar strata may, accord-
ing to circumstances, be classed either with the Upper Silurian below,
or with the Lower Devonian beds above, are we not warned against
that partial dogmatism, which sometimes leads us to hasty general-
izations founded on local phenomena, or on evidence derived from a
few isolated instances ?

In this case, however, it is satisfactory to find that one great
source of difficulty is removed. There is no question as to the posi-
tion of these beds. Found, on the one-hand, at the very base of
the Old Red Sandstone (if not below it),they constitute the uppermost
beds of the Upper Ludlow rocks on the other ; and the only ques-
tion which can arise is this: whether, on the strength of palzeonto-
logical evidence, it is more convenient to class them with the Silurian
or Devonian formations, of which they evidently form the connecting
link ? |

We are indebted to Mr. Sorby for another communication on a
comparatively new and complicated subject; and it is only due to
the author to say that he appears to have worked out his subject
zealously and conscientiously. In the last volume of the Edinburgh
New Philosophical Journal, he has published a paper “On the Phy-
sical Geography of the Old Red Sandstone Sea of the central district
of Scotland.”’ Mr. Sorby states that his general conclusions are, that
there is a most intimate connexion between the physical geography
of a sea and the currents present in it; and, since their directions
and characters can be ascertained from the structures produced in the
deposits formed under their influence, that the physical geography
of our ancient seas may be inferred within certain limits. He then
examines minutely the structure of the Old Red Sandstone rocks,
their strata and stratula produced by the action of currents occa-
sioned chiefly by the winds, or causes analogous to those which pro-
duce the great oceanic currents of the present day, and states the
following as the result of his investigations :—‘‘ My conclusions are,
that in the Old Red Sandstone period there extended across Scotland
a branch of the sea, or strait, whose northern shore was somewhere
in the line of the mica-schist rocks which extend from Aberdeen to
the mouth of the Clyde; and its southern in the direction of the
greywacke rocks that run across from St. Abb’s Head to Wigtonshire.
In this sea, at the earlier part of the period, there were considerable
tidal currents ; but when the upper beds were deposited, they were
more or less completely absent, and there were present such as were
chiefly due to the action of the wind.” :

Mr. Sorby has since extended his investigations to the south, and
has recently communicated to us a paper ‘‘On the Physical Geography
of the Tertiary Estuary of the Isle of Wight.” In this paper the
author has endeavoured to show, that from a knowledge of the struc-
ture of the sandy and other strata in this locality we may ascertain

|
li PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the direction and other peculiarities of the currents of the ancient
sea which covered this area during the tertiary period, whether those
currents are due to tidal action, to the winds, or to other predisposing
causes; and that with this knowledge of the ancient currents, we
may make out the physical geography of the coast lines of the ter-
tiary land and sea during the same epoch. The author infers, on
these grounds, that during the tertiary period there existed a wide
estuary of a large river running from west to east; that the land
from which the river came must have been to the north, the west,
and south-west, while the estuary opened into a tidal sea towards the
east; and that at the western part of the Isle of Wight area there
existed a considerable shoal. The author’s observations evince much
close examination and ingenious deductions; but I am of opinion
that we are not yet in a condition to adopt all the inferences he has
drawn from the structure of the sandy deposits, or fully to under-
stand the structure itself and the causes which may have occasioned
it. “The subject. is one which requires much more examination and
careful investigation of the various data, before we can venture to
pronounce positively on the phenomena before us.

To Mr. Godwin-Austen we have been indebted during the past
session for several valuable papers, in which interesting speculations
are combined with much careful observation. One of these papers
refers to a subject of such vast economical importance, should the
anticipated results of the author be in any degree confirmed, that I
should but ill perform my duties on this occasion were I not to
allude more particularly to the paper ‘“‘On‘the probable exten-
sion of the Coal-Measures beneath the South-Eastern parts of
England.’ Startling as the proposition may at first appear to many,
that coal may possibly be found under the chalk districts of the
south-eastern parts of England, much of this surprise will disappear
when we consider in how close proximity to the chalk of the Boulon-
nais the Coal formations between St. Omer and Calais occur. Mr.
Godwin-Austen has directed much of his attention to the study of
the palzeozoic rocks south of the Channel, and it is from his observa-
tions respecting the relative position of the Carboniferous beds of the
north of France, between Boulogne and Calais, and the Cretaceous
beds which form the south-eastern prolongation of the axis of eleva-
tion of the Wealden districts in the S8.K. of England, that he has
‘been led to the conclusions which form the subject of this commu-
nication.

The author stated, after describing the physical and geographical
position of the various coal formations existing between the valley of
the Ruhr and the district of St. Omer and Calais, where coal has
been met with in boring for water, that the views he entertains re-
specting the extension of the Coal-measures in the south-eastern
parts of England depend on the correct restoration of the boundaries
of land and water areas in the paleozoic periods. He remarked that
among the earliest rocks, as evidences of former terrestrial conditions,
it is not until we ascend as high as the upper paleeozoic deposits that
we meet with evidences of definite hydrographical areas, and that

ANNIVERSARY ADDRESS OF THE PRESIDENT. hii

many terrestrial surfaces of the carboniferous period have remained
such ever since. The author then pointed out, that in paleeozoic
times there existed a main north and south ridge traversing what is
now Western Europe, and extending from Scandinavia to North
Africa. 'To the westward of this old range there was another tract,
also running north and south, which was even then bounded to the
west by the Atlantic valley, and is now traceable in the northern and
western portions of the British Isles. From very early times there
was an increase of land from this western or Atlantic tract to-
wards the present European area by the successive elevation of the
paleeozoic sea-beds ; and it was shown that this took place along
east and west lines, one of which became the axis of an elevation
which is distinctly traceable through a long series of geological
changes. In proof of these statements, the author alluded to the
evidence derived from the geological conditions and formations of
England and France, and particularly with reference to the east
and west ridge above alluded to: the author remarked that he
regarded the absence in France of the Upper Silurian system as
having been caused by an east and west barrier cutting off commu-
nication with the Upper Silurian zoological group of Shropshire and
Scandinavia, and constituting a division between two hydrographical
areas, in the northern of which the true Upper Silurian fauna had
its development, and in the other what the author considers as its
southern equivalent, viz. the Rhenane and Devonian group ; and he
showed that there was evidence of this barrier in the shingle-beds of
the Lower Silurian formation both in Northern France and in Corn-
wall, which point to a neighbouring east and west coast-line,—in the
half arch of cleavage of the chlorite schists of the Prawle, proving
the existence of an elevated east and west range of old rocks, now
locally destroyed and replaced by the English Channel,—and in the
occurrence of an elevatory axis ranging east and west along the
southern shores of Devonshire.

The author then proceeded to consider the relation of the coal-beds
to this old east and west ridge, which he had traced from the valley
of the Ruhr by Aix-la-Chapelle through the Ardennes and the South
of Belgium by Liege, Namur, and Valenciennes, accompanied by the
paleeozoic formations lying on its northern flank, the contour of the
old coast-line being more or less clearly marked by the lithological
conditions of the conglomerates, grits, sandstones, &c. of the littoral
or the deep-sea deposits. The further continuation of this ridge to the
westward is proved by the chalk axis of elevation through Artois
(passing to the N.W. at a considerable angle to the eastern part of
the ridge), and by the denudation of the Boulonnais and of the
Weald of Kent and Sussex. At the same time, further to the west,
at Frome in Somerset, the identical series exposed in the Boulonnais
emerges again in similar unconformable relations, and Devon and ~
Cornwall supply evidence of the western extremity of this old ridge,
which united the two great north and south ranges of land, and
formed an extensive gulf-like configuration of this Western European
area in Paleozoic times. It was along the inner (southern and

VOL. XII. e

liv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

western) borders of this somewhat semicircular indentation (open
apparently to the north) that the great coal-formation had its origin.
In other words, the Rhenish and Belgian coal-fields, together with
the midland and northern Coal-measures of England, are the remains
of asuccession of fringing bands of dense vegetation occupying a
continuous tract of coast-line. At this period the central gneissic
plateau of France was a terrestrial area with lakes and rivers, and
supported a rich coal-producing vegetation, the remains of which are
preserved in the original depressions in which they were accumulated.
The author then pointed out other extensions of ancient land in va-
rious parts of Europe, and described the different physical conditions
with which they were connected. He showed that the Boulonnais
coal belonged to the Mountain Limestone series below the geological
horizon of the Franco-Belgian coal. This latter probably underlies
the oolitic rocks mm the neighbourhood of the Marquise district.

The author concluded his statement by deducing the following
inferences :—1st. that the physical configuration of Western Europe
at the period of the upper or true Coal-measure period indicates the
probable continuity of a band of coal-growth from the midland and
south-west of England to the south of Belgium; 2nd. that there
may also exist a lower stage of coal-deposits, extending somewhat
west of the Boulonnais and of equal value; 3rd. that the influence
of the old axis of flexure on the distribution of the oolitic and
cretaceous groups, favours the presumption that there is no great
thickness of overlying strata interposed between the Coal-measure
series and the present surface; 4th. that the upper Coal-measures may
be regarded as occupying a line on the north of the Weald denudation,
or conforming generally to the direction of the Valley of the Thames,
whilst the lower series may occur on a line coincident with the chalk
escarpment of that denudation.

However startling these views may at first sight appear to those
who expect to find all the intervening strata between the Carboniferous
and Cretaceous series, regularly deposited, it has nevertheless appeared
to many practical men as not at all exceeding the bounds of pro-
bability ; and when we recollect how many instances occur of different
strata being deficient in various localities, or so thinning out as not to
offer any practical difficulty to the solution of the question, the
apparent primd facie improbability is greatly diminished. More-
over, when we reflect on the vast practical results which would
accompany such a discovery as that of coal in the south-eastern
district of England, the truth of which might be tested by judicious
borings on a comparatively small scale, we can hardly refrain from
expressing a desire that such an experiment should be made. The
existence of granite masses stated to have been found in or below the
chalk formations of Kent, if indeed they are not transported boulders,
would appear to indicate that the crystalline basis of the stratified
rocks is, in some places at least, not at so great a distance from the.
surface as might otherwise have been expected, had all the different
stratified formations been deposited in their normal or typical condi-
tion, and of the same thickness as they occur in other parts of

ANNIVERSARY ADDRESS OF THE PRESIDENT. lv

England. But whether the suggestion be acted on or not in the
present day, we are greatly indebted to Mr. Godwin-Austen for
bringing forward the subject, and for bringing his knowledge of the
palzeozoic rocks of the Boulonnais to bear on the geology of the
neighbouring Wealden.

Professor Ramsay read at one of our Evening Meetings an interesting
paper “On the occurrence of Angular, Subangular, Polished, and
Striated Fragments and Boulders in the Permian Breccia of Shrop-
shire, Worcestershire, &c.’’ This formation, remarkable on account
of the imbedded fragments being angular, instead of being rounded
as in the usual conglomeratic beds of the Permian and New Red
Sandstone formation, had long ago attracted the attention of different
geological observers, and various causes had been assigned to account
for this discrepancy in the appearance of its contents. The object
of Prof. Ramsay, after carefully examining all the localities where
these breccias occur in Staffordshire and Worcestershire, and every
opening, exposed whether by nature or in quarries, is to poimt out
the probable existence of glaciers and icebergs in the Permian epoch.
And although it may be premature to consider this statement as
correct, or to adopt all the conclusions of Prof. Ramsay, it must be
admitted that there is something peculiar in this breccia formation ;
and there seems no reason for questioning the conclusion which Prof.
Ramsay has arrived at from an extensive examination of these
scratched and angular boulders, viz. that they have been derived
from a considerable distance, and that they have been transported
by the agency of water. Nor am I prepared to admit that all the
arguments by which it has been attempted to refute the theory of
Prof. Ramsay are altogether conclusive. Some of these objections
he has noticed in his paper, and more or less satisfactorily answered.
We know too little of central heat as yet, or in what proportion, if at
all, it has diminished by radiation since the Carboniferous and Permian
epochs, to found any safe conclusion on such an argument; still less,
even admitting such a supposition as the existence of central heat,
do we know the causes from whence it proceeded. It was long
considered as a geological axiom, that our earth was before its first
consolidation a mass of liquid or viscous igneous matter. But the
truth of this so-called axiom has now been seriously called in question,
and many geologists are disposed to admit the equal, if not greater,
probability of the soft or liquid state of the primitive earth being due
to aqueous rather than igneous causes.

But to return to Prof. Ramsay: surely they who would wish to
invalidate his arguments on the general ground of the improbability
of the existence of glaciers and icebergs during a period when a
tropical vegetation is supposed to have flourished in the neighbouring
districts, must have forgotten the eloquent description given by Mr.
Darwin of the glaciers of South America, when he states*, that
“‘slaciers here descend to the sea within less than two degrees and a
half from arborescent grasses, and (looking to the westward in the
same hemisphere) less than two from orchideous parasites, and within

* Researches in Geology and Natural History, p. 285.
e

lvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

a single degree of tree-ferns!’’ The same distinguished. writer alludes
further on (p. 291), to the importance of the circumstance of a
luxuriant vegetation with a tropical character encroaching so largely
on the temperate zones, under the same kind of climate that allows
of a limit of perpetual snow of little altitude, and consequent descent
of glaciers into the sea. In South America glaciers descend into the
sea in lat 46° 30'.. The occurrence also of those denizens of the
tropics, the humming-birds, at an elevation of 10,000 feet above the
sea, and along the western coast of South America from the tropics
to the forests of Tierra del Fuego, as described by the same author,
is another important fact bearing on this argument which cannot
altogether be overlooked.

These considerations seem to show, that, even admitting the tropical
character of the Permian flora and fauna, which however Prof.
Ramsay hardly does, there is no improbability of their juxtaposition
with glaciers in lat. 51°, at a period too when we are unacquainted with
the relative distribution of land and sea. It appears to me, however,
that the strongest argument against Prof. Ramsay’s theory, is to be
derived from his own account of the breccia-bed itself. Without
giving the exact thickness of this bed in any locality, the vast extent
of country over which it is distributed, amounting according to the
author’s own calculation to an area of 500 square miles, and distributed
moreover with great regularity, militates strongly against the glacial
theory. In ordinary cases we find the glacial detritus either collected
in vast irregular heaps or monticules at the termination of the glacier,
or distributed in long parallel lines or ridges, of many miles in length,
along the edges of the glacier, marking the limit of its action, and
accurately defining its extent. I am not aware that the transported
matter of glaciers is ever found spread out with the regularity of a
real subaqueous formation, as has been the case with these Permian
breccia-beds ; and even admitting some of these breccia-beds to have
been transported by the agency of icebergs floating across the waters
and transporting the detritus from a neighbouring shore, the great
extent of the beds in question would almost equally preclude the pro-
bability of such a solution of this remarkable deposit. Vast débacles
occasioned by the sudden burstings of the barriers of an extensive
inland lake, or violent disturbances of the ocean by the elevation of
mountain chains or the sea-bottom, many instances of which must
have occurred in various periods during the paleeozoic age, appear
to me a more simple and satisfactory mode of accounting for the
different phenomena described by Prof. Ramsay. During the violent

commotion caused by such an agency, the huge masses of rock, accom- ,

panied by a sea of mud, would be hurled against each other, and the
sharp angles of the disrupted masses might easily impress on the
sides of transported boulders those striee and scratches which have
given rise to the theory of their being due to glacial action or to
icebergs. The subject, however, is an interesting one, and we may
hope that the further progress of the Geological Survey will throw
additional light on the causes of the phenomena described by the
author of this paper.

~
a a

ANNIVERSARY ADDRESS OF THE PRESIDENT. lv

Mr. E. Hull has given us an interesting paper “‘ On the Physical
Geography and the Drift Phenomena of the Cotteswold Hills,” in

which he has endeavoured to account for the formation of the valleys

and intervening headlands in the Gloucester plain, by showing that
the valleys occur in the direction of slight anticlinal lines and the
headlands in the direction of synclinal lines having a mean north and
south strike. The preservation of Bredon Hill is attributed by the
author to a fault traversing the southern side of the hill from east
to west. In the second portion of his paper, Mr. Hull points out the
existence of several distinct pleistocene deposits, found at intervals
over this district. Of these the most ancient is the northern drift,
then the estuarine, and last the warp-drift; of the first no traces
are to be found on the Cotteswold Hills, which were above the sea
at the period of its deposition ; but the sands and gravels of which
it is composed, derived from the waste of the new red sandstone
and carboniferous limestone, are plentifully strewed over the vales
of Gloucester and Moreton. The occurrence of boulders of millstone-
grit near the southern extremity of the Moreton Valley, is supposed
by the author to indicate the southern extension of icebergs brought
down by the northern current. The estuarine drift, composed of
oolitic detritus and restratified northern drift, was found in the
Valleys of the Evenlode, Moreton, Cheltenham, and Stroud, containing
the remains of now extinct Mammalia. The warp-drift was found
at the height of 600 or 700 feet, equal to that which the northern
drift attains, while the estuarine drift is not found at a higher eleva-
tion than 300 feet above the sea. Traces of an ancient sea-beach
were also found by the author at the base of the inferior oolite
escarpment. It was also stated in conclusion, that in order to explain
all the pheenomena of the drifts and denudations of the country, at
least three elevations and two submersions of greater or less amount
must be supposed to have taken place. .

Some interesting discussions on the Newer Tertiary Deposits of the
Sussex Coast have also occupied our attention at the Evening Meetings.
Mr. Godwin-Austen and Mr. Martin of Pulborough have each con-
tributed some additions to our knowledge on this subject.. Mr.
Godwin-Austen fully described several of these beds, which he
considers as the glacial deposits of the district. They consist of
gravels of different kind, overlaid by brick-earth somewhat variable
m its characters. At Selsea, where the glacial deposits are 25 feet
thick, the underlying eocene clay is seen at low water perforated by
a large variety of Pholas crispata?, and overlaid by a deposit con-
taining Lutraria rugosa, Pullastra aurea, Tapes decussata, and Pecten
polymorphus, contemporaneous with the Pholades. This deposit,
clayey in places, contains a great variety of pebbles and boulders of
granitic, slaty, and old fossiliferous rocks, such as are now found in
the Cotentin and Channel Islands. The occurrence of these granitic
and slaty blocks in the yellow clay was the principal subject of the
paper. The author pointed out the difficulties that lie in the way
of supposing that they were derived from the coast of Cornwall or
direct from the shores of Brittany or the Channel Islands, and

SSS ==

lvl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

considered that his former observations on the bed of the English
Channel had prepared the way for the hypothesis he now advanced,

viz. the former existence of a land barrier composed of crystalline and _

paleeozoic rocks, crossing from Brittany to the south-east of England,
and forming a gulf or bay open to the west. Into this bay the
marine fauna represented by the Pholades and their associates ex-
tended from the westward, and in the hollow of the bay at a some-
what later period, coast-ice brought the boulders from along the old
shore-line, which is now represented by a sunken peak in mid-
channel lying south-east from the Isle of Wight, and by a shoal of
granitic detritus. The author also alluded to the alterations of level
which had subsequently taken place, and the partial destruction of some
and formation of other deposits by frequent oscillations. That these
huge boulders of crystalline and other older rocks, some of which are
more than 20 feet in circumference, have been transported byice, seems
probable enough, but there appears to me a physical difficulty in the
way of Mr. (codwin-Austen’s theory, that they were stranded in the
hollow of this supposed bay. Icebergs or coast-ice charged with such
boulders are uniformly moved by currents; and, if this bay were closed
up to the eastward, it is difficult to imagine how any current would
so set directly into the bay as to strand the floating icebergs m the
bight. The same current which brought them in, supposing a
current to have set into the bay, would, by sweeping round the coast,
have again carried them out to sea; at the same time, the occurrence

of these boulders in the drift-beds is of great interest ; but, without a

more careful comparison of the crystalline rocks on the opposite coast
and in the Channel Islands, it would be difficult to decide from whence
they may have been brought. It seems probable, however, that the
parent rocks will be found in the Channel Islands, or the numerous
reefs by which those islands are surrounded.

Mr. Martin, in his paper on some geological features of the country
between the South Downs and the Sussex Coast, refers the boulder-
drift of Mr. Godwin-Austen to another zone of Wealden drift in
addition to those which he had already described as mantling round
the nucleus of the Weald, the corresponding parts of which zone he
thinks are to be found in the Valley of the Thames. This zone he
considers as the remains of the boulder-deposit spread over the
tertiary districts of this and the adjoming parts of the North of
Europe, before their continuity was disturbed by the upheaval of
the great anticlinal axis of the South of England. Mr. Martin
regards the country under review as a sectional part of this great
anticlinal, and thinks that it must not be considered apart from
the wide geological area to which it belongs, and that its phenomena
of arrangement and drift belong to the epoch of that upheaval, thus
showing the effect of powerful diluvial currents set in motion and

_assisted at the same time by the dislocations known to abound in this

part of our island, and without the aid of which the author considers
we can arrive at no satisfactory conclusion respecting the drifts and
other pheenomena of the denudations and other surface-changes here
exhibited.

ANNIVERSARY ADDRESS OF THE PRESIDENT. lix

Amongst the interesting discoveries of fossil remains during the
past year, I may mention that of the first example of the subgenus
Bubalus yet recognized as fossil in Great Britain. It consists of the
cranial partof the skull with the horn-cores nearly perfect. Prof.Owen,
after a careful examination and comparison with recent crania,
stated, that, as far as the materials at his command enabled him to
judge, the differences between the fossil and recent Musk Buffalo are
not of specific value; he considered that the Bubalus moschatus of
the Arctic region, with its now restricted range, is the slightly modified
descendant of the contemporary of the Mammoth and the Tichorine
Rhinoceros, which with them enjoyed a much wider range both in
latitude and longitude, over lands that now form three divisions or
continents of the northern hemisphere.

Mr. Prestwich has added a communication respecting the gravel
near Maidenhead in which these remains were found. A mass of
ochreous gravel occupies the Valley of the Thames from Maidenhead
to the sea. It consists principally of subangular chalk-flmt. The
author considers the date of its deposition to be posterior to that of
the boulder-clay of Norfolk and Suffolk, and also posterior to the
gravel which caps the chalk-plateau traversed by the Valley at
Maidenhead. The low-level gravel rests at Maidenhead on chalk-
rubble, and the skull of the Musk Buffalo was found, with fragments
of other bones, Jow down in the gravel, where it begins to be mingled
with the chalk-rubble.

A communication has also been read to us by Mr. Prestwich on
the boring sunk through the chalk at Kentish Town. This boring
has pierced the following succession of beds:—London Clay,
236 feet; Woolwich and Reading Series, 613 feet; Thanet Sands,
27 feet; Middle Chalk, 2442 feet ; Lower Chalk, 2274 feet; Chalk
Marl, 172 feet; Upper Greensand, 59 feet; Gault, 85 feet; and
then 1764 feet of a series of red clays with imtercalated sandstones
and grits, the total thickness being 1290 feet, and as yet no water
had been obtained. It was naturally expected that the sands of the
Lower Greensand formation would be found immediately to succeed
the Gault. Instead of them, however, red sandy clays have presented
themselves, and the important question arises, What are these beds?
Are they a local variation of the Gault? Or have the Lower Green-
sands here assumed a new character? Or have the workmen suddenly
got into a new formation? The very few fossils met with in these
clays, if indeed they can be depended upon as really coming out of
this formation, are in favour of their bemg Middle Cretaceous, and
above the horizon of the Lower Greensand. But. the occasional:
occurrence in the clay of large rolled fragments of syenite, porphyry,
basalt, hornstone, and Old Red Sandstone, and its general mineral
features, appear to indicate a littoral character for these deposits, and
to point to the possible neighbourhood of a ridge of older rocks which |
have modified the conditions under which the lower cretaceous beds
were formed in this area. This guestion becomes one of great
interest in connexion with Mr. Godwin-Austen’s theory of the
possible occurrence of the carboniferous rocks immediately or nearly

lx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

under the Chalk of the south-east of England. The further considera-
tion of this important question was referred to a Committee, who will,
I trust, be able to report on it at some early future Meeting of this
Society. In the mean time it is to be hoped that parties will be
found with sufficient enterprise and energy to prosecute the search,
until either the water-bearing strata shall have been reached, or the
nature of this somewhat anomalous formation shall have been
ascertained.

The question of the chemical composition of granite has been
carefully studied of late years by Prof. Haughton, and numerous
papers on the subject from his pen and that of Prof. Galbraith, have
appeared in many of the scientific publications in London, in Dub-
lin, and in Edinburgh. His inquiries have hitherto been almost, if
not entirely, confined to the granites of Ireland; and some of the
results of his investigations and analyses have been recently brought
under our notice in a paper entitled ‘‘ Experimental Researches on
the Granites of Ireland.”” The first part of the paper described the
granites of the south-east of Ireland, which are reducible to three
types depending on their chemical and mineralogical composition.
The granite of the first type, which Prof. Haughton proposed to call
*‘ potash-granite,” is found in the main granitic chain of Wicklow
and Wexford, and at Carnsore in the south-east of Ireland. The
granite of the second type, which is a “‘ soda-granite,” occurs at
Rathdown and Oulast, and is distinguished from the former by a
diminution of silica and an increase of lime and soda. The third
granite is peculiar, and is found only at Croghan Kinshela, near the
gold mines of Wicklow. It consists of quartz, albite, and chlorite,
while the potash-granites of the main chain consist of quartz, ortho-
clase, and margarodite (mica). The three granitic districts of the
north-east of Ireland are then described. They are known as the
Mourne, Carlingford, and Newry districts. The granite of Mourne
consists of quartz, orthoclase, albite, and a green mica, probably
similar to margarodite. The Carlingford granite is a ‘“‘ potash-
granite,’ in which hornblende replaces mica. At the junction of
this granite with the carboniferous limestone, a remarkable change
takes place in the granite on penetrating the hmestone m dykes.
From being originally a compound of quartz, orthoclase, and horn-
blende, it is converted by the addition of lime into a compound of
quartz, hornblende, and anorthite, which last mineral was noticed for
the first time as entering into the composition of British rocks. The
Newry granites belong to the ‘ soda-granite”’ type, and resemble in
many respects the secondary granite of the Wicklow and Wexford
districts. |

I am not aware that any practical results have yet been obtained
from these analyses, and the knowledge of these elementary di-
_ stinctions in the composition of the granites. Perhaps, as the imves-
tigations are extended to the granites of other countries, where their
conditions may be different, we shall obtain some information as to
the different ages of these differently combined rocks. At all
events, we are under great obligations to Prof. Haughton for having

=
a a a arn na

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxi

undertaken these investigations, already partly carried out by
M. Delesse. |

I have much pleasure in stating, that the progress of the Geological
Survey of the Empire has been most satisfactory during the past year.
Under the able superintendence of Prof. Ramsay, no less than 610
square miles in Sussex and Hampshire have been for the first time
accurately surveyed, and as the surveyors gradually creep on towards
the metropolis, we may confidently look to a further elucidation of
those important questions connected with the supply of water to the
metropolis, &c., which have already been so ably treated of by
Mr. Prestwich and others in their memoirs on the water-bearing
strata of London.

A similar extent of surface has also been surveyed in North Wilts,
Northampton, Oxford, Warwick, Gloucester, and Berkshire. A large
extent of work in the south and middle of England, already previously
surveyed, has been inspected and prepared for publication. In the
extension of the Survey into Scotland some progress has been made
in laying down on the six-inch scale maps the outline and structure
of the coal districts around Edinburgh, more particularly of Hadding-
tonshire and Fifeshire. Nor has the Survey of Ireland under Mr.
Jukes been less actively carried on ; good progress is making in de-
lineating the rugged, broken, and almost inaccessible coasts of Cork
and Kerry. The map on the one-inch scale has also been partly
issued by the Ordnance.

Considering these active operations, and the able staff employed in
carrying out the difficult and sometimes intricate details connected
therewith, it is to be hoped that the Government will not lose sight
of the importance of the Institution of which the Geological Survey
forms such an important feature, nor of the desirableness of pre-
serving its independent action. —The Museum of Practical Geology and
the School of Mines is rapidly becoming one of the most important
scientific establishments of this metropolis ; and when we find the
Director-General in constant and direct communication with the dif-
ferent Departments of Government, who are desirous of obtaining from
him information which afew years ago they knew not where to apply
for,—when the Admiralty require information respecting the wear and
tear of our coasts, and the consequent impediments to navigation,—
when the Foreign Secretary desires to obtain reports on coal and
other minerals frum the seat of war,—when the Colonial Minister ap-
plies for proper Mineral Surveyors to explore the West India Islands
and other Colonies,—or when the Home Government calls for reports
on and analyses of our British ores, and particularly of iron, and
when we find that the Institution has now brought together for the
first time in this country accurate returns of the produce of coal and
other minerals, we may form some idea of the importance of this
establishment, and may, I think, boldly express the hope that no un-
necessary trammels will be interposed to interfere with its energies,
or to prevent its direct communication with that department of
Government under which it is placed.

With regard to the publications of the Institution, it is a great

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lxil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

satisfaction to me to announce that the geological description of the
Isle of Wight by the late distinguished palzeontologist Edward Forbes
is about to appear as one of the Memoirs of the Survey. It will, I doubt
not, sustain his well-earned reputation: the task of editing and pre-
paring this work for publication has been undertaken by Mr. Godwin-
Austen, whose knowledge of the. ground, which he had often visited
in company with his lamented friend, renders him most competent to
carry out this labour of love.

In addition to this work, a most instructive aid valuable Decade on
the Echinoderms of the Oolitic rocks, compiled by Mr. Salter and
Mr. Woodward from the fragmentary notes of Edward Forbes, is also
about to appear*.

It was with much regret that I was compelled last year to an-
nounce that the volume of the Palzeontographical Society for 1854
had not then made its appearance, but I ventured to state from
what I knew of its forthcoming contents, that it would be found
fully to maintain the high reputation acquired by its predecessors.
The volume has since made its appearance, and I appeal to all who
have witnessed its goodly size and still more goodly contents, whether
my anticipations have not been fully realized. There is another
special merit in this volume which will not be lost sight of, viz.
that it contains the completing parts of several important works,
which will enable members to arrange them in a more convenient

manner for reference and use than that in which they are now —

placed. In addition to the Permian Fossils by Prof. King, com-
pleted in a former volume, we have now the following works com-
pleted: ‘The Fossil Cirripedia of Great Britain,’ by Mr. Darwin,
in two parts; the first volume of ‘The Fossil Brachiopoda of Great
Britain,’ by Mr. Davidson ; ‘The Mollusca of the Great Oolite,’ by
Messrs. Morris and Lycett ; and ‘The Fossil Corals of Great Bri-
tam,’ by Messrs. Milne-Edwards and Jules Haime. Besides these,
this volume contains the second part of the ‘ Fossil Reptilia of the
Wealden Formations,’ by Prof. Owen; the second part of ‘The
Fossil Remains of Mollusca found in the Chalk of England,’ by Mr.
Sharpe ; and the third part of ‘The Eocene Mollusca of England,’

by Mr. F. Edwards.

In his Address from this chair in 1854, Prof. EK. Forbes pointed
out the great importance to the geological student of the publi-
cation of the interesting monographs of this Society; I therefore
trust that it will not be inopportune to give a slight account of the
contents of this volume.

Mr. Davidson’s portion of this volume completes his essay on
the Brachiopoda of the Cretaceous formations. It also contains
the completion of the genus Terebratula, the number of species

of which is extended to thirty-three, although the two last are given, |

apparently without sufficient explanation, as Waldheimia, the names
in the text and in the list of plates not corresponding. This is

* The decade has been published while these sheets are passing through the
press, but I will not trespass on the manor of my successor in the chair by alluding
any further to its great merits.

ANNIVERSARY ADDRESS OF THE PRESIDENT. lx

followed by the genera Rhynchonella with fourteen species ; Argiope,
one; Crania, one. To this the author has added a table illustra-
ting the geological distribution of all the British Cretaceous Brachio-
poda, the total number of which is forty-nine. In his supplementary
observations on the stratigraphical distribution of the species, Mr.
Davidson remarks on M. d’Archiac -having stated in his ‘ Histoire
des Progrés de la Géologie,’ that the British cretaceous strata contain
| fifty-two species of Brachiopoda; he observes that his own list of
| forty-nine greatly exceeds in reality the number of true species
recorded in M. d’Archiac’s table, inasmuch as at least twenty-two or
twenty-four of M. d’Archiac’s names are only synonyms, whereas
_ his list contains a number of species new to England and not men-
tioned in any other publication. Still he admits the possibility of
error, and observes that possibly the number of hitherto observed
species in the British cretaceous strata may not exceed forty-five,
: and adds that the correctness of this number must also depend upon:
the correctness of the age of certain other beds, particularly the
Farringdon gravel, a question into which he enters at some length.
It is impossible to praise too highly the execution of the seven
plates by which this portion of Mr. Davidson’s work is illustrated.
In the Appendix, and the supplementary additions to the Appendix,
the author has introduced certain corrections and addenda, with an
additional plate, bringing down our knowledge of the subject to the
last moment of publication.

The next essay to be noticed is the second part of Prof. Owen’s
Monograph on the Fossil Reptilia of the Wealden Formations, con-
taining the order Dinosauria and genus Iguanodon. The paper is
illustrated by nineteen plates, some of very large size, representing
different portions of osseous remains of the Iguanodon, many of
which are drawn to the natural size. The text descriptive of these
illustrations is a favourable specimen of Prof. Owen’s well-known
power of comparing and elucidating the osteology of the fossil Verte-
brata. I would particularly call attention to the lucid manner in
which he has pointed out the real analogies and nature of that
curious specimen so long considered, on the authority of Dr. Mantell,
to be the bony core of the frontal horn of the Iguanodon. Prof.
Owen shows, on grounds which appear to be incontrovertible, that
this fossil relic is in fact one of the phalangeal bones, and he sums
up the evidence he brings forward to show that it belonged to the
end of one of the toes instead of to the head of some great Wealden
Saurian, by pointing out the characters which separate the gigantic
Iguanodon from the little modern Iguana, which has an osseous
conical horn or process on the middle of its forehead.

This is followed by the Monograph by Prof. Morris and Mr.
Lycett on the Mollusca from the Great Oolite. The specimens are
derived chiefly from Minchinhampton and the coast of Yorkshire,
and this third part contains the completion of the Bivalves. It is
accompanied by seven plates representing the species described, of
which I need only say that their execution is worthy of the place
they occupy in the volumes of the Paleeontographical Society.

lxiv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Messrs. Milne-Edwards and Jules Haime have contributed a valua-
ble addition to this volume by the completion of their Monograph
on the British Fossil Corals. This fifth part of their work con-
tains the Corals from the Silurian formation, the value of which, in
a geological point of view, is apparent from their extraordinary
abundance and relative importance durmg the period when the
Silurian deposits were formed. As the authors observe, the variety
of species is here as considerable as in most of the coralliferous
rocks of a more recent date, and what adds to the importance of the
study of Silurian corals, is the good state of preservation in which
they are generally found; and so abundant are the fossil corals
found at Dudley and other localities, that at the present day more
than half the species discovered in the Silurian deposits of the West
as well as of the East Hemisphere have been found in England, chiefly
owing to the exertions of Sir R. Murchison and his followers. The
authors then observe that the British Silurian fossils were originally
described and figured by Mr. Lonsdale, who referred most of them ,
to the species previously described by Goldfuss from the Devonian
deposits of the Eifel; but they add that this supposed identity does
not exist m any of the well-characterized species. After comparing
the specimens figured by Mr. Lonsdale in Sir R. Murchison’s work
with those figured by Goldfuss and now in the Poppelsdorf Museum
at Bonn, they have ascertained that almost all are specifically differ-
ent, a conclusion at which M. d’Orbigny had also arrived, and which
is further confirmed by the researches of Prof. Sedgwick and Mr.
M‘Co

They add that the British Silurian Corals differ but little from
those of Gothland, and very much resemble those from Bohemia,
while they are generally distinct from those of the Silurian de-
posits of North America. The total number of species discovered
in the various Silurian deposits amounts to 129, all of which, with
the exception of eight, belong to the authors’ divisions of Zoan-
tharia tabulata and Z. rugosa. Of these, seventy-six have been
found in England, and about half of these have not been met with
elsewhere. Sixty-eight of these British fossils belong to the families
of Favositidee and Cyathophyllide, and the only species not he-
longing to the above-mentioned higher divisions are four Fungide.
It may also be noticed, that most of them belong to the Upper
Silurian deposits. It only remains to mention that sixteen plates
accompany this portion of the Monograph, making altogether seventy-
two plates of British Fossil Corals.

Mr. Darwin has contributed to this volume a monograph on the
Fossil Balanidze and Verrucide of Great Britain, which, with the
Lepadide already published, complete his work on the British Tho-
racic Cirripedes. Mr. Darwin observes in his Introduction, that as
yet only sixteen species in these two families have been found fossil
in Great Britain, and that of these sixteen, nine are still living forms.
It is probably owing to the extreme difficulty of identifying the
species in these Cirripede families that their study has been hitherto
so much neglected, as has been noticed by Mr. Darwin, and this is

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixv

particularly the case with the Balanidee or Sessile Cirripedes. Their
form depends greatly on their position and grouping. The surface
of attachment has a great effect on the form of the shell; for, as the
shells are added to at their bases, every portion has at one time been
in close contact with the supporting surface. Mr. Darwin observes,
that in consequence of the great variability of those features which
are generally considered as characteristic, he has been compelled for
the identification of species to have recourse to characters which
require the closest examination. Moreover, he considers that with-
out an examination of the opercular valves, it is seldom that the
Sessile Cirripedes can be satisfactorily determined in a fossil condi-
tion. The Balanidz do not appear to range lower down in the
geological series than the Eocene period, when both in Europe and in
America they were represented by few species; although they abounded
during the Miocene and Pliocene periods. But owing to the diffi-
culty of identifying species the number of nominal species is far too
great. Mr. Darwin believes that, if properly examined, it would be
found that the whole number of species of Balani in the several ter-
tiary formations, from the Eocene to the Glacial, throughout Europe
would not exceed twenty.

Mr. Sharpe’s contribution to this volume is a portion of the con-
tinuation of his valuable monograph on the Fossil Remains of Mol-
lusca found in the Chalk of England. This portion is still confined to
the Cephalopoda, and contains the description of thirteen species
of Ammonites illustrated by six plates.

The last and, to many geologists, perhaps the most interesting
contribution to this volume is the third part of Mr. F. Edwards’s
monograph of the Eocene Mollusca, or descriptions of shells from the
older Tertiaries of England. In the two former parts Mr. Edwards
had described the Cephalopoda and the Pulmonata, or free air-
breathing Mollusca. This third part contains an account of the
Prosobranchiata, one of the two divisions into which M. Milne-
Edwards has subdivided the water-breathing Gasteropoda, the other
being the Opisthobranchiata. With reference to the dental appa-
ratus of the Gasteropoda, to which much attention has recently been
paid by many distinguished naturalists for the true identification of
genera, Mr. Edwards justly observes, that however valuable it may
prove to malacologists, it can only be indirectly available to the
paleontologist. The genera described in this part are Cyprea eight
species ; Ovula one, problematical ; Marginella seven species ; Voluta
thirty-one, seven of which have been added by the author himself.
With regard to one of these, V. maga, possibly the V. magorum,
Sow., and figured imperfectly by Brocchi as a subapennine species,
Mr. Edwards observes that Prof. Beyrich has described a Volute
from Westeregeln, V. decora, Beyr., so closely resembling this
species that it is difficult to distinguish them. Should they on
actual comparison or further discoveries prove to belong to the same
‘species, Mr. Edwards observes that the name given by Prof. Beyrich
must supersede that given by himself. These genera are illustrated by
eight plates by Mr. J.deC. Sowerby. The next Part will commence

ixvi PROCEEDINGS OF THE GEOLOGICAL SOCIFTY. —

with the genus Mitra, and we are informed by the notices given out
by the officers of the Paleeontographical Society, that the forthcoming
volume for 1855 will contain the fourth Part of the Eocene Mol-
lusca with ten plates. There is, therefore, a reasonable expectation
that this work, which has long been anxiously looked for by the
students of Tertiary Geology, will now rapidly advance towards com-
letion.
: It is impossible for me even to allude to all the valuable papers
on British Geology which have appeared in the numerous metro-
politan and provincial journals during the past year, many of which
are of great importance and deserving careful study.

Foreign Grouoey.

France.—The volumes of the Bulletin of the Geological Society.

of France bear.ample testimony to the active exertions of our neigh-
bours in the cause of geological inquiry. I regret that neither time
nor space will permit me to do full justice to the many able memoirs
they contain. I must refer you to the volumes themselves for in-
formation, merely premising that the structure of the great Alpine
formations, and the geology of the principal secondary formations
seem chiefly to have attracted the attention of the French geologists.

Amongst the principal memoirs contained in the Bulletin, I may,
however, mention the following :—A Notice on the Age of the lower
and middle beds of the Coralline Group (Coral rag) in the depart-
ment of the Yonne, by M. G. Cotteau. With a complete list of
Fossils found in the Coral rag and Oxford Clay.

M. Jules Baudouin laid before the Society a geological map of the
district of Chatillon sur Seme, laid down between 1840 and 1855 on
the topographical survey of the Dépot général de la Guerre, accom-
panied by full details of the different formations which occur in that
locality. 3

M. Omboni read a communication on the sedimentary formations
of Lombardy, and on the structure of the southern fianks of the Alps,
from the Tyrol to the vicinity of the Lago Maggiore. A geological
map and section accompany the memoir. M.Omboni has proved
the existence in this region of several of the secondary formations of
Europe, and particularly of the Muschel-kalk of Werner.

The following formations are described :—1. Recent deposits ;
2. Erratic formations; 3. Tertiary; 4. Cretaceous deposits; 5. Ju-
rassic; 6. St. Casciano groups; 7. Triassic; 8. Permian; 9. Car-
boniferous ; 10. Crystalline formations.

The Marquis de Pareto has communicated a notice on the num-
mulitic formation at the foot of the Apennines.

M. Pomel communicated a geological account of the country of
the Beni Bou Said, near the frontier of Morocco.

But I must more particularly allude to an interesting series of
papers and discussions respecting the age of the Anthraxiferous
formations of the Alps.

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixvii

M. Scipion Gras* read a long communication on the geological
constitution of these beds, and the differences which distinguish
them from the Jurassic formation. In the course of this memoir,
M. Gras gives his reasons for placing these anthraxiferous beds
amongst the transition or paleeozoic rocks. He quotes the Verrucano
of Tuscany, which they greatly resemble, to support his views, and on
the strength of the resemblance between them, as observed by many
geologists, and from the fact of true carboniferous fossils having
been found in the Verrucano, he places the anthraxiferous beds of
the Alps in the same carboniferous horizon.

Some correspondence on this subject subsequently took place be-
tween M. Sismonda and M. Elie de Beaumont, with especial refer-
ences to the age of the Verrucano at Jano in Tuscany. The ques-
tion of the age of these anthraxiferous beds of the Alps is one which
has occupied the attention of every geologist who has visited the
country, and a long list of writers and of memoirs is given in the
Bulletin, all having reference to this much-discussed question. The
last communication ‘on the subject is from M. A. Sismonda, who,
im a letter addressed to M. Elie de Beaumont, gives an account of
the fossils from the Col des Encombres (Savoy) and the Col de la ~
Madgelaine in the valley of the Stura (Piedmont). They occur on the
route leading from Saint Michel-en-Maurienne to the Tarentaise, and
confirm the opinion of M. Elie de Beaumont, that the anthraxife-
rous formation of the Central Alps cannot be referred to a more
remote period than that of the Lias. The fossils occur principally
at the junction of the dark schistose crystalline limestone with the
calcareous beds called Calcaire de Villette. The writer concludes
that the anthraxiferous beds of the Alps are newer than those of
Jano in Tuscany, the latter being below the Verrucano, which he
identifies with the infra-liassic conglomerate of Valorsine and Ugine,
whereas in the Alps the anthraxiferous beds are above the con-
glomerate. Moreover, the Jano fossils are decidedly palzeozoic.
The only resemblance between the two formations consists in their
flora. But geologists now know that the flora of a formation is not
so sure an identification of age as the fauna. It would be an inter-
esting investigation to imquire into the cause of this difference.
Possibly vegetable life was not so easily destroyed by the changes
in the conditions of life and by the convulsions of the ancient world,
as the more delicately organized individuals of animal life, and the
flora of one period was thus more frequently preserved and carried
on into succeeding epochs.

Now it is generally admitted, that the anthraxiferous beds contain-
ing vegetable impressions, supposed to indicate carboniferous species,
alternate with Jurassic beds containing Belemnites, &c. ; and some
geologists have endeavoured to explain this anomaly by local inver-
sion or contortion; the most recent investigations, however, would
seem to controvert this view, for the beds are perfectly parallel,
and there appears to have been no contortion or folding over of

* Vol. xii. p. 255.

Ixvill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

them: the result is, that some authors refer the whole formation, in-
cluding the Jurassic forms, to the Carboniferous epoch, whilst others
refer the whole, including the vegetable remains, to the Jurassic
period, accordingly as they attach a greater or less importance to the
evidence of Plants or of Mollusca.

MM. Scipion Gras, Chamousset, Ewald, and Michelin refer the
whole to the coal-measures, whilst MM. Elie de Beaumont, Ad. Bron-
gniart, De la Beche, De Montalembert, Bertrand-Geslin, Sismonda,
Dufrenoy, De Collegno, and Roget (1855) consider the whole as be-
longing to the Jurassic period. The weight of evidence appears to
be in favour of referring the whole formation to the Jurassic rather
than to the Carboniferous period.

M. Barrande has also published in the Bulletin* a memoir on the

organic filling-up of the siphuncle in some of the Paleeozoic Cepha-
lopoda. This phenomenon was first incidentally noticed by the
author in the Orthoceratites of the family Vaginati. Further re-
searches showed that these were not the only creatures possessing
the faculty of secreting an organic substance, for the purpose of suc-
cessively closing up the space of the siphuncle. An examination of
all the ancient Cephalopoda, and particularly the Nautilides, led the
author to the discovery that the gradual closing up of the siphuncles
takes place, not only in the other groups of the genus Orthoceras,
but also in the allied genera of Cyrtoceras, Phragmoceras, and Gom-
phoceras, &c., and, generally speaking, in all the Nautilides with a
large siphuncle ; whilst no certain trace of it could be found in those
with a narrow siphuncle. The importance of this discovery, both ina
zoological as well as in a paleeontological point of view, has induced
the author to publish the result of his investigations. After descri-
bing the different modes in which this closmg up of the siphuncles
takes place in different groups of Cephalopoda, with particular re-
ference, however, to the various families of Orthoceras, the author
concludes with some general observations respecting the object of
this phenomenon, and observes, that the study of it leads to results
which confirm former opinions respecting the vertical distribution of
the Cephalopoda in the Paleozoic formations, and will hereafter
further tend to establish a correct geological chronology of these old
sedimentary deposits.

M. Jules Haime has communicated to the Academy of Sciences an
account of the Geology of the Island of Majorca. The oldest beds
he has described belong to the upper and middle groups of the
Liassic formation. They contain many characteristic fossils, as Be-
lemmtes umbilicatus, Ammonites Jamesoni, Mactromya lasina, Pho-
ladomya decora, Lima pectinoides, Pecten, Rhynchonella tetrahedra,
&c. He also found Oxford clay with Ammonites plicatilis and
A. athleta, Belemnites hastata, and Terebratula diphya. The Neo-
comian formation has also a great development in this island, with
its characteristic fossils. Above this are beds of the Cretaceous epoch,
overlaid by others containing Nummulites. This again is overlaid

* Vol, xii. p. 441.

——

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxix

by a freshwater lacustrine deposit, consisting of compact bituminous
limestones and marly limestones, interstratified with beds of rich
lignite or brown-coal. These beds, M. Haime thinks, may be iden-
tified with those of the gypsum of Provence. The fossils appeared
to be Melania laurea, Planorbis obtusus, Limnea pyramidalis, and
two new species, Clausilia Beaumonti and Achatina Bouvyi. Other
tertiary beds occur, belonging to the middle tertiaries and of the age
of the Sub-apennine marls. The quaternary beds are found on the
sea-shore, and their fossils all belong to species now living in the
Mediterranean. They occur on the south, east, and north sides of
the island, but those on the south side differ from those found to the
north.

The fossil evidence thus confirms the views formerly entertained
by M. Elie de Beaumont, on the authority of information derived
from M. Cambessédes. These beds, with their imbedded fossils, are
still more fully described in the Bulletin de la Soc. Géol. de France,
vol. xii. p. 234.

M..Louis Bellardi has published a complete Classified List, or Cata-
logue Raisonné, of the Nummulitic fossils of the district of Nice, in
which he has been assisted by Prof. Sismonda for the Echinoderms,
by M. d’Archiac for the Foraminifera, and by M. Jules Haime for
the Corals. M. Bellardi omits all geological description, referring to
M. Sismonda’s published work on the subject, and to the imtended
publication of Prof. Perez. His object has been to describe the whole
nummulitic fauna of the environs of Nice, for the purpose of faci-
litating a comparison between it and the nummulitic formations of
other countries. He omits all reference to the age of the nummu-
litic beds, which he considers already settled by the labours of pre-
vious geologists, but he is of opinion that the simple comparison of
the fauna of this region with that of the Paris basin proves that it
belongs unquestionably to the Eocene period, in accordance with the
opinions of MM. Deshayes, Sismonda, and others. The list of
fossils contains 372 species belonging to the following classes :—
Cephalopoda, 5; Gasteropoda, 115; Acephala, 177; Annelida, 4 ;
Echinodermata, 22; Foraminifera, 17; Polypifera, or Corals, 29 ;
Bryozoa, 2: of which 112 species are found in the Kocenes of the Paris
basin, 54 in the London basin, and 48 in Belgium.

M. d’Archiac has published in the Journal |’ Institut the outlines
of an Essay on the Geology of the mountainous district of the Cor-
biéres, communicated to the Philomathic Society in July 1855. The
district in question is situated near the Mediterranean, to the south
of Carcassone. The general features of the country had been already
correctly laid down by M. Dufrénoy and others, but M. d’Archiac
observes that he considered it would be useful to rearrange, by means
of fresh observations, the facts already known,—to endeavour to
classify them in a more methodical manner than had yet been done,
by adding certain orographical considerations hitherto neglected,
which help to explain more satisfactorily the geological details,—and,
finally, to determine several paleontological horizons, the details of
which were still imperfect.

VOL. XII. i

,

lxx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

The following table will give some idea of the geological series of
the Corbiére formations as established by M. d’Archiac :—

System. _ Formation. Group. : Etage.
Recent.
Quaternary.
Middle ? Molasse.
Tertiar . x
Sees ae f Nummulitic ............ 2.
Lower .
ot Alet, Weestts tress. 2:
3:
L
OR ded O16 te ctherwnivis =
Cretaceous 3. Wanting .
1. Wanting.
Secondary ......... Lower 4 -webeeuian vie!
3:
JMIMASRIC HLS Roe ne nee RASoinscace ssc ooeeeee Upper
TEAnSiON Weseane.. Carboniferous (Coal).
(Intermédiaire.) Devonian ?
IPTUMIANY, ea tene. ns ceaee Granite.

Igneous rocks (diorites, amygdaloids and spilites, basalts, wackes, &c.).
Metamorphic or uncertain (dolomite, cargnieule, gypsum, salt ?).

The present paper only embraces the Cretaceous formation ;
M. d’Archiac reserves for a future opportunity the Jurassic and
underlying formations.

M. Constant Prévost has announced to the Académie des Sciences*
the interesting discovery in the conglomerate-bed, between the piso-
litic limestone and the plastic clay, near Meudon, of the tibia of a
fossil bird of gigantic size. This conglomerate had, according to
M. Elie de Beaumont, already produced numerous bones and teeth
of Mammifers and Reptiles. But this discovery of a Bird was pro-
nounced by M. Valenciennes to be one of the most interesting osteo-
logical discoveries made in the Paris basin since the days of Cuvier.
The bird belonged to the family of Natatores, and must have been
nearly two or three times the size of a swan. It has been called
Gastornis parisiensis, Héb. M. Hébert subsequently announced the
discovery of a femur of the Gastornis parisiensis, found in the same
bed as that containing the tibia, and within 10 feet of it.

With reference to the paper by MM. Hébert and Renevier on the
Nummuulitic formations in Switzerland alluded to in my address last
year, I may mention that M. Renevier has since published in the “Bul-
letin de la Société Vaudoise des Sciences Naturelles,’’ a more correct
and detailed account of his subsequent investigations of this forma-
tion, although he considers that the term Nummulitic is no longer
appropriately applicable to the Tertiary strata of the Vaudoise Alps.
M. Renevier had originally divided this formation mto two beds,
viz. the Cerithium and the Nummulitic, of which the Cerithium
bed was the more recent. Subsequently, however, he received infor-

* Comptes Rendus, tome xl.

Te “te. egy

|
|
|
;

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxxi

mation that Nummulites were also found overlying the Cerithia.
He consequently made a fresh examination of the beds of La Cordaz.
This, he considers, has led to a clear and definite result, suffi-
ciently explaining the difference of opinion which had prevailed re-
specting the relative position of the two formations. The result is as
follows :—The bed with large Natice at La Cordaz, which is the same
as the Cerithium-bed of the Diableretz, is intercalated between two
nummiulitic beds, of which the upper and most recent is by far the
thickest. This idea had already been entertained by M. Studer,
who had truly anticipated that this bed is only a local appearance,
for in many places it is altogether wanting, and the thick bed of
nummulitic limestone lies directly on the Gault. With regard to its
age, M. Renevier only repeats what he and M. Hébert had already
stated; viz. that the Cerithium-bed contaims a mixture in nearly
equal proportions of the fossils of the Sable de Beauchamp and
the Fontainebleau sand. - It is therefore probable that this nummu-
litie formation of the Vaudoise Alps forms a connecting link between
the eocene and miocene formations, and thus corresponds in age with
the gypsum of Montmartre and the paleeotherian fauna of Maurmont.
_ M. Renevier adds a list of the fossils from those nummulitic
beds, contaming 70 species; observing that there are from 15 to 20
more, of which the remains are too imperfect to be determined.

M. Ange Sismonda has communicated a letter to M. Elie de
Beaumont on the Nummulitic rocks (Bull. Soc. Géol. France, vol. xii.
p- 807), in which he gives the results of his brother’s paleeontological
researches on these beds. The nummulitic formation is divisible into
two great zones. ‘The lowest has many characteristic species, with a
few of those also found in the eocene formation, as the beds of the Cor-
biéres, Biaritz, and Nice. The upper zone may be divided according
to its fossils into two subdivisions ; the lowest of these has also some
species peculiar to it, mixed with a proportionately greater number of
eocene species. To this belong the beds of Saint Bonnet and Faudon
im France, Pernant and Entrevernes in Savoy, Cordaz and the Diable-
retz in Switzerland, Ronca, Castel-Gomberto and Montecchio-Mag-
giore in the Vicentin. The upper bed of the second zone contains a
much smaller number of species exclusively nummulitic, with a few
species peculiar to it, and a certain number of miocene species. To
this belong the beds with Nummulites of Acqui, Dego, Carcare, and —
other places in the valley of the Bormida. Of these two great num-
mulitic zones M. Sismonda considers the lowest to be anterior to the
elevation of the Pyrenees; this is the “‘ Mediterranean nummulitic
formation”’ of M. Elie de Beaumont, whilst that of Acqui is subse-
quent to this great elevation, and corresponds with the period of
M. E. de Beaumont’s nummulitic formation of the “Soissonais.”’

We are indebted to Mr. Daniel Sharpe for an interesting com-
munication on some of the more recent phenomena exhibited in the
alpine valleys. Having, during the past summer, again visited the
Alps with the view of carrying out those observations which he had
so successfully commenced last year, Mr. Sharpe’s attention was
directed to the numerous phenomena visible in most of the alpme

J2

Ixxil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

valleys and on the mountain-sides, which appeared to indicate the
action of the sea at a comparatively recent period. The object of
bis paper, “On the last elevation of the Alps, with notices of the
height at which the sea has left traces of its action on their sides,”’
is to describe the phenomena themselves, and to explain the probable
causes by which they have been produced. Mr. Sharpe endeavours
to show, that after the alpine region had assumed its present form,
and the existing valleys had been excavated, the whole country was
submerged below the level of the sea, and stood 9000 feet lower
than at present; and that it then rose out of the sea by a succession
of unequal steps, separated by long intervals of time, during which
the waves produced impressions on the mountain-sides, which are
still visible. The effects thus produced are described under three
heads. I1st.—The erosion of the mountain-sides in certain regular
and definite lines, above which they rise into rugged peaks in striking
contrast with the smoother forms below. This physical feature
had already been observed by Hugi and others, although attributed
to a different agency. Mr. Sharpe shows that throughout Switzer-
land these lines of erosion occur at three distinct levels, viz. 4500,

7500, and 9000 English feet above the sea; he points out their

occurrence in different valleys having no regular communication with
each other, and argues that no action but that of water could have
produced a uniformity of level over such an extensive area, and that
a long period of time was necessary to form such deep indentations
on the mountain-sides.

2nd.—The sudden increase of steepness which occurs at the head
of every alpine valley is assumed to be due to the excavating action
of water standing for a long time at that height. A table was given
of the elevation above the sea of the heads of between forty and fifty
valleys, at various altitudes; this shows a remarkable correspond-
ence of level between the excavation of the valleys and the lines of
erosion at 4500 and 7500 feet, but the ice and snow in the upper
valleys prevent all observations with regard to the highest line at
9000 feet.

3rd.—Mr. Sharpe considers the terraces of alluvium in the
valleys, in accordance with the opmion of Mr. Darwin, Mr. Yates,
and others, to have been formed by detritus carried down into
water standing at the level of the head of the terrace. The elevation
of many of these terraces is given, and a remarkable correspondence
is Shown to have existed between the height above the sea of terraces
in valleys which have no connection with each other, and of terraces
in some valleys with the heads of other valleys.

All these effects might have been produced by a sea surrounding
the Alps, but cannot be explained by any other means; and, the level
of this sea being assumed to have been constant, the Alps must have
been rising out of the waters while these operations were going on.
The period of this, their last elevation, is described by Mr. Sharpe
to have been after the Tertiary epoch, and a great part of the vast
accumulations of sand, gravel, and rounded blocks which are seen in
the vaileys of the Alps, and covering the lowlands of Switzerland are

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxxill

considered to have been formed by the waves beating against the
mountains during their elevation.

- Finally, with reference to the question of the angular erratic
blocks on the sides of the Jura and in other districts, the author
observes that, by showing that the levels at which these blocks are
found were below the sea for a long period at the epoch of their
removal, he gets rid of the only serious difficulty opposed to the
views of those who have supposed them to have been transported by
floating ice.

Objections have been raised against some of Mr. Sharpe’s views
on the ground of no marine remains having been found in the nu-
merous terraces which represent the ancient beaches or sea-bottoms.
Much of the force of this objection disappears when we consider the
nature of the deposit or detritus which forms these terraces. The
consist almost invariably of coarse sand, gravel, and rounded boulders,
the movement of which would have prevented the preservation of the
delicate shells which the marine waters may have contained. More-
over, the objection is merely a negative one, and when we consider
the remarkable fact of the terraces of alluvium occurring at the
same height on the opposite sides of the alpine chain, as described by
Mr. Sharpe, it appears impossible to doubt their having been occa-
sioned by the agency of water which enveloped both sides of the moun-
tains at the same time and at the same level, and it appears equally
certain that this body of water must have been an oceanic body. At
all events the existence of such a sea filling up the great Swiss valleys
affords a more simple mode of accounting for the occurrence of the
angular erratic blocks on the Jura, by supposing them to have been
floated across from the central chain on icebergs, than the theory by
which they are supposed to have been carried across on glaciers fill-
ing up the whole intervening space. It is asimilar fact to that of the
occurrence of enormous fragments of granite on the island of Chiloe,
which Mr. Darwin supposes may have been carried from the main
land across the intervening arm of the sea by the same agency.

Views of a nature somewhat different from those of Mr. Sharpe
have been advocated by M. A. Morlot in a paper published in the
Edinburgh New Philosophical Journal*, ‘On the past Tertiary and
Quaternary Formations of Switzerland.” The author of this paper
alludes to the numerous terraces that occur at different heights in all
the valleys of Switzerland, but he attributes the origin of the diluvial
formation or drift of which they consist to the action of the existing
system of rivers, when their beds were at a higher level, in conse-
quence of the continent standing lower by several hundred feet.
But he adds, if the continent were to be uniformly upheaved once
more, the rivers would scoop out a deeper channel in their modern.
deposits which would then project in the shape of terraces, as is the
case with the diluvial drift. Without stopping to examine this.
apparent contradiction of rivers forming the diluvial deposit and
then scooping it out, I will mention that the main object of the
author’s paper is to point out the existence of two glacial periods

* Vol. ii. 1855, p. 14.

Ixxiv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

separated by an intermediate diluvial period, during which the gla-
ciers, which had not only covered up a great portion of Switzerland,
but the vast lowlands of Northern Europe, disappeared even in the
principal valleys of the Alps to a height of at least 3000 or 4000
feet above the present level of the sea. And this diluvial period
after a long duration was again succeeded by a second glacial period,
during which the alpine valleys were again taken possession of by
the glaciers, though to a much more limited extent, the great glacier
of the Rhone not extending beyond Geneva, and standing at Vevay
full 2500 feet lower than the first glacier. The principal proof of
this statement the author finds in a section discovered by himself in
the neighbourhood of Clarens, where the superincumbent diluvium,
7 or 9 feet thick, forming part of a terrace 100 feet above the lake,
rests upon the glacial deposit at least 40 feet thick, consisting of com-
pact blue clay containing worn and scratched alpine boulders, thus
showing the existence of the first glacial period before the diluvial
drift was deposited, while evidence of the second glacial period is
found in the abundant deposits left on the diluvial terraces.

The subject is one of great interest, but at the same time of sonuiden
able difficulty, nor is it quite clear how the author makes out that
the deposits of the second glacial period have been left on the dilu-
vial terraces which overlie the first glacial deposits, when he endea-
vours to show that the second glacier stood so much lower than the
first.

Prof. F. J. Pictet has published during the past year the third
number of his work called ‘ Matériaux pour la Paléontologie Suisse,’ or
Collection of Monographs of the fossils of the Jura and of the Alps.
It contains, 1st, the Eocene vertebrated animals of the Canton de
Vaud, and 2ndly, the fossils of the Aptian system, giving in the first
mstance the bivalves and univalves.. -We may congratulate ourselves
on the progress of a work which, by uniting together all the fossil re-
mains of Switzerland, with good descriptions and accurate engravings,
will be of great assistance in promoting the study of Paleontology.

Germany. —It was stated in my address last year that Sir R-.
Murchison and Mr. Morris had communicated to the Geological
Section of the British Association at Liverpool a short notice of their
observations on the paleeozoic rocks of the North of Germany, viz. in
the Hartz and Thiringerwald; and that a full account of them
would shortly be laid before.this Society. This pledge has been
fully redeemed, and we have had laid before us from these gentlemen
a most interesting and valuable communication ‘‘On the Paleozoic
and their associated rocks of the Thiringerwald and the Hartz.”
Although I then gave a slight sketch of some of their observations,
I cannot now omit giving a short summary of the recapitulation with
which the authors:have concluded this important: paper.

They have shown that of the two districts described, the Thiirmger-
wald alone exhibits any of the oldest sedimentary rocks, the strata
containing the lowest Silurian fossils being there underlaid, as in
Great Britain and Bohemia, by vast masses of slate and sandstone, in

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxv

which no forms of a more composite structure than Fucoids have yet
been detected. These bottom rocks and the superposed Lower Silu-
rians of that tract were, it appears, elevated into dry land, and placed
during a long period out of the reach of sedimentary influence, since
none of those strata of the unequivocal Upper Silurian of Bohemia,
or the Lower and Middle Devonian, which are so much developed in
the Hartz, are to be seen in the Thirmgerwald.

Towards the close, however, of the Devonian era, both tracts were
again covered by a sea in which animals lived differing from all
those which preceded them, whilst the recesses of that ocean, whether
in this region or in the Rhenish provinces, were spread over by vol-
canic dejections which were interlaminated with ordinary submarine
beds. These were followed by other accumulations of mud and sand,
in which thin courses of coal were formed out of the transported
stems, branches, and leaves of land-plants.

After these lower carboniferous beds had been accumulated, a great
upheaval took place over all those parts of Germany and France
where such strata occur, raising them up with those which had pre-
ceded them. The next sediments formed on the edges of all that
preceded them are the feeble equivalents of our upper coal-fields,
and these were succeeded by the rothe-todte-legende or lower red
sandstone. And here the authors observe that our country offers no
example of that great break between the lower and upper divisions
of the carboniferous group which is so very dominant a physical
feature throughout Germany and France.

It was after the deposition of the lower red sandstone that one of
the most striking of the physical revolutions of this portion of the crust
of the earth took place im the change of the geographical direction
of the masses of rock, from their normal alimement of N.E. and S.W.
to one trending from N.W. to S.E., the turbulence of the period being
decisively marked by great outbursts of porphyry and the extravasa-
tion of vast sheets of porphyritic lava.

The authors then observe that it is evident from the disturbed
condition of the secondary strata between the Thuringerwald and
the Hartz, as well as from similar appearances to the north of the
Hartz, that each of these older masses was for a long period an
area of upheaval and oscillation, by which the interjacent forma-
tions were thrown into the plicated forms which they still exhibit.
The authors further infer that there are in the Thuringerwald.
proofs of ancient movements of which no trace is to be found in the
Hartz, thus affording evidence of the truly Jocal character of such
disruptions.

It is also observed, that, while each of these tracts presents some
marked analogies with the Silurian basin of Bohemia, each differs
more from that tract than they do from each other. In their great
fundamental rocks of greenish and talcose grauwacke, the South
Thiiringerwald and the district of Prague agree, as well as in the
chief mass of the Lower Silurian rocks, though the fossils of the
primordial zone of Bohemia have not been found in the Thuringer-
wald, and all the Lower Silurian is wanting in the Hartz; and the

Ixxvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

rich Upper Silurian limestones of Bohemia have no true representa-
tives in Thuringia. Again, whilst the Hartz contains all the members
of the Devonian rocks, with a copious development of the Lower
Carboniferous, and whilst the Thiiringerwald possesses neither the
Central nor Lower Devonian bands, none of these formations have
yet been found in Bohemia, where the Silurian rocks are at once and
abruptly followed by the upper coal-beds.

We thus see at what different epochs the breaks occur in the older
rocks of Germany and France, and in the paleeozoic series of Great
Britain. But the authors observe that, notwithstanding all these dif-
ferences, whether consisting of such local dismemberments or varied
lithological conditions, the four natural paleeozoic groups of Russia,
Scandinavia, Germany, and France have been perfectly assimilated
to their congeners in Britain ; so that, despite of great breaks in each
natural division of these regions, the classification by means of
Silurian, Devonian, Carboniferous, and Permian remains is every-
where maintained. ;

I would direct the careful attention of those geologists who may
be disposed to connect the great and general mutations of life with dis-
ruptions and disturbances similar to those here alluded to, to the con-
cluding observations of this paper. The authors state that, in Ger-
many no physical dismemberment has been observed which separates
the upper palzeozoic strata, accumulated at the close of the Permian
epoch, from the lowest mesozoic strata, formed during the earliest
period of the Trias, the summit of the one being everywhere con-
formable to the base of the other; and yet the change of life which
took place at that period of quiet physical transition was absolute and
complete.

It does not however necessarily follow (and I am not certain whether
the authors mean to infer it or not), that these Upper or Triassic
beds immediately followed the deposition of the Permian. For,
although no disturbances or change of inclination of the strata may
have taken place, an indefinite period of time may have elapsed be-
tween the deposition of the two formations ; that such was the case
is indeed rendered probable by the great change of organic life ob-
served between these two formations. But no evidence of such a
lapse of time would be forthcoming if the lower bed had maintained
its horizontality during the intervening period.

We have not yet received the completion of the text of the Drs.
Sandberger’s work on the ‘ Fossils of the Rhenish Devonian System
in Nassau,’ but I understand that we may soon expect it. In the
mean time, Dr. G. Sandberger has forwarded to me a catalogue
of the principal fossils figured in it, and which may serve as cha-
racteristic types of the formation. To this he has added a table of
contents, from which it appears that the followimg organic remains
are to be described in the work :—

Genera. Species. Newly described.
PIs@esh rs eh) a ae
Crustaceawie 24s Ls te een DOr eae 6

Annulataa iin as Biv act, SL as 5

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxvil

Genera. Species. Newly described.

Mollusca :—

1. Cephalopoda ...... Dict EF Ald iy, See 198 47

2. Gasteropoda -..... E Sis ahs BO ieee ssn ca

Sep hperopoda, ... ...22) Mie beet NPS si tarde

4. Pelecypoda ...... DES eee TO eee 27

5. Brachiopoda ...... LSet. sale BA eset ok 1]

Ge Dry 0208 6 2.0... 32. Dogtitdyet dee kash 5
Echinodermata ......... ED: eked vot eaeeee 10
SOME seh: Wier sisibac as sesh LO cpates BD, Hi tatiasy ]
PATTOTIMOZOA. <.0,cainsiec0s - Ln doeeaee | ee ceee al
Plantze :—

Pee lares),.. cco) icines jist Dk cee det 5

P. vasculares ......... Te waatass 11

Totaki:i.2, T30P 42.3 Siy ee 160

—thus affording an immense addition to our knowledge of the palzeon-
tology of this formation. This is followed by a geological descrip-
tion of the different beds which constitute the formation, and a tabu-
lar view of the distribution and development of the Rhenish or Devo-
nian system, and its principal members throughout the world.

M. Barrande has published, in the ‘'Transactions of the Bohemian
Society of Science,’ an interesting account of the parallelism between
the Silurian deposits of Bohemia and Scandinavia, in which he points
out, first, with regard to stratigraphical conditions, the thinness of
the Silurian beds in Scandinavia, as compared with their vast extent
and development in Bohemia. According to M. Angelin and Sir
_R. Murchison, the beds of Scandinavia are not above 1000 feet im
thickness, whereas those of Bohemia are probably fifteen times as
thick. It also appears that the sedimentary deposits of the two
countries were formed under very different local influences, both with
regard to the nature of the elementary substances constituting the
rocks themselves, as well as with respect to the vertical arrangement
of these substances. Moreover, the paleeozoic beds of Scandinavia
have almost universally preserved their original horizontality, while
the analogous deposits of Bohemia have been much elevated and
disturbed even before the commencement of the carboniferous period.

With regard to the paleontological relations between the two
countries, Scandinavia has not yet afforded nearly so many species as
the smaller basin of Bohemia. The different classes of animals also
offer remarkable contrasts between the two countries, one species
being more abundant in one country, and another preponderating in
the other. The great development of Crustacea is a remarkable fea-
ture of the Silurian fauna of both countries, and particularly of Scan-
dinavia, where no less than 350 species of Trilobites have been
registered by M. Angelin, while those of Bohemia only amount to
275. In general, however, there is a great resemblance in the facies
of the fauna of the two countries, with the sole exception of the fish,
one species of which has been found in Bohemia, but none in Scan-
dinavia. In neither country have any remains of land or freshwater
Mollusca been discovered, or even traces of land vegetation.

Ixxvill § PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

_ After giving a detailed comparison of the nomenclatures followed
in the description of the fossils, and of the local beds and their peculiar
fossils, as well as of the general fauna itself in the two countries, the
author sums up with certain general conclusions, in which he observes
that it would be difficult to find two countries, offering at the same time
such striking contrasts in the details and such harmony on the whole,
as Bohemia and Scandinavia. Some of these contrasts are very remark-
able. Out of 2500 or 3000 species found in the two countries, there
are scarcely any identically the same. Thus, out of 350 Trilobites
in Scandinavia and 275 in Bohemia, there are only six forms common
to the two countries.

After pointing out other contrasts and analogies, the author states that
these observations have led to the refutation of two opinions hitherto
almost universally accepted.. The one is that the earliest created
beings belonged to a class of organic life holding a very low position
in point of organization. This is disproved by the high degree of de-
velopment of the Trilobites, which evidently represent the earliest
living creation on the globe. The other is the generally received
opinion of the almost universal diffusion of the same fauna, in the
older beds, over all the seas of the ancient world. The comparison
of the faunas of Scandinavia and Bohemia shows that organic life in
the oldest periods was subject to the same limited and exclusive laws
of distribution and settlement as are observed in the present day.
This is particularly the case with the Crustaceans. The Brachiopoda
alone appear to have had a more universal extension in the Silurian
epochs.

"Prof Girard of Halle has published an interesting volume on the
Geology of the North German Plain, particularly between the Elbe
and the Vistula, accompanied by a geological map of the country be-
tween Magdeburg and the Oder. This district comprises those loca-
lities in which the Tertiary formations of North Germany are beiag
now so successfully worked out by Prof. Beyrich and others, and
we therefore hail with pleasure any additional information on the
subject. The author is Professor of Mineralogy at Halle, and, except
in so far as general remarks are concerned, does not appear to have
given much attention to the paleeontology of the country. The work
is divided into three parts, the first of which is a geographical and
orographical description of the country, containing an account of

its principal physical features — hills, valleys, and river-courses. »

There are curious speculations regarding the former course of the
Vistula through the lowlands to the west of its present line, and the
possibility of the Oder having also been similarly affected. After
describing the different ranges of hills, which partly intersect and
partly bound the district in question, the author concludes the first
portion of his work in the following words :—“ To recapitulate the
foregoing sketch of the East German lowlands, it represents, as we have
already stated, a triangle, the southern side of which is formed by
certain ridges of hills equally extended and but slightly separated,
whilst the north side consists of a chain of hills broken up by nume-
rous gorges; between these hills a flat extent of country stretches

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxix

away, which towards the east assumes the character of a marshy plain,
and towards the west that of a much interrupted undulating table-land.
The waters of the Polish and German mountains flow into this low plain
from the south and from the east, first pressing themselves along its
southern barriers until they find an opportunity of breaking through
them, and reaching the intermediate lowlands, and then either fol-
lowing the general inclination to the north-west, or finding a shorter
outlet into the sea between the northern ridges.”

The second part gives a systematic view of all the geological forma-
tions which occur in the district ; especially those existing along the
southern or northern boundaries, although occasionally a few insu-
lated outliers are met with, as the island of Heligoland, the rocks
of Liineburg, &c. No crystalline rocks have been found. The oldest
formation is that of the Trias, the Bunter Sandstein of which forms the
whole of the island of Heligoland, whilst at a distance of upwards of
a hundred miles to the south-east, the similar rocks of Liineburg
are found in the direct continuation of the line of strike. The rocky
reefs on the east side of the island of Heligoland show the regular
series of overlying formations, all dipping to the north-east or east-
north-east, consisting of Muschelkalk, Middle Jura, Hils-clay or
Gault, and above it the White chalk. The followig formations are
then fully described by the author. 1. Trias formations. 2. Jurassic.
3. Chalk. 4. Tertiary. The insulated occurrence of some of these
formations at great distances from each other over this vast tract of
country is very remarkable. They point to the former existence of
islands, and of reefs in the tertiary seas, by which they were partially
worn down and covered up. The occurrence of the Coral-rag: or
Upper Jura on the banks of the Vistula, and at a great depth, discovered
in boring for salt, is pomted out as singular, being the only instance
of this particular member of the Jurassic formation having been
found in this part of the continent, inasmuch as the Jurassic rocks to
the eastward, in Courland, Lithuania, and Russia, are described by
Murchison, De Verneuil, and Keyserling as belonging to the Lower
and Middle Jura formations,

The consideration of the Cretaceous formations follows next. The
author points out the important differences which existed between
the physical character of the two cretaceous seas, the one of which
occupied the Mediterranean basin and the South of France, the other
extending from England and the North of France between Germany
and Scandinavia into Russia; but I do not understand on what
grounds the author assumes that this northern cretaceous sea (p. 54)
had no communication with the Western and Southern Ocean.
What barrier existed to the west or north-west to shut off its com-
munication with the Atlantic ?

Of the Tertiary formations, the Brown-coal deposits are considered
by the author as the oldest, and he adopts Von Buch’s opinion that
there is only one brown-coal formation in Europe. Yet he admits
that there are certain brown-coal formations, which, both from the
positions in which they are found and from their organic contents,
must have been caused by totally different agencies. He considers

Ixxx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the brown-coal generally as a marine deposit, and to have been
occasioned by the heaping together of drift-wood on the sandy bottoms
of the ancient seas, and does not admit that any great change of
level took place between the cretaceous and tertiary deposits. Next
in importance is the Septaria-clay, with its numerous fossils, over-
laid by diluvial deposits; these the author divides-into northern and
southern formations.

The third portion of the work is occupied with the geological de-
scription of particular districts.

Prof. Girard has also published during the past year another work
entitled ‘ Geological Wanderings.’ It consists of a series of letters
written in the preceding year, in which he has described some of the
chief geological features of parts of Switzerland, particularly the
Valais and neighbouring districts ; the Vivarais and its older rocks,
basalts, and volcanoes ; and finally, the Velay and Le Puy, in which
many of the phenomena connected with the igneous and plutonic
rocks of that interesting district are described and analysed. One of
the author’s chief objects i in the Velay was to inquire into the extent
and origin of the basalts, and he found there, as in the Vivarais, that
these rocks were much older than the volcanos, and that they were
entirely independent of them; he also found that the volcanic moun-
tains of the Velay consisted solely of scoriaceous outbursts, and that
no lava-stream had flowed from them; in.this respect confirming
the observations of former travellers.

Dr. Guido Sandberger of Wiesbaden has recently published in the
‘Journal of the Nassau Society for Natural History,’ an account of
the first discovery of a species of Clymenia in the Cypridina-slates
of the Devonian system, near Weilburg in Nassau. For many years
Dr. Sandberger and his brother had in vain sought throughout this
formation, and particularly in the limestone-masses contained in the
Cypridina-slates, for the genus. ‘This discovery is the more interest-
ing, as it confirms the identity of this deposit with the Cypridina-
slates of other districts.

One species only has as yet been found in Nassau, and that is
new ; the name of Clymenia subnautilina has been given to it. The
genus Clymenia was originally proposed by Count Munster, and
we are already indebted to Dr. G. Sandberger for a notice in the
‘Bulletin de la Société Impériale des Naturalistes de Moscou’ of 1853,

iving an account of the nature and characteristics of Clymenia and the
allied form of Goniatites. Some interesting remarks on the analogies.
between these two genera, by Dr. Sandberger, will also be found in his
memoir on the ‘Organization of Goniatites,”’ in the ‘ Journal of the
Nassau Society for Natural History,’ 1851. In the notice under
consideration, the author alludes to the measurement of the thick-
ness of the whorls of this species of Clymenia by means of the Lep-
tometer, an instrument invented by himself for the purpose of mea-
suring thin bodies, which could not be got at by any ordinary ruler or
compasses. He observes in a recent communication that he has given
it this name (from ezros, thin), on account of its being adapted to mea-
sure the thickness, slope, and taperness of all possible minute and thin

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxxi

flat bodies, whether concave, convex, or flat, or any combination of
these forms, as well as the dimensions of irregularly formed bodies.
It is also applicable to the measurement of crystals and minute objects
of natural history, and to other purposes connected with the arts and
industrial pursuits. Even the thickness of a sheet of paper may be
ascertained by means of it. Dr. Sandberger has presented one of
these instruments to this Society, to which I have already had occasion
to direct your attention, and for which our best thanks are due to
him.

During the past year Prof. Beyrich has published, in the ‘ Journal
of the German Geological Society,’ the third part of his work on the
shells of the tertiary formation of the North of Germany. The
genera described in this part are Tritonitum—Triton, Lam., 7 species ;
Murex, 14 species ; Tiphys, 4 species ; Spirilla, 1 species ; Leiostoma,
1 species ; Pyrula, 6 species. It is impossible to overrate the import-
ance of this work, and when we consider the attentive care which
Prof. Beyrich has brought to bear on the task he has imposed on |
himself, we are justified in looking forward to its completion as the
Inauguration of a new epoch in our knowledge of the North German
Tertiaries and of their relations to those of Belgium, France, and Eng-
land. I have fully alluded to this question on a former occasion ; I
will therefore now merely recal to your attention the objects which
Prof. Beyrich had in view in undertaking this work. When he
first began to direct his attention to this subject, he soon perceived
the insufficiency and incorrectness of all the previously existing
catalogues or lists of names of the molluscous fauna of the tertiary
beds of North Germany, and how ill-adapted they were to enable
the geologist to establish a correct comparison between it and
the fossils of other countries. They were generally unaccompained
by illustrations. This evil had been already acknowledged by the
Imperial Geological Institute of Vienna, who had charged Dr. Hornes
with the preparation of a separate work on the fossil shells of the
tertiary basin of Vienna, in which not only the names, but full descrip-
tions and accurate drawings of all the species should be given. What
Dr. Hornes had undertaken for the Vienna basin, Prof. Beyrich pro-
poses to accomplish for the North of Germany.

“It is my intention,” observes Prof. Beyrich in the first part of this
work, ‘to extend my observations to all the tertiary formations which
have been discovered from the frontiers of Belgium and of Holland,
eastward through Germany as far as the Oder. All these formations
belong undoubtedly to one series of deposits closely connected with
each other, and of which the faunas are so intimately allied by nume-
rous gradations, that the removal of any single member from the
series would destroy the continuity of the whole. In order to have
a clear insight into the relative connexions of deposits which occur at
such various and distant points, we must bring together for compa-
rison the fossils from the neighbourhood of Disseldorf, Osnabriick,
and Biinde, those of Hildesheim and Cassel, those of Limeburg and the
island of Sylt, as well as those from the neighbourhood of Magdeburg,
and from the Marches of Brandenburg. We must also examine the

!

Ixxxli PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

tertiary shells which have been transported into new positions in the
diluvial deposits, in order to obtain a perfect view of the molluscous
fauna of the tertiary seas of the North of Germany.”’

It is well known that Prof. Beyrich and others have looked upon
these German Tertiaries as Lower Miocene rather than Upper Eocene.

‘He has founded this opinion on the fact that the oldest Tertiary

formation in this part of Germany, which he calls the Magdeburg
Sands, agrees most with that of Lethen in Belgium, which belongs
to the lower portion of the Systeme Tongrien, and immediately overlies
the Systéme Lackenien, the uppermost of Dumont’s five systems,
which, taken together, are the equivalents of the Paris Eocene for-
mations up to the sand of Beauchamp, and of those of England up to
the Barton clay. In the last part of his work now under considera-
tion, Prof. Beyrich explains the reasons which have induced him to
adopt a new term to denote this particular formation instead of that
of Lower Miocene which he has hitherto used.

He observes, ‘“‘Since I determined in the introduction of this

' work, contrary to the views of Lyell, to call the North German equi-

valents of Dumont’s Tongrian and Rupelian system Lower Miocene
rather than Upper Eocene, the contents of the separate faunas, which
all belong to the same system, have been greatly increased by the
communications which I have received from all directions. The in-
dependent separation of these faunas, both from the Kocene below, as
well as from the Miocene above, with which they are only connected
at their respective limits by a greater number of common species, has
been thoroughly established at every successive step of the inquiry.
I have, therefore, thought it desirable to recognize this peculiar
Tertiary group as a separate independent formation, by giving it a
new and specific name. For this purpose I proposed, in a former
Memoir on the position of the Hessian Tertiary formations, the name
of Oligocene, a word in evident etymological connexion with the
universally adopted terminology of Lyell, and also expressing an idea
between Eocene and Miocene.”

This proposal of Prof. Beyrich is, perhaps, under the circumstances,
the best that could be adopted. It is an additional proof of what has
been already advanced in these rooms respecting the impossibility of
fixing precise limits between different formations, and of the probabi-
lity that as our knowledge increases we shall be compelled by degrees
to abandon all those breaks and subdivisions which were formerly
looked upon as the legitimate boundaries between successive geolo-
gical periods. It is a term which may be appropriately applied to the
formation of the Mayence basin, for which I have also advocated the
term of Lower Miocene instead of Upper Hocene, inasmuch as it re-
cognizes that formation as marking the commencement of a new series
of deposits, in accordance with the facts themselves, rather than the
conclusion of an old series ; and at the same time it meets the views
of those who were unwilling to recognize a Miocene facies in the
fossils of that region.

In the course of last summer I communicated to the Society a short
notice from Prof. Beyrich, in which he observed, with reference to my.

—=—_—-—

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxxxili

observations on the brown-coal of North Germany, that no German
geologists had ever stated that the Septaria-clay had been found
under the brown-coal, and that I was consequently in error in
assuming the existence of two distinct brown-coal formations, the
one above and the other below the Septaria-clay formation of Berlin,
Magdeburg, &c., as I had asserted in my Address from this chair last
year. In making this communication, I ohserved that this correction
of what I had supposed to be the order of stratification in North
Germany would be attended with important results, as we could in
this case no longer recognize that connected system of superposition
of strata which I believed had been made out between the Westeregeln
beds near Magdeburg (Toxgrien inférieur of Dumont), and the more
recent Miocene formations of the Vienna basin. I also stated that I
trusted that the exertions of the many able German geologists now
engaged in the investigation of the Tertiary formations of Germany,
would soon enable us to ascertain more correctly the true connexions
between the tertiaries of North Germany and the younger deposits of
the Vienna basin.

I have consequently been much interested in finding in the last
volume of the Journal of the German Geological Society * a commu-
nication from Dr. Koch to Prof. Beyrich, in which he states that in
the course of a geological examination of the districts of Carentz and
Conow in the neighbourhood of Domitz, he had discovered a Septaria-
clay formation. A subsequent visit, after the clay beds had been
further opened out, procured him some interesting and characteristic
fossils, proving it to belong to the true Septaria-clay. Amongst these
were Nucula Deshayesiana, Nyst, Lucina unicarinata, Nyst, or L.
obtusa, Beyr., Pleurotoma subdenticulata, Minst. Goldf., with a cast of
a Nucula resembling N. Chastelii1, Nyst, besides many well-preserved
species of Foraminifera. The position of these beds led Dr. Koch to
the conclusion that they underlie the brown-coal formation, which
is extensively developed in that district. Should the further inquiries
which Dr. Koch intended to make at a subsequent period confirm
this statement, it will show that, contrary to the hitherto-received
opinion of the German geologists, there really does exist a brown-
coal formation superior to the Septaria-clay, and it may possibly
turn out after all, as there is as yet no positive evidence against it
according to Prof. Beyrich’s own remarks, that the brown-coal for-
mation of Brandenberg really does occupy the position [ had origi-
nally assigned to it. At all events, there is still a wide field open for
future investigation and discoveries in the Tertiary: formations of
North Germany.

‘With regard to Southern Germany, however, there is no doubt of
the existence of brown-coal of a much younger date. I find in the
Neues Jahrbuch of Leonhard and Bronn for 1855, p. 206, a state-
ment that Prof. M. P. Lipold describes the brown-coal of Wildsfluth
in Upper Austria, in the district of the Inn, as belonging, according
to the vegetable remains it contains, to the upper division of the
Tertiary formation, and that it must therefore be considered as

* Zeitschrift der deutschen geol. Gesellschaft, vol. vii. part i. p. 11.

Ixxxiv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

belonging to the newest brown-coal. In the account of the mining-
industry of Austria, recently published, there is a place called Wild-
shut on the Salza, entirely agreeing with this description, where a
seam of coal, 9 feet thick, is worked. This is probably the same
place as that alluded to by Lipold, of which I have not been able to
find any further notice.

I must refer you to the Journal of the German Geological Society
for other valuable papers on various points connected with the progress
of geology during the present year. You will find in one of the last
numbers, eed only a few days ago, an important communication
from Dr. Bornemann of Mihlhausen, « on the Microscopic Fauna of the
Septaria-clay of Hermsdorf near Berlin. The author has increased
the number of species of Foraminifera, from this locality alone, from
62 given by Prof. Reuss, to 117; of the 55 new species, 47 are abso-
lutely new, and they mark a decided difference between the Tertiary
formations of the North of Germany, and those of the Vienna basin.
The number of species of Entomostraca has also been increased from
2 to 15.

The remarkable mass of igneous rocks called the Kaiserstuhl, in the

valley of the Rhine, between Strasburg and Basle, must be well known ©

to all geologists who have visited that part of Germany. It is known
to all German mineralogists as the best locality for many interesting
and scarce minerals. Prof. Sandberger’ informs me that metamor-
phosed Tertiary formations containing fossil plants, such as Daphno-
gene polymorpha, have been found in it, wedged in amongst the
basalts ; these tertiary beds must therefore have been broken up by
the igneous outbursts. The bed which overlies the pisolitic iron-ore
(Bohnerz) of Kandern contains the same plants, and is in fact un-
distinguishable from the leaf-bearing sandstone of the Mayence
basin. I may here also mention, that most of the fossils- of the Alzey
fauna have been found near Kreuznach, in the barytic sandstone of
the Hardt. Hitherto only a few of the Mayence basin fossils had
been found in that locality. And finally he informs me that the land
and freshwater shells of Wiesbaden have been found near Gratz, but
unfortunately not yet in contact with the marine beds of the Vienna
basin.

I have now to call your attention to two valuable papers by Prof.
Ludwig of Mannheim, well known for his geological investigations re-
specting the southern slopes of the Taunus,-and his intimate acquaint-
ance with the geology of the Wetterau. They are published in the last
yearly Report of the Wetterau Society for Natural History at Hanau.
The first is on the connexion between the Tertiary formations in
Lower Hesse, Upper Hesse, in the Wetterau, and on the Rhine.
Recognizing the marine sands of Alzey as the oldest of these forma-
tions, Prof. Ludwig points out the different localities at which the
various formations occur, and the relative positions of the marine,
brackish, and fresh-water deposits ; and to all who take an interest in
the tertiary geology of Northern Germany this memoir will be of the
greatest use. Looking, however, to the physical structure of the
country; he does not consider, notwithstanding the close approach of

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxxv

the fossils of the Alzey marine beds to those of Hesse-Cassel and Mag-
deburg, and others, that there was any direct communication between
the two seas. The Gulf of Alzey he considers to have been probably
in immediate connexion with the Mediterranean or Southern Ocean ;
he suggests that the molasse of Switzerland may have formed a portion
of the same formation, and that its waters did not extend northwards
of the Taunus and the Hundsriick. The marine beds of Cassel, on
the other hand, belonged to the southern prolongation of a northern
ocean. Considering the large number of fossils in these Alzey beds,
_ which have been identified with those of the North of Germany and
of Belgium, I think this complete separation is somewhat doubtful.

The following table appended to the memoir will show how Prof.
Ludwig arranges chronologically the different tertiary formations of
Germany :—

A. Pliocene. |
Basalt clay ; brown-coals of Dorheim and Annerod.
B. Miocene.

1. Systéme Bolderien of Belgium. The dark sandy clays of Winters-

wick in Holland; near Bockholt in Westphalia; from Celle near
’ Gustitz, north of Perleberg in Preignitz. Wanting m Hesse and on
the Rhine.

2. Stemberg shell-sand, marine sand of Crefeld, Osnabriick, Bide,
Hildesheim, Alfeld, Luithorst, Guntersen, from Reinhardswald,
Hesse Cassel, and Wilhelmshohe.

3. Systéme rupelien supérieur. Clays of Boom, septaria-clay of Celle,
Hohenwarth near Magdeburg. Gorzig near Kothen, Hermsdorf,
Freienwalde, Bukow, Joachimsthal, Stettin, Oberkaufungen Neu-
stadt, Eckardroth. :

Brackish and freshwater formations of the same age. Leaf-sand- °
stone partly, Littorimella-limestone, blue clay,the most recent brown-
coal formation of the Vogelsberg.

4. Systéme rupelien inférieur. Marme. Pectunculus-bed of Bergen
in Belgium, Alzey sands. Sandstone with Ostrea longirostris of
Bad Sulz, marine molasse of Switzerland.

Brackish and freshwater formations. Cyrena-marl, Cerithium-
beds with brown-coal and impressions of leaves (leaf-bearing sand-
stone in part) from the Rhine-Wetterau basin; clays with Cerithium,
Littorinella, and Melania ; brown-coals of Lower Hesse as far as the
neighbourhood of Marburg.

The second paper contains a list of all the tertiary fossils found in
the Wetterau arranged stratigraphically, and describes the relations
of the different formations in which they occur. This paper is also
one of great merit, and, in recommending it to the notice of tertiary
geologists, I will only observe that I cannot find any satisfactory
reason for considering the Cyrena-marls and Cerithium-beds to be of
the same age as the marine sands of Alzey. There can be no doubt
that near Weinheim and Alzey, the blue clays with Cerithium and
Cyrena overlie the marine sands of Alzey, and I do not understand
why Prof. Ludwig should assume a different chronology with respect
to the beds of the Wetterau where the marine sands do not occur.

The Imperial Geological Institute of Vienna has, on the occasion
VOL. XII. g

Ixxxvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

of the Universal Exhibition at Paris, published an interesting volume
respecting the mines and mineral wealth of the Austrian empire,
entitled, “‘ Geological View of the Mining Industry of the Austrian
Monarchy,” prepared and arranged by Herr v. Hauer and Herr
Foetterle. It is well arranged under the different heads of metals,
iron (special), salt, coal, &c. This is preceded by a geological sketch
of the Empire divided into four great groups or districts. These
are—1l. Bohemo-Moravo-Silesian district; 2. Alpine district; 3.
_ Carpathian district; 4. Tertiary and alluvial plains. All the geo-
logical formations occurring in each are systematically arranged and
their geographical boundaries pointed out, with a sketch of the
principal physical features of each formation. It is impossible to
estimate too highly the importance of the work as a book of refer-
ence for the geological formations of the different portions of the
Austrian Empire.

We are greatly indebted to Count Marschall of Vienna for having
undertaken to supply us with MS. notes of the proceedings of the
Imperial Geological Institute of Vienna, by which we have been put in
possession of their proceedings long before the printed notices could
otherwise have reached us. In one of his recent communications to
Mr. Jones, who is the channel through whom this correspondence is
carried on, we have an abstract of Director Haidinger’s address at
the commencement of the present session. From this we learn that
the Geological Survey of Austria is progressing rapidly and satis-
factorily. Since the death of M. Czjzek, the survey of Bohemia
has been entrusted to Dr. Hochstetter, who, in the distribution of
the different districts, has reserved to himself the N.E. portion as well
as the communication with the Saxon geologists, especially with Prof.
Cotta, with the view of connecting his map of the frontier district
with the surveys already executed by order of the Saxon government.
The districts south of the river Drave are already so far surveyed
that the Institute has now sufficient materials in hand to enable
them to construct the geological map of the whole of the Duchy of
Carinthia, together with portions of Carniola, Goritzia, and the Vene-
tian territory. (The Chevalier von Hauer has carefully examined the
country across the Alps, from Passau on the Danube to Duino on
the shores of the Adriatic, in order to exhibit to the meeting of
German naturalists, which was to have been held at Vienna in Sep-
tember last, a complete section of the whole geological structure of
the Alpine chain. This meeting, as has been already mentioned,
was postponed to the present year, in consequence of the prevailing
epidemic. ‘The environs of Tured on the shores of Lake Balaton, in
Hungary, have been surveyed by the Chevalier Zepharovich, and
considerable progress has also been made in the geological survey of
portions of Styria.

The Chevalier v. Hauer and M. Foetterle, ably assisted by Dr.
Hornes, have completed the rearrangement of the most characteristic
collection hitherto made of the fossils of the secondary deposits of
the Alps and the Carpathians, and of the nummulitic and other upper
tertiary beds. These latter connect the whole of this new series with

-

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxxvii

.

the beautiful collection already exhibited of the fossils from the
tertiary basin of Vienna. The secondary strata represented in this
series are, in ascending order, the grauwacke beds, the Werfen and
Hallstadt strata, the Dachstein limestones, the Késsen, Gresten,
Adneth, and Hierlatz strata (to most of which I had occasion to
allude in my former address), the jurassic, neocomian, Gosau, and
upper cretaceous formations. The ninth part of Dr. Hornes’s valuable
work on the ‘ Fossil Mollusca of the Vienna Tertiary Basin,’ contain-
ing the genera Cerithium, Turritella, Phasianella, Turbo, Monodonta,
Adeorbis, Xenophora, and Trochus, with five plates, has just been
published. Having on a former occasion alluded to the importance
of this work, the true value of which had been already recognized by
my predecessor, I will now only observe that when completed this
work wiil be indispensable to the student of tertiary geology.

Dr. Hornes has also communicated to the Imperial Academy of
Science at Vienna some interesting particulars respecting the pecu-
liar geological position of the Hallstadt beds which occupy a fixed
calcareous zone along the whole line of the Alps, from Hornstein to
the Tyrol, and which have so long been an enigma to geologists.
The discovery of numerous organic remains, and their careful exa-
mination have shown that this formation contains a very remarkable
fauna, peculiar to itself, exclusively Alpine, and of which no one
species can be identified with non-alpine forms, although several
show a great resemblance to forms which in other parts of Europe
are characteristic of paleeozoic and jurassic formations. This is the
more remarkable, as both in the beds above and in those below, forms
occur which are identical with non-alpine forms,—e.g. Herr v. Hauer
has found in the grauwacke beds of Dienten, five species found in
other parts of Europe, and M. Sitiss also points out several non-
alpine forms as occurring in the overlying Kossen beds. Another
peculiarity of this Hallstadt fauna is that the most typical species
show a great resemblance partly to paleeozoic and partly to jurassic
forms: thus the genera Holopella, Loxonema, and Porcellia are re-
lated to the former; whilst the species of Phasianella, Turbo, Neri-
topsis, Pleurotomaria, Cirrus, and Lima have a jurassic type.

Thus it appears that, while in a paleontological point of view these
beds cannot be satisfactorily identified with any non-alpme forma-
tions, stratigraphical investigations have recently shown that they
should be considered as the equivalents of the upper trias beds of
the rest of Europe. These remarks appear to confirm the opinion
already given by Prof. Merian.

In further reference to this subject, the following additions to the
paleontology of this district have been published in the ninth volume
of the Memoirs of the Mathematical and Natural History Class of the
Imperial: Academy of Sciences at Vienna : —“ On the Brachiopoda of
the Hallstadt beds,” by Edward Siiss, with two plates ; “ On the Gas-
teropoda and Acephala of the Hallstadt beds,” with two plates, by
Dr. Hornes; “Supplement to the knowledge of the Cephalopod
fauna of the Hallstadt beds,”’ by Franz von Hauer, with five plates.
Respecting the discovery of these fossils by Dr. Fischer . Munich,

; g

IxXxxvill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

a
Herr v. Hauer observes, that the results obtained by Hornes and
Siiss in their respective investigations entirely agree with those
which he had obtained from the study of the Cephalopoda. Not
one of the species in all these different classes had hitherto been found
beyond the Alps. They are principally entirely new forms, and
only a very few of them were known from the Saint Cascian beds.
There are no less than twelve new species of Ammonites, the whole
number previously known from the Hallstadt beds being twenty-
five.

This result appears the less extraordinary since the true geological
position of the Hallstadt beds has been more exactly determined.
They form, according to von Hauer, an upper member of the triassic
series which has never yet been found except in the Alps, and which
must be considered as about contemporary with the Keuper, so poor
im marine remains, and which is altogether without Cephalopods.
The character of the fauna of the Hallstadt beds also corresponds
well with this age. It fills up the gap which appeared to exist be-
tween the fauna of the palzeozoic and that of the secondary forma-
tions, a gap which was in a great measure owing to the scarcity of
organic remains in the trias formations beyond the Alps. It includes
forms of the paleeozoic type, as e. g. numerous Orthoceratites, Ammo-
nites, with smooth sides and lobes, completely evolved Nautilus, &c.,
combined with Ammonites of the families of the Ceratites, Arietes,
and Heterophylla, and Nautilus of the Jurassic type. Dr. Hornes
makes the same observation respecting the remarkable combination of
palzozoic and jurassic forms with reference to the Gasteropoda and
Acephala found in these Hallstadt beds.

The same volume also contains an account of the Chelonian remains
from the Austrian tertiary deposits by Dr. Karl Peters. The specimens
described belong to the genera Trionyx, Emys, and Chelydra, and Dr.
Peters states that in the description of them he has in general followed
the views of the author of the ‘ Monograph on the Fossil Reptilia
of the London Clay.’ These Chelonian remains are all derived from
the Neogene deposits of Austria; but Dr. Peters observes, that since
he had completed his memoir he has received from the brown-coal
of Siverich a fragment of a new species of Trzonyz, the first species
of tortoise yet found in the eocene formations of Austria. It comes
from the same coal-beds as those in which the Anthracotherium dalma-
tinum of Herm. v. Meyer was found, and which belong to the nummu-
litic series. Herr. v. Hauer has communicated to the same Academy a
notice of some fossils found in the Dolomite of Monte Salvatore, near
Lugano, which confirm the impression that this Dolomite and the
underlying Verrucano belong to the Trias formation. We owe the
discovery of these fossils to the Abbe Giuseppe Stabile of Lugano,
and his brother. Many of them are true Muschelkalk fossils, and
point, as Herr v. Hauer observes, to the great analogy between these
beds and those of the Trias formation of the northern Alps, and
more particularly identify them with the Hallstadt and Guttenstein
beds.

I will only further mention that Dr. Frederic Rolle has communicated

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxxix

a paper on the Echinoids of the Upper Jura beds from Nikolsburg
in Moravia, with a description of the new species found in that
locality, and refers to the previous works of MM. Ferstl, Hornes,
Stiss, and Foetterle, who had already partially examined the geology
and palzeontology of that district.

The occurrence of a fragment of carbonized wood in the rock-salt
of Wieliczka, a specimen of which had been forwarded by Prof.
Zeuschner to Prof. Hausmann of Gottingen, has been the subject of
much discussion at Vienna. The fragment which still exhibits the
structure of wood has generally a lignite appearance, although Prof.
Hausmann is rather disposed to compare it with certain species of
anthracite from the Meissner in Hesse, and also considers that it has
been exposed to and altered by the action of heat. This, it has been
observed at Vienna, would reopen the question, how far rock-salt is
to be considered as the result of an eruptive process. I do not see
it in this light. For even admitting that the wood has: been acted
on by heat, it does not necessarily follow that: that action must have
taken place after it was imbedded in the rock-salt. But the carbo-
nization of fossil wood is not necessarily the result of heat. Nor
does it appear that there is any ground for reverting to a theory now
supposed to be exploded that rock-salt is an igneous product.

It is also highly satisfactory to observe, that considerable progress
is being made in working out the geology of the more distant pro-
vinees of the Austrian Empire.

In the ‘Comptes Rendus’ for September last (p. 386) is a notice
by M. Francois Lanza on the geological formations of Dalmatia.
Omitting all reference to the tertiary beds, of which the fossiliferous
beds of the eocene period are the most important, M. Lanza con-
fines his attention for the present to the cretaceous formation. The
series of white chalk (a craie blanche) contains numerous species of the
family Rudistes, many of which are new. Of these, several species of
Radiolites and Hippurites appear to be the most important. Some
of them are of large size. M. Lanza found in the cretaceous lime-
stone of Verpolia, near Sibenico, a gigantic Hippurite of which he
possesses a fragment 80 centimetres in length, with a diameter of
10 centimetres. The author has never found any species of Inoce-
ramus in this Hippurite limestone, although he found several new
species in the supracretaceous beds of yellow marly sands, associated
with Nummulites. He also found a calcareous schist with Ichthy-
olites in the Jurassic formation. Through the labours of the Vienna
geologists we may now hope that the interesting details of the geology
of Dalmatia, apparently rich in fossils, will soon be satisfactorily
worked out.

In the Report of the Proceedings of the Imperial Institute of Geo-
logy for March 1855, Prof. Lipold has communicated additional in-
formation respecting the cretaceous and eocene formations in the N.E.
portion of Carinthia*. Dr. Hornes has lately made out fifteen fossil
species, which belong to the lowest members of the eocene formation,
and have the greatest resemblance with the fossils found in the Val

* Neues Jahrbueh fiir Mineralogie, 1855, p. 586.

XC PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

di Ronca. The lowest beds consist of unfossiliferous clays, over
which are fossiliferous marls and marly limestone, with seams of
coal; these are succeeded by yellow and white sands, above which
again are sandy and calcareous beds, abounding with Nummulites,
which form the upper member of the deposit. Echinoderms also
abound in the nummulitic limestone of Piemberg. These beds rest
on the north side of the trough, on argillaceous mica-slate, and on
the south side on the cretaceous formations. These latter, however,
are more extensively developed in the north-eastern portion of Carin-
thia, and the occurrence of Hippurites (Rudiste) leaves no doubt of
their belonging to the chalk ; here they consist of marls, sandstones,
and limestones, the latter being the most predominant. In these the
author also found several species of corals and undetermined bivalves.
The author concludes by describing the other localities in which these
cretaceous beds occur in Carinthia.

Norway.—In the last number of the Edinburgh New Philo-
sophical Journal, Mr. David Forbes has published an interesting
paper on the Silurian and Metamorphic Rocks of Norway, the result
of investigations partly undertaken at the request of Sir R. Murchison.
This communication must be considered only as an introduction to
the subject, as from the natural difficulties of the country considerable
time will be required to enable him to produce any detailed account
of the rocks, especially as regards their fossil contents. Mr. Forbes
describes the peculiar appearance of the foliation of the metamorphic
rocks on the western side of Langesund Fjord as in striking con-
trast with the Silurian beds constituting the promontory of Lange-
sund, which have a general dip of 12° to the eastward. The
appearance was so striking, that it at once annihilated all idea of its
having resulted from any alteration of the original lines of stratifica-
tion. The occurrence of miles of such vertically foliated rocks,
differmg even as they do in mineral composition, seemed to Mr.
Forbes incompatible with the idea of supposing them to represent
originally horizontal strata tilted into a vertical position. He is dis-
posed to think, that, having been originally deposited as a moderately
thick and nearly horizontal bed of sandstone, conformable to the
Silurian strata now seen overlying them at one extremity of the
section, the foliated arrangement is due to their having been affected
by the intrusion of granite veins and other agencies, thus producing
a series of cracks and; joimts, possessing comparative regularity when
viewed on a large scale. . After describing the principal geological
features and the organic remains of the district he visited, Mr. Forbes,
in concluding his remarks, again returns to the question of the vertical
foliation, and, repudiating the idea of stratification having produced
it, refers to an opinion formerly pronounced by himself, that the
particles of matter in rocks may rearrange themselves at a compara-
tively low temperature, and he believes that this theory will give the
best explanation of the phzenomenon, and that there will thus be no
difficulty in accounting for the vertical structure of these rocks.
Setting aside, then, the direction of the lines of foliation as due to
other causes, and keeping in view the character of the rock masses

ANNIVERSARY ADDRESS OF THE PRESIDENT. x¢cl

of the whole, Mr. Forbes thinks that certain dotied undulating lines
which he has drawn through the vertical foliations will represent
the old lines of stratification, and present only a series of undu-
latory beds due to upheaval or subsidence, and that he will thus be
able to analyse large tracts of gneissic formation hitherto considered
irresolvable.

When we consider the numerous cases where this vertical, or almost
vertical, foliation occurs in crystalline and metamorphic rocks, the
explanation here given becomes of great importance. At the same
time it should be observed, that unless some indication of the ancient
stratification is still visible, either in lines of colour or in some change

of mineral appearance, it does appear to be rather a bold assumption

to imagine a series of lines of stratification of which no evidence
exists, merely on the authority of a somewhat parallel system in the
Silurian deposits, which at one extremity of the section overlie these
metamorphic beds.

M. Theodor Kjerulf, to whose labours in the field of the pale-
ozoic geology of Christiania I alluded last year, has lately com-
municated to Sir R. Murchison some additional information on the
subject, obtained during the past summer. M. Kjerulf separates
the beds of the Silurian basin of Christiania into three divisions or
groups, of which the lowest two are decidedly Lower Silurian, and
the greater part of the upper group decidedly Upper Silurian. The
limit between these two groups consists of bands of limestone and
marl, containing Pentamerus in great abundance, and this bed forms
a perfect geological horizon throughout the whole district. He has
called these groups, in ascending order, Oslo Group, Oscarskal Group,
and Malmo Group. The total thickness of these formations is said
to be 1930 Norwegian feet (1980 English), of which 400 belong to
the Oslo, 700 to the Oscarskal, and 830 to the Malmo group. He
mentions the different localities where these groups are chiefly de-
veloped, and describes the contortion of the Oslo group as a great
system of waves spread over the original bottom rock of the Chris-
tiania basin or valley. This bottom rock is gneiss, mica-schist, &c.
The Malmo group is principally developed in the island of that name ;
and as the nomenclature of the groups adopted by the author is in a

great measure geographical, the true boundary between Upper and

Lower Silurian is placed zm that group, and near the-bottom. It is
difficult to understand the reasons which have induced the author to
adopt this somewhat arbitrary system of subdivision, which, to say

- the least, introduces some confusion into his classification. It

would seem more natural to have retained the lowest bed of this
group (9 & 96 of the Author’s Section) in the underlying group of
Oscarskal.

The connexion between the Malmo beds and the Lower Silurian
formations was for a long time obscure ; but the thick beds of cal-
careous sandstone (No. 8), with Tentaculites annulatus, Chetetes
(petropolitanus’?), and an Orthis cleared up the difficulty, and enabled
the author to fix the thickness of the whole formation more accurately
than had hitherto been done. The Lower Silurian beds are some-

xcli PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

what less thick than was at first supposed; while, on the other —

hand, the Upper Silurian formation is considerably thicker than was
before stated. The author gives the following table as the general
‘result :—

Feet.
Oslo group and Oscarskal group 1100] Lower Llandeilo and
Bed No.9 . 3870f Silurian. Caradoc.

Upper Wenlock and
Malmo group (without No.9). 460 ‘ Silurian. Lower Ludlow.

1930

The author then describes the metamorphic gneiss of Bugten and
Akershus, and particularly the geological features on the promontory
of Bugten, where the beds which by their fossils have been identified
with No. 9 dip partly under the gneiss and partly overlie it; and
the result to which M. Kjerulf here comes is, that the gneiss partly
overlies the Lower Malmo schists, and that the lower divisions are
altogether wanting: ‘‘ we must therefore assume,” adds the author,
“‘that both a portion of the Lower Malmo schist, as well as probably
the whole of the older Silurian formations which are here wanting,
have been altered by metamorphic action into gneiss.”” M. Kjerulf
promises to send, by another opportunity, lists of the fossils of each
of the different subdivisions. The communication is accompanied
by a series of admirable sections, prepared by M. Kjerulf, to explain
the relative positions and geographical extent of the different groups
referred to by him.

Russia.—A letter from M. Abich, published in a.recent number
of the ‘Bulletin de la Soc. Géol. de France*,’ contains some in-

teresting details of Russian geology. He mentions that the recent |

explorations of the officers of the Corps des Mines, who have examined
the regions south of the Ural, and in the neighbourhood of the Sea
of Aral, show that an extensive eocene deposit, with a molluscous
fauna rich both in genera and species, occurs on the eastern and
southern shores of that lake. They are mostly identical with those of
the Paris basin, and in an admirable state of preservation. These
eocene beds overlie nummulitic limestones, resembling those in the
Mediterranean basin, and beneath them is the chalk. The inferior
cretaceous and jurassic formations crop out on the steep banks of the
Aral. The gault and neocomian beds contain the same fossils as to
the north of the Caucasus. The eccene formations of these Aralo-
Caspian regions are again covered by the middle tertiary formation,
which forms the upper portion of the Ust Urt, the absolute elevation
of which is greater than the maximum of the mean level of the more
recent deposits called Aralo-Caspian in the whole space of the Aralo-
Caspian table-land. The soil of the whole of this region belongs to the
middle tertiary formation, and is characterized by the same fossils as
occur in Volhynia, Podolia, and Bessarabia. The existence of this vast
eocene basin, which extends far beyond the sea of Aral, will greatly
add to our data for the knowledge of the geological structure of the

* Vol. xii. p. 115.

‘
‘

ANNIVERSARY ADDRESS OF THE PRESIDENT. xclil

steppes which stretch from the foot of the Caucasus into the interior
of Central Asia. M. Abich reports that M. Helmersen is preparing
a memoir on the formations surrounding the Sea of Aral.

Italy.—A notice on the Geological Map of Sardinia, by General

A. de la Marmora, also occurs in the twelfth volume of the ‘ Bulletin,’
in which the gallant General describes with great care the principal
plates of the atlas of his geological description of that island. Some
of the plates are finished, the others are in progress. The geological
map of the island is on the same scale as that of France by MM. Elie’
de Beaumont and Dufrénoy, and the author has employed almost the
same colours for the different formations. Thirteen straight lines on
the map represent the sections through the principal features. These
form a separate plate. Two others represent the principal eruptive
phenomena. Some of the basaltic appearances, and the most recent
volcanic outbursts, are analogous to those of Auvergne.
_ A new labourer in the field of Italian geology has appeared in the
person of Crescenzo Montagna, captain of the Royal Corps of Artil-
lery of Naples, who has recently published in that city a work on
the coal of Agnana. This locality for Italian coal is, I believe,
new. Agnana is situated near Geraci, in the southern part of Cala-
bria. The object of Capt. Montagna’s work is, in the first place, to
point out the various sedimentary formations which occur in the
district he describes, and then to determine the geological age to be
ascribed to the coal in question. The work itself is interesting and
unpretending ; and, considering the difficulty of obtainmg informa-
tion, or seeing the works of other geologists in other fields, in a
country so circumstanced, both physically and politically, as the
kingdom of Naples, it evinces both energy and perseverance on
the part of the author. At the same time this very circumstance
has occasionally led him to enter on the consideration of questions
already decided, and permanently established by all geological au-
thorities.

It is clear from the fossils found by the author, that the upper
beds, which form gently undulating hills rising from the sea-side, and
which contain Cassidaria echinophora, belong to the Sub-apennine
formation. Other tertiary formations succeed in descending order ;
below these are calcareous beds, containing two, if not more, species of
Nerinea, and clearly indicating the existence of cretaceous beds. The
coal-beds underlie this formation, which reposes on argillaceous schists,
in which organic remains are scarce and uncertain. The fragmentary
relics are considered by the author as representing forms belonging
to the mountain limestone, but the evidence is as yet incomplete.

The following, in descending order, is the sequence of formations
observed and described by the author :—

I. Tertiary. 1. Subapennine. Hills at the foot of Liderno.
2. Falunian. Timpa di Tenda,—shell-beds of
Geraci and Salvi.
3. Paris and London-clay basin. White marls,
Calcaire grossier, gypsum.

Xclv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

II. Seconpary. A. Cretaceous :—
1. Cenomanian (d’Orb.).
2. Aptian.
3. Neocomian.
B. Jurassic :-—
1. Kimmeridge clay. Scolaro, and coal-beds.
2. Coral rag? Limestone of Mutolo.
3. Oxfordian. Iron ores.
IlJ. Patmozoic. Argillaceous schists.
IV. Azorc. Rocks of Monte Barone.

In the tenth volume (p. 211) of the ‘Nuovi Annali delle Scienze
Naturali” is an account, by M. Scarabelli, of the geology of
the province of Ravenna, accompanied by a geological map of the
district. The author describes it as a supplement to his former
work on the geology of the province of Bologna. He refers the
different formations to the following subdivisions— Eocene, Miocene,
Pliocene, Quaternary, and Modern. The oldest or eocene is com-
paratively unimportant. The miocene consists chiefly of a sandy
micaceous molasse, with few fossils, as Carcharodon crassidens, Car.
angustidens, Buccinum, Tellina, and Artemis. This is overlaid by
a band of gypsum or selenite, which forms a lofty and conspicuous
crest through the country nearly parallel to the high road from
Bologna to Forli. The several thick beds of this deposit give al-
together a thickness of about one hundred metres. Its general strike
is N.W. to S.E. with a dip to the N.E. Resting on this gypsum
formation are the blue fossiliferous marls which the author refers to
the pliocene epoch. These marls in their upper portion become
gradually more arenaceous, and, by degrees, almost conglomeratic,
with a gentle inclination to the plain to the N.E. Marine remains
are very abundant, and the author considers that they show an in-
termixture of true miocenic and pliocenic forms. He adds a list of
the fossils hitherto found, from which it appears that there are 30
species of Bivalves and 133 of Gasteropoda. This disproportion,
however, can hardly be correct, particularly when we consider the
marly or muddy nature of the ground, so peculiarly the habitat of
the lamellibranchiated bivalves. It is probably owing to the greater
difficulty of obtaining the bivalve shells in a perfect condition. The
author observes that fish bones have also been found. The most
interesting feature however is, that in the upper strata, and where
the marls begin to pass into yellow sands, bones of Hippopotamus
and Rhinoceros begin to make their appearance, and these, combined
with littoral marine species of shells, are also accompanied by fresh-
water shells; showing thereby that the bones were carried into an
estuary, where the marine products were mixed up with terrestrial
and fluviatile remains. In proof of this there has been recently
found in the sandy marl near the River Pratella, in a bed containing
Cardium edule, Mactra triangula, Balanus, and Paludina, a collec-
tion of thirteen or fifteen coprolitic bodies containing traces of vege-
table structure, and which therefore appear to have belonged to some

\
ee re, a

ee ee ee ee

ANNIVERSARY ADDRESS OF THE PRESIDENT. XCV

great herbivorous animal. This gradual change of the blue marls
into sandy beds probably indicates the period of the gradual rising
of the country and the increasing shallowness of the water near the
coast, when the arenaceous particles brought down by the rivers were
deposited near the coast line, whilst the lighter argillaceous sediment
was carried to a greater distance; it may perhaps be laid down as a
general geological axiom that a change from argillaceous into arena-
ceous deposits is an indication of the gradual elevation of a sea-bottom
at no great distance from the coast.

The author then proceeds to describe the beds of the quaternary
period, which form a littoral band fringing the marine deposits which
they overlie unconformably, containing the remains of Elephants,
Rhinoceros, Equus, Cervus, and other large ruminants which have
been collected near Imola, where was the delta formed by the ancient
course of the river Santerno.

An account of the formation of the modern period, which consists
of the plain of Ravenna, is reserved for a subsequent communication.

Connected with the tertiary remains of the Mediterranean basin, I
would not willingly omit a reference to Dr. Wright’s paper, on
‘Fossil Echinoderms from the island of Malta, published in the 15th
volume of the “‘ Annals and Magazine of Natural History.’ These
fossils and the details of their stratigraphical arrangement were prin-
cipally procured by Lord Ducie, to whom Dr. Wright was indebted
for much valuable information. The strata are divided into five
groups, each with its characteristic fossils. These are in descending
order: 1. Coralline limestone; 2. Yellow sand; 3. Clay; 4. Calca-
reous sandstone; 5. Hard cherty limestone. It is hardly necessary
to add that they all belong to the miocene epoch.

Spain.—Let me now direct your attention for a short period to
that peninsula which was for so many years the seat of our military
exploits ; here we shall find that the germ of geological science
observed some years ago, and detected in the works of Spanish
engineers in the Mining Review of that country, appears now to be
actively taking root, and to hold out the expectation that before
many years shall have elapsed, we may hope to see the geology of
Spain, hitherto chiefly explored by foreigners, thoroughly worked
out by the new school of Spanish geologists. We are indebted to
our old acquaintance and friend M. de Verneuil for a short but
interesting notice on the progress of geology in Spain during the last
few years, and principally durmg the year 1854. From this and
other sources I shall endeavour briefly to lay before you some of the
‘principal results of this new field of energy in geological research.

The first impetus to this new movement was given by the foun-
dation of a school of mines at Madrid about twenty years ago. In
1847 an academy of sciences was created, and shortly afterwards a
commission was appointed by the Spanish government to construct
a geographical and geological map of the Province of Madrid. It is
to M. Casciano de Prado, Vice-President of this Commission, that
we are principally indebted for the more important geological dis-
coveries recently made in that country. With the aid of MM.

xevi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Ezquerra del Bayo and Paillete, he drew attention to the paleonto-
logy of Spain. M. Ezquerra first noticed the existence of fossil
bones in the miocene formation of Madrid, and the latter, having
discovered in the Asturias and the kingdom of Leon devonian fos-
sils in a very perfect state of preservation, enabled MM. de Verneuil
and d’Archiac to write two memoirs on the paleontology of those
districts. Subsequently M. de Verneuil, in his work “ Sur la Con-
stitution Géologique de plusieurs Provinces d’ Espagne,” published
some lists of fossils found in the secondary rocks. But a great gap
still existed between the palzeozoic and jurassic formations. Slight
indications of the trias had been observed by several geologists, but
it was only in 1853 and 1854 that M. de Verneuil and his companions
in this field were fortunate enough to discover the characteristic fos-
sils of the muschel-kalk, viz. Ceratites resembling C. nodosus, Nau-
tilus bidorsatus, Myophoria levigata, and M. curvirostris. These
interesting species were obtained from Hombrados to the east of
Molina de Aragon, from the neighbourhood of Mora and of Tivisa,
not far from the mouth of the Ebro.

But to return to the recent operations of M. Casciano de Prado:
convinced that the geology of a province cannot be understood if
confined to political boundaries, this enterprising geologist extended
his investigation into all the provinces bordering those of which the
geological examination had been confided to him: thus we are in-
debted to him for the first geological map of the provinces of Madrid
and Segovia, in which the geographical features, thanks to the map
of M. Coello, are laid down with unusual care and exactitude.
During the past year M. Casciano de Prado was further instructed
to make a detailed topographical map of the different deposits of coal
in the province of Palencia. The examination of other carboniferous
basins on the southern flank of the Cantabrian chain was confined to
other persons, of whose labours M. de Verneuil has not been able to
give us an account.

Notwithstanding the political disturbances, M. de Prado continued
his labours during the whole summer. He discovered three granitic
outbursts or islands in the Cantabrian cham. ‘The Devonian and
Carboniferous formations are so arranged that the former expands
from east to west, at the expense of the latter. Thus m the pro-
vince of Leon few Carboniferous fossils are found, but many Devonian;
whilst, on the contrary, in the province of Palencia, the Carboniferous
fossils are more abundant than the Devonian. M. de Prado has
greatly added to the carboniferous fauna of Spain, for he says that
he has found more than one hundred species in the province of
Palencia alone. The results of his labours are such that he has now
been enabled to prepare a geological map of the four important pro-
vinces of Madrid, Segovia, Palencia, and Valladolid.

M. de Verneuil also calls our attention to an admirable geological
account of the kingdom of Valencia, by M. F. de Botella, published
in the Mining Review* of Spain. It is accompanied by a geological
map, the basis of which was laid down by M. de Verneuil himself, when

* Revista Minera, vol. v. pp. 562 & 675.

ANNIVERSARY ADDRESS OF THE PRESIDENT. XCV1l

travelling two years before with M. de Botella. The Spanish govern-
ment has on this occasion shown a most praiseworthy interest im the
progress of geological knowledge by confidmg to M. de Botella the
task which he desired of constructing, during the next three years, a
detailed geological map of this same kingdom of Valencia, consisting
of the three provinces of which the capitals are Alicante, Valencia,
and Castellon de la Plana. Among other interesting statements
contained in this notice are the barometrical measurements of various
heights of mountain chains made by M. de Verneuil and published
in the Bulletin de la Soc. Géol. de France, vol. xi. p. 661 ; and after
alluding to different memoirs recently published on Spanish geology
im various scientific periodicals in Germany, France, and elsewhere,
the author states that the result of his own travels in Spain, during
the last six years, will appear on a small scale in the Geological Map
of Europe, about to be published by Sir R. Murchison and. Mr. Nicol
in England, and by M. Dumont in Belgium.

I ean only briefly refer you to the ‘Bulletin de la Soc. Géol.’* for
another interesting notice on Spanish geology by M. Casciano de Prado,
called, ‘“On the Geology of Almaden and a part of the Sierra Morena,
and the Mountains of Toledo.” The country is described as one of
great difficulty in consequence of the many and violent convulsions
to which it has been exposed in all geological periods, and it is also
intersected by many mountain chains. The lower Silurian beds are
greatly developed in the central portion of the country, im Estrema-
dura and the province of Toledo, and are overlaid by the Devonian.
Characteristic fossils are abundant in some places, as Calymene Tris-
tani, Orthis testudinaria, &c.

Asia Minor.—The importance of a sufficient supply of coal to
enable them to carry on their naval and military operations in the
Turkish waters has been so much felt by our government, that, the
supplies from Heraclea not appearing sufficient, they despatched
Mr. Henry Poole, from this country, for the purpose of examining
some beds or seams of coal, the existence of which, near the Gulf of
Nicomedia, had been pointed out by the British Consul at Brusa.
Considering the physical geography of the country and the position
of the coal-beds of Heraclea with regard to the paleeozoic rocks of

Constantinople, and the cretaceous formations which occupy so large .

an area in Asia Minor, I felt tolerably confident that the result of
Mr. Poole’s examination of the country would in this respect be per-
fectly satisfactory. It appears, however, from the communications
which have been made to us by the Foreign Office and by Sir R.
Murchison, that Mr. Poole has not succeeded in finding any real
coal; he describes the route he followed in his investigations, and
observes that in the different points to which his attention was
directed he. found nothing but. lignite of a very inferior quality.
When we recollect, however, that coal has been discovered by M. de
Tchihatcheff in the eastern parts of Asia Minor, in the Taurus, and
in the neighbourhood of Erzeroumt, I do not feel disposed altogether

* Vol. xii. p. 182.

+t Bull. de la Soc. Géol. de France, vol. xi. p. 402, &c.

X¢Vill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

to give up the expectation that real coal may be found in the district
bétween Heraclea and the Gulf of Nicomedia.

In my address last year I alluded to the communication made by
M. Tchihatcheff to the Geological Society of France respecting the
geology of Asia Minor. Those remarks referred chiefly to the
southern parts of that peninsula. I now learn that he has also
made some interesting discoveries in tertiary geology along the
northern shore. An eocene deposit was unexpectedly discovered in
the neighbourhood of Samsoun, on the Black Sea, mixed up with
melaphyr rocks. Near the village of Kadikieui, amongst the hills
and ravines, were found in great numbers shells of almost all the
species which are now living in the Black Sea, as Tellina, Venus,
Cardium, Pecten, a variety of Ostrea edulis, and Rotella lanceolata.
The only extinct species found were a Natica and Turritella sub-
angulata, Brocchi. The surface of the trap-rocks on which these
shells are distributed appears to be occasionally covered with a very
thin coating of a dark marly limestone. In these thin bands, Num-
mulites Ramondi, Defr., N. irregularis, Desh., with Alveoline and
Operculine, and innumerable fragments of comminuted shells, are
found. From the occurrence of this nummulitic formation in the
neighbourhood of Samsoun, and the existence of the recent shells,
M. Tchihatcheff deduces the following conclusions :—

The melaphyrs and traps which play such an important part along
the whole of this northern shore of Asia Minor must have burst
forth before the Nummulitic period; and at a very recent period
these trap-rocks and the whole coast must have been submerged,
and the waters of the Black Sea not only covered the plain where

_ Samsoun now stands, but beat against the hills on which the village

of Kadikieui, now two leagues distant from the sea, is placed.

T am acquainted with several localities in Asia Minor where the
recent forms alluded to by M. Tchihatcheff may be found at various
elevations along the coast of the Black Sea; but I was not aware of
eocene forms having yet been found there. They are however abun-
dant im the interior, and I have myself found the nummulitie forma-
tions nearly in the meridian of Samsoun, or S.W. from it, and about
100 miles to the south; and in other parts of Asia Minor they are
abundantly met with.

Egypt.—Mr. Leonard Horner has published im the volume of the
Philosophical Transactions for 1855, an account of recent researches
near Cairo, undertaken with the view of throwing ght upon the
geological history of the alluvial land of Egypt. The following is
an outline of Mr. Horner’s argument on this subject. One of the
most difficult problems in geology is to ascertain, even approxima-
tively only, the time which has elapsed during the period of the
formation of any particular series of strata, even when the inquiry is
confined to the most recent of the tertiary deposits. In considering
the means by which this difficulty might be overcome, it occurred to
Mr. Horner that, if there were a country in which a certain alteration
in the level of the land had taken place within historical time, and
where the entire change under consideration presented throughout a

ANNIVERSARY ADDRESS OF THE PRESIDENT. XC1X

tolerable uniformity of character, we should be justified in holding
that the portion of change that had taken place within the historical
period would afford a measure of the time occupied in the production
of the antecedent part of the same change. Egypt appears to Mr.
Horner to be the only land of all parts of the world as yet known to
us that offers an instance of a great geological change that has been
in progress throughout the whole of the historical period down to
the present day, and which we have reasonable grounds for believing
had been going on with the same uniformity for ages prior to the
period when our reckoning of historical time begins. This is owing to
the annual inundation of the Nile, and the sediment that falls from its
waters on the surface of the land it overflows. The historical monu-
ments of Egypt are the oldest in the world, and afford the most ac-
curate records of the earliest period of the human race in which any
trace of civilization has been discovered, combined with records scarcely
less accurate of geological changes contemporaneous with history,
and having such a degree of uniformity as to warrant us in carrying
back the dates of changes of a like nature beyond that of the earliest
historical documents.

With these views Mr. Horner determined to endeavour to in-
vestigate the formation of the alluvial land in the valley of the Nile
in Upper and Lower Egypt, comparing the depth of sediment which
has accumulated to a considerable height above the base of the
oldest works of art near the Nile with the sediment deposited below
the base of these same monuments on the rock forming the bottom of
the channel. If, he observes, the depth of sediment above the base
of these works of art be divided by the number of centuries that have
elapsed since the date of their erection, we may obtain a measure of
the secular increase of the sediment ; requirmg, however, a correction
for causes that might make a difference in the rate of increase be-
tween earlier and later periods.

Having thus fully stated his object, Mr. Horner commences his
inquiry with an account of the physical geography and geological
structure of Egypt, an account of the inundations of the Nile, and
of the solid matter conveyed by the Nile to form its sedimentary de-
posits, and then proceeds to describe the recent researches undertaken
at his suggestion. These embrace an account of the excavations at
Heliopolis, descriptions and analyses of the soils, descriptions of the
several pits and shafts sunk, and a synopsis of the soils passed through
in the excavations. But these excavations are not yet completed,
and Mr. Horner defers all inferences as to the secular increase of the
alluvial deposits until he shall have had an opportunity of describing
the later and more extensive researches and excavations.

Trusting that Mr. Horner may be successful im arriving at a satis-
factory result from this spirited and difficult undertaking, I will only
observe, that we must not be too sanguine that these inquiries can
lead to any sound or certain conclusions on the subject. The greater
velocity of the water in the ante-historical period, in consequence of
the greater inclination of the valley before it was filled up by the
present sediment, can never be fully ascertained, or its effects cal-

Cc PROCEEDINGS OF THE GEOLOGICAL SOCIETY. |

culated, although its general effect must have been to prevent any
accumulation of deposit in the same ratio as afterwards, and from
this cause alone the rate of filling up must have been a perpetually
varying one.

You are aware that the Messrs. Schlagintweit, whose observations
on the elevation and physical structure of the Alps are so well known,
have proceeded to India for the purpose of making similar physical
and meteorological observations on the mighty chain of the Himalaya
and its lateral ranges. On their journey from Cairo to Suez they
made some interesting geological observations. Mr. A. Schlagintweit
writes as follows to his friend and patron A. von Humboldt :—“ The
greater portion of the sand of the desert appears to have been de-
rived from the easily disintegrating tertiary formations which exist in
large masses along the edge of the desert. The desert is decidedly a
marine formation. We had the good fortune, a little to the south of
Station No. 12, to discover a series of well-preserved sea-beach terraces,
about 200 feet above the present level of the sea, containing nume-
rous marine Mollusca, as Ostrea, Cardium, and Cyprea, with Cidaris,
which cannot be specifically distinguished from the corresponding
species which I obtained at Suez from the Red Sea.’’ These remarks
are interesting, as pomting to the greater extension of the Red Sea
northwards at a former period, and almost proving the connexion
within recent geological periods between the Red Sea and the
Mediterranean.

India.—From India and our Eastern colonies and possessions we
have not received many communications during the past year. But
I must not omit to mention that the Rev. Mr. Hislop has forwarded
to us a paper on the connexion of the Umret coal-beds with the plant-
beds of Nagpur, and of both of these with those of Burdwan. It
will be recollected that some time ago Messrs. Hislop and Hunter
sent to this country a valuable collection of fossil plants from the
sandstones of Nagpur, and it may be observed, that it is in conse-
quence of the identification of the Nagpur flora with that of the coal-
fields of Umret that Mr. Hislop has been able to fix the position of
the coal-formation of India. Ina former communication on the Ju-
rassic formation of the Nagpur territory, Mr. Hislop described it as
consisting of four members in the following descending order :—

1. Thick-bedded coarse ferruginous sandstone, with a few stems
of trees.

. Laminated sandstone, rich in vegetable remains.

. Clay-shales of various colours, with traces of reptiles and
worms.

4, Limestone, generally crystalline.

On that occasion Mr. Hislop stated that he considered the Indian
coal-measures as the equivalent of No. 3. Subsequent discoveries
have led him to the conclusion that their true position is amongst
the beds immediately below the ferruginous sandstone No. 1.

The arrangement of the strata of what Mr. Hislop calls the Indian
freshwater Oolitic formation is consequently somewhat modified in

GW bo

ANNIVERSARY ADDRESS OF THE PRESIDENT. Cl

this paper. The author gives the following series in descending
order :—

1. Upper sandstone series (Panna or Punna sandstone of Dr.
Carter).
2. Laminated series. Kattra shales of Dr. Carter.
a. Arenaceous, carbonaceous, or bituminous, 300 feet thick in
Nagpur, 2000 in Bengal.
6. Argillaceous shales, green, red, blue, and white, with tracks of
reptiles and worms.
e. Limestone, compact or crystalline.
3. Lower sandstone series. Tara sandstone of Dr. Carter; not

developed in Nagpur.

I may add, that, as the Indian Government have just sanctioned
the construction of a branch railway to Nagpur from the Bombay
main line, we may look forward, at no very distant period, to some
valuable information on this subject. The resident engineer of the
line, who is a member of this Society, has promised to collect all the
information in his power on the geology of Western India.

In another district the railway operations have already borne fruit.
I find in the Journal of the Geological Society of Dublin, amongst
other papers of great interest, an account of a hasty examination of
the Nerbudda Valley in Central India by Mr. Arthur Jacob. The
coal-formations and iron-deposits have been long known to exist in
this part of India, and Mr. Jacob’s object in visiting them was to
ascertain the feasibility of establishing an iron-manufacture in that
district. In doing this he has done good geological services. The coal
occurs in sandstone beds, and is sometimes much inclined, in places
dipping almost vertically. The iron also occurs in veins and nodules
of red hematite, in the sandstone which is probably Oolitic, but some-
times also in the basalt. With regard to the age of the Bengal coal-
fields, it appears from the reports lately sent home by Mr. Oldham that
they too must be considered as belonging to the Mesozoic rather than
to the Palzeozoic period.

America.—I must not omit to direct your attention to the sketch
of the geology of Canada by Messrs. Logan and Hunt, printed at
Paris for the purpose of explaining the geological map and the col-
lection of minerals sent by the Canadian Government to the Universal
Exposition of Paris. It is accompanied by an admirable reduction of
the map in question.

From this notice it appears that below the Lower Silurian system
which contains the lowest fossiliferous beds, there are found two un-
conformable Azoic systems; the lowest of them is the Laurentian
System, consisting of highly crystalline sedimentary beds, and pro-
bably corresponding with the gneiss of Finland and Scandinavia.
They are chiefly gneissoid or hornblendic schists, with some felspathic
porphyries and quartzites, associated with crystalline limestones, which
appear to have been in a state of fusion, and to have undergone
great pressure, having been forced into the fissures of the neigh-
bouring siliceous beds. Besides these stratified beds, granites,

VOL. XII.

cll PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

syenites, and intrusive diorites are also met with. The second Azoic

system occurs on the banks of Lakes Huron and Superior, and con-

sists of a series of schists, grits, limestones, and conglomerates, inter-

stratified with thick beds of diorite, and rest unconformably on the

Laurentian System. Mr. Logan gives it the name of Cambrian or.
Huronian System. It abounds with metalliferous veins, which have

hitherto been but little worked.

On the islands to the north of Lake Huron is a series of fossili-
ferous beds, resting horizontally on the inclined strata of the Hu-
ronian System. Further south they rest directly on the rocks of the
Laurentian System. They correspond with Murchison’s Lower Silu-
rian, and are overlaid by the Upper Silurian, Devonian, and Carboni-
ferous systems. These groups occupy the whole of the Canadian
portion of the great basin bounded on the north by the Laurentian
and Huronian formations.

Mr. Logan has pointed out that this basin is separated into two
portions by an anticlinal axis, which, following the valley of the
Hudson and Lake Champlain, enters Canada near the Bay of Mis-
iscoul, and running thence N.E., reaches the St. Lawrence near
Deschambault, ten leagues west of Quebec. The rocks of these two
basins present a very remarkable difference, both in their physical
and chemical aspect. The formations of the western basin are almost
horizontal, and perfectly conformable, whilst in that to the east there
is a want of conformity between the Upper and Lower Silurian, and
between the Devonian and Carboniferous systems. The various
strata of the eastern basin are, moreover, much twisted and contorted,
and have in some places undergone great chemical and mineralogical
metamorphism. A glance at the map at once points out this im-
portant difference. The conclusion is irresistibly forced upon us,
that, while on the western side the different systems succeeded one
another gradually and conformably, violent convulsions, occurring at
certain epochs, on the eastern side, interfered with the tranquil suc-
cession of the deposits; and we see that, although these breaks
occurred between the Upper and Lower Silurian periods, and between
the Devonian and Carboniferous systems, they were still only local
phenomena ; and that, however they may have affected the condition
of life in the neighbouring seas, they produced no effect on the regular
succession of deposits even in their immediate vicmity. It would be ©
difficult to find anywhere a better example of the necessity of not
attaching too great an importance to those breaks which occur in
other regions, and which, after all, may have only a local signifi-
cance.

Mr. Logan then proceeds to describe the different features of these
two basins, the western and the eastern, adding an account of the
metamorphic rocks, and of the post-tertiary and alluvial deposits.

The volume of Mr. J. W. Dawson, entitled ‘Acadian Geology,’
being an account of the geological structure and mineral resources of
Nova Scotia and portions of the neighbouring provinces of British
America, must also be noticed. The author has endeavoured to com-
bine two great desiderata ; while striving to make his work sufficiently

ANNIVERSARY ADDRESS OF THE PRESIDENT. cli

elementary and practical for his readers in the Colonies, he has not
forgotten that it should be at the same time sufficiently accurate and
original to do some service to general geology. Commencing with the
most recent formations, the author successively describes the different
formations of the Colony, giving, as to the most important feature,
a more than equal share of attention to the description of the Car-
boniferous System. It is a very remarkable feature, that in the
geology of Nova Scotia no formations occur between the drift and
the New Red Sandstone. The middle and lower Tertiaries, the Cre-
taceous and Oolitic Systems, with their subordinate groups, are all
wanting in this Colony, as in New Brunswick, Canada, and the
Northern United States. The work is accompanied by a good geolo-
gical map, and many illustrations on wood.

The recent Arctic expeditions have also added considerably to our
knowledge of the geology of these extreme northern regions. A
paper read by Sir Edward Belcher in the Geological Section at the
recent meeting of the British Association at Glasgow, indicates the
presence of Ichthyosaurian bones in the most northern part of the
Arctic land. Mr. Salter, in a paper read on the same occasion,
showed the connexion of this fact with the presence of Ammonites
and other Lias shells on the north-western edges of Melville Island,
as already described by the Rev. Prof. S. Haughton.

They are succeeded southwards in both cases by Carboniferous
limestones with several species identical with those of Great Britain,
thus giving us a marine equivalent for the coal-beds so long known
in that island. A trace of a Devonian formation then follows with
some characteristic fossils, Productus and Atrypa reticularis, and
thence the whole surface of the Polar lands as far south as Hud-
son’s Bay appears to be occupied by a grand plateau of Upper Si-
lurian rocks extending to the granitic ridge of the so-called Laurentian
chain.

Mr. Salter also called attention to a similar basin in Spitzbergen
where Permian rocks have been recognized by De Koninck, suc-
ceeded southwards, in Bear Island, by strata of the Carboniferous age,
the fossils of which were described long ago by von Buch.

An interesting account of the carboniferous fossils obtained by Sir
Edward Belcher and the officers under his command, prepared by
Mr. Salter, and of the Saurian bones by Prof. Owen, will be found in
the appendix to Sir E. Belcher’s work entitled ‘ The last of the Arctic
Voyages.’

We are indebted to Mr. Isbister for a valuable compilation of all
the information hitherto obtained respecting the geology of the
Hudson Bay Territories, and of portions of the Arctic and north-
western regions of America. This information has been partly
derived from his own observations, partly from those of the many
geologists and travellers who have explored, and of the naturalists
who have examined the organic remains of this portion of the
American continent. Mr. Isbister justly considers that, in the ab-
sence of any general view of the geological structure of this ex-
tensive but interesting region, even the most cursory classifica-

he

|

civ PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

tion of its formations might be useful to those employed in
developing the structure of the crust of the earth. The author
of the paper also adds a list of the various works relating to the
| geology of the northern part of North America, and which he has
| himself consulted. We have every reason to hope that this geolo-
| gical hiatus will now, to a great extent, be filled up by the exer-
| tions of the distinguished geologist to whom the Wollaston Palla-
| dium Medal has been this day awarded.

I greatly regret that time and space will not allow me to do full
| justice to the exertions of the geologists of the United States of
| America in the pursuit of geological investigation. At the same

time I must mention some circumstances connected with the progress
of geology in that country.

And in the first place, let me call your attention to the magnificent—
I had almost said royal—publication, of Dr. Isaac Lea of Philadelphia,
of the fossil footmarks in the red sandstone of Pottsville. Having
already published these fossil footprints in the Proceedings and Trans-
actions of the American Philosophical Society, the author found that
the reduced plate containing the six imprints of fossils was too small
to convey a correct idea of this interesting specimen. He conse-
quently determined to reproduce it of the natural size, in order that
a better representation of it, and a more correct and diffused know-
ledge of this, perhaps the oldest air-breathing animal on record,
| might be laid before geologists. The letter-press explanatory of this
large engraving, and by which it is accompanied, is reprinted almost
verbatim from the tenth volume of the Transactions of the American
Philosophical Society.

In the last number we have received of the Journal of the Academy
of Natural Sciences of Philadelphia will be found two interesting
memoirs on the discovery of paleeozoic fossils in the United States
by Messrs. J. C. Norwood and Henry Pratten, of the Ilinois Geo-
logical Survey. The first isa notice of Producti found in the western :
states and territories, with descriptions of twelve new species. ‘These
species have been found partly in the Mountain-limestone so exten-
sively developed in the western and southern states, and partly in
the marine limestone and calcareous clays of the Coal-measures.
Indeed many of the species here described are found exclusively in
this latter formation. The new species, which are exemplified by |
beautiful and accurate drawings by Mr. H. A. Ullfers, are Productus
Altonensis, Phillipsii, Rogersu, clavus, splendens, Wabashensis,
elegans, muricatus (not of De Koninck or Phillips), Portlockianus,
Prattenianus, Hildrethianus, and alternatus.

The second is a notice of the genus Chonetes as found in the
western states and territories, with descriptions of eleven new species.
M. de Koninck, in his monograph of the genus published in 1847,
enumerated twenty-three species, including those found in the United
States, as the total number then known; Mr. Dale Owen has since
added one more, and the addition now made makes the present number
known thirty-five. Of these, seventeen occur in the western states of
America, and ten in New York. Of the new species six or seven

ANNIVERSARY ADDRESS OF THE PRESIDENT. CV

were found in limestone of the Devonian period, the remainder in the
Mountain-limestone and the Coal-measures. The new species are
Chonetes Smithii, Fischeri, Littoni, Flemingti, Verneuiliana, meso-
loba, Maclurea, Tuomyi, Martini, Koninckiana, and Logant.

It is, I think, to be regretted that the authors of these papers
have taken their specific names from those of individuals, instead of
adopting the practice now prevalent amongst so many geologists of
the continent of taking some characteristic feature of the fossil as the
basis of their nomenclature. I fear, however, that the American
geologists are not alone to blame in this respect : the practice is almost
equally prevalent amongst British naturalists, but is one which should
be discouraged.

The first two numbers of a work by Mr. M. Tuomey and Mr.
F. S. Holmes on the fossils of South Carolina have reached us within
the last few months. They promise to be a valuable addition to our
knowledge of the palzontology of that state. Commencing with the
pliocene fossils, these numbers contain a description of the Polyparia
and Echinodermata found in that district, as well as the commence-
ment of the description of the Bryozoa of the same region. The
plates which accompany the work are admirably executed.

Two interesting reports by Dr. John Trask have been published
by the Senate of the State of California on the Geology of the Coast
Mountains and part of the Sierra Nevada. These ranges appear to

consist principally of granite, syenite, mica-schist, gneiss, porphyries,

and older greenstone, penetrated by innumerable dykes of basalt,
greenstone, &c., and overlaid by sedimentary sandstones which are also
frequently much disturbed by the intrusion of the later igneous rocks.
Veins of quartz of various dimensions are also of frequent occurrence.
Tertiary rocks with the remains of gigantic vertebrate animals and of
marine shells also occur on the summits and sides of the hills con-
stituting the Coast Mountains, as well as at a distance from the shore.
They occur over a considerable area, so as to leave no doubt of the
former submergence of the entire district. Although generally
referred to the miocene epoch, they appear to belong to different
periods ; and the terraced outlines of the different groups indicate
the successive steps by which the country has been elevated to its
present position. Some of the bivalves are of enormous size.
Gryphee weighing twenty pounds have been found near Luis
Obispo at a distance of fifteen miles from the coast.

These reports also contain much interesting information respecting
the gold mines, their present mode of working, and their future pro-
spects. .

zi would also here particularly call your attention to the eloquent
and admirable address of Prof. Dana, read at the last meeting of the
American Association for the Advancement of Science, held during
the past year at Providence, Rhode Island. It contains a clear and
interesting sketch of the typical features of American geology from
the oldest palzeozoic formations to the most recent tertiaries, and will
be read with interest as it deserves to be studied with attention.

M. Marcou has also published in the ‘ Bibliothéque Universelle

cvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

de Genéve’ for last year a notice on the Occurrence of Gold in Cali-
fornia. After describing the different localities and formations in
which the gold is found, M. Marcou concludes by observing that he
has arrived at the same conclusion as Sir R. Murchison respecting
the gold of the Ural, viz. that its deposit took place between the
conclusion of the miocene formation and the post-pliocene or quater-
nary period. With this difference, however, that in California the
eruptive rocks in which the gold has been formed, and which are its
true matrix, do not belong, as in the Ural, to the Silurian system,
but to the miocene or pliocene period. They certainly are more
recent than the eocene, the beds of which they have disturbed and
dislocated. Moreover in California the veins of auriferous quartz were
formed at the same time as the eruptive rocks in which they occur,
and not subsequently to them as in Russia.

Professor Henry D. Rogers has recently published, in Edinburgh,
a Geological Map of the United States and British North America.
This Map forms a portion of Keith Johnston’s Physical Atlas, and has
been engraved by him for that work. It professes to be constructed
from the most recent documents and unpublished materials. It is
therefore with the greater surprise that I find that Prof. Rogers,
contrary to the opinion of the majority of his countrymen, and of the
officers of the Geological Survey of Canada, has entirely ignored the
existence of the Lower Silurian group, and has referred the rocks
which the American geologists designate as such to the Cambrian
system. I need only refer you to the able and eloquent address of
Prof. Dana, already alluded to, for a confirmation of the statement
that the division of Upper and Lower Silurian is fully recognized by
American geologists. In alluding, near the close of his address, to
the disturbances which appear to have marked on the American
continent the separations between various epochs, Prof. Dana ob-
serves—‘ The question of the existence of a distinct Cambrian system
is decided adversely by American records. The mollusca in all their
grand divisions appear in the Lower as well as in the Upper Silurian,
and the whole is equally and alike the Molluscan or Silurian age.
The term Cambrian, therefore, if used for fossiliferous strata, must
be made subordinate to Silurian.”

In another portion of this eloquent address, Prof. Dana says, in
reviewing the succession of epochs in American geological history,
that after the close of the Azoic age, in a period of extensive meta-
morphic action and disturbance, the Silurian or Molluscan age
next opened, and continued, under various aspects and numerous sub-
divisions, until the commencement of the Devonian age or age of
fishes. Here then we have a great natural-history character by which
to designate the Silurian age, viz. from the first commencement of
molluscan life down to the period when the first vertebrate animals
appeared in the form of fishes. The Silurian or Molluscan age
is, however, distinctly divided by Prof. Dana into the Upper and
Lower Silurian, each of which is again subdivided into several
periods.

For other evidence of the opinion of American geologists on this

ANNIVERSARY ADDRESS OF THE PRESIDENT. evil

point, I will only refer you to an able review of Murchison’s ‘ Siluria,’
in ‘ Silliman’s Journal *.’

The Geological Surveys of the different States in America appear
to be making satisfactory progress. The Annual Report on the
Geological Survey of the State of Wisconsin by Dr. James Percival,
who commenced his labours in August 1854, has recently been pub-
lished. In it the rock strata of the lead region are described ; Dr.
Percival appears to be inclined to the view that the lead occurs in
veins, instead of deposits or beds. This view has not hitherto been
generally admitted.

The first Annual Report of the Geological Survey of the State of
New Jersey, for 1854, has also been lately published at New Bruns-
wick. Mr. Cook, the assistant geologist, recognizes in the cretace-
ous strata, three distinct beds of greensand marl, alternating with
strata of sand. ‘The lower marl bed is 30 feet thick, and contains
Hzogyra costata, Gryphea convexa, Ostrea falcata, Terebratula
Sayu, Belemnites Americanus, &e. The second contains Gryphea
convera and Terebratula Harlant in great numbers. In the third
bed fossils are rare.

A paper on the changes which take place in the structure and
composition of mineral veins near the surface, with particular refer-
ence to the East Tennessee Copper Mines, by J. D. Whitney, is
published in Silliman’s American Journal, vol. xx. p. 53.

South America.—I have heard with great regret of the death of
Dr. Voltz, a distinguished German naturalist and geologist, who was
travelling in South America. He was explormg Surimam and died
at Paramaribo. His most interesting discovery was that of several
quaternary deposits at different heights above each other, containing
the shells of Mollusca now found living on that coast. Prof. F. Sand-
berger, who has seen the collections he has sent home, mentions as
mstances of these Mollusca found at various elevations, Marginella
cerulescens, Purpura cataracta, Ranella granulata, and Venus
Dombyt, all of which are now found on the same coast.

It is not improbable that they belong to the same formation as
that described by Col. Henneken in St. Domingo, many of the fossils
of which were described by Mr. Moore in a former volume of our
Journal. These latter, however, were referred to the tertiary period.

Colonies of Great Britain.—From our colonies in the southern
hemisphere, we have, during the past year, received much valuable
information respecting the geological structure of those regions.
Natal, and other districts of Southern Africa, Australia, and New
Zealand have each contributed to this accession of our knowledge,
and I regret that the space allotted to an annual address will not
permit me to do more than briefly to allude to them, referrmg you
for further and more detailed information to the recent numbers of
our Quarterly Journal. From the district south of Natal we have
had a notice of some cretaceous rocks by Capt. Garden, who suc-
ceeded in collecting an interesting suite of fossils from the cliffs and
walls of caves near the river Umtafuna. These fossils have been

* Vol. xix. N. S. 1855, p. 373.

= =

cvill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

described and mostly figured in our Journal by Mr. W. H. Baily,
who observes that they bear a close affinity to the collection of fossils
from Southern India, so ably described by Prof. E. Forbes. Dr. P.C.
Sutherland has also given us some important information respecting the
geology of Natal, in a series of letters addressed to Sir R. Murchison.
Beds of sandstone and shale occur alternating with trap-rocks ; im
the former, several seams of coal have heen found of no very good
quality, and which, from the appearances of the vegetable remains
in the shale, appear to belong to the Oolitic rather than to the true
Carboniferous formation. These facts are interesting as they cor-
roborate Mr. Bain’s observations on the extension of the reptiliferous
and coal-bearing strata of the Karoo-series of the neighbouring re-
gions. Granite and other crystalline rocks also abound, and copper
in the form of malachite is not unfrequent.

The Rev. W. B. Clarke has communicated to us some papers on
the geology of Australia. We have a paper on the occurrence of
obsidian bombs in the auriferous alluvium of New South Wales, and
another on the occurrence of fossil bones in the same deposit. After
comparing this latter fact with the occurrence of mammoth remains
in the auriferous alluvium of Berezof, in the Ural Mountains, Mr.
Clarke observes that their presence would seem to imply that the
gold in this deposit was collected at a comparatively recent date.

Mr. H. Rosales has also communicated to us some fresh informa-
tion respecting the gold-fields of Ballarat, and of the Eureka and
Creswick Creeks, in Victoria, the alluvial deposit in which the gold is
now found, and the quartz-vems from which it has been derived.
Mr. Odernheimer has also forwarded, through Sir R. Murchison,
some new details respecting the geology of part of the Peel River
district. His attention had also been directed to the auriferous beds
and the gold-bearing quartz veins, and he has added some interesting
remarks on the formation of the gold, observing that he has no
doubt that it is derived from auriferous iron pyrites.

Paleontology.—Our active Assistant-Secretary, Mr. Jones, has
published in the ‘Annals and Magazine of Natural History’ some
interesting notés on Paleozoic bivalved Entomostraca. In these re-
marks he has described some species of Beyrichia from the Upper
Silurian limestones of Scandinavia. Drifted fragments of these lime-
stones occur abundantly in the diluvial sands and gravels of Mecklen-

‘burg, Brandenburg, and Pomerania. Mr. Jones having obtained frag-

ments of this rock from the gravels of Prussia and Silesia, proceeded
to examine their contents with a view of comparing the British forms
with those published by Kléden as portions of the carapace of small
Trilobites, and of reviewing the nomenclature of the species and the
terminology of the subject. Mr. Jones describes the different fossil

contents of five distinct fragments of limestone, of which one is from

near Berlin, and the others from the vicinity of Breslau. The result
of this examination was the discovery of no less than eight species of
Beyrichia, together with Cytheres, Leptena lata, the two latter
occurring in every fragment, Tentaculites, and Encrinital remains.
Mr. Jones then proceeds to describe these species of Beyrichia, illus-

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ANNIVERSARY ADDRESS OF THE PRESIDENT. cix

trating by a plate the several forms obtained from the limestone-
fragments; and by another plate, in a subsequent paper, several
British and Foreign species of the same genus.

He has also published in the same periodical an interesting account
of some species of Leperditia, another family of Palzeozoic bivalved
Entomostraca, larger than the Beyrichie, and characteristically
distinct. They are also from the Silurian rocks of Scandinavia,
Russia, Arctic America, and England, except one from the Devonian
rocks of Normandy. After narrating the general facts of our know-
ledge of these minute entomostracan bivalves, peculiar to the palzo-
zoic formations, Mr. Jones describes the principal forms of the genus,
comprising seven species, accompanied by two plates of illustra-
tions ; and, after some observations on the genus itself and its points
of resemblance with the more recent and the existing forms of Lim-
nadidze and Cypridinine, he observes that the study of this peculiar
‘group may be of use not only in showing the difficulty that exists
in coordinating the fossil genus specially referred to (so far as the
remains of the carapace will help us) with its known allies, but also
to some extent in illustrating another example ‘‘ of the combination in
extinct animals of characters which are separately manifest in exist-
ing species.”

The same publication also contains a notice by Dr. Thomas
Wright of a new genus of fossil Codaride, to which he has given
the name of Hemipedina. He observes that in his memoirs on
the Cidaridze of the Oolites, three species were described, of which
the true generic position seemed even then uncertain. The materials
then known did not justify the proposing of a separate genus for
their reception. The subsequent discovery of an interesting series of
new congeneric forms has now enabled him to rectify the determina-
tion and to propose the new genus Hemipedina for the group.
Sixteen species from different lassic and oolitic beds are described,
which, with the exception of four from France, are all English.

Mr. Thomas Davidson has published some remarks on the Sy-
stematic arrangement of recent and fossil Brachiopoda, in the 16th
volume of the ‘Annals of Natural History,’ for the purpose of sub-
mitting a more perfect arrangement of classification than the one
published in 1853. But even this classification Mr. Davidson ad-
mits must not be considered as finally correct. The paper contains
an improved table of the families and genera in the form in which it
will be published in the forthcoming foreign editions of the intro-
duction to his work on British fossil Brachiopoda, and also explains the
changes which have been proposed in the different genera and sub-
genera. The author also adds some remarks on certain interesting
observations published abroad, but which appear to have been over-
looked by British naturalists.

Amongst the many paleontological works by which the past year
has been distinguished, none are more deserving of notice than
the two additional numbers of the Palgzontographica published by

Dunker and Hermann v. Meyer. These are the third and com-
pleting fasciculus of the fourth volume, and the first of the fifth

ne
nc - —

cx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

volume. They are, as usual, accompanied by plates in no way in-
ferior to those of the preceding volumes.

Baron P. de Ryckholt has published the second part of his
Mélanges Paléontologiques, with six plates of fossils. This number
is devoted to a description of the fossils found in the neighbourhood
of Visé, on the banks of the Meuse below Liége. The formations
here observed are given by the author in the following ascending
series :—1. Devonian ; 2. Carboniferous ; 3. Clay with kidney-shaped
masses, of the age of the cretaceous gompholite of Aix-la-Chapelle ;
4. Greensand with Belemnitella quadrata, d’Orb.; 5. Gravel with
clay ; quartzose and siliceous pebbles mixed with ossiferous diluvium.

I must also mention, however briefly, Prof. King’s ingenious
communication on the Pleurodictyum problematicum*. After care-
fully describing the appearance of the specimens he obtained from
the Upper Devonian sandstone of the Eifel, which he shows to be
casts, he aliudes to the curious vermiform appendage which winds
tortuously through the substance of the cell-walls, and which, while
the Pleurodictyim was supposed to be a coral, was considered as an
extraneous serpuliform body. Prof. King then endeavours to prove
that this vermiform appendage is an integral organic portion of the
fossil, and for this and other reasons connected with its structure, he
maintains that it cannot be regarded as a member of the class
Corallaria. The appendage he believes to be the cast of a fleshy
tube included in, and protected only by, the substance of the cell-
walls,—in fact the cast of a tubular chamber which enclosed the
intestinal canal of Pleurodictyum, the animal consequently having
had two orifices to its digestive organs. In this point of view it
would bear some affinity to the Bryozoaria. In other respects again
it would present affinities with the Zoanthic type, masmuch as there
would be only one appendage to all the cells. Its occupant may
therefore, it is suggested, have been a Zoanthoid Bryozoon! In con-
clusion, the author observes, that if his view of the position of
Pleurodictyum in the animal kingdom be correct, it will represent a
type which, although not known as living, is one that there is no
difficulty in conceiving to have existed, since it forms exactly the link
that is wanting to connect the true Corals with the class Bryozoaria.
We should thus have another example of what has been described as
** the combination in extinct animals of characters which are separately
manifest in existing species.’ But time and space will not permit
me to allude to the many interesting memoirs connected with geology
and. paleeontology which have been published during the past year.
I regret that I can only refer you to them generally; but there is
scarcely a scientific periodical published in this country, or on the
continent in France, in Germany, or in Italy, which does not contain
some valuable information connected with one or other of these
branches of our science.

Miscellaneous.—The subject of cleavage, on which we had several
communications read before this Society in the preceding year, has not
again occupied our attention during the past year ; but anothergeologist

* Ann. Nat. Hist. vol. xvii. p. 131.

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ANNIVERSARY ADDRESS OF THE PRESIDENT. CX1

has in another publication entered very largely on the consideration of
this question. Mr. Henry Clifton Sorby has published in the Philo-
sophical Magazine a valuable paper on slaty cleavage, as exhibited in
the Devonian limestones of Devonshire. The question which he
proposes for consideration is, whether slaty cleavage be the result of
crystalline or mechanical action ; and he observes that a most careful
examination of these rocks, which he considers as peculiarly suitable
for the purpose, in the field, microscopically, chemically, and by
means of the polariscope, has convinced him that the structure on
which their slaty cleavage depends may be completely explained on
mechanical principles. The author’s arguments are well put to-
gether, and with regard to many supposed cases mathematically
correct ; but whether applicable to all cases of cleavage is perhaps
more than can fairly be assumed, nor does it appear to be a necessary
consequence, that because a rock has been exposed to enormous press-
ure, its surface must therefore have spread out over a more extended
Space in proportion to that pressure, as the author seems to assume
in the account of his practical experiment with the pipe-clay, and
the scales of oxide of iron. The author concludes by observing that
the cleavage of the limestones varies directly as the amount of
mechanical compression to which they have been subjected, and
that he cannot therefore hesitate to conclude that slaty cleavage is
the result of mechanical, and not of crystalline forces.

Amongst the works of a more general character, | must remind
you of the publication of Sir Charles Lyell’s last edition (fifth) of
the ‘ Manual of Elementary Geology,’ or the ancient changes of the
earth and its inhabitants, as illustrated by geological records. It is
distinguished by much additional information, derived both from the
extended observations of the author himself, and from the labours
and. researches of other geologists. A most interesting chapter in
this volume is the detailed account of the Canary Islands, and the
celebrated Island of Palma, regarded by the late Leopold von Buch
as the type of what he called a “ crater of elevation,’ or “ Erhe-
bung’s Crater.’ Sir Charles Lyell has recently personally examined
these localities, in company with Mr. Hartung of Konigsberg, to whose
zeal and talents he was indebted for much assistance, and the result
of the examination has been to callin question the ‘elevation theory”
of the celebrated Prussian geologist.

After carefully describing the physical features of the district, and
the various strata of scorize, lapilli, and lava which constitute the dif-
ferent beds, Sir Charles points out several remarkable circumstances
which militate against the elevation-crater theory. He particularly
alludes to the absence of fractures in the rim of the great cavity of
the Caldera, which must have been the result of any elevatory action.
He fairly shows the greater probability of the mass of inclined beds
and strata round the orifice bemg due to the accumulation of ejected
tuffs, lapilli, and scoriaceous matter falling round the crater, from
which they had been ejected, and thus forming a compact mass of
igneous matter of various kinds, sloping in every direction, at a con-
siderable angle.

®

cxil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

At the same time there are pheenomena which even this theory
fails to explain satisfactorily, and we shall probably not greatly err if
we assume that, while the chief amount of altitude is due to the
accumulation of ejected matter round the orifice, a certain amount of
paroxysmal elevation has taken place, although not sufficient to
support the entire theory of the late Leopold von Buch.

I may also mention that this work contains much additional infor-
mation respecting the tertiary deposits of Germany and the age of
the associated brown-coals.

Prof. Ehrenberg continues his investigations respecting the Infu-
soria with his wonted energy. Interesting notices of his discoveries,
and his communications thereon, will be found in Leonhard and
Bronn’s Jahrbuch for the past year. The remains of many forms
of Polythalamia have been found by the Professor in the green sands
of various formations, some of which are so well preserved that they
have led to interesting physiological discoveries.

A question of great mterest, both to zoologists and to geologists,
has recently attracted the attention of the Geological Society of
France and of the Academy of Sciences. The habit of several spe-
cies of zoophytes aud mollusca to perforate rocks of different kinds is
one which has not yet received a satisfactory solution. Whether
this result is produced by chemical or mechanical means has not yet
been fully proved, although the balance of evidence seems now lean-
ing towards a mechanical solution. In this state of the question, and
while many persons are still disposed to believe that these perforations

have been produced by other means, the statements lately made in

Paris, and the specimens laid before the Institute and the Geological
Society, are sufficiently interestg to merit notice on the present
occasion. It was originally supposed that calcareous rocks alone had
been perforated by these animals, but the same phenomena have
recently been observed in other rocks. M. Caillaud of Nantes has
found the granite of Poulinguen, in the Bay of Croisie, perforated by
Pholades. In this case, the strize in the hollows corresponded with
the spinous processes of the shells, and left no doubt that the effect
was here at least due to mechanical action. Here, however, the
decomposed state of the granite may have facilitated the operation.

At a more recent period, M. Eugéne Robert exhibited a block of
Silurian sandstone, belonging to the transition formation which
forms the shore of the great bay of Douarnenez, perforated by nume-
rous holes made by Hchini living in them. Each circular cavity was
exactly proportionate, both in size and shape, to the Echinoderm
in it.

Prof. Long, of Grenoble, well known for his many able geological
memoirs, has recently requested M. Valenciennes to lay before the
Academy of Sciences several specimens of perforating Hchini which
have established themselves in the granite of Guérande, in the Bay of
Croisie, near Turballe, not far from Piriac. This granite is similar
to, and in the same state of decomposition as, that of Poulinguen,
and is perforated over a space of several kilometres by Mollusks and
Echinoderms, and the Echini are evidently of the same species as

Vj

ANNIVERSARY ADDRESS OF THE PRESIDENT. exill

those which have perforated the Silurian sandstones of Douarnenez.
Whether it is the same species as the L. lividus (Lamk.) from the
Mediterranean, with which it has the greatest resemblance, remains
to be proved.

I understand that when these or similar specimens were exhibited
before the Geological Society of France, a lively discussion took
place as to the cause of the hollows in which the Echini dwelt ;
whether the Kchini had themselves made the cavities, or had only
crawled into cavities already made for them by other means. When
I was at Paris last summer, my attention was attracted by a fine spe-
cimen of granite rock, worn into numerous cavities, each containing
an Echinus, exhibited at the Palais de l Exposition. This was long
before the discussion at the Geological Society took place, and I can
only say that the decided impression on my mind was that the cavi-
ties in question were made by the animals themselves. It would be
impossible to explain, on any other supposition, the remarkable coin-
cidence between the size of the Kchinus and the depression in which
it dwelt. This hollow, it should be observed, never exceeded,
even in the case of the largest, half an inch in depth. The Echini
were there of all ages, from half an inch to two inches in diameter,
and in every case the circumference of the depressions, crowded as
they were on one another, invariably coincided with the Echinus in
it. In some cases, when the cavities had been vacated, a new comer
had attached itself, not in the pre-existing cavity, as might have been
expected, but on the intervening border, and thence wearing down
the rock had caused a depression, intersecting both the neighbouring
hollows.

A notice has reached me, announcing the intended publication of
a work entitled Etudes Géologiques, by M. Fauville of Perpignan.
Should the work thus announced ever see the light, it will contain
more novel doctrines and bolder statements than the most ingenious
or paradoxical Members of this Society are in the habit of putting
forth. Our greatest efforts will be small indeed by the side of the
ambitious doctrines of M. Fauville, who proposes to describe the
history of the earth from its first existence in a nebulous state, and
at an enormously greater distance from the sun than at present,
through the immense spiral course which it has described in space,
passing successively through the actual positions of Neptune, Uranus,
Saturn, Jupiter, Vesta, Juno, and Mars, to the moment of its final
volatilization im the immediate vicinity of the Sun, to which, in the
spiral course laid down for it by the author, it is gradually tending.

Geological Maps.—I must not omit to call your attention to the
New Geological Map of Europe, by Sir R. Murchison and Professor
Nicol, which was exhibited and explained by one of the authors at
the recent Meeting of the British Association at Glasgow, and which
is now published. This map is in fact an extension to the whole of
Europe of that of Russia and the Ural, published by Sir R. Murchi-
son in 1846. It is on the same scale, and with the same colours to
designate the various formations. It gives us, for the first time, an
idea of the geology of Spain, for which we are mainly indebted te

CX1V PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

M. de Verneuil and those Spanish geologists and miners who, with
M. Casciano de Prado, have for some years been actively employed
on the geology of that country. Indeed, had it not been for the wish
of the authors to delay its publication until they had obtained the
materials collected by M. de Verneuil respecting the geology of the
Peninsula, the map would have been published long ago. We are
greatly indebted to them for having thus filled up this blank in Eu-
ropean geology. Still all is not yet done in the Peninsula, notwith-
standing the labours and exertions of MM. d’Archiac, de Verneuil
and others. M. d’Archiac, it is well known, was the first to esta-
blish the existence of the Trias in Spain, and I have no doubt that
we shall soon obtain from him and his fellow labourers and associates
in that field much additional information on this subject.

The followmg account of the progress of the geological map of
Germany, which has been recently forwarded to me from one of those
who are actively engaged in the undertaking, will, I am sure, be read
with interest :— . |

“In Bavaria, the surveys of the Fichtelgebirge, of the Bavarian
Forest, and of the neighbourhood of Regensburg, under the direction of
Prof. Giimbel, are completed. In Darmstadt the following sections,
Bredenkopf and Gladenbach, prepared by Herr v. Dechen, that of
Budingen by Ludwig, and Giessen by Dieffenbach, who is, alas! no
more, are already finished and in the engraver’s hands. The district
of Friedberg is published. The Hessian Government has provided
ample means, and everything is progressing satisfactorily. The
German Geological Society has given over all the original sketches
and plans to M. v. Dechen, to prepare a new general Index Geolo-
gical Map of Germany. He has completed his task, and will shortly
publish the map. You probably already know that Rhenish Prussia
and Westphalia are entirely laid down, and that two sections of the
Westphalian cretaceous district have already appeared. The execu-
tion is the finest I have seen in Germany. In Baden, all our prepa-
rations are made, and. I believe we shall commence in a short time,
if peace is secured.”

I must also inform you that M. v. Dechen, the distinguished Prus-
sian mining engineer and geologist, also exhibited at Paris a Geolo-
gical Map of the Rhenish provinces of Prussia and of Westphalia.
This map, on the scale of 5th, has been prepared entirely by
M. v. Dechen, by order of the Prussian Government, and is a worthy
monument of his talent, his zeal, and his exertions.

In alluding to Mr. Mylne’s large MS. Map of the Geology of
London and its immediate vicinity, exhibited at Paris, it is impossible
to praise too highly the attention and care with which the materials
have been collected, and the artistic skill with which it has been
executed. It is to be hoped that Mr. Mylne will not long delay the
publication of it.

Before concluding these observations, which, however imperfect
they may be, have nevertheless, I fear, greatly exceeded the usual
space allotted to these Addresses, I am desirous of saying a few
words on a subject closely connected with the highest considerations

ANNIVERSARY ADDRESS OF THE PRESIDENT. CXV

of our science, and which has been argued with great ability by one
of the most philosophical writers of the day. I allude to the Essay
of Professor Baden Powell on the Philosophy of Creation. One of
the many great and transcendental questions discussed in this Essay
is the controversy as to whether we are to give a preference to the old
doctrine of the immutability of species, or to the more recently in-
troduced theory of transmutation. The question is undoubtedly one
of great difficulty, but it is not the less necessary that we should
endeavour to form a definite opinion on the subject, founded on the
fullest and most authentic information we can obtam. It may in-
deed, in some respects, be said to be one of the most important
questions in geological investigation. Why do we endeavour to ob-
tain correct information respecting the true order and arrangement
of stratification? Why do we endeavour to obtain the most perfect
collections of the organic remains of each stratum and formation, and
to ascertain the different classes and groups of organized beings which
have dwelt and flourished on the surface of the globe at the different
periods of its existence? Surely not for the sake of such collections
and such knowledge of stratification per se. For, although, owing to
peculiar circumstances, many geologists may not have the opportu-
nity of carrying their investigations beyond these points, it should
never be forgotten that all such information is but a stepping-stone
to higher generalizations. It is but the alphabet of one of the lan-
guages in which Nature speaks to us, and by means of which we
must endeavour to unravel the past history of our globe, and to form
some idea, so far as our finite faculties permit us, of the first origin,
and inductively of the final objects, of creation. In this point of view,
the question as to the immutability or transmutation of species is
one which touches the very existence of our science, and I am there-
fore desirous of briefly poimting out what appears to be a fallacy in
some of the statements of Prof. Powell on this subject.

The arguments of the various writers on both sides are fully and
fairly given in this work, and the author professes merely to point out
the bearings of the question, the difficulties in which it is involved, and
to controvert what he considers hasty and untenable assertions on either
side. But while doing this, it is impossible to avoid the conviction
that he has a decided bias to one side, that he considers the doctrine
of transmutation of species more consistent with sound philosophical
induction than what he calls the hypothesis of an eternal immuta-
bility. I shall not pretend to occupy your time by going through
arguments so well known to every paleontologist and geologist. I
ouly wish, as I said before, to point out one or two conclusions which
involve what appear to me a fallacy. —

After showing how the successive investigations of the great com-
parative anatomists and zoologists of the last half-century have re-
sulted in the establishment of the doctrine of the unity of compo-
sition of animal forms, a result to which the researches of Prof. Owen
have mainly contributed, he proceeds to the examination of the
question of species. He points out the existence of subspecies and
varieties, many of which become permanent, and alludes to the

CXV1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

number of new species constantly discovered which have to be in-
serted between other allied species already known, inferring that the
specific differences between each must by such additions tend to di-
minish continually, and that all species tend to be connected by more
and more close affinities. Thus, he argues, all differences gradually
disappear, and there results no greater difference between two
allied species than between varieties of the same species, and con-
sequently no difficulty in admitting that the difference which does
exist is not greater than what might be expected as the result of local
circumstances, modifying external forms, and thus practically pro-
ducing transmutation. Indeed he goes still further, and adopting an
infinite duration of time, and an infinite number of species, he argues
that there will ultimately be no perceptible difference at all between
two allied species. The following is his argument :—

“ But, while the number of species thus tends to become infinitely
great, the extreme difference between man (let us suppose) at one end
and a zoophyte at the other end of the scale is constant and finite ;
hence the average difference between any two species tends to be-
come znjinitely small; multiplied by the number of species, it must
still be equal to a finite quantity ; and the product being fincée if the
first factor be infinity, the second must be zero.”

This argument appears to involve a fallacy. If this infinite num-
ber of allied species is to prove the transmutation of one form into
another by showing that the difference between them is infinitely
small, it would be necessary to prove either that they had all existed
contemporaneously together, or that the allied forms immediately
succeeded each other. But when the author calls in the aid of long
geological epochs in which some of these closely allied forms existed
at long intervening periods, I cannot see how the question of trans-
mutation is thereby strengthened. If A, B, and C are the allied forms,
and A and C existed either together or in immediately succeeding
periods, and B, which is the connecting link to fill up the gap be-
tween them, is only found to exist after many millions of years, or
even only after the other two had died out, the theory of transmu-
tation cannot be supported by assuming the gradual change of A into
C, through the intervening form of B. If every possible gradation
of form existed in the fauna of one period and of one region, or of
successive periods and neighbouring regions, then indeed the advocates
of the transmutation theory might endeavour to maintain that all
these forms were only varieties of one type occasioned by the pecu-
liar conditions of life in which each was placed; but this conclusion
is no longer valid when long periods have intervened between the
existence of one form and that of the other. The utmost argument
that could be drawn from such premises would be a confirmation of
the great doctrine of unity of plan in the creation of all organized life,
extending through all ages of the world.

Another fallacy may, I think, be detected in the manner in which
Prof. Powell, after stating the arguments on both sides, pots out
the real alternative. He says, ‘‘ the only question is as to the sense
in which such change of species is to be understood ; whether indi-

ANNIVERSARY ADDRESS OF THE PRESIDENT. CXVil

viduals naturally produced from parents were modified by successive
variations of parts in any stage of early growth or rudimental deve-
lopment, until in one or more generations the whole species became
in fact a different one ; or whether we are to believe that the whole
race perished without reproducing itself, while, independent of it,
another new race, or other new individuals (by whatever means)
came into existence, of a nature closely allied to the last, and differing
often by the slightest shades, yet unconnected with them by descent ;
whether there was a propagation of the same principle of vitality
(in whatever germ it may be imagined to have been conveyed), or
whether a new principle or germ originated independently of any
preceding, out of its existing inorganic elements.”

In the sentence which I have just quoted, there are two sets of
alternatives, and I think that in each set the author has inserted a
fallacy in stating the second alternative respecting the theory of im-
mutability. In the first set he has assumed, without any warrant,
that a whole former race has perished and is succeeded by another of
a closely allied nature and often differing only by the slightest shades.
In such a case, viz. where the difference is very slight, it may be
possible that the second race is really the descendant of that pre-
viously existing, slightly modified by the external conditions of life

in which it was placed. But the author has omitted all reference to

those species which occur in the new or upper formations, whose
resemblances or analogies to those of the preceding period are very
distant or imperfect, and which cannot therefore be looked upon as
the descendants or modifications of the pre-existing forms. There
are undoubtedly species which have been continued through many
geological periods, have survived many local disturbances, and which,
while others may have perished, have been kept alive by greater vital
energies or other influences, and have become the associates of new
forms introduced for the first time and having no resemblance to or
analogy with the forms which had preceded them. We know that
some species pass into many varieties, sometimes even contempora-
neously with the existence of the typical form ; there is, therefore,
surely nothing inconsistent with the theory of immutability in sup-
posing, under peculiar circumstances, that varieties of some species
may also take the place in a subsequent period of the original typical
form. ‘This, however, is the exception, and not the rule.

With regard to the second set of alternatives in the passage I have
quoted, I think Prof. Powell is too much begging the question when
he concludes the sentence with these words: “out of its existing
inorganic elements.”’ Surely this is taking too physical or material
a view of the matter, and one not required by those principles of in-
ductive philosophy which he so strongly supports. The advocates
of immutability of species do not generally talk of a principle of
vitality originating out of inorganic elements. When old forms die
out, and are succeeded by new, the matter of which the new consist
is derived from the existing inorganic elements ; but the life or prin-
ciple of vitality by which it is animated must proceed from a different
source, from that same source, mysterious it may be, which first

VOL. XII. t

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CXVill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

breathed life into those creatures which dwelt in the oldest paleeozoic
ages. Organic life on this earth must have had a beginning, and
that beginning must have proceeded from a source very different
from that dead matter which formed the visible body ; and from
that same source proceeded the principle of vitality which animated
the new forms when successively created on the earth. And with
reference to this question, I must emphatically deny the right
assumed by Prof. Powell, when he puts what he calls an imaginary
case of a truly new species making its appearance, to question those
who deny the theory of transmutation, how this new species made
its appearance ; whether it appeared as an ovum or seed, or at what
period of growth, &e. When Prof. Powell can state in what form
the first living organisms appeared on the earth’s surface, he may
| demand an answer to this question. It is the more remarkable
that Prof. Powell should make this demand, as he has stated, in
a former part of the Essay, that in a geological point of view the
| term ‘“Creation”’ signifies the fact of origination of a particular
| form of animal or vegetable life, without implying anything as to
the precise mode of such origination : not that I think this definition
altogether satisfactory, but yet it might have precluded him from
making such a demand.
: But I have been led into a longer statement than I had intended.
I will merely add that, notwithstanding these criticisms that I have
ventured on, the essays of Prof. Powell deserve a careful and atten-
tive reading. They are eminently suggestive and replete with deep
| thoughts and scientific views, and form an interesting element of the
geological, or rather geognostic, literature of the day.

As in some measure connected with the same subject, I must
direct your attention to a paper published by Mr. Alfred Wallace*
on the law which has regulated the introduction of new species. Mr.
Wallace is a naturalist of no ordinary calibre. His travels in South
| America and elsewhere are a sufficient guarantee of his high merits ;
: he now writes from Sarawak, Borneo. From a careful examination
of the actual distribution of existing forms of animal life, and the
gradual but complete renewal of the forms of life in successive geo-
logical epochs, he has deduced the following law :— Every species
has come into existence coincident both in space and time with a
pre-existing closely allied species. The question is one of great
importance, and deserving the careful investigation of every geologist ;
but I think it may be doubted whether this assumed law can be
maintained as a universal generalization.

GENTLEMEN,—Having thus, however imperfectly, gone through
my allotted task, it only remains for me, before quitting this Chair,
to thank you for the forbearance you have shown to my shortcomings,
and to entreat your indulgence for what I may have neglected during
the period I have had the honour of presiding over this Society. I
know that there are many who might have brought more varied in-
formation and geological knowledge to bear on the discussions at our

* Ann. of Nat. Hist. vol. xvi. p. 104.

ANNIVERSARY ADDRESS OF THE PRESIDENT. Cx1x

Evening Meetings ; but I think I may also say that there are none
who take a livelier interest in the welfare and prosperity of the
Society. And whether it will be our destiny long to occupy these
apartments, with which our existence almost seems identified, or
whether we shall one day find ourselves located in some scientific
palace in juxtaposition with other scientific bodies, I trust that you
will ever find me taking the same warm interest as now in our pro-
ceedings, and ready to afford all the assistance in my power towards
furthering the objects of our common cause. I congratulate you on
the choice of my successor, which you have this day made. I feel
that I resign this Chair to one who is intimately acquainted with all
the details of the Society, to one who has long lived and moved and
spoken amongst us,—who is thoroughly acquainted with every branch
of our science, and who will at the same time impart fresh vigour to
our proceedings, and give additional interest to the further progress
of geological research.

‘a
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THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

NoveMBeER 7, 1855.
Willian Harrison, Esq., was elected a Fellow.
The following communications were read :—

1. On the Coat of the NortuH-weEsteRN Districts of Asta
Minor. By H. Poor, Esq. Communicated by the Foreign

Office.
(Abstract.)

Mr. Poors, in his Reports to Government on the result of his
journey to Asia Minor to examine into the probability of workable
coal being found in the country near Brussa and Ghio* (Bithynia),
in which coal had been reported to occur, states that he travelled
from Ghio inland along the south bank of the river flowing from the
Lake Ascanias, around the shore of the lake by a south-east route,
passing Niceea and along the north shore, until he returned to the
village of Ortokoi, without finding any trace of coal. Marble and
limestones prevailed along the whole line, except at Solis, where a
narrow band of nearly vertical sandstone cropped out: On the south

* Known also as Gemlik.
VOL. XII.—PART I. B

“|

2 PROCEEDINGS OF THE GEOLOGICAL society. _[Noyv.7,

and east sides of the lake a conglomerate occurred, dipping with a
slight inclination towards the lake. Ouram Mountain, in the rear
of Niczea, appeared to be composed of tufa. Tufa also occurs on the
shore near Keramid.

Between Ghio and Brussa the prevailing rocks are limestone, con-
glomerate, and sandstone.

In consequence of rumours of the existence of coal near the Lake
of Apollonia, Mr. Poole travelled round that lake, but met with
none. Limestone and sandstone prevail there.

Subsequently Mr. Poole went from Yallova (in company with Mr.
Sandison) inland to Ortokoi, without finding any traces of a coal-
formation. He next went from Yallova westwards along the coast
as far as Kourikoi, where a bed of lignite, 9 inches thick, occurs; this
is said to have been worked to some extent (by a 60 yards’ level) by
the Armenians four years since; thence he went inland to Sulimanli
without seeing any indications of coal. He then proceeded to visit
Arli Effendi’s coal, near the village of Tchoukurkoi, S.E. of Yallova
at three hours’ distance. Along a ravine here lignite occurs in a
seam varying from 1 to 4 feet in thickness, and dipping S. 23° E. at
an angle of 52°, with coarse sandstone above and below it. This
lignite also has been worked some years since by the Armenians. It
was from this lignite that samples had been sent to Mr. Sandison* ;
but in Mr. Poole’s opinion it is of no promise.

Another excursion was to the Lake Sabandji, where a thin seam
of lignite crossing the road on the south of the lake, and a lignite at
Ak Sophé, to the east of the lake, were visited. Nowhere did Mr.
Poole find proof of the existence of good workable coal in the districts
above referred to.

Subsequently he proceeded to visit the Kosloo and Zungeldek
coal-district. ,

In a lettert+ to Sir R. Murchison, Mr. Poole makes the following
observations on the geology of the districts through which he passed
on his last tour of inspection. Going from Constantinople to Yallova
in an open boat, he observed that at Touzla Point the limestone has
been squeezed into zigzags, with intervening concentric bands, as if
pressure had been applied from below. Salt is made from a small
lake near the Point; and lead-mines are worked at two hours’
distance. ar

From Yallova, writes Mr. Poole, I rode to the top of the ridge
which overlooks Ortokoi, where I had been on my former tour ; after
crossing the plain, I found coarse sandstone dipping S8.E. at about
45°. The next ridge had soft red sand overlying micaceous rock,
which dipped 23° N. 34° W. After crossing the ridge, the rock
was nearly vertical, dipping 8. and E. I then crossed to the west
side of the brook, and found limestone all along its western side,

Going along the shore from Yallova in a westerly direction, at
Ghiuz Tepé, I met with sandstone, dipping S. 48°, full of broken

* See Quart. Journ. Geol. Soc. vol. xi. p. 476.
+ Dated Constantinople, Sept. 21, 1855.

1855. ] POOLE—COAL OF ASIA MINOR. 3

shells; at Sivri Tepé the sandstone dipped 20° S. 80° W.; and a
little further on thin seams of lignite occurred, dipping 42° S. 75° W.
Between Yallova and Ghiuz the earth was much cracked by the late
earthquakes ; and in some places large pieces had sunk 20 to 40 fcet
perpendicularly down. Near Kourikoi is another seam of lignite
(referred to above, p. 2).

I then rode inland to visit the Sultan’s Baths at the back of Suli-
manli. The first hills were of white limestone; and in the valley
was white marl, with thin seams of lignite. After an hour’s ride we
crossed a vein of greenstone, 4 feet wide, dipping 62° to 68°S., and
striking EH. and W. The next hill was of coarse conglomerate, dip
21° S. 45° E.; the ground then became much disturbed, and at the
baths the limestone is nearly vertical ; strike N. and S. The tem-
perature of the spring was 148° Fahrenheit. On the south side of
the Baths the rock was clay-ironstone, dipping E., nearly vertical.

North of the village Tchoukurkoi (where Arli Effendi’s coal is)
we found the soil to be red and white marls; and we followed the
river until we reached the shore of the Sea of Marmora, along which
we rode until we got to Dil Point, from thence we crossed by a ferry
to the northern shore. Here blue limestone, dipping N. 58°, came
down to the water’s edge: thence to Tauschandjik, the rocks were
white sandstone and coarse conglomerate. About one mile from
Iskeli are large caverns in the limestone, which dips about 8.E. ;
this was succeeded by coarse conglomerate; the rocks then receded
from the shore, and from the pieces on the road and in the brooks
appeared to be red sandstone.

The cliffs at the Lake Sabandji are very high, and composed of
rounded stones and sand, evidently an ancient beach. The tradition
is that the lake was formed at the same time that Nicomedia was
destroyed by earthquake: there is no outlet from the lake, though
several streams run into it. :

From Lake Sabandji we went through Ada Basar, crossing the
Sangarius three times, to the shore of the Black Sea. White
limestone prevailed until we got to Ak-caia (about one hour east of
Atsche shehr); this Point is some hundred feet high, of fine sandstone,
nearly perpendicular, full of large concretions; a great many also
lie on the shore with the waves breaking over them.

The rocks were principally limestone until we reached Heraclea,
which is built on a coarse sandstone. ‘The road is so bad and tedious
from Heraclea to Kosloo that we went in a boat. Mr. Barclay has
promised to make you during the winter a plan of the Coal-district ;
which is not continuous, but in patches along the coast for several miles,
and averaging about one and a half mile in breadth ; therefore I shall
not attempt to describe it at the present time. There are ten known
seams at Kosloo; and four are seen in one hill-side at Zungeldek.

I found Stigmaria, Calamites, and Sigillaria in the floor of the
coal, but they are scarce; some Ferns were found in one of the
seams formerly worked at Kosloo, but I could not meet with any.

B2

4 PROCEEDINGS OF THE GEOLOGICAL sociETy. __[Nov. 7,

There is not any later formation overlying the coal-formation, and
in many places the coal-deposits have been removed. The mines are
much disturbed by faults crossing in every direction, and the seams
are in general inclined at an angle of about 30°.

The particulars of his first journey in Asia Minor in search of coal
are not referred to in the above abstract, but have been communicated
by the author since his return to England.

On this occasion Mr. Poole travelled from Ghio to the Lake
Ascanias and thence by Bazarkoi to Ortokoi; and in the ravine
between Ortokoi and Yenikoi he examined five seams of lignite, dipping
for the most part at a high angle to the N. From one of these
seams, 20 inches thick, a quantity had been obtained for a steamer
and found useless. The thickest and lowest seam, about 7 feet thick,
is full of small shells (Planorbis and Limneus’). Mr. Poole also
examined the Hassan Deré seam, in a ravine to the westward. This
much nearer approaches coal in its character, and has been worked
by the Armenians to some extent ; but the works were destroyed by
the late earthquakes (Quart. Journ. Geol. Soc. vol. xi. p. 543). At
Hassan Deré the Nummulitic Limestone, dipping to the south, occurs
within 200 yards of the coal, which dips to the N.W.; but, from
the very much disturbed state of the stratification, the relations of
the several rocks are not apparent.

2. On the Newer Tertiary Deposits of the Sussex Coast.
By R. Gopwin-Ausren, Esq., F.R.S., F.G.S.

(Abstract.)
[The publication of this Paper is deferred. |

From Brighton, westwards, between the chalk-hills and the sea, the
surface of the country is formed, first, by a raised terrace of “red
gravels,” lying on the sloping base of the chalk-hills, and on the old
tertiary deposits; secondly, the gravels of the Chichester levels, or
the “‘white gravels.’ These latter are distinctly bedded and seamed
with sand, and are more water-worn than the red gravels which pass
under them; thirdly, the white gravels are overlaid by “ brick-
earth,” which is somewhat variable in its characters. 'These, with
their equivalents, are the Glacial deposits of the district in question.

The coast-sections, though very limited in extent, exhibit several
important phenomena illustrative of the history of these newer ter-
tiary accumulations. At Selsea, where the Glacial deposits are about
25 feet thick, the underlying Eocene clay is seen, at extreme low
water, to be perforated by a very large variety of Pholas crispata,
and to be overlaid by a deposit containing Lutraria rugosa, Pullas-
tra aurea, Tapes decussata, and Pecten polymorphus, contempora-
neous with the Pholades. Elsewhere brown clays, or local ferru-
ginous gravels, cover unconformably the Eocene beds. The surface

1855. ] AUSTEN—SUSSEX TERTIARIES. 5

of the brown clay is deeply eroded, and bears a yellowish clay,
which contains large chalk-flints, and a great variety of pebbles and
boulders of granitic, slaty, and old fossiliferous rocks, such as are
now found in the Cotentin and the Channel Islands. One boulder
of porphyritic granite measures 27 feet in circumference. A few sea
shells (Iittorina, &c.) occur in the yellow clay.

This deposit the author regards as the equivalent of the “ white
gravel”’ in its extension southwards, the gravel having been littoral,
and the clay with boulders a deposit formed in somewhat deeper
water of this portion of the glacial sea.

The coast-sections exhibit the surface of the yellow clay as having
been eroded and covered by a variable deposit, sometimes gravelly
_ and sometimes sandy, and containing marine shells (Cardium edule,
Ostrea edulis, Turritella terebra, &c.). This band contains also
fragments of the old crystalline rocks, obtained from the destruction
of the underlying yellow clay.

On the shelly and pebbly band lies the brick-earth, an unstratified
earthy clay deposit, with small fragments of flmt, and a few pebbles,
and with occasional silt-like patches.

The particular subject of this paper was the occurrence of the
granitic and slaty detritus im the yellow clay. These blocks are
especially numerous near Bracklesham, Selsea, and Pagham. The
author explained the difficulties that lie in the way of supposing
that they were derived from the Cornwall coast, or direct from the
shores of Brittany or the Channel Islands. His previous observa-
tions, however, on the bed of the English Channel had prepared the
way for the explanation of the hypothesis he now advanced—of the
former existence of a land-barrier, composed of crystalline and paleo-
zoic rocks, crossing from Brittany to the south-east of England, and
forming a gulf or bay open to the west.

Into this bay the marine fauna represented by the Pholas crispata
and its associates extended from the westward; and in the hollow of
the bay, at a rather later period, coast-ice brought the boulders from
along the old shore-line, which is now represented by a sunken peak
im mid-channel and a shoal of granitic detritus.

Alteration of level succeeded ; and the partial destruction of the
yellow clay deposit afforded the overlying pebble-bed, and, in the
author’s opinion, the granitic blocks found in the old raised beach
at Brighton.

Mr. Godwin-Austen thinks it probable that the superficial brick-
earth of the district under notice was formed in a land-locked lagoon,
subject to periodical freezing; and that the “ elephant-bed” at
Brighton is one of its many and variable equivalents (in this case
probably subaérial).

The brick-earth area has been subsequently encroached upon by
the estuaries of Pagham,- Portsmouth, &c.; and the successive oscil-
lations in the level of the land are evidenced in the estuarine depo-
sits and submerged forests of Pagham, Bracklesham, Portsmouth,
&e.

With regard to the latest movements, the author’s observations

6 PROCEEDINGS OF THE GEOLOGICAL society. {[ Noy. 21,

showed that from Lewes Levels to Chichester Harbour, and on to
Hurst Castle, the coast exhibits signs of undergoing elevation at the
present day. The coast of the Isle of Wight opposite seems, on the
contrary, to be suffering depression; whilst the back of the island
exhibits some curious signs of local oscillation.

NOVEMBER 21, 1855.
James Gay Sawkins, Esq., was elected a Fellow.

The following communications were read :—

1. On the Borine through the CuauKx af KentisH Town,
_ Lonpon. By J. Presrwicn, Esq., F.R.S., Sec. G.S.

Ir is little more than half a century since Artesian wells were brought
into use in and around London. The success of the first works led
to so rapid an extension of this mode of procuring water that the
source of supply, which was from the sands under the London Clay,
proved insufficient for the demand. Consequently, in order to ob-
tain a better supply of water, a large number of the wells more re-
cently constructed have been carried down to variable depths into
the underlying chalk. Nevertheless, the water-level in the Artesian
wells, which, im 1822, rose to the level of Thames high-water-mark,
now stands in London at about 50 feet below that level, and continues
to fall at the rate of about 1} to 2 feet annually.

From a previous acquaintance with the London Tertiary district,
and from the attention which the question of the water-supply
attracted at the time, I was led, in 1849, to make some inquiries
into the bearing of the geological structure of the country around
London with reference to the question of the deep-well-supply. The
result of that inquiry I published early in 1851 *, and the conclusion
to which I arrived was that the dimensions of the Lower Tertiary
sands were insufficient to furnish any increased supply, and that the
chalk not being, properly speaking, a water-bearing deposit, 7. e. one
transmitting water freely in all directions through its mass, could
ouly yield at that depth beneath the surface, and from its outcrop,
an uncertain and moderate supply. I further showed, that from be-
neath the chalk there cropped out, both to the north and south of
London, a large mass of light-yellow, ochreous, and white siliceous
sands, geologically known as the Lower Greensand, 300 to 500 feet
thick, extremely permeable, and yielding generally, in its surface-
wells and springs, water of good quality. As I found that the
effective area and thickness of this deposit was ten times greater
than that of the Lower Tertiaries, and its outcrop considerably higher,

* “ A Geological Inquiry respecting the Water-bearing Strata of the country
around London.” 8vo. Van Voorst, 1851.

1855.] PRESTWICH—BORING AT KENTISH TOWN. 7

I was led to anticipate a water-supply proportionately larger, and
capable of rising through Artesian wells to a height of 100 feet or
more above the level of the Thames at London*.

The practicability of such a work was proved a few years since in
France by the Artesian well of Grenelle at Paris, which, after traversing
_ 148 feet of Tertiary strata, and 1394 feet of Chalk, reached the
Lower Greensand, and from this source a large and well-maintained
supply of excellent water has since been continually flowing, and
rises 130 feet above the surface. There are several such wells
through the Chalk at Tours, Elbceuf, and elsewhere, some for private,
and others for town supplies, and the greater number are perfectly
successful. In London the conditions for a work of this descrip-
tion appeared even more favourable than in Paris, for the Lower
Greensand in England is much thicker than in France, and the out-
crop is nearer to London than to Paris and relatively higher.

The only apparently serious objection urged against such a work
here was the thickness of the chalk, which was variously estimated
from 1000 to 1700 feet thick ; but I showed, that, although it had
proved to be more than 1000 feet thick at Saffron Walden, it was
probably much’less at London, for there was reason to believe
that the upper beds of the chalk had been extensively denuded, as
they trended towards the area of the Weald, before the Tertiary period,
and that the chalk with flints around London, which it had been
customary to call the Upper Chalk, belonged in reality to the Middle
Chalk. Taking the mean of several sections drawn through Lon-
don, I concluded that the chalk would not be found to be more
than 600 to 650 feet thick. Adding to this 200 feet as the thick-
ness of the superimposed Tertiary strata, which at London vary
from 100 to 300 feet, and assigning 40 to 50 feet to the underlying
Upper Greensand, and 100 to 150 feet to the Gault, I estimated that
the Lower Greensand beneath London might be reached at a depth not
exceeding 1000 to 1100 feet. I suggested that the experiment should
be made in low ground, and instanced St. James’s Park as a favour-
able locality for obtaining by this means natural fountains rising to a
considerable height above the surface.

We are indebted, however, to the Hampstead Water-Works Com-
pany for the first attempt to solve this problem practically ; but, as
the surface of the ground at their Works at Kentish Town is 174 feet
above Thames high-water-mark, the situation is not so favourable as
might have been wished. A few years since this Company sunk
a well through the Tertiary strata (at that spot 324 feet thick), to a
depth of 215 feet in the chalk, making a total depth of shaft of

* T calculated the effective area of the Lower Tertiary sands to be 24 square
miles, and that of the Lower Greensand 230 square miles; whilst I estimated the
mean thickness of the permeable beds of the former to be 19 feet, and of the
latter 200 feet. As it appears that the present water-supply obtained from Arte-
sian wells in the Lower Tertiary sands amounts to about 3 to 4 million gallons in
the twenty-four hours, I considered it not improbable that from 20,000,000 to
30,000,000 gallons might be drawn from the Lower Greensand by means of
Artesian wells, without affecting the permanence of the water-level.

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

539 feet. The supply of water from this source being found insuffi-
cient for their purpose, the Directors of the Company, in 1852, con-
sulted MM. Degousée and Laurent, the eminent well-engineers of
Paris, on the advisability of smking through the Chalk into the
Lower Greensand. In November of that year these gentlemen came
to London, and I accompanied them to those places in the neighbour-
hood of Merstham and Reigate where the outcrop of the chalk and
underlying clays and sands is best exposed. ‘The conclusion to which
they arrived was precisely similar to my own, and on their report
the Directors resolved to undertake the work. Accordingly, on the
10th of June, 1853, bormg was commenced in the chalk at the bot-
tom of this well.

At a depth of 569 feet from the surface the chalk with flints ended ;
greyish chalk without flints, becoming more argillaceous in descend-
ing, was then traversed for a thickness of 294 feet. (See the sectional
list of strata traversed by the boring, pp.13&14.) The chalk-marl next
succeeded, and continued for 473 feet. This would give a total thick-
ness to the chalk of 586 feet. The chalk-marl passes so insensibly
into slightly sandy marls representing the Upper Greensand, and
these into the Gault, that it is difficult to draw any satisfactory lines
of division. I have taken as the representative of the Upper Green-
sand the more arenaceous and chloritic beds. They are 723 feet thick.
These strata, however, were here, on the whole, so argillaceous that
they were not permeable, and they consequently afforded no additional
supply of water. The Gault was found underlying the Upper Green-
sand in the usual order, and presented the ordinary character of a fine
grey calcareous clay, 1304 feet thick. At the base of this mass of
clay a layer full of the phosphatic nodules, so common at the base
of the Gault at Folkestone and elsewhere, was met with.

Thus far all the strata were in regular succession, and there was
every reason to believe that the same order which prevailed at their
outcrop, and with which there seemed to be nothing to interfere, would
be continued underground ; and that after traversing this band of
phosphatic concretions, the hght-coloured siliceous sands of the
Lower Greensand would succeed. The ordinary probabilities of the
geological sequence being maintained throughout this central area
seemed then so strong, that when the works were at that point, just a
year since, having occasion to speak on the subject at the Institute
of Civil Engineers, I did not hesitate to express my conviction that
a very few more turns of the auger would tap these sands. . This
opinion has unfortunately proved incorrect. Instead of meeting
with loose sands, the next bed which presented itself was one of red
argillaceous sand and sandstone, 1 foot thick: 12 feet of red clays
(some mottled light bluish-green) and sandstones then succeeded ;
followed by a singular conglomerate, 2 feet thick, containing pebbles,
of a considerable size, of various old and crystalline rocks : amongst
these were dark grey syenites, greenstones, red claystone-porphyry,
trap-rock, a grey semitranslucent quartz or hornstone, and a granular
schist with traces of fossils. Then came 26 feet of red clays, underlaid
by red sand and a bed of small rolled pebbles. These were followed

| =

1855.| © PRESTWICH—BORING AT KENTISH TOWN. 9

by 42 feet of alternating beds of very hard light grey and red sand-
stones, sometimes concretionary and calcareous, and of argillaceous
reddish sands. Then by thick beds of red clay, with subordinate
seams of micaceous red and light green sandstones and of reddish
argillaceous sands, to a further thickness of 74 feet ; ending at a
depth of 1302 feet in a hard micaceous light-coloured sandstone *.

The only spring of water met with beneath the Gault was in the
thin sand and pebble bed, No. 40. A rise took place in the water-
level of the well of 3 feet when this bed was first reached, but it was
not maintained.

The bore-hole, which commenced with a diameter of 12 inches,
was first reduced to 10, and then to 8 inches. It is tubed throngh
the chalk, gault, and the first 60 feet of the red beds, but the last
portion of 128 feet is not yet tubed.

The result of this important work is very unexpected, and presents
great geological difficulties. It raises a question of much interest both
in a scientific and practical point of view, and it will require further
careful inquiry and observation to enable us to determine to what
series these red clays and sandstones may belong, and thus estimate
whether or not there is a probability of meeting with water-
bearing strata at a yet greater depth. Do these red beds form an ex-
ceptional condition of the base of the Gault? Are they local beds of
the Lower Greensand? Do they belong to the mottled clays and sand-
stones of the Wealden? Or are they to be placed with the New Red
Sandstone? On the first three suppositions beds of water-bearing
sands may yet occur; on the last, however, the chance of finding
water would be more doubtful, although even then not altogether im-
possible. The Lower Greensand crops out with so much regularity
both to the north and south of London, and skirts the Gault so
continuously, that from a surface-examination of the ground there
could be no apparent reason for supposing that the same deposit was
not continuous underground and would be met with beneath Len-
don. I must confess that I never contemplated the probability of
any break in the order of superposition ; but, although it may prove
that my anticipations were wrong, still | would observe that geology
had nevertheless indicated the possibility of other conditions; for
Mr. Godwin-Austen, taking a wider field of observation, and basing
his deductions upon phenomena carefully studied in Belgium and
the west of England, came to the remarkable conclusion, commu-
nicated to this Society last spring, that the axis of the Ardennes
was prolonged. under the cretaceous series of the south of England,
and reappeared again on the surface in Somersetshire ; and he
inferred that it was probable that the coal-measures might be found
under part of the London Tertiary and Wealden districts. The evi-
dence adduced by Mr. Austen is of that nature that I am prepared to
admit the possibility of such a case, and therefore consider that the

* Since writing the above the property has passed into the possession of the

New River Company, and the works are at present suspended at this point.—
[J. P., January 1856.]

10 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 2],

pheenomena presented by the Kentish Town well must be taken into
consideration in connexion with his ingenious hypothesis*. The
exact state of the question remains, however, yet to be decided. No
satisfactory proof of these beds belonging to the New Red Sandstone
group has hitherto been met with. In mineral character they cer-
tainly closely resemble the Red Marls, and unless some proof on
other grounds can be adduced to the contrary, it is a point in
favour of such a correlation.

As it is well known that the Gault in some places passes into a red
clay, I at first considered it possible that these strata might be the
result of a like change, but the great thickness of the beds and the
alternations with sandstones militate against that view. Secondly, I
would remark, that near Dorking the Lower Greensand is capped by
a local bed of bright red clay ; but it is only 8 feet thick, and there-
fore the same objection holds, although the possibility of such a
variation is indicated. Next, with regard to the Weald clay: there
is here no objection with regard to dimension, and the occurrence
of mottled red clays and subordinate sandstones is a common feature
in this deposit ; still the absence of all freshwater fossils does favour
this correlation. With respect to the evidence obtainable from
organic series in these red beds, if the nature of the work, at so
great a depth and so far out of reach, did not present an unavoidable
source of error, we have evidence such as might solve the difficulty
presented by mineral characters. Several fragments of apparently
cretaceous Ammonites and Belemnites have been brought up by the
auger, but it may be doubtful whether those may have fallen down
the sides of the bore-hole. Still, on the other side, it is to be ob-
served that no such fossils were found in the Gault itself, and that the
bore-hole is tubed to the depth of 1172 feet; and M. Jus, who has
superintended this work, and carefully noted the occurrence and posi-
tion of the fossils, informs me that it was in one bed especially, viz.
the pebble bed (No. 40 of the sectional list, p. 13), at a depth of 1158
feet, that a small Belemnite was particularly abundant, and that in
one case the fossil was imbedded in sandstone and not loose. For
the last week all the fresh clay has been carefully washed and sifted,
but no more fossils have been found.

Mr. D. Sharpe has had the kindness to examine these fossils,
and the following are the remarks he has made upon them :—

“17 Soho Square, 16th November 1855.

“ My pEAR Sitr,—Among the fragments of organic remains from
the Artesian well at Kentish Town, there are very few which admit
of even a conjectural determination, and only one which can be
named with certainty; this is the Ammonites inflatus, Sow., which
also passes under the name of J. rostratus; the specimen is suffi-
ciently large and perfect to show all the distinctive characters of the
species, viz. a strong keel, back broad, sides flattened, with strong

* Still, admitting such a possibility, the Lower Greensand must range up to the

flanks of this ridge, and might, therefore, nevertheless be found underground at
other points at or near London, beyond the interference of the central axis.

1855. | PRESTWICH—BORING AT KENTISH TOWN. 1]

slightly curved ribs, either single or bifurcating, and thickest near
the back, where they are crossed by several transverse furrows, which
in the cast are but faintly seen ; the lobes of the septa are fully shown
in the specimen, and exactly agree with those of 4. inflatus; so that
no doubt can exist as to its identity. In mineral condition also the
Specimen exactly agrees with that of the same species from the phos-
phatic nodules in the brick-fields near Cambridge, which are supposed
to belong to the top of the Gault.

“‘ The species is also common in the Upper Greensand in many
localities; M. d’Orbigny quotes it as found throughout France in
the Craie chloritée and in the upper part of the Gault, so that every-
thing conspires to lead us to place the bed in which this specimen
was found, marked No. 80, 1196 feet (No. 53 of following section),
as belonging to the upper part of the Gault.

“Tn the tray marked No. 97 (str. 60) is a small fragment of an
Ammonite which I think to be A. cristatus, De Luc, a species only
known in the Gault; but the fragment is so small and so much worn,
that I name it with the greatest doubt; it is in a reddish clay.

“Tn tray No. 97, in company with the last-named Ammonite, and
also in the tray labelled ‘353,84 métr.’ (str. 40), are several fragments
of small Belemnites, which correspond in size with B. minimus of the
Gault ; but I can state almost with certainty that they do not belong
to that species ; their section is more square than in B. minimus, and
the sides have not the double line which marks that species. One
specimen differs from all the rest; it is the point, and appears to
have a furrow down each side as in B. bicanaliculatus, Blainville,
which M. d’Orbigny places in the Neocomian beds; it is, however,
possible that these apparent furrows may have been produced by the
friction of the borer, as the fragment is evidently rubbed. On the
whole, no safe conclusion can be drawn from the fragments of Belem-
nites. In the tray ‘353,84 métres,’ there are also some fragments
of Ammonites, of which nothing can even be guessed.

*T can form no opinion whatever about the specimens in the other

trays; some of them are organic, others appear to be only nodules.
“ “Yours sincerely,

. . = cé 33
“ Joseph Prestwich, jun., Esq.” DANIEL SHARPE.

Specimens of these clays and sands have been examined by
Mr. Rupert Jones and Mr. Roper for the smaller microscopic fossils,
and Iam indebted to these gentlemen for the following observations.

“Tachbrook Street, Nov. 21, 1859.

*‘ My DEAR Si1r,—The blue clay (Gault) of the boring at Kentish
Town has afforded to my friend Mr. W. K. Parker a plentiful supply
of Foraminifera, which I find to be characteristic of the Gault of
Kent, &c. ; the red clays and sands, however, of which I have washed
and examined four or five specimens, have yielded nothing organic,
as far as Mr. Parker or myself have been able to discover.

’ “Yours sincerely, — .
“T. RupERT JONES.”

“J. Prestwich, jun., Hsq., Sec. G.S. Se. §e.”

12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 2],

*“ Pembury Road, Clapton, 19th Nov. 1855.

“My pear S1r,—Agreeably to your request, I have made as
careful an examination of the three specimens from the Kentish Town
well that the limited time would allow, and my opinion is that no
traces of Diatomacea or other siliceous organized matter will be
found in any of them. The specimens, Nos. 56 and 102 (str. 33 & 63),
appear to contain a considerable quantity of lime, but I was unable
to detect any remains of Foraminifera or other shells of which it
might be expected to form a component part.

‘“< Yours very truly,
“F.S. S. Roper.”

“J. Prestwich, jun., Esq., Se. §c.”

If the position of the fossils could be accepted without a doubt,
we should feel obliged, however perplexing and exceptionable the
mineral characters might be*, to consider these beds as belonging
either to the Gault or to the upper part of the Lower Greensand,
and there would then still be a reasonable possibility of finding
beneath these red clays and sandstones in the one case the yet intact
mass of the Lower Greensand, or in the other case a considerable
thickness of sands forming a lower division of this group. Otherwise
in mineral character these beds closely resemble parts of the New
Red Sandstone. The boring tools also seemed to indicate that the
strata had a very considerable dip. It is possible, however, that this
may arise from the laminz of false stratification as well as from true
bedding. This is the more probable, as M. Jus states that for the
last few feet the strata seem to be horizontal.

The object of bringing this paper before the Society is to describe
briefly the principal features of this very interesting work, and to elicit
some further opinion upon the probable age of these singular red clays
and sandstones. -As the point involves the important question of
an additional source of water-supply, we must necessarily feel much
interest in the success of the operation. I have abstained from
treating of the difficulties of the undertaking, of the sure and skilful
mode of proceeding, and of the rate of progress, in order to confine
attention to the more essential considerations involving the probability
of its successful termination. Many of these considerations I have
but slightly touched upon, for the paper has unavoidably been drawn
up at a very short notice, but I trust 1 have omitted none of the
main facts.

A careful record has been kept of all the strata traversed in the boring.
These particulars I annex. As I have not introduced all the subdivisions
of the Chalk made in the original document, the numbers of the strata will
not agree with those there given. In the beds beneath the mass of the
Gault I have, however, given each mineral change as noted in the course
of the work.

* On recently examining one of the few small, well-rounded pebbles of Stra-
tum 40, it seemed to me closely to resemble some of the light-brown, waxy,
semitransparent chert of the Lower Greensand of Kent and Surrey. If so, it
would be a satisfactory proof that this red series was newer than some portions
of the Lower Greensand.—T[J. P., Jan. 1856.]

1855.]

PRESTWICH—BORING AT KENTISH TOWN. 13

Section of the Boring at Kentish Town.

(London. Clay [ 1. Yellow clay ....0i2....secscssecassee faeee

3 (236 ft.). 2. Blue clay, with Septaria...............
* 3. Mottled (red, yellow, and blue) clay
ie 4, White sand, with flint-pebbles ......
x 5. Black sands ; Passing iNtO ...ce.ceceee
~ | Woolwich and} 6. Mottled green and red clay ...... eee
ss Reading Series| 7. Clayey sands ........sescsscossscescnees
3 4 (61 ft. 6in.). | 8. Dark-grey sands with seams of clay
= 9. Quick-sands, ash-coloured ............
: (LOS, Biint-pebilesh <x. ceceeoceosstencevcoeurs
: 11. Ash-coloured sands.........cccssseceees
a 12. Arpillageous SanGS, J. 2jescccdesesascce
& | Thanet Sands | 13. Dark-grey clayey sands ...............

eer a.)....U 14

Bed of angular green-coated flints...

6 f 15. Chalk with flints........ teevoveosseceecs
16. Hard chalk without flints ....... wedes
17. Chalk, less hard, with few flints

18. Nodular chalk, with three beds of

Middle Chalk tabular flints ...... PE re Pere eee

with flints < 19. Chalk, with seams of tabular flint

(244 ft. 6 in.). and a few nodular flints .........

as 20. Chalk, with a few flints and some

2 Patches) Of SANG) cc cc.c23.-05.ds055e%

© 21. Very light-grey chalk, with a few

23 | L HUTS weewencneccsceses saucers Ralleicieaee
M

5 22. Light-grey chalk, with a few thin

= his ae [ Weir oe chalk-marl subordinate...

oa (tas 204 = mis \ 93, Grey chalk-marl, with compact and

( +): marly beds and occasional pyrites

248 Grey mists ss est destve SR Jacek

Chalk-marl 25. Harder grey marl, rather sandy and

(47 ft. 6 in.). _ with occasional iron-pyrites ......

L Aes bata TOLKY WaUhdse.. ssisedessseevasss

Uprrer 27. Bluish-grey marl, rather sandy; the

GREENSAND lower part more argillaceous......

(72 ft. 6 in.). 8. Dark-green sand, mixed with grey clay

29. Bluish-grey micaceous clay, slightly

ae cH Lag Saabecedseouae ; eee Pe cewaes

, . Ditto, with two seams of argillaceous

(130 ft. 6in.). PECENSANG) ), 4-50 newese tes d peatiesieee

aia, Micaceous DIUG-Elay. svsccclescodss csc

Depth.
fepine. (ft: in.

— 324 6
119
8
31

13

39 0

Grid
84 11—1113 6

[continued at p. 14.

14

PROCEEDINGS OF THE GEOLOGICAL society. [Nov. 21,

Section of the Boring at Kentish Town (continued).

(32.
33.
34,
35.
36.

mining it.

. Micaceous red clays, mottled in places
. Seams of white fissile sandstone and red sand
. Mottled sandstone
. Red sand and sandstone with small pebbles and Belem-

. Seams of red sandstone and white sands
. Pebbly red sands, and fissile sandstone....... Avieln ayfes)snen cis
. White and red sandstone
. Fine light-red sands
« Hard fissile sandstone... ....s00. Jcwes.ssae oan
. Very fine light-red sand
. Pure red clay
. Red and mottled clayey sands, with some iron-pyrites...
. Red sandy micaceous clay with fissile sandstone
. Compact hard greenish sandstone
» VeEy micacequs redclay 2. amc: Ace sany sre se ache acesee see
. Grey and red clayey sands
. Light-coloured soft sandstone with fragments of dm-

. Red sand and sandstone (highly inclined ?)
. Greenish sandstone
. White and grey clayey sands, with iron-pyrites ....... Ke
. Reddish argillaceous sands, with seams of sandstone ...
. Micaceous red clay
. Seam of greenish sandstone
. Red mottled and micaceous clay, with patches of light-

. Red quartzose and micaceous sandstone
. Brownish-red clayey sand and sandstone
. Very hard micaceous sandstone, with small pebbles of

have established elsewhere.

have noticed at the outcrops.
reading of them.—[J. P., January 1856. }

Red and yellow sands, and sandstone ,.+.......4 Saaldye os
Compact red clay, with patches of variegated sandstone.
Pure dark red clay «. .....cssss-cerwsns geese enero cack are
Red clay, whitish sands, and mottled sandstone ........
Hard red conglomerate, with pebbles of syenite, green-
stone, trap-rock, quartz, hornstone, red claystone-
porphyry, and fossiliferous schist, well rounded, and
varying in size from a marble to a cannon-ball

nites, and a few small phosphatic nodules ............

Power ees COS OO COS eer eeseeeseeterees
SOCOM Oe eer erees COSeereceeBOseovsssseecsese
oececoeseseeeasons
Sree eeP OO eeeeseO SS SSorereesces ss eosesee

POSS HSE HE SSH AEHHSEHES HH SHE SHOH eee eeessSenegeseOOaae

@ectetece

MOVERS SON Sas Fs dene ae ease ee Ac cade aioe

Pee e eres er EOP seeserasseseosssesseseeeteoess

POC ee HSOPEH ees eee eee SOEeeSOOOHSesepertHPHEe

COSHH HF OOSeaeeeesereseFOOTer Eee

coloured sand, and fragments of Ammonites and of a
Seaphthe © \racsuidentideceasnasuategsuerae atesk ue cdletae estab
Red compact micaceous clay, with Belemnites ............

eeeeesooeteFsoeses

Peters eserssoessee

white quartz

SOHO SH emcees OASESSeeeFFOESSeneesesesesseseseseeee

» Light red argillaceous sand .1.......ssseseceveeesseeseeeenes
. Red sandstone, micaceous and quartzose ........+....00+
- Light red clayey sands (with small angular fragments

of chert or flint ?)

SOHC CEHHH eee EHH eesasessecee HEPA eeeHPnassee

. Whitish and greenish hard sandstone (horizontal ?)

Depth.

ft. in. ft.imy
1

4

4

3

KHOouwoonwooooso rm OO ©

arRnDOOOCN

oo ooo oooem

6
—1302 0

Note.—The upper strata are grouped in conformity with the divisions I
The grouping of the Chalk, Greensand, and
Gault is rather arbitrary, for the change is so gradual that it is impossible
in a mere boring to say where one ends and the other begins.
duced those divisions which seem to me most in conformity with those I
They are slightly altered from my first

I have intro-

* This specimen was mislaid before Mr. Sharpe had an opportunity of exa-

1855.| MURCHISON—LESMAHAGO SILURIANS. 15

2. On the Discovery, by Mr. Rosert Siimon, of Fosstts zn
the Uppermost Siturtan Rocks near LesMAHAGO im Scot-
LAND, with OBsERVATIONS on the relations of the PaL#ozoIc
Strata in that part of LanarxwsHire. By Sir Roperick
Imepry Murcuison, D.C.L., F.R.S., V.P.G.S., and Director-
General of the Geological Survey.

CONTENTS.
Introduction.
General Relations of the Rocks of the Lesmahago District.
Upper Silurian Rocks.
Old Red Sandstone.
Lower Carboniferous Rocks.
Igneous Rocks of the District of Lesmahago.
Conclusion.
Appendix (Sections of Coal-measures).

Introduction.—At the last meeting of the British Association, Mr.

Robert Slimon brought to Glasgow two remarkable collections of
fossils from the extensive parish of Lesmahago, in which he practises
as a surgeon. One of these collections was derived from the bands
of carboniferous limestone, which there alternate with coal, and are
characterized by a great abundance of fine specimens of Producti,
Encrinites, Corals, and other remains peculiar to deposits of that age.
The other consisted of specimens of Crustaceans in dark-coloured
schist or flag, and to two or three specimens of which my attention,
as President of the Geological Section, was fortunately called by
Mr. Page. The magnificent collection of Mr. R. Shimon had, in fact,
remained almost unobserved, in a hall which few geologists visited.
- The moment I cast my eye over these remarkable Crustaceans,
which much resembled Pterygoti, and saw the matrix in which they
were imbedded, it occurred to me that they probably pertained to
the Uppermost Silurian zone. It became, therefore, necessary to
visit the locality in question, chiefly for the purpose of ascertaining
the physical relations of the dark schist with large Crustaceans to
the Old Red Sandstone. For, as I was aware that the genus Ptery-
gotus had been found as low in the Silurian rocks as the Upper
Caradoc band, it might prove that there was the same great hiatus
near Lesmahago as had up to this time been supposed to prevail all
over Scotland, and that no representative of the Uppermost Silurian
existed. On the other hand, the band in question might prove to be
that which I shall endeavour to show it is—viz. the true represent-
ative of the highest Silurian zone, as developed in Herefordshire,
Shropshire, and Westmoreland in England, in Russia on the Conti-
nent of Europe, and also in North America.

Having requested Professor Ramsay to accompany me, we visited
Lesmahago together, and there found to our gratification, that the
worthy and modest Mr. Slimon had not only a much richer collec-
tion of the fossils in question than he brought to Glasgow, but had
also an accurate acquaintance with many of the prominent and de-
tailed features of the tract. Guided by him to the best natural sec-
tions, and particularly to the spot on * Logan Water,” hitherto

i |

16 PROCEEDINGS OF THE GEOLOGICAL SoOciETy. [Noy. 21,

famous only in Scottish song, where he had found the Crustacean
fossils, we afterwards endeavoured to obtain a general notion of the
relations of all the rock-masses of the district. For the better under-
standing of the subject I induced Mr. Slimon to prepare a rough
geological map, which is exhibited, and to the sides of which he has
annexed two sections explaining the order of the carboniferous strata
of two tracts in his neighbourhood (see Appendix, p. 25). I also
submit a rude approximation to what will in the sequel be better
worked out, by exhibiting the County Map of Lanark, on which
I have endeavoured to combine the outlines of Mr. Slimon’s Map as
correcting those of other observers; no one having previously in-
dicated any more ancient rock in this tract than the Old Red Sand-
stone; the tract which I now consider to be Silurian having usually
been coloured as Carboniferous*.

I must at once apologize for the imperfections necessarily attached
to this slight sketch of a district of which no real map exists. As
soon, however, as the Engineer Corps under the able direction of
Colonel James shall have published the first outlines of the Ordnance
Survey, I can assure my associates that the Geological Surveyors will
vigorously set to work to determine all those relations which are now
briefly touched upon in an essay, which is simply intended as a tem-
porary frame to hold together a few materials which are of deep
interest in paleeozoic geology.

General Relations of the Rocks of the Lesmahago District.—In a
former communication, I invited attention to the general direction of
the great masses of the Silurian rocks of the 8. of Scotland, which
have been described by various authors under that name since the
discovery in them of many well-known Silurian fossils+. I then sug-
gested, that judging from some of those organic remains, as found in
the environs of Girvan, there were indications, in that parallel, of an
ascending order from the Lower Silurian rocks (which unquestion-
ably form the great mass of the S. Scottish greywacke) to the Upper
Silurians. At the same time it was noticed, that the strike of the
Girvan strata would carry them nearly to the Silurian rocks of the
Pentland Hills 8. of Edinburgh, which have the same general direc-
tion, 7. e. nearly from N.E. to S.W. Now, if a line be drawn from
the rocks N. of Girvan to the northern face of the Pentland Hills, it
is seen to pass over an intervening tract, throughout which basins of
carboniferous rocks, surrounded by girdles of old red sandstone and
diversified by a great abundance of igneous rocks (porphyry, green-
stone, &c.), are represented in all the published geological maps.
The discovery made by Mr. Slimon of fossils which prove to be of
Upper Silurian age, over a considerable area in the extensive parish of
Lesmahago (for this Scottish parish has a length of twenty-five miles),
has advanced therefore the northern frontier of the Silurian or slaty
rocks ; some of the localities in question being not less than twenty
miles to the north-west of their previously defined boundary. ‘The
extent to which the Lesmahago Silurians may be hereafter shown to

* See the maps of M‘Culloch, Phillips, Knipe, &c.
t+ Quart. Journ. Geol. Soc. vol. vii. p. 137.

1855. | MU RCHISON—LESMAHAGO SILURIANS.

be connected upon the surface with

those of the tracts around the Lead :

Hills and other parts of Ayrshire
and Dumfriesshire, on the S. and
S.E., must be a work of future la-
bour. That work will demonstrate
whether these Lesmahago rocks
constitute an advanced Silurian
promontory or headland, or whe-
ther, as is most probable, they form
an outlier of that age.

The large parish of Lesmahago
is pre-eminently distinguished in its
western part by dome-shaped hills,
which rise to the S. W. of the River
Clyde, and on the left bank of that
river, where it forms the well-known
beautiful Falls of Bonnington and
Stonebyres, near the town of La-
nark. The rock over which the
Clyde cascades is the Old Red
Sandstone, which formation, ex-

tending to the W. and 8.W. to the °

village and parish of Lesmahago, is
overlaid on the north and south by
carboniferous limestones and coal ;
whilst on the south-west it is un-
derlaid by the dark and schistose
rocks to which attention is now
specially invited. |
Upper Silurian Rocks.—The re-
lations of these dark grey, schistose
strata of clay-slate to the Old Red
Sandstone are seen on the banks of
the Nethan River and also on those
of other tributaries of the Clyde,
particularly the Logan Water, on
each of which rivers Mr. Shimon
has marked the junction between
the grey Silurian and the Old Red
rocks. The Silurian beds rise up
into several hills of considerable

altitude, one of which (Nutberry,

1715 feet above the sea) we as-
cended. Judging from the outline
of the country, and the exten-
sive range of similar high moor-
lands, I am disposed to think that

these rocks may be found to spread .-

north and westward over the hills
VOL. XIIL—PART I.

Distance about 7 miles.

Diagram exhibiting the General Relations of the Paleozoic Rocks in the Parish of Lesmahago.

Q

n
n vo
os
=
SS
2
a)
oo 2
SF
oy 2
Ice
aS 5
= O &
iS eayi<>|
BmWN
e
a
ad
rS)
°
HH
v2) a
= axe)
2 2
eas
f=} oO a
S) re i=
Q @ =
a oe
(Ss) = wm
5 & 3
ae a
=) =)
“Sek CC CaC Raby
eS -« og XL he
Oia Se [a4 See sya
Sa eT soot civa5
Seen is acah 2
CIC tac eae
Zn elspa Seman
BeOS
LEO RRS Ra = iar
. ° - - &
Di. e& * om -
SES ere see)
2 fol eee ae
ee fealty cect
et ieee oR
o 5 o 2=
[=e Se an 5
O..e 2 "oS
~~ God OaCh (o)
naa >So: Ss
oS Bu
stunEsga
esatoogs
astago+ere
oo Ss o
4 oo St aes
O+~QGmuits
=) 3S
SEER Sa
Sr aeos ss
NAANROADS
> § os oro
Oe) i ees
= 8
%
©
Cc

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

of Dunside and Middlefield, 1300 to 1500 feet high, and may even
range to Cairn Table on the south, the summit of which according to
the Trigonometrical Surveyors is 1944 feet above the sea. Advancing
eastwards from the range of hills on the flank of Nutberry, in one
part of which Mr. Shimon discovered an Orthoceratite, and descending
the Logan Water to about a mile below the farmhouse of Dunside
you reach the uppermost band of the grey strata in which were disco-
vered those remarkable Crustaceans, which have been above referred to.

The lowest portions of the Silurian rocks which fell under the
inspection of Prof. Ramsay and myself are those which are traversed
by the Nethan River as it flows from the Priest Hill and Nutberry Hill
to Cumberhead. Several dislocations and convolutions which are
seen on that line among the Silurian strata, as well as in the contiguous
Old Red, are well explained by the frequent protrusion of porphyry
(usually a red quartziferous porphyry). On the whole, however,
it was manifest to both Prof. Ramsay and myself, that in receding
from the Old Red boundary, and in ascending to the higher hills by
the course of the Nethan, we made a gathering, descending section—
because the strata succeeding to each other with a prevalent dip to the
N.E. or E.N.E. consisted successively of differently constituted mate-
rials. Thus, whilst the uppermost strata were dark grey and schistose,
other layers of lighter colours were more siliceous and formed stone-
bands. These are followed by other courses of shale and schists in
which are nodular concretions, occasionally calcareous, in which we
looked in vain to find a few fossils which could have led us to suppose
what they might very well prove to be from mineral aspect, the repre-
sentatives of the Wenlock formation. It is from one of these strata
that Mr. Slimon procured the-«Orthoceratite above alluded to, but
which is too imperfect to be specifically determmed. With some
undulations and several breaks, particularly in the proximity of the
intrusive porphyry, all these Silurian strata are inclined towards the
E.N.E. and N.E., and at angles varying from 12° and 15° to verticality
where they roll over in flexures.

The inferior beds exposed in the section of the Nethan are here
and there mineralized, and specially so where trap-rocks, chiefly
green-stone, have penetrated the strata; veins of lead-ore and much
sulphate of barytes being there apparent on the surface.

The section, however, which best exhibits the relations of the
Silurian rocks to the Old Red Sandstone is seen on the banks of
Logan Water between the farms of Dunside and Ach Robert. The
last of the decidedly dark grey and schistose beds observable in
descending from the flanks of the Silurian hills (Nutberry, &c.) are
those in which all the fossils described by Mr. Salter (see p. 26) were
found by Mr. Slimon. These dark fossiliferous rocks, the clay-slate of
mineralogists, are immediately overlaid by and pass up into red sand-
stone, in which there are several alternations of more or less greyish or
greenish-grey bands ; the whole, like the beds in the Nethan, dipping
to the E.N.E. or N.E., as represented in the generalized Section, p.17.

Old Red Sandstone.—In the traverse along the Logan Water I
did not observe any unconformity between the grey beds with Crus-
taceans and other fossils and the overlying red sandstones, the lowest

1855. | MURCHISON—LESMAHAGO SILURIANS. 19

courses of which are marked upon Mr. Slimon’s map as “‘ Red Silu-
rians.” For my own part, however, I would rather consider these
red strata as constituting the base of the Old Red Sandstone, because
they graduate up into and alternate with pebbly conglomerates which
are largely developed near Ach Robert and Waterside.

Some of the porpkyries which are associated with the red rocks in
this part of the series seemed to be interstratified and of age contem-
poraneous with the sandstones with which they dip symmetrically,
and like which they are jointed and exhibit the way-boards of sedi-
mentary deposits. In mineral characters and in their interstratifica-
tion with red sediments, these rocks, though of much older date,
present much the aspect of some of the porphyries of the Rothe-todte-
liegende of the Permian age in Germany.

The conglomerates of the Old Red of this tract differ strikingly
from those of the same age in the North Highlands, where the so-
called lower conglomerate is usually a very coarse breccia, the huge
fragments of which are more or less angular; whilst here they are
all worn and rounded pebbles, the largest of which scarcely ever
reaches a foot in its greatest diameter.

Most of the pebbles consist of grey and pink quartz-rock, but these
are mixed with other varieties of crystalline and some igneous rocks.
This conglomerate zone, which is fairly interstratified in red sand-
stone and ranges from N. to S., as laid down on Mr. Slimon’s
map, is much nearer to the dark grey Silurian on the Nethan river
than it is to the same rock on the Logan Water; whilst on the
Kype Water the two rocks are still further removed from each other.
Time and detailed examination will determine whether this deviation
of outline be due to breaks and unconformable arrangements, or simply
to changes in the degree of inclination of the strata. By comparing
the only watercourses which we examined, I am led to think that the
difference of the angle of dip may sufficiently explain these diversities
of superficial area ; because on the Logan Water we found the in-
clination varying from 7° to 12° only on an average ; the red beds with
imbedded porphyries and conglomerates as well as the inferior grey
beds sloping off to the N.E. or E.N.E. at these low angles except
where they rolled over bosses of porphyry. On the Nethan banks,
on the contrary, the beds are more highly inclined.

In ascending order the Old Red Sandstone, including all that portion
of it which lies above the conglomerate and extends by Lesmahago
to the Clyde and Lanark, is usually of a lighter colour and freer
quality than the subjacent beds, and occupies a very varied outline in
reference to the carboniferous limestone and coal-fields on either side
of it and under which it is seen to dip. On the banks of the Nethan
Water where we examined them, the junctions are much broken,
and on the whole it would appear, that the older rocks have been so
convoluted as to form the southern edge of the great central Scottish
Coal-field, or the complete girdle of the Douglas coal-basin ; the 8. W.
side of which is flanked by the Old Red of the Hawkshaw Hills, and
also, according to Mr. Slimon, by the Silurian rock of Bremerside Hill.

Lower Carboniferous Rocks.—The lower edges of the Carboni-
ferous rocks being attained, the ascending series from them through

C2

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

various bands of limestone and interstratified courses of coal and
iron-ore is admirably exposed in the beds of some of the watercourses
which flow from the loftier hills of older rocks*.

Upon the only instructive traverse which we made, and to which
we were conducted by Mr. Slimon, viz. up the Coal Burn and along
the steep banks of the Poniel Water, which flow through grounds
now occupied by the productive coal and iron works of Brockley, &c.,
we were highly gratified in seeing a splendid development of lime-
stones, shales, sandstones, coal, and ironstone, a precise account of
which and an accurate register of the fossils in each zone are much
to be desired. We examined the so-called “black band” of iron-
stone at Coal Burn (see Appendix, p. 25), and found it to be asso-
ciated with an indurated bituminous shale, which in Staffordshire
would be called “black bat.” The strata being very slightly in-
clined, the ironstone (8 inches thick) is worked by a gallery on the
side of the slope. In this locality the black band dips under a suc-
cession of strata of shale and sandstone, to which five seams of coal are
subordinate as well as one band of limestone. On the other hand, the
black band is here underlaid, as seen indeed in the open sections of
the watercourses before alluded to, by a much thicker succession of
similar shales and sandstones, including seven seams of coal and three
limestones. The lowest of the latter is a hard, concretionary, nodular,
white limestone, which immediately lies upon the Old Red Sand-
stone ; but no fossils have yet been found in it. The massive and
thick-bedded limestone, however, which overlies it, with the interven-
tion of some sandstone only, is laden with the large and small Pro-
ducti, a profusion of Encrinites, and many characteristic shells, some
of which are also found in the limestone near the top of the series.

As Mr. Slimon has obliged me by preparmg a working section of
the beds passed through in this tract of Coal Burn and Brockley, and
another of the Auchenheath Pits, situated on the opposite or northern
basin, and not far from the junction of the Nethan with the Clyde
(see Appendix, p.25), the geologist who compares them will see how,
with a strong general petrographical resemblance, the order of the
carboniferous strata on the other side of the dividing Old Red of
Lesmahago is distinguished from that upon the south flank of the
same formation; particularly in the much fuller development of
strata above the ‘‘ black band”’ of ironstone.. At Auchenheath the
shafts pass through a much more copious series of sandstones, shale,
and limestone before that iron-ore is reached; there being no fewer
than five calcareous zones above it. For, whilst in a much less ver-
tical space in the Coal Burn tract there are five seams of coal above
the black band, the very deep sections of Auchenheath there present
three seams of coal only superior to that ironstone. If it be objected
that the black band is merely a casual and accidental layer of rich iron
ore, and that when these fields shall have been elaborately worked out,
similar ore may be found to exist in more courses than one, and at
varigus levels—a feature which is by no means improbable,—still in
reference to the very limited area now under consideration, where the

* A notice of the Lesmahago and Douglas Coal-field was read by Mr. Bryce at the
British Association Meeting at Edinburgh ; see Brit. Assoc. Rep. 1850, Sect. p. 77.

1855. | MURCHISON—LESMAHAGO SILURIANS. 21

two localities compared are a few miles only distant from each other,
the geologist must see, by the facts laid before him, how very rapidly
mineral matter of one sort thins out and is represented at a short
distance only by a very different stratum.

When the trigonometrical surveys of these important mining tracts
shall have been published, the geological surveyors will determine the
extent to which the coal-fields of Scotland can be distinguished as
consisting of lower and upper masses, a subject already treated of by
Mr. Page*, and will explain with precision whether to the south of
Edinburgh there are or are not strata of younger age than those now
alluded to. In the mean time it is clear, that all the coal-tracts around
Lesmahago belong to the older or Mountain Limestone series. They
are, in short, of the same age as the coal-fields of North Northumber-
land, Berwickshire, and other tracts in Scotland; and in foreign coun-
tries, as those of the Donetz in Southern Russia, and of Kosloo in Asia
Minor, both of which are subordinate to bands of Productus-limestone.

Igneous Rocks of the District of Lesmahago.—Allusion has already
been made to certain porphyries, some of which alternate with bands
of the Old Red Sandstone and conglomerate, and others of which seem
to have been erupted through the Upper Silurian rocks and the Old Red
also. According to the map of Mr. Slimon, these porphyries, of which
there are two varieties, felspathic and quartziferous, are both chiefly as-
sociated with the Old Red Sandstone, and never occur in the coal-fields.

One of the largest bands of porphyry traverses the River Clyde
below the Fall of Stonebyres, and, trending to the S.W.andS. through
the Old Red Sandstone, sends off several branches, three or four of
which curve round and cross the Nethan River.

Another branch runs to Dunduf, from whence it ranges to Todlaw.
This last-mentioned dome was probably a great centre of eruption,
from whence a long course extends from Ach Robert to the flank of
Bremerside Hill.

In short, these porphyries seem to have been the active agents,
which, at one period alternating with the red sediments, afterwards
burst through the Old Red Sandstone and raised it into those dome-
shaped masses which separate the great coal-fields of the Clyde from
the detached coal-basin of Douglas. Tinto Hill and its south-western
ramifications constitute another and much more extensive outburst
of similar porphyry, which forms the south-western portion of that
long range of igneous rocks which extends on the E.N.E. to the
Pentland Hills.

But independently of these porphyries, the parish of Lesmahago is
distinguished by a remarkable dyke of greenstone, which Mr. Slimon
has traced from the coal-field of Douglas, across the Old Red Sand-
stone of the Hawkshaw Hills, and then through the porphyry zone
of Todlaw and the Old Red Conglomerate, and which he has further
followed for several miles across the heath-covered Silurian hills
in nearly a rectilinear course. Where Prof. Ramsay and myself
examined this dyke, 7. e. high up the Nethan Water, we found it to
be a fine-grained greenstone of about 25 paces in width ; having the
direction of 33° S. of E. The Silurian schists on either side of it

* See Report British Assoc. Advancement of Science, 1854, Sect. p. 92.

22 PROCEEDINGS OF THE GEOLOGICAL sociETy. [Nov. 21,

preserved their prevalent slight inclination to the N.E. and seemed
to be but slightly altered. The prisms of the greenstone being as
usual at right angles to the cooling masses on either side, really resem-
bled beds (slightly disturbed only) in the general mass of the schist
or shale—so much do the two classes of dark rock resemble each
other, until the hammer is applied to them—and even then the trap-
rock is seen to have assumed to a considerable extent the scaly or
fissile character of the Silurian deposit which it bisects.

On following this dyke from the Nethan to the very summit of
Nutberry Hill which it occupies, we observed that its width (varying
somewhat in different spots) was marked by the grassy verdant
tint of the vegetation above it, as contrasted with the brown colour
of the heath on either side of it upon the schist.

In descending the Logan Water, and at a short distance from the
junction of the Upper Silurian and Old Red, a boss of intrusive por-
phyry appears, and again red sandstones follow with another and
stronger course of porphyry which has a hornblendic character. A
conglomerate then appears, succeeded by other red fissile sandy schists,
and next red rocks alternating with light greenish or bluish-grey and
slightly micaceous sandstones, which are, in fact, intercalated im red
rocks ; other thin courses of porphyry are then observable, and then a
pebbly conglomerate, between which and the ordinary Old Red Sand-
stone of the parish of Lesmahago there is a considerable development
of porphyry, which seemed tv be regularly bedded and to dip away
m conformity with the sandstones.

Whilst some of this porphyry has all the aspect of having been
emitted contemporaneously with the sandstone and aggregated under
the same waters in which that formation was deposited, other bosses,
one of which is hornblendic, have manifestly been intruded into
the strata after their formation ; for both the conglomerates and
the sandstones are seen to be arched over such intruding rock and
occasionally dislocated by its protrusion.

Conclusion.—The preceding sketch of the general relations of the
palzeozoic and igneous rocks of the parish of Lesmahago indicates
the value of the researches of Mr. Slimon, more particularly in his
discovery of the uppermost Silurian fossils. Having incited that
gentleman to send to the Museum of Practical Geology a complete
suite of his carboniferous fossils, all observations on the deposits of
that age are reserved for a future occasion.

In regard to the Old Red Sandstone it has been shown, that its in-
ferior member in this district is dovetailed into the grey Silurian schists
and flagstones beneath it. Hence I conclude, that the greater part
of the red rocks exposed on the slopes of the higher greywacke hills of
the parish of Lesmahago belong truly to the lower division only of
the system of deposits which in the North Highlands (Sutherland,
Caithness, and Ross) constitute the Old Red Sandstone, as there
composed of inferior sandstone and conglomerate, central flagstones
and bituminous schists, and overlying red sandstones. If my readers
will refer to the abstract of a communication which I made to the
Geological Section at the last meeting of the British Association,
copies of which I have addressed to this Society, they will see how

_—

1855. ] MU RCHISON—LESMAHAGO SILURIANS. 23

different in grandeur and diversity of structure is the great North
Highland Series, when compared with the Old Red Sandstone of
Lanarkshire. This last constitutes, as I am disposed to believe, little
more than one of the three great divisions of that vast northern series
which is, I conceive, a full equivalent in time of all the rocks called
Devonian in any region of Kurope.

In Lanarkshire neither the micaceous red flagstones associated with
the conglomerates, nor the beds beneath or above them, have as yet
afforded any trace of fishes, even under the vigilant eye of Mr.
Slimon. If such should be discovered in the uppermost of these red
strata of Lesmahago, and that they be found to belong to Holoptychius,
then indeed we may infer that we have here a representative, though
on a very small scale only, of the upper member of the group.
But, not speculating further on this collateral pot, I beg to conclude
with a very few observations upon the Crustacean beds of the newly
discovered Upper Silurian rocks of Scotland.

Rising out as these dark grey beds do, upon the Logan Water banks,
from beneath the Lower Old Red, they occupy precisely the same
horizon as that uppermost zone of the Silurians of Shropshire and
Herefordshire which includes the bone-bed and the Downton Castle
building-stone, and to which, as it graduates up into the Old Red, the
name of “'Tilestones”’ has from its flaglike character been given.

Near Ludlow, Hereford, and several other places, the thin course
with small fish-bones has been traced over an extensive area, and
in several places where the fishes are wanting the band is still well
characterized by the associated large Crustaceans, chiefly Pterygotus.
Recently Mr. Banks has discovered in those strata near Kington
which J formerly referred to this age, some very beautiful forms of
this genus, of which he sent me the drawings and descriptions, and
which have been submitted to the Society. Together with the Pte-
rygotz Mr. Banks found fossils formerly confounded with the genus
Cephalaspis, Ag., but now separated. The species are new, but much
like C. Lloydi, Ag., hitherto known only in the overlymg Old Red.

Large Crustaceans of the group of Hurypteride* (Burmeister), to
which the Pterygotus belongs, have also been found in the Tilestones
of Westmoreland, and it is curious to observe that in most of these
localities they are accompanied by the small Lingula cornea (Sil.
Syst.) of the Ludlow district.

In Podolia similar large Crustaceans analogous to Pterygoti were
found in strata rising out from beneath rocks which are known to be
of Devonian age, and to these Dr. Fischer gave the name of Lury-
pterus tetragonophthalmus. Recently M. Kichwald+ has detected
several of these large Crustaceans, one of which he figures as Eury-
pterus remipes, Dekay, in the Isle of Oesel in the Baltic,—7. e. in
a limestone which my colleagues and myself referred to the highest
Silurian stage; so that in the North as in the South of Russia, the
zone under consideration, when clearly exposed, is everywhere cha-
racterized by large and peculiar Crustaceans of this group, no one of
which has ever been found low in the Silurian rocks.

* See Paleoz. Fossils Cambridge Museum, Fasc. 1.
tT Bull. Soc. Imp. Nat. Moscou, 1854, vol. xxvii. p. 100.

24 PROCEEDINGS OF THE GEOLOGICAL society. ([Nov. 21.

In North America it has been long known, from the writings of
Dekay and Harlan, that large Zuryptert occur in a so-called black
greywacke slate at Westmoreland in Oneida County, New York,
which will probably be found to be on the parallel of the Upper
Ludlow Rock. The discovery of the large Eurypteride in the same
zone as at Lesmahago in other regions is therefore peculiarly satis-
factory. It is however to be observed, that in tracts far removed
from each other, different, though closely allied, species make their
appearance. Thus, whilst the Pterygotus is perhaps the usual and
most characteristic type, the species found in Scotland* is said to be
different from that known in the Silurian region. Near Kendal in
Westmoreland the genus Hurypterus occurs with Pterygotus ; whilst
in Russia the former seems to be the prevalent genus.

In the Lanarkshire case, Mr. Salter finds the same sculptured
plates which have been usually referred to the Pterygotus, and also
the small Lingula cornea and Trochus helicites of the Uppermost
Ludlow Rock. With these he has also detected in the rich collection
of Mr. Slimon five or six new forms of a large crustacean which he
terms Himantopterus, and describes in the following memoir, p. 26.
With them too, another genus, the Leptocheles of M‘Coy f, has been
found, which the fine specimens now collected show to be simply the
caudal portion of the Ceratiocaris, a genus which is found as low
as the Wenlock Limestone. And yet, with these distinctions of vary-
ing forms, which are everywhere recognizable in the Silurian zones of
similar age in distinct regions, we find this group of animals con-
sistently and uniformly defining the same zone of sediment over the
Northern hemisphere.

Wherever these large Crustaceans are found, and with them small
Inngule and other fossils, we may be sure that we are at or near the
very summit of all rocks to which the term Silurian can be applied,
and that the next overlying stratum belongs to the first great era of
fishes, the Devonian or Old Red Sandstone ; for the thin transition-
band now under consideration still remains what I stated it to be
twenty-one years ago, the lowest in which the trace of a true verte-
brated animal has been detected.

In Seotland, where we had despaired of finding any representative
of the Ludlow formation, the discovery of Mr. Slimon is indeed highly
gratifymg. Perforated as are the lower edges of the coal-basins which
occur along the northern frontier of the Silurian rocks of the South of
Scotland, by various igneous rocks which have to a great extent up-
heaved the Old Red Sandstone, we may, after this discovery, look to
the detection of other links to connect the Orthoceratite-rocks of the
Pentland Hills with the shelly deposits of Girvan and the younger
strata of Lesmahago, and thus evolve a full series of both Lower and
Upper Silurian Rocks in North Britain, where their very existence
was until recently almost ignored.

* I have directed that these remarkable Crustaceans, as well as others of the
same age in Herefordshire, be figured and fully described in a Decade of the Me-
moirs of the Geological Survey of Britain.—R. I. M., January 1856.

+ See Pal. Foss. Cambr. Mus. PI.I E.fig.7; Quart. Journ. Geol. Soc. vol. ix. p.13;
and also a full recognition of Prof. M‘Coy’s ability in separating some of these
crustaceans from fishes with which they had been confounded, in “ Siluria,” p. 236.

APPENDIX.
Sections of the Coal-measures near Lesmahago, by Mr. R. Suimon.

Section at Coal Burn.

Superficial soil, sand, and gravel. ft.
Blaise and limestone............ 10
‘TCT SG Os SO ee oe i eek
MC PREONEE os sae sccm cides acicese 15
Blaise and blue freestone ...... 4
RT RISE scenic ean ci'dicceneceise 3
Gasiand dross coal .:.:........ 1

Waikey blaise ......0..0.9++...000 4
Freestone and blaise........... 2

IDrOSS| COal: cas cesicenceene Pa eectes 2 3
ERIC DV race ese ct- cos <cscessmcees 0
Dross coal, with 6 ae 3

UGE CORI ic ctecsseccccse ce

REL CLAW Ia o2 ce asicdictwsacseeheds 2
PECSEONG coccesiiconccsseisbcccecwc 7
Blue faikes...... Seeeetncawie si Bese ee
UNI fone doce Guwceees cccccees sce 3
PAE AN erst iccceseacwansscesectae 3
COANE sacedccsaesenonecndesceces 2
BREGSTONG bh ccas ck <cevcecasvidscees ns 6
WANKE@S anes cececascedes ss xcse See cek es

PR ERISC ce tase sao oa nisisio'edet Sie sac 4
Black band, ironstone ......... 0
HRI DESC Mada a ceil vacoen Masten Sh acess 3

Clay, DANG TON, ..ccccencaseees 0

LESTE ee ae ee ee 3

EIMILINVA COAL (0 c= v<ohessenecn sce 0

SE CROLAY: Sirnicciee nancies asians cies s' 1

Od Atte ccesec.cess nedseesedceie des 4
AStard’ StONe .cloesceccavcsses 0
ACO al bh ccloswietsaiaewnnvls cee Weeeaneecns 4
Mire clay... Ate oP ROADEG MEE See 16
Barkes and DIaise: oc. .0ccccscoss 8
Olay DAG WOW ......ccccccesees 0
BAAISO sas cee sonced ove devaakeasess 6
lan MANU deseo siicwsscceasict oct 0
ISIS GR Aee cad acoecacadastae cosas ets 2
Oley ADAG vomniceciaenssicdaaecoe ass 2
Ba laiSS arses passe csoaes ccuscouacces 12
BARENClAy tweer rene cane LEASAnS 3
WGA es A bi seaeek seta F1

PRUAIS gate Nether ois teres totic nskices 3
CODE yh NAc Ser ee ae 1

EWEATSO Roar c seicclo ce van vieicis)aicee au sien 12
Freestone and blaise SOSROB CE AAE Lig

Fire clay and blaise ............ 3
Coal, with 6 inches of stone... 6
Babes and Gills aJ0255.c.cceksess 42
Blaise and ironstone band ... 12
Woaly SHUI co. 5. .s0.0<0caeae a
LTEN GG Oy oe aS e ae an A 1

LPTKYE) oe eo ge eC 5
IEGECSEONE™ Joe Jk desetcnidassehecues 16
Blaise and ironstone............ 12
TINESTONE 2k duenactvesauaesvaecdee ]

Grey Das "...cts-veascsccesouse 20
MYOHStONGE ° 5.0. cesecsatsoceeeane 0
Blaise and limestone............ 46
Sandstone.

Nodular limestone.

- Upper Old Red.

Old Red Sandstone.
Red Silurian (Slimon).
Silurian, upper black.

in.

KH rnoo°woranococeo

—_ fp
=

SONNTOOOONOOOOOHOQCSOCS

tole

Smomoooanocoooooooooa oon kh Ow

Section at Auchenheath.

25

Superficial soil, sand, and gravel. ft. in.

RFECSCONE Ua cudpecesaccectssscacecce
Sand shales with ater SRarChee
Faikey blaise and freestone...... 40
MIME STONE F 28. da .8-. acu cdeessceeee I
5 US) aS aR ae oe ee 10
Arden limestone ..... euaniaesisens 5
Mirevelayan satis .ctcces veveses 1
Hard sandstone: «.:c000ccccceceoes 2
Freestone a3 05ee cies isc cul Berke 30
f LU aR RS Age Cat re eae a 4
himestorie? 2582.62 adee docs ctcs see 1
Blaise) Jack hac eiiaree aceseetentoss 8
Iamestone: 28584 o0e ace sae 3
Hire: Clayy sgcyoss~ daacheneeeeecleestes 4
ETeestOne 22022 0)4.20 tae eeoeee. 8
1 ATTY he a aie 8 Cea 4
BEGeStOne jietecncuthees easetiee tas 60:
laSeN 3 hicseccs Cot a arewa in aed Aa 10
Limestone: | c.6i2. igaiewon), Beak 5
BTEC Clay? see Sch ah oteke sonnets 5
REGSLONG ct. u5. dese cc eens Aateee pelt
IAISOM Machete occ ectcetuce sc eek 5
MECESEONE oy Mo. thecs toe tos menace 43
AIS Oi seb eoss sae se cneocot ee 6
WWI IMSEONEe Je scueoctomacdcacosece 5
BTAISG a setae oaalcleccenetien csededd 9
MCENUON Crenereeneee dvds k's Moc otece 4
151 AS). CO Pe ACM a an pee 0
SUM. COall cs. -tevecseseestont eee. ]
Baukes/elay | esac: .cessndedesense 1
CLOVE eae alee: Aner ee aR Pe 4
HANGS eaerryat sons pam sseoaue cats 5
EGESTOMC reso se sete eesecctcscds 4
[ENTER tes A i a ee 4
AIK E Saas ee, oe LR eho ee 2
Gas. Coals (eager, es ccaswetoad 0
Black band, ironstone ...........- 0
Tills, ironstone balls .......0..-. 3
(OE LAS REE ay | Ue Ai ashe eed 0
Rime clavate te tet ut tadcescite 1
Dross: Coal a, 3:ss3.c eeehs PBs ex 3
RRECSTONG Mh eee Racca a
| BILCATICYSS 05 SRR Salt RE a ae 8
HreeStoneretc tet e cock fe eceaec 9
BSIAISC)Mase aA e a ieec eee ee 20
BFEESLOMG contre, hee. 4
LEE TSS . ELE cae le an ae 4
BreestOme passe socscse kena ocisssdue 2
Caterer Fes Ost cavinscwcwe 0
SUILIS) eds Cee Coe meee aaa 5
EASICORIBE EET Sco cutceseeeees 1
LCDS 7 15 See ae eee ee 0
IRERCNAN ec. eat ten senstnclsa side « 1
(COL 5 ie a ee ee 0
Freestone.

Limestone.

[The coal is 35 fathoms above
this. |

— ~
OwmWPROSOSCSGDCOCCCOCSOAOMMmMUGqgeooooceocROoOonaweeonocowmooocoomoocoowoosco

—_

26 PROCEEDINGS OF THE GEOLOGICAL society. [Nov. 2],

3. On some new Crustacea from the Uppermost SILURIAN
Rocks. By. J. W. Satter, Esq., F.G.S8. With a Note on the 4
Structure and Arrinities of Himantortervs. By T. H. 4
Huxtey, Esq., F.R.S.

Tue occurrence of large Crustacea other than Trilobites in the older
Paleeozoic rocks is so rare, that we are scarcely prepared for the
simultaneous discovery of five or six new forms, of dimensions
equalling those of the crabs and lobsters of the present day.

Except the large Pterygotus of the Tilestone beds, and the Cera-
tiocaris from Westmoreland, scarcely any remains of these have yet
been made out in Britain. But there have been sundry indications
in the occurrence of large tail-spines and fragmentary carapaces, all of
which have been most carefully treasured up to wait for further evi-
dence, such as that now afforded by the discoveries of Mr. Slimon*.

His admirable collection not only fully explaims the meaning of

much that was fragmentary before, as in the case of the Ceratiocaris,

but gives us new forms of a group of which we knew very little,
except that it contained the gigantic Hurypterus of De Kay and :
the Pterygotus of Agassiz, and was doubtfully referable to the
Pecilopoda.

Of the affinities of the Hurypteride I am not called upon to say
much here, as we hope to fully describe these specimens in the pub-
lications of the Survey. The family has been regarded as a group
of the Paleade by Burmeister ; but their relation to the Trilobites
I] seems more than doubtful. Since then Ferd. Romert has suggested
i) their affinity with Limulus, pomting out, however, the great differ-
il ences in the feet. Prof. M‘Coy has adopted this view, and united
AH Pterygotus and Eurypterus in the family Eurypteride, Burm., the
fz principal character of which, as distinguished from the Limuli, is the
i very obvious one of the free-jointed rings of the abdomen. And in
ii this association I should have been content to leave them, but for
ny the suggestion of a much more complete affinity by Mr. Huxley,
which will, I think, when he has worked it out for us, explain not
only these forms, but also the group of Ceratiocaris and its allies

. above mentioned, which are far from uncommon in the Ludlow rocks.
Ml And it may, perhaps, include my Cambrian genus Hymenocaris, and
thus relieve the Phyllopoda from the burden of these old and ano-
malous Paleozoic forms. As Mr. Huxley has promised to adda full
note upon the subject, I will not enter further into it here.

The beautiful figure by Ferd. Romer of the Lurypterus remipes,
and Eichwald’s late discovery of the LH. tetragonophthalmus im the
Isle of Oeselt, have furnished good materials for understanding that
genus. The latter zoologist especially has been enabled to figure
clearly the jointed feet and the sculpture of the rings of the body.
And this sculpture is so exactly that of Pterygotus on a small scale,

* See the preceding paper, p. 15.
+ Palzontographica, vol. i. p. 193.
t¢ Bulletin de la Soc. Imp. des Naturalistes de Moscou, 1854, no. 1. p. 100. pl. 1.

1855. | SALTER—-HIMANTOPTERUS. 27

as to suggest immediately an affinity between that large Crustacean,
with strong didactyle pincer-like feet, and these with the principal
feet, at least, adapted for swimming (“‘ruderblattchen’’). The
entire form of Pterygotus, however, is so little known, that it is
impossible to say it did not possess a pair of natatory feet*, and large
pincer-like antennze ; and, on the other hand, the anterior pair in
our fossils are chelate organs, and nearly all the figures of Hurypterus
show something of the same kind. The affinity then with Pterygotus
may be closer than we yet know of.

Eurypterus, De Kay, is a large and elongated Crustacean, with an
entire semioval or subquadrate carapace, on which the large sessile
eyes are placed, in the manner of those of Limulus, wide apart, but
towards the middle of the head. The body is ovato-lanceolate, broad
in front and attenuated behind, and terminated by a pointed or acu-
minated tail. There are 10 or 11 body-joints, exclusive of the tail-
jot ; and the hinder (abdominal) rings are subquadrate; the ante-
rior (thoracic) rings widely transverse.

The limbs or appendages are three on each side, according to the
very perfect figures given by Eichwald ; the two anterior of which
are simple appendages, of about five joints each, with small chelate
tips. The hindermost pair are much broader and longer, consisting
of five joints, of which the two terminal ones are rather suddenly
dilated and form a long-oval palette.

HIMANTOPTERU Ss, gen. Nov.

In the specimens here described, although the general form is
much the same as that of Hurypterus, there is this essential difference,
that the eves are placed, not on the surface of the head, but on the
anterior or antero-lateral margin, and quite at the edge. Together
with this, the swimming feet are of a more linear form or rather
thong-shaped. The name Himantopterus+ may be therefore appro-
priate for the genus to which these specimens belong.

They are closely allied to Hurypterus, like which they have a
comparatively small carapace, with the single pair of maxillary feet
for swimming, but, so far as we yet know, with only one pair of
antennze. These latter organs are linear, narrower than the paddles,
and consist of few joints; the last joint is strongly didactyle, with
rather long chele. The accompanying woodcut (p. 28) shows the
general characters of the genus.

A genus nearly allied to this has been described by H. von Meyer
and Dr. Jordan, from imperfect specimens in the coal of Saar-
bruckt. Von Meyer’s genus differs at a glance from our fossils in
the sudden reduction of width in the abdominal joints; there are

* Agassiz’s figure of the principal limb (Poiss. Foss. Vieux Grés Rouge, tab. A)
looks exactly like one of the swimming feet of Himantopterus : and the very large
pincer-like limbs in that case must surely be antenne. ;

+ From the Greek iwds, iwavros, a thong, and wrepor, a wing.

+ Dunker and Von Meyer’s Palzontographica, vol. iv. pt. 1. p. 8. pl. 2. fig. 1.

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

six wide thoracic rings, somewhat falcate at their outer extremities ;
but the number of joints of the abdomen, the position of the eyes,

Figs. 1-7.—Diagrams of Himantopterus.

1. H. bilobus ; half the nat. length ; position of the jaws, on the ander side of
the head, indicated at a.

2 a, one of the jaws and its scale-like markings ; 2 4, a portion magnified.

3. H. maximus ; part of the head, one-fifth the natural length.

4. H. acuminatus ; tail-joint, one-third the length.

5. H. lanceolatus; last two joints, about one-half the natural size.

6. H. perornatus ; part of three thoracic rings, to show the falcral point aud
the scale-like sculpturing on the forward half.

7. Scale-like appendages ; many of these lie loose on the surfaces of stone in
which the fossils occur.

and the appendages are not known; and we should not be justified
therefore in uniting the two forms on such fragmentary evidence.
From the figure I should suspect the eyes are lateral, as in Himan-
topterus ; the sculpture is like that of our fossils, and the size not
less than that of our smallest species.

There are five species of Himantopterus in the Lanarkshire locality,
and one from South Wales, already known.

1855. | SALTER—HIMANTOPTERUS. 29

1. HIMANTOPTERUS ACUMINATUS, sp. nov. Fig. 4.

H. pedalis et ultra, elongatus, articulis 12, quorum quinque ultimis sub-
quadratis, penultimo oblongo; caudaé magna, ovata, et in apiculum
serratum longum producta.

Of this fine species, which must have been nearly 2 feet long, we
have specimens which show the whole of the thoracic and abdo-
minal segments united. The former are broader than, but not
abruptly distinct from, those of the abdomen. They are transverse,
a little produced at their posterior lateral edges, and have along the
middle of the dorsal line either one or two (probably one) short spines
projecting backwards.

The abdominal segments are but little broader than long. The
penultimate, indeed, is quite as long as broad; and the terminal
joint, of which we have specimens 5 inches long, is contracted and
convex at the base, then rather suddenly expanded into an ovate
form, and produced into a long apiculus (fig. 4). A keel runs the
whole length of the segment, and the sides both of the expanded
portion and of the apiculus are crenate (less strongly than in our
figure).

We have but little of the carapace, and cannot be sure that the
next described species does not belong to it. Of the limbs, there
are the large swimming feet, consisting of a very large basal joint
(coxa), and five others: the first narrow, the second irregular in
shape, the third, where the backward bend of the limb takes place,
subtriangular but rounded in front. The penultimate joint is much
longer than broad, and deeply bilobed at the tip ; the terminal one
is an ovate palette, two anda half times as long as broad. The scaly
sculpture occurs on all the joints of the limb.

With these limbs lie a pair of antenne (?) of equal length. They
consist of about five rather inflated joints, terminated by a small
uncinate jomt. They appear to be united at the base.

2. H. maximus, sp. nov. Fig. 3.

H. capite feré 8 uncias longo, 54 lato, oblongo, vix suburceolato, lateribus
anticé contractis; fronte rotundato; oculis magnis, oblongis, ad an-
gulos externos fixis; margine antico et laterali tuberculato-crenatis.

If we estimate the length of this species by taking the propor-
tionate length of the head to the body, which we find in the H.
bilobus (fig. 1), the entire creature must have been at least 3 feet
long ; or, if we suppose it to have had the same proportions as H.
acuminatus, which has more elongated body-joints, the case would
not be different.

We have two specimens of the head, and both present the
same characters in the eyes, and in the rugoso-crenulate anterior
margin.

30 PROCEEDINGS OF THE GEOLOGICAL society. [Nov. 21,

3. H. BrLosus, sp. nov. Fig. 1.

H. 6-7-uncialis, ovato-elongatus ; articulis 11 vel 12, omnibus transversis,
ultimo subquadrato; cauda oblonga, ad apicem profundé divisa.

Of H. bilobus, which is the common species at Lesmahago, we
have more materials for illustrating the generic characters than of
any of the others. There are complete specimens with the head,
five or six thoracic, and six abdominal rings, tail, swimming-feet,
and antennee all in their places; and several specimens show these
various parts dissected. It is only in this species that we can see
the maxille im their right position, with their serrate edges and
broad foliaceous basal joints. The antenne also (probably only one
pair) are in their position, attached to the anterior part of the head.
They are linear, of few joimts, and are deeply chelate at the tip. The
swimming-feet, attached to the posterior parts of the cephalic shield,
are short ; the portion which projects from beneath the carapace,
and is directed backwards, being not above one-fourth the entire
length of the body, and reaching to the fifth rmg. The speci-
mens being all nearly of a size, it is presumed we have the adult
form.

The body, in our best specimens, is elongate-oval in front, and
gradually attenuated into the abdomen, from which it is not easily
distinguished. If we reckon the five* anterior rings for the tho-
racic ones, these are widely transverse, the length even of the last
ring being not more than one-third its width. Their posterior angles
are very slightly produced backwards. The six posterior rmgs are
all much wider than long, except the penultimate joint. which ap-
proximates to square. Its hinder angles are produced to lap over the
rounded anterior edges of the caudal joimt. The latter is only two-
thirds as wide as long, and fully double the length of the penulti-
mate joint. It is widest behind, with the posterior angles rounded
off, and is deeply cleft more than half way up. No median keel
like that of H. acuminatus can be detected on any of the body-joints
except the last but one; the upper part of the tail is keeled also for
a short distance.

The carapace is half-oval, and only one-fifth wider than long.
The position of the eyes is very forward on the sides, and they some-
what interrupt the general oval contour. They are broadly cres-

‘ centic and convex; and their extreme length is rather more than

half that of the head. No lenses can be seen on their smooth sur-
face.

The maxillee (or mandibles) occupy nearly all the under side of
the head ; they are 4-jomted; the basal joint greatly the largest,
and somewhat of a spherical-triangular form; the second and third
joints are narrow and wedge-shaped, and the terminal one short and

* Or six. There is some evidence of a narrow anterior segment in addition to
the eleven body-rings; and, as three other species have the anterior segment
narrow, and eleven rings behind it, it is probably the case here; and we have
so represented it in the diagram (fig. 1, p. 28).

1855. ] SALTER—-HIMANTOPTERUS. 31

wide, with a strongly serrate edge. The whole surface is orna-
mented with scale-like sculpture. The hypostome, or anterior part
of the under side of the head, is transverse, and from beneath it
spring the linear but rather broad antennze, which are considerably
longer than the carapace.

The swimming-feet are formed of six joints, the basal or coxal
joint very large ; a second, third, and fourth of irregular shape; the
angle of the bent limb being formed by the third (rather than the
fourth, as in H. acuminatus); and the fifth and sixth are elon-
gated, but not much wider than the rest; the penultimate joint is
the larger of the two, and is notched to receive the terminal ovate
palette. These swimming-feet always start exactly from the angle
of the carapace, where it joims the first body-rmg ; and we are able
hence to ascertain the true hinder edge of the carapace when it is
otherwise obscured by pressure.

There are some flat appendages, of a cordate-ovate form, which
are frequently associated with this species, but their nature is wholly
unknown. It is possible they may be scale-like appendages at the
base of the antennze. One is figured in the woodcut (fig. 7).

4. H. PERORNATUS, sp. nov. Fig. 6.

H. maguus, pedalis et ultra 4 uncias latus ; capite sublevi; thorace valdé
sculpto, et ex segmentis 6 latissimis curvatis composito; segmento
primo angusto lateribus rotundatis, secundo subfalcato, reliquis sub-
parallelis ; segmentis omnibus anticé squamulis minutis ornatis, posticé
subleevibus ; angulis capitis acutis; oculis anticis (minoribus ?) granu-
latis.

Of all our specimens this one only shows the true consistence of
the corneous crust, and the slight general convexity, which, it is
probable, all the species possessed. The head is fully half a broad
oval, and has the eyes rather forward, but small (in proportion to
those of H. b:lobus), and these show the lenses well.

The head is smooth, or at least shows none of the peculiar sculp-
ture so visible on the thorax-rings ; and these only show it on the
anterior half and on the sides, the posterior half of each segment
being smooth. The sculpture consists of short scaly markings,
directed backwards like those of Pterygotus, but far smaller ; and
these are very prominent, though of small size, and rather irregular
as to the amount of curvature. They are very like those on the
Eurypterus figured by Eichwald, and above referred to. Probably
this sculpture is characteristic of the whole family of the Lury-

teride.

The fuleral point of these wide body-segments (fig. 6) is very near
Sths of an inch in a segment 4 inches broad) to their ends, and the
forward curve of the segment is changed at this point for a straight.
outward direction. One of these pleuree, broken out from the specimen,
showed that there was an incurved sculptured portion for a short
distance on the under side, like that of the Trilobite.

32 PROCEEDINGS OF THE GEOLOGICAL SociETy. [Noyv. 21,

5. H. LANCEOLATUS, sp. nov. Fig. 5.

H. elongatus, posticé attenuatus ; articulis 12, quorum 10 transversis, penul-
timo oblongo, cauda acuta producta.

This is the smallest of the Lesmahago species. It is elongate,
attenuated behind, consisting of twelve body-rings, which are sculp-
tured anteriorly, as in the last species, and are all transverse, except
the penultimate, which is elongate-oblong. The tail-joint is a gra-
dually pointed spine, longer than the preceding joint, and appears to
be keeled along the middle. (Its base is less bulbous than it is in
our figure.)

The swimming-feet are narrow, and extend back to the sixth
body-joint.

Locality.—All the above are from the same locality, —Lesmahago
in Lanarkshire ; and were discovered in the uppermost Silurian rock
by Mr. Slimon*.

Another species of the genus occurs in the Tilestone of Kington,
Herefordshire, and has been for some time known to me. I propose
to call it H. Banksii. .

6. H. Banxksit, sp. nov.

H. parvulus, 2-3-uncialis; capite convexo, parabolico, ad frontem suban-
gulato ; oculis gibbis lateralibus, ad medium capitis, prominentibus ; an-
nulis trunci valdé transversis.

This small neat species, of which we have many specimens in the
Museum of Practical Geology, occurs with Pterygotus and spines
both of Crustaceans and of Fish, in the yellow tilestone beds of King-
ton, Herefordshire. It is there associated with the Platyschisma?
helicites and Lnngula cornea. ‘These are the two species of shells
which appear to accompany the fossils of Lanarkshire above de-
scribed,—a good argument, therefore, even without other evidence,
for regarding those beds as the uppermost portions of the Ludlow
rock.

The head is 1} inch long, and fully as much broad ; it is semioval,
produced and angulated anteriorly, regularly convex, with a thick
margin, on which the prominent oval eyes are placed rather more
than half-way up the head. They are small in comparison with
those of some of the cther species. The posterior head-angles are
retuse, and the hinder margin is quite plain and even, as in the other
species. We do not possess the body, except imperfect portions of
the first nine rings ; and these agree in general form with those of
the H. lanceolatus. Both have a close scale-like sculpturing on their
forward margin, and together with them at Kington occur also tail-
spines, scattered in the rock, which may possibly belong to them,
and which are narrower than those of the Lanarkshire fossil. As

* See the preceding paper, by Sir R. I. Murchison.

1855. | SALTER— HIMANTOPTERUS. 33

we do not yet know the head of the latter, we must for the present
keep the species distinct; and I propose to dedicate it to Mr. R.
Banks of Kington, who has lately been making discoveries amongst
the tile-stones, and has sent good specimens of this and other fossils
to London.

Phyllopoda®

Among the Lanarkshire specimens, so well collected by Mr. Sli-
mon, are perfect forms of the genus Ceratiocaris, M‘Coy*. Only
the carapace has hitherto been discovered; but the occurrence of
body-rings in the Dudley limestone has been for some time known ;
and in the Ludlow Museum I lately saw such body-segments con-
nected with the long triple tail-spines now known under the name of
Leptochelest.

Fortunately these specimens from Lesmahago have all the parts
in juxtaposition, and show the animal to have been a large Apus-like
Crustacean, with a carapace bent sharply down the dorsal line,
pointed anteriorly and truncated behind, and with an elongate ab-
domen of at least five, if not six, joints,—the hinder ones longest.
The last joint is a thick striated spine, with a bulbous articulation,
and has a pair of lateral spines or appendages at its base, nearly as
long as itself.

Fig. 8.—Diagram of Ceratiocaris, M‘Coy, with body and tail-spines
attached ; from perfect specimens found in Lanarkshire.

The resemblance to Hymenocaris, except in the presence of the
strong caudal spines, is sufficiently clear from the accompanying
woodcut (fig. 8).

Now that we know the entire structure of this genus, it must be
removed from the Limnadiade.

It has a nearer resemblance to Apus and Dithyrocaris, but differs
at once from the latter genus by the deflected sides of the carapace,
and apparently too by the want of regularly-shaped smooth eyes, for

* Synopsis Brit. Pal. Foss. Cambridge Mus. fasc. 1. p. 137.
+ M‘Coy, Syn. Brit. Pal. Foss. Camb. Mus. fase. 1. p. 175.
VOL. XII.—PART I. D

4

ets

os

ee eT

34 PROCEEDINGS OF THE GEOLOGICAL socirtTy. [Nov. 21,

we have no evidence that the prominent spot (described by M‘Coy)
on the anterior portion, is an eye, though it is very probable that
there are lenses at this point.

Perhaps there may be no true relation with the Phyllopods in this
form any more than in Himantopterus with the Pcecilopods. It may
be, as Mr. Huxley suggests, also one of the Stomapoda; and there
are some indications of long antennze, which may perhaps, with the
apparent absence of abdominal appendages, help to connect it by
analogy with some known forms of the group last mentioned.

In the meantime it is curious to see how gradually we have arrived
at our present knowledge of its structure. The carapaces had been
known for some time; but from their resemblance to bivalve shells
had lain unnoticed in cabinets. Prof. M‘Coy and myself both inde-
pendently recognized their Crustacean structure, which he fully pub-
lished in his work on the Cambridge fossils ; and he discovered the
eye, which I had not observed. In the meantime Prof. M‘Coy and
M. Barrande both recognized the Crustacean character of the tail-
spines; the former distinguishing them from fish-defences*, with
which they had been confounded ; and the latter, from better speci-
mens, making them out to be the tail, and not the pincers, of an
unknown Crustacean.

In the Dudley limestone the carapace and some of the body-joints
were found near together, by Mr. John Gray of that place; and in
the Ludlow Museum, as above noted, are the joints of the abdomen
connected with the terminal spines. Lastly, Mr. Slimon’s speci-
mens show the entire form, and give some hint as to the appendages.
It is hoped ere long to illustrate them fully.

OBSERVATIONS on the STRUCTURE and AFFINITIES 0f H1imMAn-
TOPTERUS. By T. H. Hux.ey, Esq., F.R.S.

From what has been stated in the preceding pages, it would appear
that the following propositions embody all that is at present certainly
known with regard to the great structural features of the genus
Himantopterus.

1. The body is composed of a comparatively small carapace, suc-
ceeded by eleven or twelve free segments, the last of which is bilobed,
lanceolate, or wide anteriorly and acuminated posteriorly.

2. At the margin of the carapace on each side lies a rounded or.
oval eminence, which there is every reason to regard as an eye.

3. The free segments have no appendages. The cephalothorax
presents three pairs: an anterior, probably chelate pair, occupying
the position of antennze; a middle pair of broad, short, foliaceous, ser-
rated organs, which have the appearance of mandibles; a posterior pair
of long flattened, jointed appendages, terminated by anoval palette, and
not improbably having an articulated filamentous appendage attached
to their penultimate or ante-penultimate joint.

* Quart. Journ. Geol. Soc. vol. ix. p. 13.

e+

1855. | HUXLEY— HIMANTOPTERUS. 35

4. Lastly, many parts of the body of Himantopterus present a
peculiar imbricated sculpture, resembling that exhibited by Ptery-
gotus.

Assuming these data to be correct, the question is,—In what group
of animals can we find an analogous structure? and there are obvious
reasons for at once narrowing the field of inquiry to the Crustacea,
and confining the search to the different subdivisions of that great

roup.
ee if not for Himantopterus, at least for the very closely
allied genus Hurypterus, have been sought by different naturalists
among the Pecilopoda, the Phyllopoda (particularly Apus), and the
Copepoda; and M. Milne-Kdwards has suggested that Hurypterus
possibly holds an intermediate position between the Copepoda and
the Isopoda.

1. If we compare Himantopterus with Apus, we find points of
resemblance in the form and position of the sessile eyes,—in the posi-
tion of the antennee and of the great natatorial feet, and, toa certain
extent, in their form,—in the structure of the jaws,—and finally, if
Apus productus be compared with Himantopterus acuminatus and
HI. bilobus, in the terminal segment.

The discrepancies, however, are even more striking and important.
The number of free segments in Apus is thrice as great as in Himan-
topterus; the carapaceextends as afree fold far back overthem; all the
thoracic, and the great majority of the abdominal segments possess
foliaceous appendages (which would certainly have been preserved in
as perfect a state as other similarly constituted parts, had they existed
in Himantopterus) ; and lastly, the penultimate segment carries long
articulated styliform appendages.

2. A certain similarity between Himantopterus and Limulus in
their carapace and eyes, the large size of the terminal segment and
the chelate form of the antenne in both, may be regarded as the
most salient resemblances of the two genera. To these might be
added a sculpture, not altogether unlike that of Himantopterus, on
some parts of Limulus, and a certain resemblance in fundamental
structure between the last ambulatory feet of Zemulus and the great
swimming members of Himantopterus.

The differences consist in the number and great development of
the locomotive members in Limulus, the coalescence of its abdominal
segments, their well-developed appendages, and the much smaller
total number of segments.

3. Himantopterus resembles many Copepods in the form and rela-
tive proportions of the carapace and free segments, in the sessile posi-
tion of the eyes, in the great locomotive antennee and. post-buccal
appendages, and in the absence of the majority of the abdominal
appendages. )

But the thoracic appendages are always well developed in the
Copepods, and the number of free segments is never so great as in
Himontopterus.

While the relations of Himantopterus with the Peecilopods, Cope-
pods, and: Phyllopods, then, must by no means be overlooked, they

D2

36 PROCEEDINGS OF THE GEOLOGICAL sociETy. [Noy. 21,

would appear not to be sufficiently close, while the differences, on the
other hand, are too numerous to justify its arrangement in either of
these families.

There is another Crustacean group, however, which presents a
much greater approximation to Himantopterus in some of its forms,
—the family of the Stomapods.

This small and not very well-defined group occupies nearly a cen-
tral position among the Crustacea; and its members, like those of
most central groups, while presenting a strong general similarity, dif-
fer very widely in details. The genus usually regarded as the type
of the family—Squil/a—is not more like Himantopterus than an
ordinary Macruran would be; but if we turn from Squzlla to Eric-
thys and Mysis, and thence to Cuma and its allies, we shall find we
have passed by a series of insensible gradations from the close ally of
the Podophthalmous Macrura to a sessile-eyed Crustacean, with the
internal antennze almost rudimentary, with a very small carapace, like
that of a Copepod in its proportions, and with twelve free segments,
the anterior of which only carry appendages, all the abdominal ones,
except the penultimate, being in some cases deprived of them.

The characters just mentioned are common to the genera Cuma,
Bodotria, Alauna, and Calyptoceros (the last a new genus lately dis-
covered by myself in the Bristol Channel) : and, in addition, Calyp-
toceros (and probably Cuma) exhibits very markedly that peculiar
sculpture which forms so prominent a feature of Himantopterus.

The differences between these ‘‘Cumoid’’ crustaceans and the
latter genus consist principally in the shape of the antenne and the
development of the thoracic appendages in the former, each thoracic
segment being provided with a pair of simply constructed members.
In addition there is a pair of appendages to the penultimate abdominal
segment, of which no trace has been found in Himantopterus.

As regards the two former discrepancies, however, we find in Erie-
thys that the three posterior pairs of thoracic appendages are reduced
to mere rudiments, even the two pairs which precede them being very
small. The largest uf all the thoracic appendages are the first and
second maxillipedes, the former being terminated by an oval plate-
like joint. The external antennee carry a similar oval plate on a long
stem.

Reductions and modifications of the appendages of a Cumoid Crus-
tacean of a similar character to these would produce a form wonder-
fully similar to Himantopterus.

But such reductions and modifications carried still further, and
bringing us still nearer the ancient form, are to be met with, not,
indeed, in any adult Crustacean at present known, but in those
remarkable larvee of the Podophthalmous Malacostraca which were
once known under the name of Zoea.

In their earliest condition these larvee possess sessile eyes, a short
carapace, a long jointed abdomen without appendages, and with the
terminal segment sometimes entire, sometimes bifid; the only append-
ages beside the minute trophi, consisting of a single pair of antennze
and a varying number of maxillipedes, so modified in form, as to serve,

1855. | HUXLEY—HIMANTOPTERUS. 37

in conjunction with the abdomen, as a powerful swimming appa-
ratus.

The nearest approach to Himantopterus which could be con-
structed out of the elements afforded by existing Crustacea, then,
would be produced by superinducmmg upon the general form of a
Cumoid Crustacean such a modification of the appendages as we find
among the Zozeeeform Macruran larvee.

It must not be supposed, however, that, because on this account
Himantopterus may with some propriety be termed a “‘ larval” form
it is therefore an “‘ embryonic” form, or represents any embryonic
stage of Crustacean development. On the contrary, so far as it is
“Jarval”’ so far it is not “ embryonic,” inasmuch as the form of the
Decapod larva is a wide and sudden deviation from the regular course
of embryonic development in the Crustaceans, in apparent adaptation
to peculiar exigencies.

Nothing has produced more confusion in the application of natural
history to geological problems than the ambiguous use of the word
‘“embryonic,” applied as it is, sometimes in the sense of ‘‘correspond-
ence with a developmental stage,” sometimes in that of “similarity
to a larval condition.” The structure of Himantopterus is anything
but embryonic in the former, proper sense,—very much so in the
latter.

38

PROCEEDINGS
OF

THE GEOLOGICAL SOCIETY.

POSTPONED PAPER.

On the Possible Extension of the Coat-Mrasures beneath the

SoutH-Hastern Part of ENeuanp. By R. Gopwin-AvustTen,
Esq., F.R.S., F.G.S.

[Read May 30, 1855*.]
[Puate I[.|

ContTENTS.
Introduction.

A. Nature of the evidence which serves to determine the form of the surface of
the Coal-growths.

1. The British area. 2. Belgian area. 3. The Boulonnais. 4. Franco-
Belgic sections.
Results.

Inferences from the relative positions of the subordinate members of the
Carboniferous series.
1. Old Red Sandstone. 2. Mountain Limestone.
Outline of the geography of Western Europe during the Coal-growth
period.
B. Axis of Artois.
C. Relations of overlying Secondary Formations.
1. New Red Sandstone. 2. Oolitic series. 3. Wealden series. 4. Creta-

ceous series. 5. Nummulitic group (lowest beds of the Northern facies).
General inferences.

Introduction.—The views contained in the present communication,
and which are essentially speculative, require the admission of certain
generalizations, from which, however, competent geologists will not
perhaps be disposed to dissent.

1. The early palzeozoic strata, like all others, were formed by the
gradual accumulations of coast-line waste; and, so far as the evidence
goes which is to be derived from the districts hitherto observed, the
nature of the change from the older to the newer paleeozoic groups

* For the Proceedings of this evening’s Meeting, see vol. xi. p. 532.

AUSTEN—EXTENSION OF THE COAL-MEASURES. 39

was one of contracting areas, by the conversion of sea-bed into
land-surface. This process was one of almost endless alternation
from one state to the other ; but the general tendency was to an in-
crease on the side of dry land. It is only towards the upper portions
of the palzeozoic group that we acquire any definite boundaries for
areas of land and water: it is on the correct restoration of these lines
that the following speculations are mainly founded. With respect to
those terrestrial masses which are represented only by the oldest
paleeozoic groups, it may suffice to say that they have mostly disap-
peared. We can, however, ascertain something as to their mineral
composition, and the spaces they occupied; and in this way we can
sketch out the surface of the Northern Hemisphere under its earliest
arrangements. These differed widely from such as obtain now. The
land was mainly extra-European ; and it must be obvious to every geo-
logist who has a clear view present to him, of the large proportion in
which sea-bed of subsequent date constitutes the present European
land-area, at how early a date some of these early features began to
be effaced. Any restoration of the European surface for this very
early period must be purely ideal ; whilst the restoration of the many
land-surfaces of the true Carboniferous period is real,—what was dry
land then has, in many instances, continued so ever since, and is so
now.

2. Of the widely spread terrestrial surface of the true coal-measure
period, portions attained a considerable vertical elevation. The evi-
dence of this may be derived either from the character of part of the
vegetation of the period; or from the scale of the alluvial action of
that time. In contrast to this, there is a feature which seems to
distinguish this period physically from all subsequent periods, and
which consists in the vast expanse of continuous horizontal surface
which the land-area presented, bordering on, and at very slight ele-
vations above, the sea-level.

3. All coal may be taken as the product of a vegetation which grew
on the spots where it is now found: the extreme purity of the car-
bonaceous matter, however thin the seams may be, is sufficient proof
of this. There may have been accumulations of drifted vegetable
matter then, as now; but no true coal-stratum was ever so formed.
The botanical character of the coal-vegetation does not belong to this
Inquiry ; it can, however, be divided into upland and lowland ; and as
to that of the low-level surface, it must have been composed of dense
growths of like plants, such as were capable of maintaining them
selves, like the peat-vegetation of modern times, for indefinite periods
over the same spots.

From the Valley of the Roer to that of the Scheldt, near Valenciennes,
there extends for 170 miles from E. to W. a continuous band of pro-
ductive coal-measures. This great coal-field has usually been de-
scribed as situated on the north-west edge of a mass of older rocks,
of which a principal part is known as the Ardennes range: such is,
however, rather a geographical than a geological account of its posi-
tion, as it omits considerations of some importance. On the north-

40 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

east this coal-band is overlaid in the direction of the Valley of the
Rhine by Upper Tertiary sands, and is lost for an interval of 40 miles,
when it reappears in Westphalia, under exactly the circumstances of
position which it has in Belgium. On the south-west of Valenciennes
the coal is worked beneath White Chalk, and a subjacent conglo-
merate (Tourtia) of the age of the Gault.

The national importance of the Valenciennes coal-field gave rise
from early times to numerous speculations as to its probable extension;
trial-shafts were sunk at various times and at enormous cost over a
very wide area, which, though unremunerative so far as theadventurers
were concerned, may have served to indicate the line of the present
workings. The continuity of the coal-beds beneath the chalk of the
north of France may be considered to have been proved for 80 miles
west of Valenciennes, along a line passing by Douay and Bethune
and south of Lillers.

For a long time the engineers of the School of Mines, guided by
theoretical considerations, directed their researches towards Arras ;
even now speculations based on the supposed parallelism of one part of
the coal-field with the ‘System of the Hundsriick,”’ and of another
with that of the Vendée, of M. Elie de Beaumont’s theory, are put for-
ward; and in this way the line of the coal-measures is carried by
Ferques and Hardinghen into the Boulonnais, of which the several
small coal-basins are represented as the natural termination (Burat,
p. 361).

M. Dumont has also apparently adopted this view, from the direc-
tion which he has conjecturally given as that of the coal beneath the
Chalk.

These last speculations would not, perhaps, have been ventured
on had the real structure of the Boulonnais been better known. The
coal-series of this district is fnterposed between two great groups
of limestone, of which the upper, with Terebratula elongata, repre-
sents the upper Mountain Limestone of Visé, which underlies the
productive coal-measures of the Liége basin. The Boulonnais coal
is most probably a great expansion (the result of more favourable
physical conditions) of M. Dumont’s middle division of his ‘* Con-
drusian ’ group, consisting of ‘‘ Psammite, Macigno, and Anthra-
eile: 7

It may be as well to state here distinctly that the fragmentary cha-
racter of the Boulonnais coal-formation is not in any way dependent
on original conditions of formation, but of disturbances of long sub-
sequent date: viewed apart from these accidents, the paleeozoic group
dips away beneath the oolitic series in the south-west, and no doubt
whatever can be raised as to its continuity in that direction*. The
upper or true coal-measure series of the Franco-Belgian frontier is
not presented in the Boulonnais denudation; but will probably be
found to occur beneath the oolitic rocks on the south of Marquise.

When my communication on the Boulonnais+ was read, the trial-
shaft at Guines had not been carried through. This was soon after

* Quart. Journ. Geol. Soc. vol. ix. p. 233. f Ibid. p. 231, &c.

AUSTEN—EXTENSION OF THE COAL-MEASURES. 4]

effected, and the White Chalk and certain subjacent beds, altogether
about 800 feet, were found superposed on palzeozoic sandstone and
shale.

At Calais, which is about 18 miles to the north of the old coal-
works at Ferques, an artesian well was carried through the thickness
of the Chalk, and at a depth of 1100 feet beds were met with which
have been identified as true coal-measures*. By the aid of the fore-
going data, it becomes easy to carry on the section of the palzeozoic
series, as exhibited in the Boulonnais+.

Ep 3 N.
4 ’ ———<—_—___—_——— Cretaceous seres.—$<<$£$__—___—_—__— a
= Oolitic series. ——»— 4
E oO A 1S)
=. g Si
58S SRS.
eo isi ks) ae
= £ se ea <
7) a (Dy ae 24 g
© © dy)
Fess < EE%A 4S
y as $ : %%2% 2%
ig oS g 3 BN ue whonel
Soe A § % Olen cee ene
gy ns, . a oe so) as -) @ np ? 2) gS
& FSG Seog CBord nate Ae
SiS eS 88 8-2 S eau? Bese Se
E Aces og es onee FS B% te ° &
fy isi ss ssss g ATAEAARATAL
xv ov . a oe 4 os = 2 = Oe =
SSSR ESTES HERS 626 oe be eee
Ds 8, 2 ly Mo Wa Bo 25 Ge (5 Wore) Gh Yo Ws Be 210 8) 5 1G 5 el Be BS Slo
ee ee \ ;
<—-Carb.series. Upper Eifelian. Middle Eifelian. Upper Eifelian. Carb. Series. —>—

By this it will be seen that on the north the cretaceous strata im-
mediately overlie a higher portion of the paleeozoic series than the
oolites do in the south, thus giving considerable extension to the area
over which that series is wanting.

The circumstance, that a portion of the coal-measures should have
been recognized so near us as at Calais, has suggested the following
Inquiries, which relate,—

1. To the amount of @ priort evidence as to whether the coal-series
may be continued further West, across the Straits of Dover, and so
beneath our south-eastern counties.

2. Whether, if so, the coal-measures are likely to occur under such
condition of depth, with respect to the overlying formations, as would
render them available to us.

The solution of such questions depends on a great variety of con-
siderations ; and more than ordinary caution is imposed on any one
who would venture on an affirmative opinion. ‘‘Le probléme qui, sou-
levent les recherches de mines de houille dans le nord de la France,
se rattache en derniére analyse au plus grandes questions que la
géologie puisse traiter relativement aux couches houilliers de ces
contrées; celle de la forme, encore indéterminée, du bassin dans
lequel elles se sont déposés, celles de la disposition des terrains qui
ont recouvert le terrain houillier dans une grande partie de son
étendue.”’

* Prestwich, Geological Inquiry respecting Water-bearing Strata, &c., p. 208.
+ Quart. Journ. Geol. Soe. fc.

25

SS

—

42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Such is M. E. de Beaumont’s view both of the importance of the
inquiry, and of the main points which it involves. The question
itself may be of greater importance to France than to this country,
from her relatively limited supply of coal; yet, considering the
demand we are now making on our own coal-fields, it may not be
amiss that the theoretical geologist should point out in every case
such areas as may possibly furnish us with fresh supplies.

[ Note.—<s, in tracing out the progressive changes which took place
in the physical outlines of Western Europe during early times, I had
been led to a belief that the systematic representation at present

in use is not the true one, I must be allowed to state that in the

followmg pages the term “Carboniferous” will include the con-
ditions —whether terrestrial, freshwater, or marine—from the Mar-
wood beds and their equivalents upwards. This is the ‘“ Upper
Paleozoic Group.”

The ‘‘ Lower Palzeozoic Group ”’ will designate all marine sedimen-
tary strata up to “ Lower Silurian,” inclusive.

The ‘‘ Middle Group” will comprise two series, which I cannot
but consider to have been equivalent, viz. the “Upper Silurian ”’ and
the “ Devonian.”’ |

A. Form of the Terrestrial Surface of the Coal-growths.
BrirTisH AREA.

The restoration of the physical features of Western Europe in
their earliest form can only be indicated here in outline. There
existed a continuous range extending from the Arctic circle, perhaps
as low as north Africa, running north and south, and nearly equal in
extent with the great linear ranges of the American continent. Of
this range the Scandinavian portion now remains, extending through
16° of latitude. It can be traced beneath the overlying deposits of
Northern Germany ; it reappears through the eocene series of Bel-
gium; is preserved in the Spessart, Vosgean, and Schwartzwald ranges;
expands into the central plateau of France on the west, and the
Estrelles (Var) on the east, and is represented in the Mediterranean
area by Corsica and Sardinia.

To the west, old land lay to the north and west of the British
Islands group: this land did not wholly disappear until some long

‘ subsequent period, and in its southern extension formed the boundary

of the great European basin ; but, although this land encroached more
on the Atlantic than land does now, yet that great valley, which from
earliest times has been the parting line between two sets of represent-
ative and synchronous faunas, is a physical feature of earliest date.
The greater part by far of the earth’s visible mineral surface being
derivative, the sources of the oldest sedimentary strata must neces-
sarily be concealed beneath what is now sea; indeed it would be
difficult to fix on any masses which supplied the materials of the
oldest British strata,—these masses have wholly disappeared. The
arrangement of these early deposits was in subordination to masses

AUSTEN—EXTENSION OF THE COAL-MEASURES. 43

having some such positions as above described ; and, as there is an
exact relation and balance between the amount of sedimentary matter
and the coast-line from which it is derived, the extent and dimensions
of the paleeozoic masses afford an indication of how vast a region that
was which has disappeared.

The lines of saliency and depression which have subsequently
shaped out and formed our present Western European areas have been
mostly transverse to the direction of the original lines. With refer-
ence to the present inquiry, we have only to compare the palzeozoic
region which extends south from the Department of the Manche with
that of our own western counties, to ascertain what was the character
of the changes of the middle and lower palzeozoic periods. |

If we take zoological considerations as a guide, the southernmost of
these areas seems to have been subject to fewer changes favourable
to the immigration of new and successive occupants than the Silurian
region of Sir R. Murchison was. The nature of the difference is this,
the sequence of animal life was not the same through the same periods
of time over adjoining areas. The geographical variation in the marine
fauna was, perhaps, greater during the palzeozoic period than it is at
present ; but making every allowance for this, it will be found insuf-
ficient to meet the nature of the change which takes place.

I would indicate as an inquiry to be made,—why it is that the
lower palzeozoic group of Western France, as the slates of Parennes,
and their equivalents, should differ so materially, as to their contents,
from the Llandeilo and Bala groups, of which they are received as
the synchronous products. Ascending higher in the same French
series, the want of parallelism with our own becomes still more
striking ; and in estimating the value of this with reference to the
restoration of any salient lines, it must be remembered, that the
French sections show perfect continuity throughout*, and that the
value of this evidence over-rides all other in a question of chrono-
logical sequence ; and also that the palzeozoic series of western France,
as a whole, is synchronous with that of the British area.

In France the palzozoic series consists of a Lower Silurian, an
Eifelian, and finally of a Carboniferous division, which last commences
with a group corresponding to the Marwood beds, as in the Boulon-
nais. ‘The observations of Mr. Haughton enable us to extend the
area of like conditions for the lower carboniferous group as far as
Anglesea.

In the total absence of any direct physical evidence, we are not
warranted in supposing that any portions are relatively wanting
between the paleeozoic groups of Western France and England ; but
merely that in parts, and from local causes, what are true equivalents
are differently represented. That which we recognize in the English
series as an Upper Silurian fauna does not seem to have found ad-
mission into the area of the paleeozoic seas of France, nor indeed into
those of southern and eastern Europe. It may be suggested, perhaps,
that the oceanic region then may have been one and the same, but

* Bull. Géol. Soc. Fr. vol. ii. pl. 11.

44 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

that the two areas were not under conditions alike favourable for the
development of such a fauna. The answer to this is obvious ;—the
area over which a marine fauna such as we term Devonian comes in
succession on a Lower Silurian one is so vast and so varied in the
conditions which it indicates, compared with that in which an Upper
succeeds a Lower Silurian, that it is physically out of the question that
in the first-named area an Upper Silurian series of forms should have
been wholly excluded.

With respect to the lower paleeozoic group of the French and
Southern European area, as known to us through the researches of
M. de Verneuil and Mr. D. Sharpe, there is enough to warrant a
comparison with our own typical Silurian series ; still it is clear that
at this early time there were two regions,—each having a facies of its
own, dependent on community of forms, and the limits of which lay
somewhere in the line of the Bristol Channel.

Zoological considerations such as these require and imply the exist-
ence of parting barriers, even where no physical evidence whatever
of such may-now remain. Geology in its future progress will be
called upon to define the positions and extent of many lines of partage.
The difficulty in the present instance is not great; assuming such a

line we find the character of the accumulations on either side to be~

as such conditions would require. On the French side, the quartz
shingle-beds at the base of the slate-series of Jersey,—the siliceous
conglomerate and sandstones of the Cotentin, mark the early existence
of coast-line in that direction. In this case palzeozoic sedimentary
strata are produced out of the abrasion of older portions of the same
great series, as the result of the elevation of deep-sea sediment (already
mineralized) to the sea-surface: and this change was progressive.
The Silurian series of the West of France presents at least two groups
separated by thick pebble-beds ; and this change is accompanied by
the transgressive passage of one series over the other, as in the “buttes
de Clécy.”” These lines affect east and west directions, from the
lowest ranges of the satiny and fibrous chloritic slate series upwards.

On our side of the English Channel, the successive bands of shingle
subordinate to the Lower Silurian series of Cornwall equally require
the presence of a former coast-line, in somewhat close proximity there.
Attention was first called to the existence of rocks of this age in this
quarter by Prof. Sedgwick*.

The direction of these bands indicates the relative position of the
coast, for I am disposed to consider the conglomerates of the Lizard
district to be of the same Silurian age. Guided by these considera-
tions, and their bearing on the direction which upraised older paleo-
zoic beds assumed, we may feel assured that the lower or western
end of the Channel area was occupied by ridges or axes extending
eastwards. It is this line whose influence may be first traced in the
difference between the two Lower Silurian regions which have been
indicated above; a divergence which becomes greater as the series

* Quart. Journ. Geol. Soc. vol. viii. pp. 10, 11, &e.

AUSTEN—EXTENSION OF THE COAL-MEASURES. 4d

ascends, until at last it forms a barrier betwixt two distinct marine
provinces.

The existence and progressive growth of an old ridge in this position
does not rest on zoological considerations alone. On the advancing land
of the Cotentin, the older palzeozoic series is brought up along the coast
east and west from beneath the sandstones and conglomerates of the
Montagne de Roule, &c. On our side it is preserved in the fibrous
chloritic slates of the Bolt and Prawle, and in the crystalline rocks of
the Eddystone.

Prof. Sedgwick, speaking of the oganenees which have affected the
South Cornish district*, expresses bis opinion that a force has acted
on the side of St. Austle, and a contemporary force on the south of
the Dodman, and between these two forces the present surface has
been broken and placed in its present contorted position ; and again
(p. 19) he says “we have indications of an elevatory axis ranging
(nearly east and west) along the south coasts of Devonshire and
Cornwall.”

These two axes, however, were not contemporaneous; the Channel
axis had a priority of origin, and was the line of resistance which
contributed to cause the contortions m the sedimentary beds to the
north of it, when the granitic intrusions of the west of England took
place.

Another proof is to be derived from a new branch of Geological
inquiry. Cleavage-structure of great masses is very generally ad-
mitted to have resulted directly from the mechanical tension to which
they have been subjected in the process of elevation: the limits of
an area of elevation are therefore clearly indicated,—being those
within which the cleavage-planes have an arched arrangement. This
law, for which we are indebted to Mr. D. Sharpet+, with the deduc-
tion from it,—that the lines of vertical cleavage are the partings of
contiguous systems, will henceforth mainly guide us in determining
the extent, succession, and relative ages of early ranges. Applying
these considerations to our western counties, it will be found that,
taken in its broadest part, Devonshire presents an arch extending
north and south from Bickington to the South Hams: then follows
a band of vertical cleavage-structure ; beyond this a second arc is
seen to take its origin, and is continued south as far as the fibrous
chloritic slates which form the coast-line of the Prawle; all this area
is only a small section of an arch; but, by the aid of the foregoing
law, it becomes as satisfactory a proof to the geologist that it was once
continued on, as the face of a single stone on a ruined bridge may be
to the antiquarian of the character of the structure of which it once
formed a part. From this mere abutment preserved in the projecting
headlands of South Devon, we may replace with certainty an elevated
area to the South ; for without it, what now remains could not neve
been produced.

It might further be shown that the span of the Channel arch was

* Quart. Journ. Geol. Soc. vol. viii. p. 10.
+ Phil. Trans. 1852.

46 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

not less than that of the Devon arch, and that in its extension (the
direction of the major axis of the ellipse) it was carried as far east-
wards as the meridian of London.

Passing over to the district of South Wales, we may apply consi-
derations akin to those employed with reference to the South Devon
and Cornish area, and with like results. A mass of oldest sedimentary
strata makes its appearance near, and extends S. and E. of St. Davids ;
subordinate to which are bands of shingle. The lines of quartzose
conglomerate occurring in the grauwacke overlying the former—
so singularly like some of the beds of the Old Red Sandstone that
they were at one time mistaken for them, but which are now known
to be of Lower Silurian age—would imply that the source of such
a form of detritus was not far distant.

This Silurian section is interesting, Inasmuch as, in the imperfect
representation we get of the upper group, we see to what extent the
character of that fauna becomes modified by local conditions ; and
also that local conditions, and the variations they produce, are not
sufficient to account for that absence of the upper group which has
been remarked upon with respect to Cornwall and the West of
France.

In like manner the cleavage theory shows that the Bristol Channel
area must at one time have been the line of an axis of elevation, of
which the direction coincided with the strike of the old group of
St. Davids, and that of North Devon. This was probably the eastern
extremity of an elliptical area, of which the maximum breadth was
placed at some distance to the west.

Independently of these considerations, there is to be observed in
this same district the relation of unconformity between the Old Red
Sandstone and the Culm-series, as also that of both of the foregoing
with the Silurian and older rocks,—relations which must always exist
towards the original limits of formations where the destruction and
removal of mineral material alone take place. Here then as at the
western opening of the English Channel we have clear indications of
an old coast-line, and of land which has long since disappeared.

The whole terrestrial surface thus restored would present an in-
dented. outline produced by advancing ridges of old paleeozoic sedi-
mentary strata, and extending from the main Atlantic mass in east
and west directions. This growth of land from the Atlantic side,
towards the European area, by means of the successive elevation of
paleeozoic sea-bed, commenced from very early times. It was a phy-
sical change of this kind, which produced what may be designated
as ‘‘the Mid European line,” and which at length constituted a parting
barrier between two hydrographical areas, in the northern of which
the true upper Silurian fauna had its development together with
northern relations, and of which the southern equivalent is that as-
semblage of forms which is usually known as the Devonian*.

* This view will form the subject of a special memoir, but it was necessary to
state it here, inasmuch as it helps towards a determination of the form which the
palzozoic terrestrial area of Western Europe ultimately assumed.

TP f* er ee eee

ee.
we gf ot

7:

AUSTEN —EXTENSION OF THE COAL-MEASURES. 46*

EXPLANATION OF THE Map, Puate I.

The map which accompanies the present communication must not
be viewed as a geological one—as representing the actual arrange-
ment of the mineral masses which compose the present surface—nor
yet as a map of Western Europe at any definite period of past time.

One of the objects of the memoir which it illustrates is to trace
out the gradual formation of an old terrestrial area, that over which
the coal-growths ultimately established themselves. It is hoped that
the descriptive portions of the paper will be found nearly sufficient
for this purpose, and that the introduction of a few leading lines,
such as may serve to indicate the direction of the masses which in
turn imparted a definite physical configuration to the area in question,
is all that is requisite to guide the reader, and enable him to follow
more easily the kind of evidence on which the conclusions have been
based.

Over the British portion of the area, a local group, known as the
“Old Red Sandstone,’ has been tinted, because it serves to indicate
very definite physical conditions at a definite period. From the date
of this group the Carboniferous formation may be viewed as a great
fluvio-marine series of the later Palzeozoic period, during the whole
of which the facies of the contemporary marie fauna was such as is
known as that of the Mountain-limestone series. It must however
be borne in mind, that in the North of Ireland the distinction be-
tween the marine Carboniferous sandstones and lacustrine Old Red
Sandstone has not been traced as it has for the South.

A very extensive series of maps would be required to convey any
adequate representation of the successive changes which Western
Europe underwent in its physical arrangement ere it reached the
maximum extent of terrestrial surface which it presented at the time
of the great coal-growths ; but the time may come when general
views as to past conditions will require to be thus illustrated.

The geographical arrangements on which the internal basin con-
taining the Palzeozoic fluvio-marine groups depended were preserved
through a long subsequent period ; the same area became that of the
“New Red conglomerates, sands, and clays” of English geologists,
and which, if in part “‘ Permian”’ and part “Triassic,” are such only
in the form of equivalents, these groups being here the accumulations
and depositions of lacustrine waters and their tributary rivers.

No restoration of the area of the coal-growths has been attempted
on the side of the old Scandinavian chain; it could have easily
been shown, however, that all the subsequent secondary and tertiary
formations had their limits against this mass, and that all these les
have been carrried downwards by the progressive subsidence to which
this chain has been subjected, even to times very near to the present.
In the Coal-measure period the materials of the sandstones of our
northern and midland districts must have been brought down by
streams which had their origins in that region.

We have only to imagine an extension of the Scandinavian chain,
encroaching on the area of the North Sea, and along a line north and

“S

MIEDDIE AW D

PALAO

me, _ MIDDLE af
Qf
AND -
“LOWER PALHOZOIC PERIOD

ZOLG :PwH

Duar: me Geol Soo, Vol XM. PLT

iM) JE) TE) 1D; Ase

LAND
SUREACE
AND AETER
CARBONIFEROUS

PERIOD.

ee M? R. GODWIN-AUSTENS PAPER

ae ee nN
SS

Mt A IP

to illustrate

on the possible Extension

of the

COAL MEASURES.

REFERENCE.

Valioxore

~) Oolitic
outlines of (se

Wialdav
Lower Getactous

Old Tied. Sanitstone Tiaels.

SBE Cel Measure Trucs

{Probable Extension of Gal-Measure
| Graas.

{CML coast-lone( tn the Channal-Area)
| duran the Naver Tertinry Prod.

Sone
BPRS S,

x

Fal

46** PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

south, to enable us to define the form of that internal depressed area
over which the low-level coal-growths of France, Belgium, and
Britain were accumulated.

The second special object of the memoir was to show that the area
thus defined was subsequently disturbed, whereby lines of elevated
strata were produced, one of which, having a general direction from
east to west, has had the effect of placing the Coal-measures near the
present surface along a great portion of its course. This line, as well
as those which indicate the fluence it has exercised with reference
to the distribution and limitation of the secondary groups, are ren-
dered sufficiently distinct, allowance being made for the scale of the
map. |
oa being the nature of the map, the names of places have been
omitted; their positions, however, in many instances are indicated ;
and as the map has been carefully drawn, the reader will have no
difficulty in following the exact course of every line indicated on it,
by reference to any ordinary geographical map.

;
,
i
:

AUSTEN—EXTENSION OF THE COAL-MEASURES. 47

BELGIAN AREA.

The lower tertiary strata of Belgium (Nummulitic formation),
between Bruxelles and the great coal band, overlie a surface of paleeo-
zoic rocks, without the intervention of any member of the secondary
formations. At Tournay these tertiary strata pass over the edges
of the cretaceous rocks, and both are wholly unconformable with
the carboniferous limestone there. From Tournay by Ath as far
north as Hall, Wavre, and Jodoigne, there is a regular descending
series of palzeozoic groups, presenting a like series of undulations
with those to be observed on the south side of the coal-band, as from
Bellignies eastward, and which on that side rise into the ridges of
the Condros and the Ardennes. The breadth for which this con-
dition of surface, next beneath the Nummulitic series, can be traced
north of the coal-measures is about thirty miles. In an east and
west direction a like relation is known to exist from the meridian of
Namur to that of Lille, or from eighty to ninety miles, whilst the
trough-shaped arrangement of the coal-strata, in both directions as
towards Liége and Lillers, leaves no doubt whatever that this rise of
the older groups in the north has a much greater extension than
what is here assigned to it.

A restoration of this palzeozoic surface is given in the accompany-
ing map (Pl.I.). If, in conjunction with this representation, a line of
section should be drawn from the summit of the Ardennes across the
whole series, it would present a plane surface, with a uniform slope
northwards descending from an elevation of 2000 feet to somewhat
below the sea-level. Of this surface every part stood in a like rela-
tion to the secondary formations; or, in other words, at their periods
the palzeozoic group north of the coal-band must have had an eleva-
tion equal or nearly so to that on the south,—it must have been part
of the same raised area,—and it must have received its relative depres- ~
sion subsequently to the secondary period and synchronously with
the overspread of the nummulitic group. .

By means of the well-defined boundary-line of the oolitic forma-
tions of the Germanic area, we can extend this old paleeozoic surface
further north; and, guided by the lines of the coarse infra-liassic
conglomerates of Malmédy and Stavelot, we may infer that at this
early period the northern mass then had, relatively with the Ardennes
range, a somewhat higher level: the island of Heligoland, distant
about 300 miles north of the localities here in question, being the
nearest spot at which we are certified of the existence of any infra-
liassic strata* ; and where the lower beds, consisting of sands, indi-
cate shallow-water conditions at that time.

Tue BouLonnals.
I have elsewhere shown+ that the middle and upper palzeozoic
* Beitrage zur geognostischen Kenntniss des Norddeutschen Tiefland, von

Otto Volger.
tT Quart. Journ. Geol. Soc. vol. ix. p. 244.

7

48 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

series of the Boulonnais district present the clearest evidences of
great variations in the depth of the sea in which their several com-
ponent sedimentary beds were formed ; and that the sea-bed at several
successive periods had become terrestrial surface ; yet for all this,
such movements had not produced any sensible unconformity between
different parts of the series. To this it may be added that the re-
currence of a terrestrial vegetation in parts of the series where it is
not usually found,—as first beneath the Ferques limestone, next in
the yellow sandstone above, and again subordinately to the mountain-
limestone,—would indicate, that such local phenomena must have
been dependent on the permanent presence of an area of dry land, at
no great distance and throughout the whole of the middle and upper
paleeozoic periods ; such an area could not have found place to the
east of the Boulonnais; and, for reasons which will more fully appear
in the sequel, it may be fixed somewhere to the west, within the space
now occupied by the English Channel,—an extension of that mineral
axis which on other considerations has been shown to have occupied
the lower extremity of that area.

FrANCO-BELGIC SECTIONS.

In the Bellignies section, distant about 100 miles to the east of
that of the Boulonnais, there is a ike concordance, extending down to
the sandstone and conglomerate group which underlies the Stringoce-
phalus-limestone ; and a like general concordance holds true over the
whole area from the Ardennes to the Belgian coal-field.

In the Pepinster section the series is a continuous one from the
slates in the neighbourhood of Spa up to the highest portion of the
coal-measures.

The Eifel series is again in perfect sequence from the Goniatite-
shales, above the great calcareous group, down to the slates of the
valley of the Lieser.

It was at one time supposed that the slates of the north-east of the
Ardennes, as from Spa to Stavelot and Viel-Salm, which are un-
doubtedly of great antiquity, were unconformable beneath the series
of the Pepinster section; but no such unconformity exists, nor are
the lowest strata there older than the slate-rocks of the Middle
Rhine (Coblentzien of Dumont).

The first question which arises out of these consideration is,
whether the Stringocephalus-limestone, and its equivalent beds in the
valley of the Vesdre, at one time formed a continuous mass with the
Eifel series. An examination of the conglomerate beds which extend
from Malmédy to Stavelot is conclusive on this point. The materials
of this conglomerate have been derived either from the Eifel limestones,
or from the red arenaceous beds which next underlie them,—all the
Eifel species might be collected out of it. The condition of the
rolled corals shows that the limestone masses from which they have
been derived more resembled such as occur on the Eifel side of the
Ardennes than on the Belgian, consisting of friable beds, from which

AUSTEN—EXTENSION OF THE COAL-MEASURES. 49

the included fossils would be easily separable, rather than of the com-
pact flat-bedded limestones of the valley of the Vesdre. The destruc-
tion of such beds as those about Stadkyll and Gerolstein would pro-
duce just such a conglomerate as that of Malmédy.

If then we restore the whole of this area to its original position,
we find, with reference to submarine conditions, that the Stringoce-
phalus-limestone group on the Hifel side presents a great development
of marie forms which lived there, whilst they diminish in the direc-
tion of the Vesdre beds, and it is also in this direction that the
mineral character of the limestone group changes, and passes into
shales,—this takes place from south to north.

The distribution of sedimentary matter being dependent on the
moving power of water, and on the specific gravity of the materials
moved, such conditions as those here indicated inform us that the
land side of such an area of water must have been to the north of the
group of deposits in question.

Again in the next subjacent group—that of which the conglomerate
of Burnot forms a subordinate part, we meet with the clearest evi-
dence of its relation to an old coast-lme. The whole mass of this
conglomerate is littoral shingle or gravel: along the valley of the
Vesdre, it is some twenty feet m thickness: it is somewhat less in
the wood of Stanu: in the Kifel country it has lost its marginal
character and become a sandstone,—a change which marks the out-
ward extension of the sea-bed to have been for this zone what it was
for the limestone group—or from north to south.

With reference to the Bellignies section, the differences which this
group there presents consist in the greater coarseness of the materials
of the Cailloux du Diable, together with a greater thickness of the
conglomerates and sandstones ; where it rises again to the south, near
Mondrepuis, its composition is not so coarse, being made up of small
lenticular shingle, with thick beds of coarse sands. This conglomerate
band again rises on the north of the Mons coal-basin ; the distance
between these extreme points gives forty miles for the width of the
zone of marginal sea-bed here ; as in former instances, the gradation
in composition shows that the passage from coarse to finer sea-bed
takes place from north to south.

Lastly the extension of a mass of shingle along a line 120 miles in
extent, from near Valenciennes to beyond Eupen, is wholly in-
explicable except under the supposition, that it marks the direction
of old marginal and submarginal! zones of sea-bed.

The limestones of the right bank of the Rhine, near Dusseldorf,
are a prolongation of those of the valley of the Vesdre, and indicate
similar conditions ; but in the underlying group the conglomerate
band disappears, and is represented by a sandstone series. The
interval of the valley of the Rhine may be taken at about 35 miles,
so that in a north-east direction there is a mineral change such as
takes place in the south-east.

The line along which these data have been taken, and which
trends irregularly east and west, shows with respect to certain beds,
of which the mineral character affords definite indications, that at

VOL. XII.—PART I. E

50 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

one part the coast-line must have been much nearer than at the other,

and that, if we take the distance from Boulogne to Hirson at 300
miles, the middle portion of it is that which answers to such a
position.

There are other considerations, should the foregoing not be deemed
altogether sufficient, which bear out the inference that the coast-line
to which these shingle-beds were subordinate lay to the north.

The only test as to whether any zone of an old sea-bed is complete,
is the form of section it gives when measured at right angles to its
greatest direction, such direction being always in certain parallelism
with the coast-line. The littoral zone, commencing with the highest
marginal beds, parts gradually with its well-known characteristics,
and passes into the next lower zone of sands: in like manner the fine
earthy sediment forming clays and shales is succeeded by that of
lighter calcareous matter, and which from its specific gravity is
capable of thickening out over wide areas, so that all geological
groups, with a like mineral composition, when so measured, are
found to be great lenticular masses: and such is the form of the
Belgian subordinate bands.

It has been shown that the broad range of the Ardennes acquired
an amount of relative elevation at some time after the completion of
the series above the Eifel limestone: it could not therefore have been
in a position to have furnished any of the materials towards the under-
lying conglomerate or shingle group ; and, as this zone is a perfect one,
the source of its materials must necessarily have been on the north,—
a view which is further confirmed by the character of the materials
which form the shingles and which enter into the composition of the
middle and upper paleeozoic sandstone groups.

So much of the palzeozoic series as is to be seen north of the
Belgian coal-field is nowhere of greater age than the middle Rhine
beds; the sandstones which are subordinate to the Eifel (Givet) lime-
stone, those of the next higher group with Cucullea Hardingii and
C. trapezium, those associated with the Boulonnais coal, and with our
dark millstone grit series, all imply the synchronous existence of wide
subaérial areas composed of crystalline micaceous rocks, as well as
hardened and mineralized sedimentary ones. No such mineral masses
occur along the axis of the Ardennes or Hundsriick ranges ; and it is
only on the north, therefore, that they could have found a place,
where they may reasonably be supposed to have risen from beneath
the old rocks of Hal and Jodoigne.

. This old terrestrial area was a southern extension of the Scandi-
navian range: portions of it became depressed or broken down at
definite geological periods ; but subsequently to early paleeozoic times
it exhibited a salient mass, on either side of which the middle groups
had their limits (Upper Silurian and Devonian), and the existence of
which in parts can be traced upwards far into the tertiary period.
The area over which the erratics of Western Europe (Germanic area)
are distributed, conforms to this extension of the Scandinavian range.

Along the Ruhr the true coal-measures have a visible breadth of
at least sixteen miles; they have, however, a much greater real one

AUSTEN—EXTENSION OF THE COAL-MEASURES. 51

inasmuch as they dip away under the cretaceous series of Westphalia,
—beneath which they are worked,—they have a considerable width
beneath the sands of Aix-la-Chapelle, but from this point they con-
tract rapidly. This diminution across the Belgian area is not owing
to any falling off in the thickness of the component beds, but results
from the complicated folding of the masses, whereby they are caused
to assume a deep trough-shaped arrangement, accompanied by an
endless succession of zigzag folds. This part of the Belgian coal-
band, if restored to its original horizontal position, would occupy
more than four times its present surface-breadth.

From the expansion which the mountain-limestone takes west of
Mons, it is evident that the whole series expands again ; from which
it may be inferred that the coal-measures beneath the chalk of the
north of France will be found to have wider dimensions than has
been generally supposed: that such is the case is already indicated
by the extent which they have been proved to have west of Bethune ;
and it becomes an important consideration as to their western ex-
tension.

All dislocations of the earth’s crust having been produced by the
action of some force acting in the plane of the disturbed beds, such as
that of contraction, any movements producing ridges such as those
of the Rhenish-Ardennes System would be attended by the greatest
amount of dislocation at any point where it had a pre-existent trans-
verse range.

Such are the considerations by which we are enabled to sketch out
- some of the earlier physical arrangements of Western Europe.

Tur CARBONIFEROUS SERIES.

§ 1. Old Red Sandstone.

An early condition of the surface of part of the European area at
this period is very clearly indicated by the arrangements and com-
position of the typical Old Red Sandstone formation.

Much confusion in the chronology of geological changes has been
caused by the reference of this formation to the marine series. If
due weight be allowed to the facts of an accompanying terrestrial
and fluviatile vegetation, to the occurrence of the genus Cyclas,
together with air-breathing oviparous quadrupeds and. terrestrial
Chelonians, the early suggestion of Dr. Fleming, though based on
other considerations, will surely be adopted; and the Old Red
Sandstone of Scotland will be referred to the lacustrine series of
formations. The “ Old Red Sandstone” Fishes offer a subject well
worthy of special treatment, with reference to the conditions of the
area of water in which they lived; but the conclusions would pro-
bably be m accordance with those of Dr. Mantell *—that these con-
ditions were such as those of the Lepidosteus and Polypterus.

Of the three divisions into which Sir R. Murchison divided the

* Quart. Journ. Geol. Soc. vol. viii. p. 108.
E 2

52 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. »

‘**Old Red Sandstone”’ series of the Welsh area, the lowest or “ Tile-
stone group,” which alone contains the remains of marine forms, has
been since very generally referred to the “‘ Upper Ludlow” deposits.
The two higher divisions alone represent the typical “Old Red
Sandstone ;” of these the argillo-calcareous or “ Cornstone’’ group
contains just such an assemblage of Fishes as is met with in the
paleeozoic fluvio-lacustrine deposits of Scotland ; whilst the upper or
“conglomerate and sandstone group,” which as yet has only afforded
the remains of a Holoptychius, includes somewhat abundantly the
spoil of a terrestrial surface. On such considerations the “‘Old Red
Sandstone”? of Hereford, Monmouth, and Somerset becomes the re-
presentative of another freshwater area, the relation and extent of
which are indicated in the accompanying Map (Pl. 1.). Had not
the true character of these two peculiar assemblages of depositions
been misapprehended, the creation of a ‘“‘ Devonian System”? would
not have been needed.

We as yet possess very little detail respecting the so-called ‘‘ Old
Red Sandstone” of the Irish area: from a short communication on
the South of that district by Messrs. Jukes and Salter *, we learn
that the “Old Red Sandstone”? is overlaid by the ‘ Yellow sand-
stone”? group, and that the two form one continuous series, charac-
terized throughout by the remains of a terrestrial vegetation (Knorria,
Stigmaria). It is in this series that the large Anodons (dnodon
Jukesit, Forbes) occur both on the north near Thomastown and on
the south near Cork, together with the remarkable Fern-like plant-
remains (Cyclopteris Hibernica, Forbes) ; whilst no marine forms
whatever have been met with either in the ‘‘Old Red Sandstones,”’
or the ‘‘ Yellow sandstones.” Such being the case, we have satis-
factory indications of a third fluvio-lacustrine deposit, of wider di-
mensions than those of the Welsh and Scotch areas, but yet hardly
equalling in extent the larger members of the great lake group of
North America.

The lacustrine formations of Ireland are everywhere overlaid by a
great detrital series of marine origin, and containing the assemblage
of carboniferous forms which occur in beds beneath the Mountain
Limestone of Pembrokeshire, in the sandstones of Marwood, and in
like sandstones in the Boulonnais+. Messrs. Jukes and Salter
notice a very interesting fact with respect to the series above the
“yellow sandstone” (which they have termed the ‘“ Coomhola
grits’), which consists in its unequal thickness from EK. to W.; so
that, whilst in the E. it may be taken at from 50 to 60 feet, it has
been estimated at 5000 feet in Bantry Bay. We know from this
that the depression which brought the marine series over the lacus-
trine one was accompanied by a greater amount of depression on the
W. than on the E.,—a fact which is further supported by other
considerations.

The lacustrine ‘ Old Red Sandstone”? of Ireland everywhere over- —

* Meeting of Brit. Assoc. 1855.
+ Quart. Journ. Geol. Soc. vol. ix. p. 231.

AUSTEN—EXTENSION OF THE COAL-MEASURES. 5

lies a surface of “ Old Silurian” rocks: the two are unconformable,
and the older had already undergone those changes which imparted
to it its present mineral character, at some time anterior to the newer
formation, which has in fact heen mainly derived from it. Again,
the Irish area does not present that assemblage of marine forms
aes is known as “‘ Upper Silurian,”’ nor yet a true “ Devonian ”’

r ‘‘Kifelian”’ fauna; so that from these combined considerations
we are justified in the inferences—Ist. That the Irish area was
wholly included in that movement of elevation which effected the
olden Siluro-Cambrian sea-beds ; and, 2ndly, that it became a terres-
trial surface anteriorly to the oldest carboniferous depositions.

Lacustrine formations imply subordination to areas of land: with
respect to the Irish area, the extension of this land was to the north
and west, and as in all cases the extent of the lacustrine area may be
taken as a fair measure of the terrestrial surface from which it was
supplied, that land must have had great expansion, or elevation, or
both.

The limits of the lacustrine Old Red Sandstone of the Welsh
area are tolerably well defined ; they hardly extended as far north as
ordinary geological maps now carry that group, inasmuch as the red
beds which underlie the coal-measures of Coalbrook Dale belong to
the uppermost Ludlow beds, with Lingula cornea, &c.

In the South Staffordshire coal-district, and which may be taken
as an extension of that of the Forest of Wyre and Coalbrook Dale,
the coal-measures rest immediately on marine Silurian strata; and
this relative position, to the exclusion of any Old Red Sandstone, is
continued as far as Charnwood Forest, where the coal-measures rest
on some of the oldest portions of the Palzeozoic series.

This old ridge, which is thus clearly defined as to range, if not to
its full former extent, was a limiting barrier to the “Old Red Sand-
stone,” and a parting barrier to two areas of typical Mountain Lime-
stone ;—considerations which clearly indicate very early terrestrial
conditions in this direction ; or else that it was placed out of the
reach of the depositions of that time, from another set of considera-
tions, to which reference will be made in the sequel.

There are traces of “‘Old Red Sandstone” at intermediate places
between the two great areas of Wales and Scotland ; and these are
of interest, as they indicate with equal clearness an immediate sub-
ordination to a terrestrial surface. The little patches which are
dotted along the eastern skirts of the mass of the old slate moun-
tains of Westmoreland and Cumberland are in every case so closely
related to the rocks of the particular locality, as to suggest that they
are the alluvial beds of the ancient valley-courses of that region.
A like local relationship, as was long agd observed by M. Boué*, is
to be traced along the whole of the junction-line of the “Old Red
Sandstone of Scotland;’’ and here the accumulation often parts
with its character of water-rounded conglomerate, and assumes that
of the angular talus so common in subaérial detritus.

* Géol. de l’Ecosse.

54 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

We cannot trace the true ‘“ Old Red Sandstone” of the English
area further S. and E. than Frome; and all that we can ascertain
with respect to its boundary-line in that direction is derived from
the consideration that it there consists of beds of rounded conglo-
merate,—or of a marginal character,—and that it does not appear in
Normandy, where the true coal-measure series rests immediately and
unconformably on the oldest slate-rocks of that country*. We
may hence deduce, Ist, that the.boundary-line coincided with, and
was dependent on, the general direction of the land of the line of
the Channel axis, whilst the character of the conglomerate itself
about Frome would show that the line was not very remote.

Here, and before the remaining portions of the Carboniferous
series are noticed, it may be as well to state that geological history
viewed largely presents throughout a frequent recurrence of two
distinct orders of change, dependent on cosmical laws, of the very
nature of which we can as yet form but vague conjectures. Of
these changes, the one consists in the formation at definite times of
elevations and depressions of the earth’s crust, and hence of definite
geographical areas, of which we can in most instances determine,
even now, the main physical features: with respect to this order of
change, the direction in which the forces have acted would seem to
indicate contraction of the earth’s crust. At periods intermediate
to these we have evidence of a process of adjustment, whereby areas
co-extensive with great zones, or even hemispheres, of the globe
have been brought into conformity with the oceanic level; and
during which times marine deposits of wide range have been brought
unconformably over all preceding conditions of surface. In both
eases the progress of change was gradual. The line of demarca-
tion between the two distinct Lower Silurian assemblages becomes
one of absolute separation between the areas of the Upper Silurian
and Devonian faunas. The Mountain Limestone and its equiva-
lents, on the other hand, represents for the Paleozoic period both
the greatest amount of expansion, and the greatest uniformity with
respect to its included fauna ;—its relations to the deposits of the
great Paleeozoic périod are just what those of the Chalk and its
equivalents are to the Cretaceous. It is by this law of physical
change that we should be mainly guided in determining the minor
equivalents of the geological scale of depositions.

In this way the several groups of “Old Red Sandstone” take
their places as subordinate to an area of dry land, and as evidences of
the positions and extent of the depressions of its surface: and inas-
much as the geological scale is one of successive sea-beds, the forma-
tion must be considered as hors de série, and be placed on a parallel
and equivalent one; thus holding, with reference to the lower and
upper Palzeozoic formations, a position which corresponds with that
which the Purbeck- Wealden series does to the Oolitic and Cretaceous
groups.

* Proc. Geol. Soe. vol. ii. p. 2.

AUSTEN-——EXTENSION OF THE COAL-MEASURES. 55

By placing the so-called independent formations or systems—
the “Upper Silurian” and ‘“ Devonian’”—as equivalents one of
another, the “Old Red Sandstone” of the British area becomes
disentangled from relationships which are wholly without the sup-
port of fossil evidence, and inconsistent with the progress and nature
of the physical changes of the Mid-Paleozoic period over Western
Europe.

§ 2. Mountain or Carboniferous Limestone.

No definite geological group, limited by mineral uniformity, can,
by itself, be the representative of a period of time; this considera-
tion has, however, been too often lost sight of; and in this way the
“Old Red Sandstone”? has been made to precede the Mountain
Limestone, and each has been taken to indicate distinct periods.

The West-European area of typical Mountain Limestone—that
over which it presents the largest dimensions, where it is less sub-
divided, and purest,—admits of most precise geographical limitation.
It is mcluded within an elliptical space, which may be represented
by a line drawn from South Wales, through Somerset and Belgium,
into Westphalia, and thence, through Hanover, back into Derbyshire.
This was dependent on one hydrographic basin. Ireland presents
another, and the Russian area a third. All these are synchronous
with one another, though very unlike in the sequence and compo-
sition of their subordinate beds. It requires but a very trifling
acquaintance with the law of change in the composition of sea-beds to
lead to the conclusion that the Mountain Limestone presents the ex-
treme outward depositions of waters charged with calcareous matter ;
whilst outside and beyond the area thus defined, it will be found to
put on characters the significance of all which is equally clear. One
definite form ever implies every other modification of sea-bed: in
this case the Mountain Limestone serves to mark the central por-
tion of an enclosed sea, around which must have been grouped
every other gradation of detrital matter up to marginal sand and

ravel.
: Prof. Phillips was the first to call attention to the change which
the Mountain Limestone series undergoes from Derbyshire into York-
shire, and how also, by taking three distinct sections ranging some-
what §. to N. within the latter county, it could be plainly seen,
that the group was constantly parting with its mdividuality from
below upwards, by the substitution of earthy detrital beds for cal-
eareous ones. This process is continued on into Northumberland,
where the whole of the Great Scar Limestones become represented
by an endless alternation of shales, limestones, sandstones, and coal.
Whoever will carefully follow out the process of change presented
by the Carboniferous series from our midland counties into Scotland
will readily satisfy himself that it must be viewed as a synchronous
whole,—that there is no descending order,—and that such a suppo-
sition, if fully set forth, implies a set of physical impossibilities, on
which, however, we have not space here to enlarge. The Carboni-

06 ‘PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

ferous series of Berwickshire is not older or inferior to the Mouritain
Limestone, but is its representative in a zone more nearly subordimate
to the terrestrial surface of the time; such are also the calciferous
grits of the Mid-Lothian district. The coal-growths alternated with
every portion of these depositions, with the exception of those of
some extreme depths; but even with respect to these, we see, as in
the Boulonnais, that the continuity of the pure Mountain Limestone
series was there once interrupted, by its elevation, first into the sand
zones of the time, afterwards into subaérial conditions*, followed by
a return of that surface to the region of pure marine calcareous
deposits.

The area of pure Mountain Limestone has really a somewhat
greater extension southwards than as above indicated: this is a con-
sideration of some importance, masmuch as every portion of this area
of sea-bed appears ultimately to have been brought up into those
conditions by which it became covered by coal-growths. The line
through Belgium must be made to include the district of the Con-
dros, and that known as “‘ entre Sambre et Meuse.’ The Carboni-
ferous series which thence passes beneath the Cretaceous beds of the
N.E. of France is very extensive, and it is obvious that the calcareous
mass of Berlaimont, conformably with the structure of the region to
the east of it, requires considerable extension and expansion, perhaps
equal to that presented in the Meuse section about Dinant ; if so, it
is not impossible but that some coal-beds may exist in the direction
of Loquinol.

Tournay is the most N.W. point at which the Mountain Lime-
stone is exposed in the Belgian district; but, as will be seen by the
Map, it has a considerable spread beneath ; it was found immediately
below the chalk at and north of Lille, and it ranges thence to some
point between Cassel and St. Omery.

The massive character of the Carboniferous series in the Boulon-
nais, as it passes under the Oolitic deposits, west and south, indicates
continuity in those directions: in like manner we may feel sure that
the Mendip limestones are continued south and east from Frome ;
so that the Mountain Limestone area may he safely carried beneath
our own S.E. counties across the eastern end of the Channel, and so
into Picardy ; but as such, it nowhere reappears from beneath the
secondary formations round the great depression of the Paris basin.

This mere sketch may perhaps suffice ; and without troubling
ourselves with the progressive changes in the distribution of the
areas of land and water during the Middle and later Palzeozoic periods,
or without overlaying the suggestions of the present communication
by the mass of detail by which we may ascertain what the geogra-

* Quart. Journ. Geol. Soc. vol. ix. p. 243.
+ See the Memoir of M. d’Archiac, Etudes sur la Formation Crétacée, &e.,
PP. 118 e¢ seg., in Mémoires de la Soc. Géol. de France, 2 sér. vol. ii.

t The object of the present paper is to point out lines along which coal may
possibly be met with. The more speculative points will form the subject of an
“Inquiry into the Physical Geography of the Paleozoic period, ” which will
shortly be laid before the Geological Society.

AUSTEN-——EXTENSION OF THE COAL-MEASURES. 57

phical arrangements of those times were, most of which, however,
will be found indicated in the accompanying Map (PI. I.), the
following may be taken as an outline of the geography of Western
Europe at that early time.

Outline of the Geography of Western Europe at the Coal-growth
Period.

The central gneissic plateau of France was then a terrestrial area,
supporting a rich coal-vegetation, with ranges of hills which must
have had considerable elevation, and lines of valley of which we can
still determine the directions, occupied by lakes and river-courses.
The great linear depression of the Rhone had not then been effected.
This area extended S. and E., so as to be connected with the old
land of the Department of the Var*. Over all this tract there is to
be observed a remarkable uniformity in the conditions under which
the coal deposits have been formed, as well as in the drifted vege-
tation: it may be characterized as the “upland facies” of the Car-
boniferous period.

The Coal-measures here occupy depressions, which were such at
the time of the coal-growths; the lowest beds consist of distinct
subaérial detritus and alluvia, of which all the materials have been
derived from the slopes immediately adjacent: the coal-seams, in
their great depths, as compared with their extent, indicate the vast
periods of uninterrupted growth of vegetable matter, and contrast
strongly with the frequent alternations common throughout those
deposits, which we know, from the subordinate beds, must have been
formed at the sea-level. Lastly, in the peculiar Fern-like forms
(Cyclopteris, Odontopteris) which so abound in the sedimentary beds
and drifted sands of these basins, we have the indications, not of a
different period of vegetation, but merely that of the higher regions
of the district. Although the Coal-strata are now compressed, by
the contractions which have effected the whole of this old central
region of France, yet all these distinct features, as to the original
arrangements of its surface, are sufficiently distinct. This district
is moreover interesting, as it is one of those which ante-dates the
period of the carboniferous deposits, and which must have served
during that long lapse of time to renew the vegetation over that
endless succession of submerged and terrestrial surfaces which the
lower levels present. |

The extent of this old land must not be estimated by what has
been designated above as the Central gneissic plateau, as that is now
circumscribed by the secondary group of depositions ; because these
last have been brought by a process of overlap, and unconformably,
over these former terrestrial surfaces: nor must the present character
of the surface be taken as a guide as to its original inequalities ; for

* Mém. de la Soc. Géol. de France, 2 sér. vol. iii. p. 315; also Explication dela
Carte Géologique de France, p. 470.

58 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

whether from local elevation, or from climatal conditions, there are
certain appearances over the whole which imply that at one time the
temperature must have been very low, as glacier-action can alone
account for the presence of the large angular blocks which occur in
the lowest detrital beds of many of the Southern coal-basins.

This central district of France was continued, and connected by
means of the Hastern Pyrenees, with the old land-surface of the
Spanish Peninsula.

In the Vosges mountains we find two distinct levels of coal-growth
surfaces; one immediately beneath the Vosges sandstone, but un-
conformable with it, and belonging to the great Coal-measure
period, or that of the widest range of terrestrial conditions; the
other subordinate to the slate and limestone series there, and not in
conformity with the higher group: this last may perhaps be of the
age of the anthracitic seams in the Devonian or Kifelian series, in
places contiguous to the land-surfaces of that time, as in Devonshire,
the Cotentin, and the Boulonnais*. ,

The present depression between the Vosges and Schwarzwald
ranges is of very recent date: anterior to this they constituted one
group, which comprised the Odenwald in its extension northwards.

No marine remains have as yet been discovered in the Saarbriick
coal group, nor in its extension towards Mayence; whilst the terres-
trial forms which it is constantly affording, as well as the aspect of its
sedimentary beds, give it all the essential features of an old lacustrine
group,—an internal land-locked area,—of which the deposits have
been accumulated over the edges of disturbed older Palzeozoic strata :
it has much of the character belonging to the estuaries or deltas of
rivers carrying down great quantities of sand, and the cross-bedding
which these beds now present suggests that the current was to the
S.W., or that the area opened out into the sea in that direction.
The great extension which is now being given to the Coal-measures
beneath the plain of Lorraine points to the existence of a belt
ranging in one direction towards the Vosges, and in the other towards
Luxembourg. ;

Across the ranges of the Hundsriick and the Ardennes, the great
Belgian coal-band presents very different relations to the underlying
formations ; it is in ascending sequence, offering the fullest and clearest
succession of the Rhenane (Devonian) and Carboniferous groups, and
resolving itself ultimately into a vast assemblage of earthy sedimentary
strata, which alternate almost indefinitely with terrestrial surfaces.
The evidence of this stage of conditions is preserved along a trough
more than 150 miles in length, and of singularly disproportionate
breadth. The abundance of shells of the genus Unio, at various
levels, and overlying the coal-bands, would seem to give a fresh-
water character to the whole series, but for the occasional intercala-
tion of beds containing Orthocerata, Goniatites, Aviculopecten, such
as occur in our own Yorkshire series, but which in Belgium range
from the Alum-shales, or the base of the Coal-measures, at occasional
levels, upwards.

* Mémoires pour servir, &c., par MM. Dufrénoy et E. de Beaumont, vol. i.

AUSTEN——EXTENSION OF THE COAL-MEASURES. 59

Combining these features and conditions with those presented by
our own Northern, Midland, and Southern Coal-measure series, we
arrive at the relative positions of areas of land im various quarters,
and which, if taken in conjunction with the extent which has been
assigned to the Scandinavian range, define the boundaries of an
internal sea, around and occasionally over large parts of which
the peculiar vegetation of the time was developed and entombed as
the area rose and sank. A region with a central depressed area,
such as Australia is supposed to present, and going down, by means
of a long series of oscillations, would ultimately present just such
an assemblage of deposits as our own Carboniferous group.

B. Axis or ARTOIS.

In the physical topography of the old County of Artois there is a
linear ridge, which, commencing at the S.H. extremity of the Bou-
lonnais denudation, extends in a direction S. of Arras (W. 34° N.):
its highest points are a little 8. of Desire, the hill north of Senlecques,
and near the windmill on the road from Boulogne to St. Omer, about
two miles beyond the village of Escouilles, which reach nearly 700
feet : thence the line may be drawn by Bellevue, 616 feet, Coupelle
Neuve, Crépy, Fiefs, 609 feet, Sains, Tangry, Valhum, Aulin, Orlen-
court, 550 feet, to the E. of Tinques, and then S. by Pénin to Grand
Rullecourt, 543 feet, the altitudes decreasing from N.W. to S.E.;
nor does it cease near Arras, but trends away with a rather more
southerly direction towards St. Quentin. On one side, the Lys, the
Scarpe, the Scheldt, and other streams take their rise and flow into
the North Sea. On the other, the Canche, the Authie, and the
Somme discharge into the English Channel. It will also be seen

_ by reference to the map that the physical structure of the whole

district as far as the Valley of the Seime is in strict parallelism with
the line of Artois. |

In 1845, M. d’Archiac, in a memoir already referred to, pointed
out the influence which a line, coinciding with that of the axis of
Artois, had had on the character and limits of the Middle and Lower
Cretaceous deposits. The most remarkable point connected with this
axis was noticed by Monnet as far back as 1780*, who showed that
along a line which lies a little to the north of the watershed the
Chalk had been fissured, so that traces of the old world (Paleozoic
strata) were to be seen in apposition with the new, as the Chalk was
then considered.

If any relation can be traced between the lines of disturbances and
fractures presented by the uppermost strata along the axis of Artois
with those which have happened along the same line at times long
antecedent to the formation of such overlying strata, and if this
repetition can be referred to a necessary law, then the surface-struc-
ture throughout such lines becomes a serviceable indication of that of

* Description Minéralogique de la France, Atlas, pl. 3.

rei

60 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the older subjacent series: in this way our own Wealden area, as
well as the districts around it, may be made to indicate the arrange-
ment of the Paleeozoic strata beneath.

The district of old sedimentary strata which bounds the coal-band
of Belgium on the S. from Aix-la-Chapelle westwards gradually sub-
sides and disappears beneath the Cretaceous series of deposits along
a line from Valenciennes to Hirson, which runs somewhat transversely
to the direction of the old range. This feature is due to a subsidence
of post-cretaceous date, for the continuity of the coal-band is in no
way affected by it ; and, though the symmetrical form and direction
of the trough are disturbed at Valenciennes, the phenomena which
the workings present there are just such as would be caused by the
passage of a line of fracture and flexure. Whoever has examined the
line along which the old series disappears from Quievrain south, must
feel satisfied that all the folds which it presents in the district
‘entre Sambre et Meuse”’ are continued on beneath the Lower Ter-
tiary and the Cretaceous series of the adjoining part of France.

Subsequently to the formation of the folds or undulations here
imparted to the Devonian and Carboniferous beds, the surface of the
district became worn down, by a process for which it would be diffi-
cult to account or explain; and this took place prior to the super-
position of the Cretaceous series. This appearance is met with again
in the Boulonnais, with this difference only, that the Oolitic deposits
there rest on the tabular surfaces of the folded Palzeozoic series.
English geologists are familiar with a like form of surface, with rela-
tion to the Oolitic series about Frome.

The form of the area in which the Carboniferous series was accu-
mulated has already been indicated. The position of the coal-measures
on the S. of the Hundsriick, where, in a trough parallel to the chain,
they rest unconformably on Devonian or Rhenane strata, shows that
the broad series of undulations which, commencing with the Hunds-
ruck, are carried on through the Hifel and the Ardennes, the Condros ~
and down into the Belgian coal-basin, must have had their origin on
the S.E. before the commencement of the Carboniferous deposits on
the N.W., the consequence of which is that over the French portion of
the Carboniferous area its deposits are found resting unconformably.
This transgressive passage of the uppermost portions of the Palzeozoic
group over the lower from N. to S., and which probably determines
the condition and age of the beds ranging beneath the great Paris
basin, is altogether distinct from the causes which have produced the
arrangement of old surface beneath the Chalk axis of Artois.

The valley of the Meuse from Liége west presents a line of frac-
ture, along which beds of the age of the Devonshire shales and lime-
stones are brought to the level of the Coal-measures by great vertical
faults, or else narrow ridges of still lower portions of the series are
thrust up. It is owing to this that there is that want of uniformity
and regular succession on the S. of the Belgian coal-field, which is
to be observed on the N. This great line of disturbance can be
traced as far as Quievrain, and has been proved by the works of the
Valenciennes district. From this place the character of the older

AUSTEN—EXTENSION OF THE COAL-MEASURES. 61

strata is only known from the trial-shafts, sinkings, and other works
which have been now carried as far as Therouanne, along the course
of the coal-trough, beyond which point the existence of productive
coal-measures has not been proved. Numerous sinkings have, how-
ever, been made over the intervening area, ending with the Artesian well
at Calais, where the coal-measures were again met with. An account
of many of these sinkings will be found in M. d’Archiac’s memoir*,
from communications by M. Degous¢e. The results of these researches
will be found recorded on the accompanying Map, and it is evident
from these that the Mountain Limestone series westwards from
Tournay takes the same expansion that it does eastwards of that
place. At Houdain, on the S. side of the basin, older parts of the
series are in juxtaposition to the coal, whilst at other places the
limestone (either Carboniferous or Hifelian) intervenes, so that we
have quite sufficient to warrant the conclusion that the line of fault
and disturbance of the Meuse valley is carried on beneath the chalk
of Artois, and with like relations to the coal-band. By a careful
comparison of the rock-specimens obtained in the researches for coal
in the Department of the Pas de Calais, and which are preserved in
the offices of the several companies, the subcretaceous arrangement
of the Paleozoic groups could be accurately laid down; and such a
work would be a most important contribution to Economical Geology.

The character of the disturbance which ranges along the lower side
of the Franco-Belgian coal-band is, that where, by means of a vertical
fault, the coal-series and some lower portions are brought to the
same level, the dimensions of the coal are greatest, and where the
older series rises into ridges and anticlinals, the coal-band narrows :
this is simply the result of that levelling of the surface before alluded
to, which is so remarkable a feature of this line of disturbance, and
by which portions have been planed off in exact proportion to the
elevation they received : in this way the contraction of the coal-band
towards Therouanne is the result of the widening of the anticlinal to
the S.W. of that place, Here, on the line of greatest elevations of
the axis of Artois, the thickness of the chalk is least ; and where the
line of abrupt fault is most marked, as from Houdain to Lievin, the
mass of overlying tertiary strata is the thickest. The whole line in its
geological features and its structure is in strict agreement with the
underlying older surface.

Another feature which has influenced the contraction of the Car-
boniferous series in the direction of St. Omer is the rise and expan-
sion of the older Rhenane series south of and beneath the hill of
Cassel. ;

From such considerations we may infer that on the N. limit of the
Boulonnais denudation there is a continuation of the Carboniferous
and Devonian groups, by means of a great linear disturbance, as they
are presented in immediate relation to the great coal-band from
Valenciennes by Namur to Liége. This is the old axis of Artois;
and the date to which the production of this line must be referred is

* Mém. de la Soc. Géol. de France, 2 sér. tom. ii. p. 118 e¢ seg.

62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

some time subsequent to the accumulation of the uppermost coal-
measures ; allowing time too for the accomplishment of all those
changes in the beds of vegetable matter, as well as in the associated
strata, whereby they became converted into mineral coal and crystal-
line limestones.

This line of disturbance traversed the district of the coal-growths,
from E. to W., from the Boulonnais, far into the mid-European
area.

To those who adopt implicitly the notions of M. Elie de Beau-
mont as to the correspondence between the ages and directions of
linear disturbances, and as to the dependence of the obvious physical
features of the earth’s surface on such disturbances, it would be suf-
ficient that we should here point to the structure of the 8.E. portion
of England* to satisfy them that it belongs, in all its incidents, to
that band of flexures and disturbance which ranges from the Bou-
lonnais eastwards; and the presumption based on such external phy-
sical characters would acquire the value of a certainty, when, as at
Frome, the great sheet of Carboniferous Limestone, of the age of that
exposed in the Boulonnais, is seen to emerge from beneath the Chalk
axis with exactly the same relations to the Oolitic group, and having
the Coal-measures in convenient proximity to the surface on the N.

The study of the structure of the axis of Artois suggests thus
much, that there is a strict coincidence between the disturbances
which its oldest and newest sedimentary groups present: this is a
subject which might be extended to any length, both from its
importance in physical geology, and from the abundance of illustra-
tion which this particular line of country affords ; enough, however,
for the results of the present inquiry will suggest itself to any one
who can bring to this study of a good physical map a competent
knowledge of the geological structure of the country from the Rhine
to the West of England between the 50° and 52° N. lat.

, The general law seems to be, that when any band of the earthy
crust has been greatly folded or fractured, each subsequent disturb-
ance follows the very same lines,—and that, simply because they are
the lines of least resistance.

In this way, marked physical features in any region become un-
erring guides as to the character and extent of the earliest disturb-
ances which took place there :. the sharp axis of Artois is continued
across our area by the range of the North Downs and those of Hants.

There is this feature to be observed along the whole of this line, that
on the north limit of this ridge the beds dip suddenly and rapidly,
and hence a line of fractures, extending from near Arras to the E.
end of the Boulonnais, and from the N.W. point of the Wealden
denudation to the valley of Devizes. This relative depression on the
north has preserved the Nummulitic series (Lower Tertiary), just as
along the Franco-Belgian line the depression on the north was the
cause of the preservation of the great coal-trough. Applying this
consideration to the structure of our area from Kent into Somerset,

* See particularly Mr. Hopkins’s map in vol. vii. of Trans. Geol. Soc,

AUSTEN—EXTENSION OF THE COAL-MEASURES. 63

we may feel sure that a like arrangement of the older strata runs
from the valley of the Thames into that of the Kennet ; along this
line the coal-measures may be reasonably supposed to have been
preserved.

Guided by the old surface from the Boulonnais eastwards, it is
most probable that the breadth of elevated strata south of the above-
named line, presented such a series of folds as is now to be seen
“entre Sambre et Meuse’’ and in the Condros, and that this band was
much denuded. In this direction, however, from the Boulonnais W.,
the Carboniferous Limestone contains a subordinate coal-measure
series, and the Devonian group presents a like tendency beneath the
Ferques limestone.

To what extent and in what area the denuding process may
have extended over the surface of the Paleeozoic strata to the S. of
the line of Artois, both in France and Engiand, we have but few
data even from speculation : nor is the inquiry of much importance,
inasmuch as, should the coal-measures be preserved, they could only
be reached beneath enormous thicknesses of secondary strata. The
most favourable places for investigation would be points on the S. of
the Wealden denudation where the transverse valleys cut deep, and
where the Lower Greensand is much reduced in thickness locally.

The axis of Artois, though a most important feature in its limited
extent, is a portion then of a long line of complicated disturbance
extending from the western to the mid-European area, the detailed
history of which would be a most valuable contribution to physical
geology. In the present communication I have only sought to draw
attention to just as much as should show its age, its continuity, and
its prominence through long periods subsequent to its first pro-
duction.

C. RELATIONS OF THE OVERLYING SECONDARY FORMATIONS.

There are doubtless many areas beneath which the coal-measures
of our own country may be fairly presumed to extend, but which
could only be reached at such vast depths as forbid the prospect of
their ever being rendered available: this consideration suggests the
third point in the present inquiry, in which the great groups of the
geological scale younger than the coal-measures will be taken in
ascending order.

§ 1. New Red Sandstone. Permian or Triassic.

An enormous accumulation of conglomerates, sandstones, and clays
are interposed between the Paleozoic rocks of the West of England
and the lowest beds of the Oolitic group: it may represent in time
either the Permian or more probably the Triassic series, or perhaps
both. The local character of the conglomerate shows that it was
bounded on the W. by a terrestrial area. A like assemblage occurs
against the K. slope of the old rocks of the Cotentin and Calvados,

64 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

and contains much rounded shingle; but it has no great extent, as
the Oolite series of Calvados rests immediately on rocks of the Silu-
rian age. No beds referable to either of these formations are to be
found beneath the Oolites, from the Boulonnais as far as the valley
between the ranges of the Ardennes and the Hundsriick, near Lux-
embourg. The Triassic group passes EK. of the old land-surface,
along the valley of the Weser, where it rests on the coal-measures
near Osnabruck. Heligoland also presents characteristic Bunter-
Sandstein and Muschelkalk. There is therefore a large extent of
surface, ranging E. and W., over which beds of this age are entirely
wanting. Researches which have been made beneath the Chalk show
that it is wanting along a line of twenty-five miles to the N.E. of
Marquise ; and, as it is absent over the Mendip ridge, we may infer
that it stands in like relation to any line which may connect these two
points.

§ 2. Oolitic Series.

No beds of this age ever appear to have been deposited over an
area more than equalling the whole of England in extent, ranging
through eighteen degrees of longitude, from the German Ocean east-
wards, and with a breadth of four degrees of latitude, if not more ; for
it is difficult to determine to what extent the German Ocean area was
one of dry land at this period.

The Oolites of Yorkshire and Lincolnshire were dependent on a
land which lay to the east; and this consideration is of importance,
as far as antecedent geographical arrangements affect our present
inquiry.

From Tournay to Hirson, no beds of Oolitic age occur between
the Palzeozoic and Cretaceous formations. At Hirson, deposits are
met with which represent imperfectly any of our subdivisions of this
series, but which may be taken as the equivalents of the sub-medial
portion—from the Lias to the Cornbrash inclusive ; the whole being
much reduced in thickness, and overlaid unconformably by the Cre-
taceous group.

In the Boulonnais, which, though more than 100 miles distant, is
the nearest point at which the Oolite series again occurs, the lowest
beds are seen, as at Leulinghen, resting on Carboniferous Limestone.
The Oolitic group, as here exhibited, extends from the Coral rag or
Great Oolite up to the Portland beds; for here again, as at Hirson,
the grouping of the fossils is not so definite as in our 8.W. counties.
About Marquise, the oolitic beds set on with all the usual characters
of somewhat shallow-water conditions, and on a surface much worked
over by perforating animals: in all respects the conditions correspond
with those of the Department of the Aisne*, and showing that the
Oolitic series was limited and influenced at both places by a pre-
existing ridge of old strata. Beds of Oolitic age were wanting beneath
the Cretaceous strata in the trial-shafts at Tilloy and Monchy-les-

* D’Archiac, Mém. de la Soc. Géol. de France, tom. v.

—— eo

AUSTEN—EXTENSION OF THE COAL-MEASURES. 65

Preux, S.E. of Arras. This intermediate point gives an approxi-
mate outline for the range of the Oolite series beneath the Chalk of
the North of France ; and this, it will be seen, is parallel with the pre-
sent axis of Artois: we hence infer that the limitation of the Oolitic
group arose from the same physical barrier along the whole line.

Taking the two extremities of this line, there is this difference to
be observed, that whereas on the E. the series commences with the
lower and extends to the middle Oolites, on the W. it commences
with the middle and is continued to the upper.

In the Boulonnais the Oolitic group is brought up against the old
ridge here in question by a process of overlap, a circumstance which
indicates contemporary subsidence. On the E. the upper Oolitic
beds have been removed as they approach the ridge, and the surface
thus produced is overlaid by the lowest beds of the Cretaceous series :
or, confining ourselves for the present to the Belgic-French area, it
is clear that the destruction of the Oolitic surface commenced on the
E. before it did on the -W.; thus showing a movement correspond-
ing in order and results with what took place at a subsequent date
with respect to the Cretaceous beds.

The original limitation of the Oolitic group, and the subsequent
abrasion of some of its beds, were both dependent on a rise of old
Paleozoic strata, of which the trend, for one part at least, was in
conformity with the line of Artois; but this line, as we have seen,
was not then the mere ridge that it is at present,—it became an axis
by the subsidence of the tract which extended to the N., and this
took place gradually, during the course of more than one subsequent
geological period.

The line of the chalk axis of Artois can be prolonged westwards,
by means of like pheenomena of elevation and fracture, into the di-
strict of Bath and Frome: whether this line was throughout de-
pendent on the same early physical features, is a question which must
long continue matter of speculation: what is known is this, that the
relations of the Oolitic beds to the Mendip anticlinal are just such
as have been noticed in the Boulonnais; and further, that .the
Mendip anticlinal emerges from beneath, and is in continuation of,
the great axis of Secondary strata of the South of England.

The littoral limits of the Oolitic series on the N. were dependent
on the extent of that area of land-surface which, including portions of
Belgium, Holland, and the southern extremity of the German Ocean,
became narrower in its extension towards our own area; so that, if
we trace an imaginary line which shall fall in with the anticlinal at
Frome, it may possibly represent and complete the tract in ques-
tion; inasmuch as we know that such line represents a zoological
boundary—that on either side of which the Oolitic fauna puts on a
change: N. of this line the facies is Germanic, to the S. it is Nor-
manic*. |

These considerations suggest the probability that the Oolitic series
of depositions may be wanting over an area part of which is now

* Morris, Quart. Journ. Geol. Soc. vol. ix. p. 317.
VOL. XII.—PART I. F

66 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

represented by our S.E. counties, and along a line to the N. of the
Wealden denudation.

To what extent the Oolitic group may exist beneath the Wealden
and Cretaceous groups of Kent, Sussex, and Surrey, is a more difficult
question ; but, the continuity of the old ridge being granted, we may
infer that, relatively as to its breadth, it exercised along our area a
like influence to that it had along its continental course, and that,
whilst the ascending members of the group were brought up against
it by a process of successive overlap, as in the Boulonnais, so also
they were abraded and denuded from above downwards, as has hap-
pened there. We shall see reasons for assuming that such a con-
dition of surface existed, when noticing the composition of the Lower
Cretaceous sand-group.

§ 3. Wealden Series.

T suggested in 1850* that the so-called Wealden strata would be
found to be referable to two distinct geological periods of time,—the
Oolitic and Cretaceous ; and, apparently, from the movements which
took place in the Western European area at those times, the secondary
lacustrine series of the South of England corresponds with the
Upper Oolitic and Lower Cretaceous or Neocomian group, whilst to
the N. it may be the equivalent of older portions of the Oolitic
series.

In the course of an excursion into Belgium in 1852, together
with several members of this Society—the late Prof. E. Forbes, Mr.
D. Sharpe, Mr. Prestwich, and Mr. Tylor,—we were shown by M.
Dumont an old land-surface near Tournay, in an intermediate posi-
tion between the Carboniferous Limestone and the lowest Cretaceous
beds ; again, near Mons, we were conducted by Mr. Lambert to a
most striking instance of such conditions. Both these localities
occur in that area which was dry land during the whole of the Per-
mian, Triassic, and Oolitic periods. The evidence as to age from the
contents of these beds has not as yet been worked out.

The lowest strata exposed in our 8.E. counties belong to the
Secondary lacustrine series; of this, the portion known as Weald
clay may be seen on the W., as at Punfield, in Swanage Bay, to
alternate with, and therefore be synchronous with, the marine Neo-
comian group}. No Neocomian beds occur anywhere W. of Pun-
field whilst Wealden strata do; and, as freshwater formations imply
subordination to land-surface, it is clear that the direction in which
it lay must have been W. and S. at the time when that subsidence
was taking place which brought the Neocomian sea-group into the
area of the Wealden lake.

Some beds in the Boulonnais which immediately overlie the Port-

* Quart. Journ. Geol. Soc. vol. vi. p. 467.

t+ The evidences of this were brought before the Geological Society in 1850,
and I gave the fossils to the Jermyn Street Museum, it being the intention of my
friend the late Prof. Edward Forbes to have described them in his account of the
Purbeck and Wealden deposits.

AUSTEN—EXTENSION OF THE COAL-MEASURES. 67

land Oolite there, and which swarm with an obscure bivalve shell,
belong to the Purbeck series, so that the limits of the lacustrine area
are defined in this direction.

The occurrence of the Wealden Unio (U. Martini) through a con-
siderable vertical thickness of the Lower Cretaceous group of the
Department of the Haute-Marne points out the relative position of
the land at that time; and earlier still there were the Purbeck-
Wealden conditions, indicated by the fluvio-marine formation de-
scribed by M. Cornuel*, and which are a continuation of those to be
observed in the Boulonnais. Independently of this agreement
between two localities somewhat distant, there is also this, that the
deposits of iron-ore, which represent subaérial conditions, exactly
agree as to position, so that it is on such considerations that the line
of limitation of the Neocomian group has been drawn from the Bou-
lonnais in a 8.E. direction.

Some sections near Beauvais, which were particularly examined
in 1852 by the Members of the Geological Society above named
(p. 66), show an alternation of marine Neocomian with Wealden
conditions, such as occurs at Punfieldt. In this way the area of
Wealden conditions becomes defined ; being bounded on one side by
the old ridge of the axis of Artois, and its extension to the 8.E,; on
the opposite side by a land-surface extending from our own western
districts towards and across France (Seine Inférieure) in a line parallel
with the Pays de Bray. Its northern limit would @ priori have
been defined by the extension of the old axis of Artois; and, if we
may take the northern chalk-escarpment of our Wealden denudation
to represent the N. limits of that axis, then the Wealden deposits
cannot be expected much beyond that line: or the Wealden lake was
defined on the N. by the extension of that old land which, as we have
shown, existed from early times to the N. of Belgium and Holland.
It was the same tract which in part supported the Secondary lacus-
trine deposits of Hanover.

The place and form of the Wealden Valley become defined, as
does also the geological structure of the country around it; and it is
thus that a peculiarity in the composition of its beds is satisfactorily
explained,—all the Wealden sandstones and conglomerates point to
their having been derived from the spoil of crystalline and meta-
morphic paleozoic strata; and of this character would be all the
materials carried down by the streams from the old lands to the N.,
as well as from those of the Channel area.

The Wealden depression opened seawards on the 8.W.

The foregoing observations have reference to the probable abrupt
termination of the Wealden group on the N. Such a supposition
may perhaps appear unreasonable to those who consider only the
great dimensions of this series of depositions ; but such, however, is
the character of all the old lacustrine and many modern estuarine
formations with which we are acquainted: should time suffice for

* Mém, de la Soc. Géol. de France, tom. iv. pp. 229-290.
+ Topographie Géognostique du Dép. de l’Oise, par L. Graves; Lyell, Quart,
Journ. Geol. Soc. vol. vii, p. lix, 5
EF

68 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the filling-up of the basin of the Lake of Geneva by the detritus
brought down by the Rhone, that limited area would present accu-
mulations which in places would be nearly 1000 feet in thickness.

It is very desirable with reference to the present inquiry that we
should know what next underlies the Wealden group at some point
near the Chalk-escarpment of Kent. Though the thickness of the
Wealden group has been estimated at 1000 feet, such dimensions
do not constitute any difficulty ;—the elevation of the beds and the
emergence of the lowest strata, together with the deep valley-sections
of the Wealden area, are conditions which offer many favourable
points for such researches.

§ 4. Cretaceous Series.

On the eastern end of the axis of Artois, near Bellignies, the
Devonian or Eifelian series is overlaid directly by the Tourtia, an
accumulation of mid-Cretaceous age, and the fauna of which has been
fully described by M. d’Archiac*. 'This Tourtia everywhere under-
lies the Chalk along the axis of Artois, as may be seen at each of
the small denudations or fractures which the ridge presents ; it was
found near Arras, and occurs over the whole line of the coal-basin of
the Franco-Belgian frontier ; it is well seen near Tournay, and was
met with at Lille, as also N. of St. Omer. It is a conglomerate of
old crystalline and palzeozoic rocks, much water-worn, together with a
basis which is either argillaceous, sandy, or calcareous, and, as such,
is just such an accumulation as would be formed against a subsiding
ridge. The peculiar character of its fauna was the consequence of
such local conditions. The Neocomian group (Lower Greensand)
is altogether wanting over the district here described; and this cir-
cumstance, taken in conjunction with the trend of the country towards
the Department of the Haute-Marne, before this lower portion is met
with, shows that it was an arrangement which was dependent ona
physical barrier.

It is possible that some coarse quartzose sands, usually green;
which underlie the true fossiliferous Gault clay of the Boulonnais
may represent the Lower Greensand of our side of the Channel: the
evidence of any included fossils is wanting, and from certain appear-
ances of passage from one condition to the other, I at one time sup-
posed that they were sands of the Gault. These sands thin away
against the ridge of Paleeozoic rocks, so that they are wanting in
many sections, as at Blacourt, where the blue Gault clay fills the
inequalities of the limestone surface. A calcareous grit, composed of
the detritus of old rocks, underlies the Gault at Wissant; and
M. d’Archiac has called attention to the agreement between the
lowest Cretaceous beds of the Calais well with those of the Wissant
section. If these represent the Lower Greensand, it is here reduced
to a thickness of five yards.

The limit of the area of the ‘‘ Lower Greensand” or Neocomian
group is easily traced. It commences at Punfield on the W. in the

* Mém. de la Soc, Géol. de France, t. ii. p. 291.

;
OO es ee ee

:
4
i
’

AUSTEN—EXTENSION OF THE COAL-MEASURES. 69

form of a thin band of limestone, included in dark Wealden shales,
with much vegetable matter, and containing a curious assemblage of
marine, brackish, and freshwater shells. From this point there jis
no evidence of the presence of any beds of Lower Greensand along
the base of the Chalk-escarpment of Dorsetshire, nor in the Vale of
Wardour, nor yet at Warminster ; and this arrangement is just what
should take place, supposing that the axis of Frome should represent
that of Artois, or any of the anticlinals which form part of the same
system.

‘True littoral Lower Greensand shingle occurs near Devizes, and
thence on to Calne. The precise age of these beds is that of
M. d’Orbigny’s Urgonian series, or upper division of the Neocomian
group*. Iam still of opinion that the weight and the worth of the
evidence of the fossils are in favour of the Neocomian age of the
Farrmgdon gravels, and that in their inquiries geologists must be
guided by the forms which do not pass up into higher members of
the series, rather than by those that doy: if so, the following species
determine the question : Terebratula Celtica, T. oblonga, T. prelonga,
T. sella, T. tamarindus, Rhynchonella Gibbsiana, R. parvirostris,
Salenia punctata, Goniopygus peltatus, Nucleclites Neocomiensis.
The beds containing these are situated on the N. of the Frome axis,
so that it would seem that that lme had caused an advancing ridge
into the area of the lowest Cretaceous deposits, and produced an
irregular boundary-line on the W. From Punfield (Dorset) a line
may be drawn passing outside the Isle of Wight, and to the 8.W. of
the Pays de Bray, beyond which no Lower Greensand occurs. Ac-
cording to a recent discovery by M. Cornueltf, freshwater shells have
been washed into the Neocomian marine beds of Champagne, as has
happened at Atherfield, indicating the proximity of land on either side;
so that the Neocomian area of the N.of France and 8.E. of England
resolves itself into a channel, having a main direction at right angles
to our present English Channel, and open only at its 8.E. extremity,
where it communicated with the great expanse of the ocean in which
the earlier Neocomian groups of the 8. of Europe were deposited. It
will be thus seen that the two areas of the Anglo-Gallic Wealden
and Neocomian groups are nearly co-terminous ; in other words, an
area of fresh water, bounded by ranges of land having a main direc-
tion of W. 31° N., was, by a process of gradual subsidence, converted
into an arm of the great Southern-Europe ocean, and it was on such
views that the lines drawn on the Map (pl. I.), were arrived at.

It remains that we should inquire as to the amount of evidence
which can be arrived at as to a boundary-line im the North. As in
all cases the materials of a detrital-sedimentary group have been
derived from coast-line waste, an examination of these, particularly
when of the character of coarse sands and conglomerates, will never
fail to afford curious results.

* Quart. Journ. Geol. Soc. vol. vi. p. 469.

+ See Sharpe, Quart. Journ. Geol. Soc. vol. x., p. 176; and Davidson, ‘ British
Cretaceous Brachiopoda,’ (Pal. Soc.) p. 106 e¢ seg.

t Bull. Soc. Géol. de France, 2nd series, t, xi. p. 47.

70 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

The boundary-lines of the Neocomian group are now for the most
part concealed : any good geological map will, however, show that it
must have been defined in places by members of the Oolitic series,
and that on the N.E. it passed transgressively over them. That
this position was brought about by a process of overlap is clear from
many considerations, the most satisfactory one being that the lowest
or argillaceous portion is of limited extent compared with the higher
or Urgonian division, and yet the whole of the fauna indicates depths
of from seven to ten fathoms of water only. There are sections
which show that in places the Lower Greensand of our 8.E. counties
has a thickness of 800 feet, as between Guildford and Dorking, and
the whole of this consisting of quartzose sand or shingle.

The materials which compose the shingle-beds are identical with
those of the Farringdon gravels, which have been already described,
and I cannot do better therefore than borrow a few lines from that
paper :—‘ The mineral character of the pebbles which compose this
gravel suggests considerations of much interest in the history aud
source of origin of the materials which compose the secondary depo-
sits of this country. The pebbles, as a mass, have been derived from
altered sedimentary strata—such as shales converted into flinty slates
or hornstone, and which must also have contained great subordinate
veins of quartz-rock: water-worn crystals of felspar may also be
detected, indicating the loose structure of the mass of felspathic
granite, or porphyry, from which they were separated. The mine-
ralogical character of the coast-line whence the materials of the
Farringdon gravel were derived is thus clearly indicated, and is one
which must necessarily, from the well-known distribution of masses
of crystalline rocks, have existed at some considerable distance from
the spot to which the gravel has been transported.’ (Quart. Journ.
Geol. Soc. vol. vi. p. 458.) These accumulations rest on Kimmeridge
clay and Coral rag; they could only have been produced on a coast-
line, and they must have followed that line to their present positions.

If sections be taken at intervals within the Wealden area, as from
Farnham to Maidstone, an insight will be got as to the change which
the beds of the Lower Greensand undergo from S. to N., and it will
then be seen that the subordinate shingle-bands become coarser notth-
wards, so that.at the latter place rounded blocks of granite have been
met with nearly afoot in diameter. Such a fact as this is of itself suffi-
cient to indicate the direction in which the coast-line of the Lower
Greensand lay; and, coupling it with the evidence of its thinning-out
and disappearance in the Boulonnais, we are enabled to carry on the
line of the old axis of Artois, and to feel sure that, in its passage
somewhere to the N. of our Wealden denudation, it presented at
the period in question a like physical feature, and exercised the
same influence there that it did along its continental course. The
Farringdon shingle-beds followed this line of coast, from the old
Paleozoic rocks on the E., from which all the materials could be
derived.

It was on such considerations that I had defined the limits of the
Lower Greensand group, when I received some information from

AUSTEN—EXTENSION OF THE COAL-MEASURES. 71

Mr. Prestwich which confirmed the view I had taken in a most
remarkable manner. The boring at Kentish Town, after having
been carried through the whole thickness of the Chalk and the
Gault, passed to beds of red marl and sandstone, to the exclusion of
any beds having the least resemblance to any portion of the Lower
Greensand. Since this paper was originally read, the details of the
Kentish Town well have been communicated to the Society*. The
presence of a coarse conglomerate bed subordinate to the Gault,
is a feature wholly at variance with the composition of that deposit
round the whole circuit of the Wealden denudation ; but that it be-
longs to the Gault is probable from the presence of a Belemnite very
like Belemnites Listeri. Considering this conglomerate with refer-
ence to the size and mineral character of the rocks it contains, it is a
good representative of the calcareous portions of the Tourtia of the
Pas de Calais, and of Belgium, and its presence on our side of the
Channel shows that the peculiar physical line which, as was shown
long since by M. d’Archiac, both defined and caused that local
accumulation was extended across into our area.

The Tourtia conglomerate belongs to the northern slope of the old
Palzeozoic axis of Artois, and in this way the Kentish Town boring
directly solves one of the most important points of this inquiry.
Taking the narrow dimensions of the axis of Artois, when compared
with the great expanse of the Wealden, with its high anticlinals, it
might have been urged that some of these marked the course of the
old line of disturbance, and hence the field over which the coal-band
might be expected to occur would have been materially enlarged.
We can now feel certain that the Kentish Town conglomerate has
reference to the same northern slope ; that the axis, therefore, passes
beneath the range of the North Downs ; and that the depression of
the Thames Valley represents, and is physically a continuation of,
that which, extending from Valenciennes by Douai, Bethune, The-
rouanne, and thence to Calais, includes the great coal-trough of those
countries.

Whatever may have been the original range of the Oolitic group
over the area now covered by the Wealden and Cretaceous formations
of the S.E. of England, there is evidence that it has been reduced by
the abrading action of the Lower Greensand sea along its coast-line.
The shingle-beds of the Lower Greensand of Surrey and Kent con-
tain, in addition to the materials already alluded to, a considerable
number of extraneous fossils, such as the bones and teeth of Oolitic
Saurians, Ammonites Lamberti and A. crenatus of the Oxford Clay,
in great abundance, together with Terebratula jfimbria and Rhyn-
chonella oolitica. |

Beds of this Oolitic age are brought up, as we have seen, against
the 8. slope of the French axis, and hence we see that the coast-line
acted on during the Lower Greensand accumulations consisted. partly
of oolitic and partly of older rocks, and that for a given breadth the

* Vide supra, p. 6.
_.t For the composition of the conglomerate-band passed through by the Kentish
Town well, I beg to refer to Mr. Prestwich’s paper.

vy. PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Oolite series is not likely to offer any serious impediment in the way
of researches for coal, nor of enquiries as to the structure and arrange-
ment of the rock-series underlying the district bordering on the
Thames Valley.

§ 5. Nummulitic group.

The axis of Artois has hitherto been viewed (D’Archiac, J. c.)
with reference to its influence on the characters of the Cretaceous
and Nummulitic series, as these are presented both along and on
either side of it; the influence being just such as would be exercised
by a great physical limit, and which is indicated both by the compo-
sition of the beds as they overlap, and by the included marine fauna:
but this influence is far more strongly marked in the Cretaceous
series than it is in the Tertiary.

As a general rule, the members of the Nummulitic group thicken
away on either side of this axis (to the north and south), thus show-
ing that removal has taken place along the higher portions of the
line, over every part of which it originally passed. The Chalk strata
also thicken away in the same direction; so that, although from the
Boulonnais to the province of Hainault the Nummulitic strata are
found resting on chalk only, it is on the lower parts of that series
and on reduced portions of it that it is seen along the central ridge,—
indicating that precisely the same movements, attended by the same
results, were repeated along the very same line at two very distinct
periods of time ;—Ist, subsequently to the completion of the Creta-
ceous series; 2ndly, after the accumulation of the Lower Nummu-
litie group.

Chalk strata have been largely removed from off the surface of
the province of Hainault, and this clearing must have taken place
before the Nummulitic period, as beds of that age there overlie the
truncated edges of the Chalk, and cover the old Palzeozoic series. In
the Boulonnais, to the W. of the axis of Artois, although Nummu-
litic beds come close to the edge of the chalk-escarpment, they are
not found within that area. Here too the denudation has extended
to the whole thickness of the Cretaceous series. This, therefore,
has been effected subsequently to the Nummulitic period; although
the two periods are so wide apart in time, the amount of removal
over the Boulonnais during some post-Nummulitic period corresponds
exactly with what was effected at the Belgic extremity of the axis,
during the interval between the Cretaceous and Nummulitic groups.

There are many points on which I have not thought it proper to
inquire in the preceding pages ; of these perhaps the most important
is that of the arrangements of the Palzeozoic rocks from 'Therouanne
to Calais. We have, however, evidence to warrant the following
general inferences :-—

Ist. That the physical configuration of Western Europe at the
close of the Paleozoic period is sufficiently clearly defined to admit

-

AUSTEN——EXTENSION OF THE COAL-MEASURES. 73

of the restoration of the original surfaces which supported the coal-
vegetation.

2ndly. That the Permian and Triassic groups indicate the earliest
changes which the form of this area experienced.

drdly. That at an early time a line of disturbed surface was pro-
duced, having a general E. and W. direction, and which, traversing a
portion of the area of the coal-growths, has placed all the members
of that series along its course either at or near the present surface.

Athly. That the physical and geological evidence derived from
the S. of England concurs in showing that this area has followed
these changes, and been a part of the zone along which all those
movements have taken place which have tended to preserve the
great Franco-Belgian coal-band and render it available.

The present communication must be considered only as a first
attempt ; but it is one which, from its economical importance, cannot
fail to attract attention in proportion as the extension of productive
coal-measures becomes proved from Therouanne eastwards: it will
not be deemed too much to say, that we have strong d-priori reasons
for supposing that the course of a band of coal-measures coincides
with, and may some day be reached, along the line of the valley of
the Thames, whilst some of the deeper-seated coal, as well as certain
overlying and limited basins, may occur along and beneath some of
the longitudinal folds of the Wealden denudation.

What is now above measure needed is, that we should obtain one
single point of verification as to the depth at which any part of the
Paleozoic group occurs beneath our S.H. area: the state of the
question is such, that from this one single point, once ascertained,
the rest of the investigation might be conducted, for practical pur-
poses, with perfect certainty, and it is therefore of importance that
the question and its possible results should not be lost sight of by
all those who may be promoting deep sinkings at any places over the
area which has been here indicated.

74

DONATIONS

TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY,
From July \st, 1855, to October 31st, 1855.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

American Academy of Arts and Sciences, Proceedings (Boston),
vol. vii. pages 161-232.
C. T. Jackson and A. A. Hayes.—Native Copper from Lake
Superior, 195.

American Journal of Science and Arts. 2nd Ser. No. 59. Sept. 1855.
From Prof. Silliman, For. Mem. G.S.
N.S. Menross.—The Pitch lake of Trinidad, 153.
W. P. Blake.—On the Grooving and Polishing of hard rocks and
minerals by drifting sand, 178.
J. L. Smith.— American Minerals, pt. v., 242.
Aluminium and Sodium, 258.
Peat gas, 261.
Mineralogical Notices, 269.
G. Gibbs.—Geology of the country East of Cascade Mountains,
Oregon, 275.
Obituary Notice of Mr. T. Weaver, 297.
G. Gibbs.— Volcanoes at Paget’s Sound, 297.
Coal of Bellingham Bay, 298.
Notices of Books, &c. 301.

Athenzeum, June to October, 1855. From C. W. Dilke, Esq., F.G.S.

Belgium. Académie Royale des Sciences, des Lettres et des Beaux-
Arts de Belgique. Bibliographie Académique, ou Liste des
Ouvrages publiées par les Membres, Correspondants et Associés
résidents, 1854, 8°, 1855.

———- ——, | ANNIE OOD.

ee
[= e

— —. Mémoires couronnés. Collect. in 8°, vol. vi.
deux. partie. 1855.

Mémoires. Vol. xxviii. 1854.

if De Koninck et H. Le Hon.—Recherches sur les Crinoides du
terrain carbonifére de la Belgique.

L. De Koninck.—Sur un nouveau genre de Crinoides du terrain
carbonifére de |’ Angleterre.

eel

DONATIONS. 75

Belgium. Académie Royale des Sciences, des Lettres et des Beaux-
Arts de Belgique (continued). Mémoires. Vol. xxix. 1855.
J. C. Houzeau.—Sur la direction et la grandeur des Soulévements

qui ont affecté le sol de la Belgique.

eee

; Bulletins. Vol. xxi., deux. partie. 1854.
L. De Koninck.—Fossil bones from Campine, 552.

D’Omalius d’Halloy.—Fossil bones from Dinant, 552.

De Walque.—Lias of Luxembourg, 210.

Dumont.—Systematic table of formations, 1018.

.. Vol. xxii. prem. partie. 1853.

Bengal Asiatic Society, Journal. New Series, No. 72. 1855, No. 2.
Dr. Falconer.—Colossochelys atlas, 173.
Capt. Saxton.—Coal and iron ore from the Gungpur Raja’s
territory (plate), 185.

No. 73. 1855, No. 3.

Marcadieu.—On the Kooloo iron mines and the Mannikurn
Valley, 191.

Royle.—On the graphite of Kumaon and Travancore, 203.

Piddington.— On the kunkurs and iron ores of Burdwan, 212.

On the Cuttack coal of Talcheer, 240.

On meteorites from Segowlee and Allahabad, 247.

Samuels.—On the coalfields of Talcheer, 248.

Piddington.—On the gold-dust of Midnapore, 250.

— On the copper ores of Pushak and Mahaldiram, 251.

Berlin. Konigl. Preuss. Akad. der Wissenschaften zu Berlin, Ab-
handlungen, aus dem Jahre 1854. 4°, 1855.
Beyrich. Ueber die Lagerung der Kreideformation im Schlesis-
chen Gebirge, 57 (map).

» Monatsberichte, 1855.

Ewald.—Beitrag zur Kenntniss der untersten Liasbildungen im
Magdeburgischen und Halberstadtischen, 1.

Weiss.— Ueber das Rhomboedrische Krystallsystem, 7, 90.

Ehrenberg.—Ueber den unzeifelhaften Ursprung des Marmors
der Grafschaft Antrim in Iveland aus Polythalamienkreide, 9.

Erlauterungen tber den Griinsand im Zeuglodon-

kalke Alabama’s in Nord-Amerika, als besonders wohlerhal-

tene Polythalamienformen, 86.

Ueber die weitere Entwicklung der Kenntniss des
Griinsandes als griinen Polythalamien-Steinkerne u.s.w.
und iiber den Meeresgrund aus 12,900 Fuss Tiefe, 172.

—— Ueber neve Erkenntniss immer grésserer Organisa-
ps der Polythalamien, durch deren urweltliche Steinkerne,

— Ueber ein Europaisches marines Polygastern-Lager,
und iiber verlarvte Polythalamien in den Marinen Polygas-
tern Tripeln von Virginien und Simbirsk, 292.

Mitscherlitsch.—Ueber die Krystallform und die isomeren
Zustande des Selens und die Krystallform des Jod, 409.

Zeitschrift der Deutschen Geologischen Gesellschaft,
6. Band. 4. Heft. August—October, 1864.
Verhandlungen der Gesellschaft, 617.

76 DONATIONS.

Berlin. Zeitschrift der Deutschen Geologischen Gesellschaft (con-
tinued).
Sechster allgemeine Versamml. derd. Geol.Ges. zu Gottingen, 621.
Briefliche Mittheilungen, 668.
Noggerath.—Ueber gediegen Blei, naturliche Bleiglitte und
Mennige, 674. |
Miiller.—Die Alaunerze der Tertiarformation, 707 (plate).
Beyrich.—Die Conchylien des norddeutschen Tertiargebirges
(drittes Stiick), 726 (plates).
Fraas.—Squatina acanthoderma, der Meerengel von Nusplingen,
782 (3 plates).
7. Band. 1. Heft. 1855.
Verhandlungen der Gesellschaft, 1.
Briefliche Mittheilungen, 11.
Roth.—Veranderte Kreide von Divisberge bei Belfast, 14.
Glimmer nach Andalusit, 15.
Huyssen.—Die Soolquellen des Westfalischen Kreidegebirges,
ihr Vorkommen und muthmaaslicher Ursprung, 17 (plates).
Castendyck.—Die Rotheisenstein-Lagenstatte der Grube Briloner
Eisenberg bei Olsberg, 252 (plate).
Reuss.—Ein Beitrag zur genaueren Kenntniss der Kreidegebilde
Meklenburgs, 261 (5 plates).
Noeggerath.—Notiz tuber eimige knochenfiihrende Hohlen im
Regienrungs-Bezirk Arnsberg, 293.

British Association for the Advancement of Science. Report of the
24th Meeting, held at Liverpool in September, 1854.
R. Mallet.—Earthquake phenomena, 1.
J. E. Portlock.—Report of Earthquake Committee, 370.
J. A. Davies—Decomposition of Magnesian limestone at Brods-
worth, Sect. 66.
D. Forbes.—Minerals from Norway, — 67.
A. Bryson.—Structure of the Silurian slates of Peebleshire, — 78.
J. Buckman.—Fossil bones from Stroud Valley, — 78.
Coal deposits of Virginia, — 78.
P. P. Carpenter.—Fossil bones and shells from Birlingham,
Worcestershire, — 79.
R. Chambers.—Glacial phenomena in Scotland and North of
England, — 78.
J. G. Cumming.—Recent changes in the area of the Irish sea,

- J. Cunningham.—Submarine Forest at Leasowe, — 81.

Sir P. Egerton.—Ganoid scale from India, — 82.

G. Ehrenberg.—Microscopic shells in Silurian rocks, — 82.

E. Forbes.—Foliation of metamorphic rocks in Scotland, — 82.

R. J. Gardner and W. H. Baily.—Cretaceous fossils in South

Africa, — 83.

G. B. Greenough.—Geology of India, — 83.

R. Harkness.—Fossil crustacean tracks in Dumfriesshire, — 86.
| — Silurian Anthracite and Fucoids of South Scot-
land, — 86.

! Mineral charcoal, — 86.

a Fossil Annelid tracks in the County of Clare, — 86.
| KE. Hull.—Section near Liverpool, — 86. ;
| J. B. Jukes.— Geological map of Wicklow, — 87.
| Sir R. I. Murchison.—Paleozoic rocks of Germany, — 87.

—=_-

DONATIONS. 7h

British Association for the Advancement of Science (continued).
J. Nasmyth.—Lunar volcanic craters, — 91.
D. Page.—Palzozoic rocks of Scotland, — 91.
J. Price.—Carboniferous limestone near Abergele, — 93.
A. C. Ramsay.—Paleozoic glaciers, — 93.
Ancient glaciers in Wales, — 94.
J. I. Whitty.—Silurian Anthracite of Cavan, — 95.
Balfour.— Vegetable bodies im coal, — 97.
Redfern.—Torbanehill coal, — 102.

Canadian Journal. May 1855.
Geological survey of Canada, 234.
Canadian minerals at the Paris Exhibition, 241.
Elevation of land in the human period, 244.
Ege of Zpyornis, 244.
Newly discovered fossil bird at Paris, 244.

June 1855.
Notice of Sir Henry de la Beche and Mr. Greenough, 262.
The Great Minnesota copper-mine, 266.
Mines and miners, 266.

——. July 1855.
Lyell’s Manual of Geology, noticed, 285.
Geological survey of Canada, 289.
Eruption of Vesuvius, 293.

. August 1855.
Mather.—Earthboring machine, 297.
Owen.—Dicynodon tigriceps, 317.
Chemical Society of London, Quarterly Journal, Vol. viii. No. 3.
October 1855. No. 31.
H. St. C. Deville.—On Aluminium, 239.

H. Debray.—On Glucinum, 242.
C. von Hauer.—On Cadmium, 250.

Copenhagen. Kgl. danske Vid. Selskabs Forhandl. Oversigt, 1854.
Forchhammer and Rink.—Meteorites from Greenland, 1.
Forchhammer.—Influence of salt in the formation of minerals,

&e., 91.
Steenstrup, Forchhammer, and Worsaae.—Geological-antiquarian
researches, 191.

Dijon, l Académie des Sciences, Arts et Belles Lettres de. Mémoires,
Deux. sér. vol. ii. (Année 1854). 1855.
A. Perrey.—Note ‘sur les Tremblements de Terre en 1853, avec
Suppléments pour les Années antérieures. Sect. des Sc. 1.

Edinburgh Royal Society, Transactions. Vol. xxi. Part 2. 1855.

Proceedings. Vol. iii. No. 45.

Dr. Fleming.—Stratified traps of Edinburgh, 268.

C. Maclaren.—Ancient moraines in Argyleshire, 279.

E. Blackwell and J. Forbes.— Movements of the Chamouni glaciers
in winter, 283.

R. Harkness.—Annelid tracks in the millstone grit, 294.

Dr. Scoular.—Occurrence of British newer pliocene shells in the
Arctic seas, and of tertiary plants in Greenland, 301.

R, Chambers.—Glacial phenomena in Peeblesshire and Selkirk-
shire, 308.:

Dr, Fleming.—Stigmaria, 316.

ss

78 DONATIONS.

Franklin Institute, Journal. 3rd Series. Vol. xxix. No.6, June 1855,
Chapman.—Object of salt in the sea, 384.
F. Field.—Analysis of a surface-soil from the Desert of Atacama,
407.

3rd Series. Vol, xxx. No.1. July 1855.

: : ; No.2. August 1855.
C. Mather.—Earthboring machinery, 129.

——_—. —————. ———-. — No.3. September 1855.

Halle. Zeitschrift fiir die gesammten Naturwissenschaften, heraus-
gegeben von dem Naturw. Vereine fir Sachsen u. Thiiringen in
Halle. Vol.iv. 1854.

E, Sochting.—Ueber Eimschliisse von Mineralien in krystalli-
sirten Mineralien, 1.

‘Ueber die urspriingliche Zusammensetzung einiger
pyroxeninischen Gesteine, 194, 358.

Weichsel.—Ueber die Erdfalle und ein isolirtes Vorkommen von
Muschelkalkdolomit am westlichen Harzrande bei Seesen,
433 (with a plate).

W. Baer.—Ueber die Bereitung des Leuchtgases aus Holz, Torf
und Braunkohlen, 123.

Chop.— Ueber den Muschelkalk bei Sondershausen, 219.

C. Giebel.— Ueber das Milchgebiss der Felis spelea, 295 (with
plate).

Ueber Castor turfz, 296.

—— Ueber Nautilus intermedius, 297.

— Palaconchyliologisches, 366.

-— Die Pecten-arten im Muschelkalk, 441.

Fossile Oberscheukel von Bos, 446.

Mette.—Vorkommen von Eisenstein bei Brambach, 292.

Baling Fier Giee Megalodus scutatus und Gervillia inflata,
364,

Wagner.—Die Braunkohlenablagerung bei Aschersleben, 291.

Literatur.—Oryctognosie; Geologie; Palzontologie.

Institute of Actuaries, Assurance Magazine. Vol. vi, pt. 1. Oct. 1855.

Journal of the Indian Archipelago and Eastern Asia. Vol. ix.
Nos. 1-3 (none). January to March 1855. From J. R. Logan,
Esq., F.G.S. .

Literary Gazette, June to October. From L. Reeve, Esq., F.G.8.

Liverpool Literary and Philosophical Society, Proceedings. No. 9.
1855.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Ser.
Vol. ix. No. 62, Supplement. July 1855. From R. Taylor,
Esq., F.G.S.

R. P. Greg.—Crystalline form of Leucophane, 510.
F, M. Jennings.—Analysis of the potash and soda felspars of
one of the Dublin mountains, 51].

~~

DONATIONS. 79

London, Edinburgh, and Dublin Philosophical Magazine (continued).
Vol. x. No. 63. July 1855.
R. P. Greg.—Meteorites from South America, 12, 14.
S. Haughton.—Chemical composition of the granites of the S.E.
of Ireland, 23.
D. Heddle.—Analysis of lunnite from Cornwall, 39.
H. Moseley.—The descent of glaciers, 60.

No. 64. August 1855.

C. Darwin.—The grooving power of icebergs on an undulatory
surface, 96.

R. T. Forster.—Molecular constitution of crystals (2 plates), 108.

J. G, Galbraith.—Felspars of the granites of the Dublin and
Wicklow mountains, 115.

R, P, Greg.—Glottalite and Zeuxite, 118.

Wohler.—Fall of meteoric stones in Hanover, 150.

———. No. 65. September 1855.
ot B. Northeote.—Salt in agriculture, 179.

. No. 66. October 1855,
i. Rose.—Preparation of aluminium, 233.
S. Haughton.—Serpentines and soapstones, 253,
J. D. Forbes.—The descent of glaciers, 300.
R. T. Forster.—Molecular constitution of crystals, 310,

é November 1855. No. 67. Vol. x. 4th
Series.
J. D. Dana.—On the molecular constitution of crystals, 329.

J. H. Pratt.—On the curvature of the Indian Are, 340.
A. Dick.—On the preparation of Aluminium from Kryolite, 364.
F, M. Jennings.—On the potash and soda felspars of the Dublin
mountains, 365.
_ Sir R, I. Murchison.—On a supposed Aerolite, 366.
- C. von Hauer.—On the acetates of manganese, cadmium, and
nickel, 391.

Milan, I. R. Istituto Lombardo di Scienze, Lettere ed Arti e
Biblioteca Italiana, Giornale, Nuova Serie, fase. 33-36.
1854-55.

Curioni.—Sugli schisti bituminosi di Tignale sul Lago di Garda,
257.

Moscow. Société Impériale des Naturalistes de Moscou, Bulletin.
Vol. xxvi. Année 1853. . No.3. 1853.

A. Andrzeiowski.—Systéme Tyraique (seconde partie), 3

F, A. Fallon.—Ueber die Lagerung und Beschaffenheit des Ser-
pentins im dem von der Chemnitzer Eisenbahn durchschnit-
tenen Theile des Granulitgebirges, 274.

V. Kiprijanoff.—Fisch-iiberreste im Kurskschen eisenhaltigen
Sandsteime (4. Aufsatz), 286 (with a plate).

A Map of Russian North America, with the Voleanoes, &e.

No, 4. 1853.
G. Sandberger.—Clymeniz et Goniatites, 299.

Se SS,

80 DONATIONS.

Moscow. Société Impériale des Naturalistes de Moscou, Bulletin
(continued). Vol. xxvii. Année 1854. No.1. 1854.
Ed. von Eichwald.—Die Grauwackenschichten von Liev- und
Esth-land (2 plates), 3
J. G. Biittner.— Geognostisch-geologische Ansichten entnommen
aus Kurland’s Erdlagerungen, 233.
D. J. Planer.—Entdeckung eines Steinkohlenlager’s am West-
Abhange des Ural’s, 267.
R. Hermann.—Halb-Kalk-Diallag von Achmatowsk, 273.

Notes on Books. Vol. i. No. 1. May 1855. From Messrs.
Longman & Co.

Paris. Académie des Sciences, Comptes rendus. 1855. Prem.
Sem. Tomexl. Nos. 18-26. Avril—Juin.

Descloizeaux.— Recherches physiques et crystallographiques sur
le quartz, 1019.

Deville.—Sur le silicium et le titane, 1034.

Prost.—Tremblement de terre de Nice, 1043.

pee .—Sur les deux formations nummulitiques, Piémont,

70

Boué.—Sur la géologie de la Turquie de Europe, 1104.

D’Abbadie.—Oscillations du sol, 1106.

Gervais.—Sur les mammiféres fossils de Amérique méridionale.
1112.

Dumas.—Un échantillon d’un gisement d’or découvert en Algérie.
1138.

Hoeffer.—Sur la cause des tremblements de terre, 1184.

Sismonda.—Sur la constitution géologique de la Tarentaise et de
la Maurienne, 1193.

Tissier.—Sur l’aluminium, 1202.

Hébert.—Sur le fémur du Gastornis parisiensis, 1214.

Nicaise—Sur la géologie et la minéralogie d’une partie du .

département d’Alger, 1241, 1296.

Deville.—Sur l’éruption du Westwe du 1& Mai 1855, 1247.

Gueymard.—Sur le platine des Alpes, 1274.

Deville.—Sur Valuminium, 1298.

Haime.—Sur la géologie de Vile Majoraue, 1301.

Rivot.—Sur le gisement du cuivre natif au lac Supérieur, 1306.

Kuhlmann.—Sur les chaux hydrauliques, les pierres artificielles
et sur diverses nouvelles applications des silicates alcalins
solubles, 1335.

Hunt.—Sur les sources acides et les gypses du Haut Canada,
1348.

Rozet.—Sur la géologie des Alpes francaises, 1359.

Serres.—De Mouréze et des ses colonnades de rochers, 1367.

. ————. Tables, deux: Sem. 1856. Vol. xxxix.
1855, deux. Sem. Vol. xli. Nos. 1-12.

Arnoux.—Sur la nature minéralogique de la province de Quang-
Nave, 178.

Hunt.—Sur quelques roches feldspathiques du Canada, 192.

Fournet.—Tremblement de terre du 25 Juillet a Lyon, 201.

Seguin.— a Fontenay ; Sace, — a Wesserling ; Niépee,
— a Allevard ; Lallemand, — a Verdun, 203.

Regnault et Prost. —Sur le méme phénoméne, 204, 214.

Paris.

DONATIONS. 8l

Académie des Sciences (continued).

Rousse.—Sur des Asteries fossiles trouvées dans un terrain erétacé
de P Algérie, 224.

Kuhlmann.—Sur les chaux hydrauliques, etc., 289.

Hunt.—Sur les eaux minérales du Canada, 301.

Le tremblement de terre du 25 Juillet 1855, 318.

Nodot.—Un nouveau genre d’ Edente fossile renfermant plusieurs
espéces voisines de Glyptodons, 335.

Lanza.—Sur les formations géognostiques de la Dalmatie, 386.

Frezin.—Dégagement de gaz hydrogéne carboné dans un point
de la vailée de l’Arve, 410.

Annales des Mines. Cing. Sér. Vol. vi. 4 Livr. 1854.
Lyell et Hall.—Rapport sur la partie géologique de l’exposition
de New York, 1. '
Castel.—Rapport sur une explosion d’hydrogéne carboné dans
les travaux d’une mine de fer, 94.
Damour.—Sur la cristallisation de la brongniardite, 146.

: 5 Livy. 1854.

Garella et Huyst.—Rapport sur les mines de houille d’Heraclea,
173 (map).

Villeneuve, H. de.—Etudes sur la drainage en France, dans les
rapports avec la météorologie et la géologie, 293.

Archives du Muséum d’Histoire Naturelle. Tome vii.

Livr. 314, 1855; and Tome viii. Livr. 1 & 2 (in one). 1855.

—~——.. Socicté Géologique de France, Bulletin, deux. Sér. Index,

Vol. xi.

¥ . Vol. xn. feuill. 12-18. Fevr. 1855.

De Rouville.—Découverte d’un nouveau gisement de poissons
fossiles 4 Beaufort, prés de Crest (Dréme), 178.

Casiano de Prado.—Sur la géologie d’Almaden, d’une partie de
la Sierra Morena et des montagnes de Toléde (pl. vi.), 182.

Rozet.—Mémoire géologique sur les Alpes francaises (pl. vii.),
204.

Scipion Gras.—Sur la constitution géologique du terrain anthra-

cifére alpin et les différences qui le séparent du terrain

jurassique (pl. vill. et 1x.), 265.

, Feuill. 19-23. Fevr.—Avr. 1855.

Daubrée.—Recherches sur la production artificielle des minévraux
des familles des silicates et des aluminates, 299.

Albert Gaudry.—Analyses des relations publi¢es sur les éruptions
voleaniques de Vile d’Hawau (Sandwich), 306.

Ch. Martins.—Sur les érosions des roches calecaires dues aux
agents atmospheériques (pl. x.), 314.

Ang. Sismonda.—Sur la constitution géologique des Alpes mari-
times et de quelques montagnes de la Toscane, 320.

eer la perowskite trouvée dans la vallée de Zermatt,

32.

Ch. Gaillardot.— Description géologique de la montagne appelée
Djebel Khaisotin, au nord de Damas, 338.

Charrel.—Sur un fait pouvant indiquer l’époque géologique de
la formation de certaines grottes et cavernes, 349.

VOL. XII.—PART If. G

82 DONATIONS.

Paris. Société Géologique de France (continued). .

Edm. Hébert.—Sur plusieurs fossiles remarquables du bassin de
Paris, 349.

Agassiz.—Sur le développement des étres, 353,

J. Barrande.—Compte rendu d’un Mémoire de M. Th. Kjerulf,
sur Je bassin silurien des environs de Christiania, 356.

J. Delanotie.—Moyen simple de constater la présence du fer, de
la magnésie et du manganése dans les dolomies, les marnes
et les calcaires, 361. m

Aug. Laugel.—Du clivage des roches, 363.

—. Feuill. 24-32. Avr. & Mai, 1855.

L. Pareto.—Sur le terrain nummulitique du pied des Apennins
(pl. xi.), 370.

H. Coquand.—Sur les fers pisolitiques de la Charente, 395.

Lassaigne.—Sur le procédé proposé par M. Delanoiie peur l’essai
des calcaires, 399.

Lyell.—Extrait d’un rapport sur la partie géologique de l’expo-
sition de New York, en 1853, 400.

E. Gueymard.—Sur le platine des Alpes, 429.

Greenough.—Sur la géologie de l’Inde, 433.

J. Barrande.—Remplissage organique du siphon dans certains
céphalopodes paléozoiques (pl. xii.), 441.

A. Pomel.—Notice géologique sur le pays des Beni-Bou-Said,
prés de la frontiére du Maroc, 439.

Logan.—Sur des Graptolithes de la formation silurienne des.
environs de Quebec (Canada), 504.

A. Sismonda.—Sur les deux formations nummulitiques du Pié-
mont (extrait d’une lettre 4 M. Elie de Beaumont), 509.

Ch. Lory.—Sur les assises inférieures de la montagne de Crussol,
prés de Valence (Drome), 519.

Photographic Society, Journal. Nos. 31-35. June to Oct. 1855.

Royal Asiatic Society of Great Britain and Ireland, J ournal. Vol. xv.
Part 2. 1855.

Royal Geographical Society, Anniversary Address by the Earl of
Ellesmere, 1855.

Royal Institution of Great Britam, Notices of Meetings. Part 5.
November 1854 to July 1855.

G. B. Airy.—Pendulum experiments made in the Harton Colliery
for ascertaining the mean density of the Earth, 17.

J. Dickenson.— Water supply of London, 47.

T. H. Huxley.—The hypothesis of progressive development of
animal life in time, 82.

Sir C. Lyell.—Erratic blocks in Massachusetts, 86.

Royal Society, Proceedings. Vol. vii. No. 13.
No. 15.

Scarborough Philosophical and Archeological Society, 23rd Report.
1855.
Dr. Murray.—The minerals of Scarborough, 25.
Abstract of the Proceedings of the Geological Section of the British
Association, 1854, 44.
J. Leckenby.—The geographical position of certain clay-beds in
Filey Bay, 49.

—-

DONATIONS. 83

Royal Society, Proceedings. Vol. vii. No. 14.
J.D. Forbes.—On the Rev. M. Moseley’s theory of the descent
of glaciers, 412.
Sir R. Murchison.—Supposed meteorite from Battersea, 421.

Scottish Meteorological Association, Prospectus.
Report of Preliminary Meeting.
Society of Arts, Journal. Vol. ii. Nos. 134-153.
Statistical Society, Journal. Vol. xviii. Part3. September 1855.

Stockholm. Kongl. Vetenskaps-Akademiens Handlingar for ar
1853. Forra Afdelningen. 1855.

. Kongl. Vetenskaps-Akademiens Forhandlingar, Ofver-
sigt. Elfte Argangen 1854. 1855.
C. W. Blomstrand.—Bitrag till Sverges mmeralgeografi, 296.
A. Erdmann and E. W. Olbers.—Om ett jodhaltigt mineralvatten,
81.
L. Igelstro6m and L. Svanberg.—Mineralier fran Elfsdals hirad,
66. .

tS

Nya Svenska mineralier, 156.
A Retzius.—Fossilt os petrosum af en hval, 111.

. Ars-Berrattelser om Botaniska Arbeten och Upptackter
for Aven 1845-1848. Till Kongl. Vetenskaps-A kademien afgifna
af J. EK. Wikstrém. Sednare Delen. 1855.

————.._ Berittelser om Framstegen i Insekternas, Myriapodernas
och Arachnidernas Naturalhistoria for 1851 och 1852. ‘Till
Kongl. Vetenskaps-Akademien afgifven af C. N. Boheman.
1854.

Vaud. Société Vaudoise des Sciences Naturelles, Bulletin. No. 33.
Vol. iv. 1854,
ee and Morlot.—Earthquakes at Villeneuve and Devens,
47, 48.
Morlot.—Fossil teeth from Soleure, 48.
Chavannes.—Impressed erratic pebbles, 49.
Morlot.—Wood, leaves, and shells dug up at Clarens, 49.
Delaharpe.—Fossil tortoise from Lausanne, 51.
Heer.—Fossil palms, 52.
Morlot and others.—Glacial phenomena, 53.
Delaharpe.—Fossil leaves from Lutry, 54.
Morlot.—Impressed pebbles from Lavaux, 55.
Fossil bovine tooth from Chiésaz, 56.
a Bones from the glacial drift near Lausanne, 7].
Zollikoffer.—Geology of the vicinity of Sesto Calende, 72 (with
2 plates).
Morlot.—The Tunnel at Lausanne, 82 (plate).
Blanchet.—Tertiaries at Vaud, 85.
Morlot.—Terraces of the Lake Leman, 92.

Vienna. Kais. Akademie der Wissenschaften, Almanach. 1855.
i G 2

84 DONATIONS.

Vienna. Kaiserl. Akademie der Denkschriften, Math.-Nat. Class.
Band vii. 1854.
Ettinghausen.—Die Eocene Flora des Monte Promina, 17 (14
plates).

Band ix. 1855.

Von Hauer. —Beitrage zur Kenntniss der Cephalopoden-Fauna
der Hallstatter Schichten, 141 (5 plates).

Reuss.—Ueber zwei Polyparien aus dem Hallstatter Schichten,
167 (plate).

Peters. = Sahildlordtenreate aus dem Oesterreichischen Tertiar-
Ablagerungen, 1 [2nd part] (6 plates).

Suess.—Ueber die Brachiopoden der Hallst’étter Schichten, 23
(2 plates).

Hornes.— Ueher die Gasteropoden und Acephalen der Hallstatter
Schichten, 33 (2 plates).

—_—_—. ————.._ Sitzungsberichte, Math.-Nat.Cl. Band xiv.
Heft 1. October 1854.

Haidinger.—Graphische Methode annahernder Winkelmessun-
gen, besonders au kleimeren Krystallen, 3.

Nuricsény und Spangler.—Analyse des Mineralwassers zu Rog-
gendorf, Banat, /21.

. Heft 2. November 1854.
Kenngott. _-Mineralogische Notizen (plates), 243.
Haidinger.—Glimmer und Pennin, 295, 330.
Schrotten.—Zirkonium-oxyd, 352.

Heft 3. December 1854.

Reslhuber. —Ueber die ‘Temperatur der Quellen von Krems-
minster, 385.

Hochstetter.—Die Sinterniederschlage die Karlsbadder Quellen,
416.

Band xv. Heft 1. Janner 1855.

Haidinger. —Jod-Tellur-Methyl, 3.

Hauer, R. v.— Ueber einige Cadmium-Salze, 23.

Belli.—Ueber das in Pavia stattgehabte Erdbehben, 44.

Leydolt.— Ueber eime neue Methode, die Structur und Zusammen-
getzung der Krystalle zu untersuchen, mit besonderer
Beriicksichtung der Varietaten des rhomboedischen Quarzes
(plates), 59.

; Heft 2. Februar 1855

Eehaniel eae stullulee aes Untersuchungen, 200.

Kenngott. —Mineralogische Notizen, 234.

Hornes.—Ueber die Gaster opoden und Acephalen der Hallstatter
Schichten, 276.

Pohl.—Analyse des Brunnenwassers, Wien, 303.

Miiller.—Nachtrag zu seiner |. c. Abhandlung, iiber ein fossiles
Cetaceon aus Radaboj (Delphinopsis Freyerii), 345 (plate).

Heft 3. Marz 1855.

Haidinger.—Ueber die zuweilen im geschmeidigen Eisen ent-
standene krystallinische Structur, verglichen mit jener des
Meteoreisens, 354 (plate).

—

—_—

—_

Vienna.

Vienna.

DONATIONS. 85

Kais. (continued).

Russegger.—Das Erdbeben in Schemnitz am 31 Janner 1855,
368

Kreil.—Ueber einen neuen Erdbebenmesser, 370.

Hauer.—Ueber einige Fossilien aus dem Dolomite des Monte
Salvatore bei Lugano, 407 (plate).

Rolle.—Die Echinoiden der oberen Jura-Schichten von Nikols-
burg in Mahren, 521.

—————. ———. Bandxvi. Heft 1. April 1855.

Sandberger.—Ueber Anoplotheca, eme neue Brachiopoden-
Gattung, 5 (plate).

Reuss.—Paleontologische Miscellen, 144.

Haidinger.—Die Krystalle des essigsauren Manganoxyduls, 145.

Kenngott.—Mineralogische Notizen, 152.

Hauer.—Ueber die Cephalopoden aus dem Lias der nordéstlichen
Alpen, 183.

K. K. Central-Anstalt fir Meteorologie und Erdmagnetis-

mus, Jahrbucher. Jahrgang 1851. Vol. ii. 1855.

K. K. Geologische Reichsanstalt, Jahrbuch. Jahrgang

1850. No. 2. April to June.

Achill de Zigno.—Uebersicht der geschichteten Gebirge der
venetianischen Alpen (plate), 181.

A. v. Morlot.—Ueher das hohe Alter des Kupferbergbaues am
Mitterberg in Salzburg, 197.

Ueber die Spuren emes befestigten romischen Hisen-
werkes in der Wochein in Oberkrain (plate), 199.

Joseph Trinker.— Der Adelsvorschub am Heizenberg und
Kleinkogl (plate), 213.

Karl Koristka.—Die Resultate aus Karl Kreil’s Bereisungen des
osterreichischen Kaiserstaates. Zweite Abtheilung, 220.

Ludwig Zeuschner.—Ueber die Verschiedenheit der Entstehung
der Salzablagerungen in den Karpathen und im den Salz-
burger Alpen, 235.

Ueber die Entwicklung der oberen Glieder der
Kreide-Formation nordlich von Krakau, 242.
A. v. Morlot.—Ueber die geologischen Verhaltnisse von Raibl
(plate) 255.
Ueber die geologischen Verhaltnisse zu Radoboj in
Kroatien, 269.

Hermann Schlagintweit.— Ueber die Regenverhiltnisse der
Alpen, 280.

Adolph Schlagintweit.— Untersuchungen tiber die Isogeother-
men der Alpen (plate), 287.

Otto Sendtner.—Berichtigung emiger Angaben Schlagintweit’s
in Betreff der Isogeothermen der Alpen, 301.

Gustav Adolph Kenngott.—Ueber den Dopplerit, 303.

Gregor v. Helmersen.—Die neuesten Fortschritte der Geologie in
Russland, 307.

Uebersicht der Production und Geldgebahrung des Pribramer
Hauptwerkes, 310.

Albin Heinrich.—Bemerkungen zu den “ Trigonometrischen
Hohenbestimmungen im Troppauer und Teschner Kreise in
Schlesien,” 314.

86

Vienna.

DONATIONS.

K. K. Geologische Reichsanstalt (continued).

Reinhold Freiherr v. Reichenbach.—Ueber Salpeter-Erzeugung,
316.

J. Szab6.—Salpeter-Erzeugung in Ungarn, 324.

P. Guido Schenzl.— Analyse der Bleispeise von Oeblarn in
Obersteyermark, 343.

Letters ; Reports and Proceedings of the Imp. Geol. Institute,
347, &e.

———. Nos.3 & 4. July to December 1850.

A. v. Morlot.—Ueber die geologischen Verhiltnisse von Ober-
krain, 389.

M. V. Lipold.—Versuche der continuirlichen Wehren-Verwasse-
rung im Salzberge zu Aussee, 411.

Alois von Hubert.—Ueber die colorinetrische Kupferprobe, 415.

Carl Koristka.—Die Resultate aus Carl Kreil’s Bereisungen des
Osterreichischen Kaiserstaates, 423.

Carl Baron von Callot.—Ueber Dachschiefer-Erzeugung mit
besonderer Riicksicht auf die Schieferbriiche in k. k. Schle-
sien und Mahren, 436.

Dr. Ignaz Moser.—Ueber die Salpeterdistricte i Ungarn, 453.

Christ. Doppler.—Ueber altere magnetische Declinationsbeo-
bachtungen, 472.

Adolph Senoner. — Zusammenstellung der bisher gemachten
Hohenmessungen in den Kronlandern Oesterreich ob und
unter der Enns und Salzburg, 522.

Reports and Proceedings of the Imp. Geol. Instit., 552, &c.

A. Patera.—Versuch ezur Extraction des Silbers aus semen Erzen
auf nassem Wege, 573.

Fr. Foetterle-—Der Eisenbahnbau am Semmering am Schlusse
des Jahres 1850, 576.

M. Hornes.—Ueber die Faluns im Siidwesten von Frankreich
von Hrn. J. Delbos, 587.

M. V. Lipold.—Ueber das Vorkommen von Braunkohlen zu
Wildshuth im Innkreise in Oberosterreich, 599.

H. Prinzinger.—Ueber die Schiefergebirge im siidlichen Theile ~

des Kronlandes Salzburg, 602.

W. Haidinger.—Der Strontianit von Radoboj, 606.

Der Gymnit von Fleims, 607.

F. Seeland.—Ueber die von der kaiser, Akademie der Wissen-
schaften eingeleitete Untersuchung der Braun- und Steim-
kohlen Oesterreichs, 609.

Allgemeine Berichte iiber die von den eimzelnen Sectionen der
k. k. geologischen Reichsanstalt im Sommer 1850 unter-
nommenen Reisen und Arbeiten, 617.

J. Kudernatsch. — Die neuen Bergbau-Unternehmungen im
Banat, 705.

J. Juhoss.—Reiseberichte aus England und Californien, 718.

A. v. Hubert.—Analysen von 24 verschiedenen Kalksteinen aus
Siidtirol, 729.

Reports and Proceedings of the Imp. Geol. Instit., 734, &e.

Jahrgang 1854. No.4. Oct. to Dec.

August Em. Reuss.— Beitrage zur geognostischen Kenntniss
Mahrens, 659.

Karl Peters.—Die geologischen Verhiltnisse des Oberpinzgaues,
insbesondere der Centralalpen, 766.

|

DONATIONS. 87

Vienna. K. K. Geologische Reichsanstalt (continued).

Karl Peters.—Die geologischen Verhaltnisse der Nordseite des
Radstadter Tauern, 808.

Dionys Stur.—Die geologische Beschaffenheit der Centralalpen
zwischen dem Hoch-Golling und dem Venediger, 818.

N. v. Kokscharow.—Ueber den Klinochlor von Achmatowsk
und den zweiaxigen Glimmer vom Vesuv, 832.

M. A. F. Prestel.—Ueber die krystallinische Structur des Meteor-
eisens, als Kriterium desselben, 866.

Reports and Proceedings of the Imp. Geol. Instit. 868, &c.

Mineral Price-list, 913.

II. GEOLOGICAL CONTENTS OF PERIODICALS
PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 2nd Ser. vol. xvi. No. 91.
July 1855.
Prof. Goeppert.—On fossil palms, 55.
T. H. Huxley.—On the hypothesis of progressive Hisvelapuient
of animal life in time, 69.

No. 92. August 1855.

T. Rupert Jones.—Beyrichiz from Scandinavian limestones
(plate), 81.

T. Wright.—A new genus of fossil Cilinide, 94.

J. G. Jeffreys.—The descent of glaciers, 122.

Dr. Fleming.—Calamites and Sternbergize, 144.

R. Harkness.—Subfossil Diatomacez in Dumfriesshire, 145.

————. No. 93. September 1855.
T. Rupert Jones.—Some British and Foreign Beyrichiz (plate),
163.

A. R. Wallace.—On the law which has regulated the introduction
of new species, 184.

T. Wright.—On some new species of Hemipedina from the
Oolites, 196.

No. 94. October 1855.

————. No. 95. November 1855.
Hochstetter.—Bohemian forests and peat bogs, 378.

Edinburgh New Philosophical Journal. New Series. Vol. ii.
No. 1. July 1855.
J. Davy.—Lake district of Westmoreland, 1.
A. Morlot.—Post tertiary formations of Switzerland (plate), 14.
W.s, ial .—Downward movements East of the Malverns,
3

R. Harkness.—Subfossil Diatomacez in Dumfriesshire, 54.

James Napier.—Trap dykes in Arran (plate), 81.

T. H. Rowney.—Chemical composition of mineral charcoal, 141,

Warren’s Remarks on fossil impressions in Connecticut, noticed,
180.

88 DONATIONS,

Edinburgh New Philosophical Journal (continued).
R. Chambers.—Glacial phenomena in Peeblesshire, &c., 184,
Dr. Fleming.—Stigmaria, 189.
Calamites and Sternbergia, 205.
C. I Hench sr LO aes &c., in the boulder clay of Caithness,
—— Discovery of fossils in the Durness limestones,
Sutherlandshire, 197.
Tunnel through the Malverns, and discovery of graphite, 209.
Prof. Oldham.—Age of the Bengal coal-fields, 210.
A. Damour.—Euclase, 217.
Igelstrom.—Svanbergite, 217.
Whitney.—Statisties of the production of metals during 1854, 218.
Earthquake at Constantinople, 221.
Earthquake at Brussa, 222.

No. 2. October 1855.

R. Harkness.—Geology of Dingle Promontory, Ireland (2 plates),
St cle oe

R. Harkness and J. Blyth.— Cleavage of the Devonian rocks in
the S.W. of Ireland, 245.

Plurality of worlds, &e., 267.

T. H. Rowney.—Composition of two mineral pigments, 306.

C. G. Williams.—On some basic constituents of coal naphtha, 324.

Dawson’s Acadian Geology, noticed, 380.

Symonds’s Old Stones, noticed, 380.

British Association, Proceedings, 396.

Leonhard und Bronn’s Neues Jahrbuch fir Min., Geogn., Geol. und
Petref. Jahrgang 1855. 2 Heft.

K. C. v. Leonhard.—Krystallisirung von Schlacken, 129.

G. H. O. Volger.—Tauriszit, em neues subgenus des Eisen-
Vitriols, 152. |

A. v. Strombeck.— Ueber das Hils- Konglomerat und den Speeton-
Clay bei Braunschweig, 159. :

W.K. J. Gutberlet.—Spherosiderit und Bohnerz in Basaltischen
Gesteinen, 168.

Letters; Notices of Books, and of Mineralogy, Geology, and
Fossils.

——. 3 Heft.
J. Portia Cae der Prototype von Nautilus (plate),
257.
G. H. O. Volger.—Die Hemiedrie des Kubus und Granatoeders,
286

Fr. Weiss—Die Grund-Gesetze der mechanischen Geologie,
2. Abth. (plate), 288. .
Letters; Notices of Books, Mineralogy, Geology, and Fossils.

———. 4 Heft.

J. Barrande.—Ueber die Ausfiillung des Siphons gewisser palao-

zoischer Cephalopoden auf Organischen Wege, 385 (with a
late).

A Miller.—Einige Pseudomorphosen aus dem Teufelsgrunde im
Miinsterthal im Breisgau, 411.

Quenstedt.— Uebér Gaviale und Ichthyosauren des Schwabischen
Jura’s, 421.

DONATIONS. 89

Leonhard und Bronn’s Neues Jahrbuch fiir Min., Geogn., Geol. und
Petref (continued).
W. K. J. Gutberlet.—Die Zeit-Folge der hoheren Oxydation des
Mangan und Eisen Oxydules und ihre geologische Bedeu-
tung, 430.
Letters; Notices of Books, and of Mineralogy, Geology, and
Fossils.

Palzeontographica. (Dunker und Von Meyer’s.) Vol. iv. pt. 3.1855.
H. von Meyer.—Crocodilus Buetikonensis, aus der Stisswasser-
Molasse von Biitikon in der Schweiz, 67 (plate). _
Ferd. Roemer.—Palzoteuthis, eine Gattung nackter Cephalo-
poden aus Devonischer Schichten der Eifel, 72 (plate).
H. von Meyer.—Ueber den Nager von Waltsch in Bohmen, 75
(plate).
as Physichthys Hoeninghausi, aus dem Uebergangskalke
der Kifel, 80 (plate).
Schildkrote und Vogel aus dem Fischschiefer von
Glarus, 84 (plate).
_— Helochelys Danubma, aus dem Griinsande von
Kelheim in Bayern, 96 (plate).
—— __Trachyteuthis ensiformis, aus dem lithographischen
Schiefer in Bayern, 106 (plate).

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Itales.

Arnott, N. On the Smokeless Fireplace, Chimney-valves, and other
means, old and new, of obtaining healthful warmth and ven-
tilation.

Ashley, J. M. The Relations of Science.

Baltic Pilot. Supplementary Sailing Directions. 1855. From the
Lords Commissioners of the Admiralty.

Binney, E. W. On the Permian beds of the north-west of England.

Black Sea Pilot; by the Chev. T. de Marigny. 1855. From the
Lords Commissioners of the Admiralty.

Bothnia Pilot; by Admiral Gust. af Klint. 1855. From the Lords
Commissioners of the Admiralty.

Candolle, A. de. Géographie Botanique Raisonnée ou exposition
des faits principaux et des lois concernant la Distribution Géo-
graphique des Plantes de PEpoque Actuelle. 2 vols.

Catalogue of Charts, Plans, Views, and Sailing Directions, &c. 1855.
From the Lords Commissioners of the Admiralty.

Dawson, J.W. Acadian Geology ; an Account of the Geological
Structure and Mineral resources of Nova Scotia.

90 DONATIONS.

De la Beche, Sir H. T., & T. Reeks. Catalogue of Specimens illus-
trative of the Composition and Manufacture of British Pottery.
From the Museum of Practical Geology.

Dilke, C. W. Catalogue of a Collection of Works on or having
reference to the Exhibition of 1851, in the possession of
C. Wentworth Dilke.

Forchhammer, J. G. Ueber den Einfluss des Kochsalzes auf die
Bildung der Mineralien.

Graty, A. M. du. Mémoire sur les productions minérales de la
Confédération Argentine.

Hauer, F. R. von. Der Cephalopoden-Fauna der Hallstatter
Schichten.

Hauer, F. R. von, & F. Foetterle. Geologische Uebersicht der
Bergbaue der Oesterreichischen Monarchie. Im Auftrage der
K. K. Geologischen Reichsanstalt zusammengestellt. Mit
einem Vorworte von W. Haidinger. - Herausgegeben von dem
K. K. Central-Comité fur die allgemeine Agricultur- und Indus-
trie-Ausstellung in Paris.

Hooker, J. D., & T. Thomson. Introductory Essay to the Flora
Indica.

Horner, L. An account of some recent Researches near Cairo,
undertaken with the view of throwing light upon the Geological
History of the Alluvial Land of Egypt. Instituted by Leonard
Horner, Esq. Part I.

Houzeau, J. C. Essai d’une Géographie Physique de la Belgique.

Jennings, F. M. On an Analysis of the Potash and Soda Felspars
of one of the Dublin Mountains.

Lyell, Six C. On certain Trains of Erratic Blocks on the Western
Borders of Massachusetts.

Lyell, Sir C., & J. Hall. Rapport sur la partie Géologique de
PExposition de New York. (Traduit de Anglais par M. 4.
Laugel.)

Manual of Scientific Inquiry; prepared for the use of Officers in
Her Majesty’s Navy, and Travellers in general. Edited by
Sir J. F. W. Herschel, Bart. 2nd Edit. From W. J. Hamilton,
Esq., Pres. G.S.

Martins, Ch. Note sur les Erosions des Roches Calcaires dues aux
Agents Atmosphériques, mais simulant des traces de grands
courants diluviens.

Meteorological Observations taken at the Stations of the Royal
Engineers in the Year 1853-54, Abstracts from the. Edited
by Lneut.-Col. H. James, R.E.

Meyer, H. von. Zur Fauna der Vorwelt. Zweite Abtheilung. 5 & 6
Lief.

DONATIONS. — 91
Montagna, C. Saggio di Studii sul Carbone Fossile di Agnana.
Part I. Geoiogia.

Parliamentary Reports. Further Papers relative to the Discovery
of Gold in Australia. From Sir P. G. Egerton, Bart., M.P.,
£.G.S.

- New York Industrial Exhibition. Special Report of
Sir C. Lyell. From Sir P. G. Egerton, Bart., M.P., F.G.S.

—-—. Papers relating to Coal derivable from the Mines near
Heraclea. From Sir P. G. Egerton, Bart., M.P., F.G.S.

Phillips, J. Manual of Geology, Practical and Theoretical. From
Messrs. Griffin, the Publishers.

Pictet, F. J. Matériaux pour la Paléontologie Suisse, ou recueil de
Monegraphies sur les Fossiles du Jura et des Alpes.

Practical Rules for ascertaiming and applying the Deviations of the
Compass caused by the Iron in a Ship. 1855. From the Lords
Commissioners of the Admiralty.

Quetelet, A. Notices extraites de lAnnuaire de l’Observatoire
Royai de Bruxelles pour 1855.

ee

Sur la relation entre les Températures et la Durée de
la Végétation des Plantes.

Renevier, H. Seconde Note sur la Géologie des Alpes Vaudoises.

Report to be presented by the Parliamentary Committee to the
British Association, on the question, Whether any measures
could be adopted by the Government that would improve the
position of Science or its Cultivators in this country. From the
British Association. “

Ricca. Discorso sopra le opere del P. D. Ambrogio Soldani.
From the Accademia det Fisiocritict di Siena.

Sandberger, F. Ueber Anoplotheca, eme neue Brachiopoden-
Gattung.

Suess, E. Notice sur ’ Appareil Brachial des Thécidées. Traduite
_ par M. le Comte de Marschall. Et Observations sur le méme
sujet, par M. EL. Deslongchamps.

Tuomey, M., & F. 8S. Holmes. Fossils of South Carolina, 4°. parts
1&2: ae

Zeisczner, C. Geognostische Schilderung der Gangverhaltnisse bei
Kotterbach im Zipser Comitat.

1048 Volumes of Books, 57 unbound Volumes, and Sundry Maps,
Plates, and Pamphlets. Bequeathed by the late G. B.
Greenough, Esq.

A

F r
PAV '%

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

DecEMBER 5, 1855.

Henry Conybeare, Esq., John Lubbock, Esq., and R. H. Jarvis,
Esq., were elected Fellows.

The following Communications were read :—

1. On the Titestoness, or DowNTON SANDSTONES, in the Neigh-
bourhood of Kineton, and their Contents. By R. W. Banks, Esq.

(Communicated by Sir Roderick I. Murchison, V.P.G.S.)
[Puate II.]

On a reference to the Geological Maps of the Ordnance Survey of
the Counties of Radnor and Hereford, it will be seen that the line of
junction of the Old Red Sandstone with the Ludlow rocks proceeds
i a north-easterly direction from the Painscastle Hills to Kington,
and thence skirts the range of hills which run in the direction of
Shobdon and Richards Castle, to Ludlow. The present notice will
be mainly confined to an account of the junction-beds in the neigh-
bourhood of Kington.

At Kington a tongue-like portion of red sandstone runs out north-
wardly from the general mass to Bradnor Hill. The extreme point
of it is marked on the Geological Survey Map as Tilestone. The

VOL. XII.—PART I. H

a |

94 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 5,

quarry from which the remains hereafter mentioned were obtained
is situated on this spot, between Bradnor Farm and the Quarry
House.

The lane which leads from Newton to Bradnor Hill in the direc-
tion of the quarry affords a good section of the beds which here
immediately underlie the tilestone.

The lowest fossiliferous bed exposed in the lane is the equivalent
of the Ludlow bone-bed, here a soft liver-coloured layer, varying
from two to three inches in thickness, and containing, generally, Or-
thoceras gregarium, O. politum (M‘Coy), Goniophora cymbeformis,
Orthonota amygdalina, Orbicula rugata, Holopella, Chonetes lata,
Cornulites serpularius, Cucullella antiqua, Modiolopsis levis, Rhyn-
chonella nucula, and Bellerophon carinatus, occasionally also the
spines of Leptocheles, Onchus tenuistriatus, the shagreen of Sphago-
dus, and small shining black pipes and fluted plates which resemble
figures 37 to 45, plate 4, of the “Silurian System,” in illustration of
the contents of the Ludlow bone-bed, and may perhaps be referred to
Serpulites.

Above this layer, before the tilestone is reached, layers of Ortho-
nota amygdalina and Trochus helicites, much flattened, occur. The
uppermost beds are thin shaly beds of tilestone, containing a Lingula
of a very small size (probably Lingula minima), grouped together in
masses, and occasional traces of Pterygotus.

In the quarry the beds of stone dip to the east, at an angle of 15°;
immediately under the surface-soil a few tilestones are obtained ;—
next three beds of a bluish-white stone* occur, about 12 feet in
thickness, used for wall-stone. These beds of stone are very hard
and close-grained, containing but little mica, except in the uppermost
layers, and are unfossiliferous.

Between these upper beds and the underlying bed is a greyish
layer, varying from three to six inches in thickness, occasionally of a
blackish-grey colour, from the quantity of vegetable remains mixed
up with it, and containing on the western side of the quarry the re-
mains of Fish (Pteraspis) and of Pterygotus and other Crustaceans.
This layer, when dry, is tough, and the remains are with difficulty
removed from it ; but, when placed in water, it separates easily, where-
ever the remains occur, and, if left in water, soon decomposes into mud.
It appears to have been just such a muddy sediment, accompanied
with sea-weeds, as was suited to Crustaceans. The organic remains in
this layer retain their dermal covering, which is often glossy and in a
more perfect state than in the underlying beds of Downton sandstone.
Small round rusty nodules, sometimes irregular, occur in this layer:
in abundance, but no Molluscat.

* Neither these, nor the blue portion of the Downton beds hereafter noticed,
effervesce with sulphuric acid.

+ The nodules appear to be due to vegetable remains. This layer is probably
the same as the layer containing remains of carbonized vegetables at the bottom of
the Old Red Sandstone of Clun Forest, in the sandy beds above the tilestune at
Hagley Park and in the railway-cutting near Flaxley, noticed by Sir R. I. Murchi-
son, “ Siluria,” pp. 139, 140, 237, 245.

1855. ] BANKS—TILESTONES OF KINGTON. 95

The next bed, which is probably identical with the Downton sand-
stone, consists of a yellowish-white close-grained sandstone, on the
east side of the quarry passing gradually into a blue and still harder
stone, which contains occasional traces of Pterygotus, but more fre-
quently Lingula cornea. The yellow portion of this bed contains
throughout Pterygotus and Fish (Péeraspis) with an occasional
Trochus helicites ; but the remains are not so abundant as in the grey
layers and underlying bed. This bed is from 3 to 4 feet thick.

This is followed by a grey layer, similar in composition and con-
tents to the grey layer before noticed. The next, or bottom bed of
the quarry is a yellow sandstone of still better quality, capable of
being dressed to a very fine surface, and much used in building. It
is about 4 feet in thickness. The lowest portion of it consists in
many parts of the quarry of large flagstones, from a foot to eighteen
inches thick, used for gravestones; these lie on the Ludlow rock,
here a very hard unmanageable stone, termed by the quarrymen
*‘oreenstone.’ The Pterygotus and Fish-remains occur down to the
very bottom; where first appear in considerable abundance the spines
of Leptocheles*: Trochus helicites, much depressed, and the small
Lingula before noticed, also occur in these lowest portions of the bed.

Before noticing the remains obtained from this quarry, other
quarries in the neighbourhood will be referred to in order to show
that the same remains occur there in a similar position and under
like circumstances.

About a quarter of a mile lower down Bradnor Hill, at Ivy Chim-
ney, is another sandstone quarry. Among the refuse stones of former
workings the Fish-heads+ (Pteraspis, Kner; Cephalaspis, Agassiz)
occur. The recent workings exhibit micaceous unfossiliferous sand-
stone, and do not reach the Downton beds. The micaceous beds afford
a confirmation of the course of the line of drift, noticed in the “ Silu-
rian System,” p.512. A large boulder about a yard in diameter, com-
posed of red and white quartz-pebbles{, imbedded in a hard cement,
has been excavated and lies in the quarry. Water-worn pebbles, at first
sight like granite, of the syenite of Stanner Rocks, are abundant, and
limestones, the surfaces of which retain traces of Corals and yet are so
calcined. as to crumble in the hand, exhibiting when broken the un-
altered crystalline limestone of Old Radnor, are also imbedded. All
these foreign materials were probably drifted here with the deposits
which now form the sandstone beds. A little lower down the hill is
another quarry, lying near the Iron-foundry ; the bottom beds of
yellow stone are exposed. ‘Traces of the gréy layer between the beds
exist. In the few stones recently raised I found traces of Pterygotus,
one-half of the head of a Pteraspis, and a Lingula cornea. Here the

* Imperfect casts of a small bivalved Crustacean also occur here, which Mr.

Rupert Jones has recognized as a Leperditia and referred with doubt to L.

marginata, Keyserl. sp. See Ann. N. Hist. for Feb. 1856, p. 95.
_ + The remains of Fish here referred to are those figured in PI. II. figs. 1-3.
See the appended descriptions of two species, Pteraspis truncatus and P.
Banksii, p. 100.
t See the notice of this rock, “ Silurian System,” p. 314.
H 2

96 PROCEEDINGS OF THE GEOLOGICAL socieTy. [Dec. 5,

conglomerate of red and white quartz, imbedded in the sandstone,
again occurs.

The yellow, or Downton beds, are worked in a quarry on the
Lodge Farm, in the adjoiming parish of Huntington, and contain
traces of Pterygotus and Pteraspis truncatus.

A quarry, now abandoned, was some years since opened on New
Barn Farm, Kington, on the sloping ground on the southern side
of the Arrow. ‘The surface-soil is not more than four feet above
the Ludlow rock. Among the refuse stones I found a portion of
Pterygotus, in a stone corresponding in composition with the lowest
beds at Bradnor Quarry, and Pteraspides in a micaceous sandstone.
The ground slopes abruptly from the quarry towards the river ; and on
the slope, some feet below the sandstone, the bone-bed, containing in
addition to the Mollusca before named, Theca Forbesii, is exposed.

The similarity in appearance of the stone, of which the church
and many of the houses in New Radnor and its neighbourhood are
constructed, with the lowest Bradnor beds, induced me to examine
the quarry from which it was obtained. The road to this quarry pro-
ceeds from New Radnor to Harley, and then up a narrow valley by
the side of one of the streams which run from the Forest of Radnor to
the blue flag- or slate-quarry ; a steep road here skirts and gradually
ascends the hill on the opposite side of the valley. In the last steep
ascent, stones containing Chonetes lata, Orthoceras bullatum, and
other common forms of the Upper Ludlow rock, occur on the surface.
The sandstone-quarry is situated at a very considerable height, not
far from, and to the north-east of, the Trigonometrical Station. It
is a mere outlying patch of sandstone, reposing on the Ludlow rocks.
The yellow bed of sandstone alone occurs,—from 8 to 9 feet thick,
almost free from mica*, and with the surface of the beds coated
over with small crystals of quartz. The quarry has not been worked
for some years. In the refuse stone, Pterygotus and the small
Lingula occur.

Between Shobdon and Mortimer’s Cross on the side of the turn-
pike-road is a quarry, the lowest beds of which are Downton sand-
stone, similar in composition with, but rather more of a yellow tint
than, the same beds on Radnor Forest and Bradnor Hill. Lingula
cornea occurs in abundance, with occasional traces of Pterygotus in
the refuse stone of the Downton beds, the lowest bed of which was
not exposed when I visited the quarry. The layer of carbonized
vegetables is also present.

At the bottom of the old red sandstones on the right bank of
the Teme, near Ludford, and opposite to the Paper Mills, is a thin

layer containing carbonized vegetables, lying immediately underneath _

the old red sandstone and on a bed of bluish-white marl. In this
layer Mr. Lightbody and myself found spines of Leptocheles and a
Fish-bone+, about three inches in length and a quarter of an inch in

* The grains of mica are very minute and apparently enter but little into the
composition of these beds.

+ Prof. Huxley has examined this, and believes it to be either the j jaw or tooth
of a Chimeroid ? Fish.

1855.] BANKS—TILESTONES OF KINGTON. 97

width. The lithological composition of the bed overlying this layer is
that of the old red sandstoné,—a coarse-grained micaceous grey stone,
altogether unlike the tilestone-beds. Above the bone-bed at Ludford
we noticed in the tilestone-beds near the surface Lingula cornea.
The range of the Pterygotus has been shown to extend low in the
Ludlow Rocks*. I have met with only one trace of it below the
tilestones,—in the shales on the side of the descent of Knill Garra-
way, which contain Cardiola inter rupta, Graptolithus Ludensis, and
Orthoceras primevum. This specimen, viewed with the naked eye,
appears nothing more than a black marking of an inch in length ;
with the aid of the microscope scales of Pterygotus appear ; but
there is nothing to indicate to what part of the animal it belonged.
The specimens in my possession prove that the Pterygotus was more
abundant in the Tilestones than in any of the underlying strata.

The Pterygotus of the Tilestones is probably identical with the
Pterygotus so graphically described by Mr. H. Miller in the eighth
chapter of his ‘Old Red Sandstone.’ It was a lobster-like animal
with a flexible tail, composed of several segments and probably ter-
minated by natatory fins. Mr. Miller considers that the terminal
flap of the tail was entire; but it is possible that he may have con-
sidered as the terminal flap one of the curiously edged segments
presenting on the upper and under side a convex surface covered with
scale-like markings.

The Pterygotus possessed two most distinctive features, which are
wanting in Limulus: a flexible tail, composed of segments, and a series
of regular jaw-feet ; while the only species of Limulus+ known have,
as a caudal appendage, a straight pointed stylet without joints, and,
in common with many of the Pecilopodat, have, as a substitute for
jaw-feet, spiny appendages at the base or haunches of the first six
pairs of feet.

In the specimens of the joints, which formed the base of the feet
of Pterygotus, there is no vestige of any such appendage. I think I
may therefore venture to differ from the generally received opinion
that Pterygotus was one of the Pecilopoda, allied to Limulus of the
Indian Seas.

The illustrations§ accompanying the present notice contain three
distinct. jaw-feet, with some of their appendages,—joints of some of
the first pairs of feet,—fingers of the forceps,—portions of the cara-
pace,—and a few segments of the tail, with the natatory appendages.

amas Siluria,” p. 142, 237, 346; Strickland and Salter, Quart. Journ. Geol. Soc.
vol. viii. p. 386; Symonds, Edin. New Philos. Journ. April 1855.

ft See Cuvier, Le Régne Animal; Les Crustacés, par M. Milne-Edwards; p. 249
et seq. and plate 76.

t “Mais c’est surtout par Pabserice de mandibules et de machoires ordinaires
qu ils (Pecilopoda) s’éloignent de tous les autres Crustacés ;”’ ibid. p. 247.

§ Mr. Banks’s beautiful drawings of the several portions of Pterygote contained
in his collection are not reproduced with this memoir, but have been at his request
transferred to the Museum of Practical Geology for the illustration of the descrip-
tion of Pterygotus which is intended to be published in the Memoirs of that Insti-
tution.—Ep. Q. J.

98 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Dec. 5,

The remains of Pteraspides before referred to are, I believe,
undescribed. There are two species, differing essentially in form,
although nearly allied in structure. Both possess under the outer
dermal covering the granular texture, on the existence of which
M. Agassiz * laid so much stress in pronouncing his opinion on the
head of Cephalaspis Lloydii; but instead of granules, resting on
lamine, the lower end of each of the granules fits into an irregular
hexagon (PI. II. fig.2¢). In addition, the bony enamel of the Old
Red fish is wholly wanting. Both had a dermal covering, marked
with very distinct longitudinal striz +, which in most of the speci-
mens has wholly or partially disappeared.

Many of the specimens from the Tilestone are in a state of disinte-
gration ; the granules lie separated on the surface, and the hexagons,
thus exposed, are visible to the naked eye. To use Mr. Miller’s
description in reference to Cheiracanthus and Diplacanthus,—“ The
cranium seems to have been covered, as in the Shark family, by
skin, and the skin by minute shagreen-like scales; and all of the
interior cerebral framework which appears underneath exists simply
as faint impressions of an undivided body, covered by what seems
to be osseous points,—bony molecules, it is probable, which were
encrusted in the cartilage t.”

The most prominent features of the species illustrated by Pl. IT.
fig. 2. are a round snout, followed by a sharp projection on either side,
with horns attached to the sides of the posterior part of the head.
The strize of the horns are almost regularly parallel and so continue,
though with less regularity, over the sharp projections and round
the snout. On the upper, or raised portion of the head, the strize
proceed from the ridge in somewhat curved longitudinal lines, every
fourth one of which is larger and more prominent than the others,
until they meet in the centre above the snout. On the underside of
the sharp projections before referred to are protuberances which
seem to be projecting horny eyes, similar to those of crustaceans.

The other species (PI. IT. fig. 1) has an almost square, slightly in-
curved snout, without lateral horns, or trace of eyes; the strize are
less regular, and there is an indication of an upper jaw. For other
details I must refer to the drawings and the specimens, which
accompany this notice.

These fossils occur in places in considerable abundance. Like
the Pterygotus, with which they are often found im juxtaposition,
they appear to have congregated in masses and to have frequented
the same haunts.

Of another specimen, which occupies a doubtful place between
the Crustaceans and Fish, I must defer an account until I can fur-
nish an accurate illustration of it. The portion I have found is

* See ‘The Silurian System,’ p. 595.

+ Such longitudinal striz are visible on the head ef Cephalaspis Lioydii in the
Museum at Ludlow. °

+ Footprints of the Creator, p. 43.

1855. | BANKS—TILESTONES OF KINGTON. 99

about two or three inches in length. The surface appears to be
covered with shagreen, with an underlayer of minute closely-set
circular hollows, which traverse the surface with the greatest regu-
larity.

Fa peaitien of a Crustacean, probably a species of Eurypterus,
was found in the grey layer before noticed (see Pl. Il. fig. 4); it 1s
very imperfect ; the trace of the dermal covering is slight, and the
posterior segments, which would throw a greater light on its proper
position, are wanting. The posterior portion of the head, at the
junction with the thorax, is bounded by an almost straight line,
of an equal width with the bands, which are entire from side to
side and without any longitudinal depression. Mr. Salter proposes
to name it HE. pygmeus. One specimen which I lately found had
a distinct swimming-foot on the left side, resembling those figured
by various authors who have written on the genus.

I have figured also some specimens of the Crustacean named Hz-
mantopterus Banksit by Mr. Salter*. The species is not uncommon
in the Kington beds, and is represented by detached heads (PI. II.
figs. 5a, 56, 5c), body-rings (figs. 5 d, 5 e), and spines (fig. 6),
which are very possibly the caudal spines.

It is very probable that traces of the same remains will be found
to exist wherever the Downton sandstone (or tilestones) occurs and
is regularly quarried, but the continued working of the Bradnor
Quarry has afforded unusual means of investigation. In a quarry
abandoned, or where the strata are merely exposed, there’is neces-
sarily but little opportunity of learning the contents of the beds;
for m many portions of the tilestone beds an occasional slight
marking is the only indication of the existence of these remains,
while in other portions they occur congregated together in great
abundance.

Adopting the test made use of by M. Alcide d’Orbigny + in order
to ascertain whether these beds belong to the Old Red Sandstone,
as was originally considered by Sir R. Murchison, or to the Ludlow
Rocks,—the absence of the Mollusca of the Ludlow Rocks and the
presence of Fishes and Crustaceans, which have never been found
in the Ludlow Rock, and the greater development of Pterygotus,
which occurs in Scotland in the middle beds of the Old Red Sand-
stone {, lead to the conclusion that these Downton, or Tilestone beds,
should be considered as separate from the beds in which the Mol-
luses of the Upper Ludlow rock occur, and be classed as the bottom
beds of the Old Red Sandstone.

Doubtful as it is whether the buckler-like fossil remains above
referred to belonged to Fishes or to Crustaceans, it is certain that

* Quart. Journ. Geol. Soc. No. 45. p. 32.

+ Cours élémentaire de Paléontologie, vol. ii. pp. 245, 256. Caractéres strati-
graphiques négatifs, § 1598. Car. strat. positifs, § 1598. Des exceptions aux
limites des faunes géologiques, §§ 1605—1609.

{ See Miller’s ‘Old Red Sandstone,’ 5th edit. p. 177-179.

100 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 5,

they are closely allied to Cephalaspis Lloyd and C. Lewisii. This
fact will probably be sufficient to remove all doubt that the beds in
which they occur form part of the Old Red Sandstone.

Traces of these remains have been recently found in the tilestone
beds at Northfield, Shobdon, by the Rey. J. F. Crouch, President
of the Woolhope Field Club.

APPENDIX.

Prof. Huxley and Mr. Salter have carefully examined the cephalic
bucklers referred to above, and have compared them with the remains
of previously described species; and Prof. Huxley is now minutely
examining their structure in order to determine their true relationship,
either to Crustaceans or to Fishes. In the meantime, and until we
may hope for a complete account of these fossils, I have been favoured
by the above gentlemen with short descriptions of the two figured
species, which are easily distinguishable from those found in the
Cornstones of the Old Red Sandstone. 7

‘‘Preraspis, Kner*, 1847.

As it is evident,—whether these shields be eventually referred to
Fish, as suggested by Agassiz, or to Crustaceans, to which opinion
some naturalists incline,—that they must be separated generically
from the broad cornuted heads of Cephalaspis Lyelli, we cannot do
better than adopt the name suggested by Dr. R. Kner.

The characters of the two new species may stand as follows :—

Pteraspis truncatus, Huxley and Salter.

P. capite elongato, ovato, regulariter convexo, anticé truncato vel
emarginato, posticé contracto, gibbo, carimato, brevispinoso :
superficie lineis undosis longitudinalibus distinctis tenuissimé
interstriatis.

Pteraspis Banks, Huxley and Salter.

P. capite laté elliptico subdepresso, posticé truncato carinato bre-
vispinoso, anticé contracto, et utroque tuberculo marginali ;
lateribus planis et quasi alatis: superficie striis tenuissimis cos-
tulisque ornata, et ante medium capitis tuberculis 9-11 clavatis
é linea mediana radiantibus.

There is another species, very like the P. ¢runcatus, in the Upper
Ludlow Rock, lately discovered by the geologists at Ludlow. It will
be described hereafter.”’ |

* Ueber die beiden Arten Cephalaspis Lloydii und Lewisii, Agassiz, und einige
diesen zunachst stehenden Schalenreste: Haidinger’s Naturw. Abhandl. vol. i.
p- 159, pl. 5.

Ford & We st,lmp.

CRBone,]ith.

‘RWB. del.

FOSSILS FROM THE TILESTONES

of Kington.

1855. | BANKS—TILESTONES OF KINGTON. 101

Fig.

Fig.

EXPLANATION OF PLATE II.

1. Piteraspis truncatus, Haxley and Salter.
1 a. Cephalic buckler, or head, showing the upper surface; natural size.

1 4. Cephalic buckler, or head, showing the upper surface ; enlarged one-
half, to show the striz.

1c. Cephalic buckler of another specimen (natural size); the greater
part of the surface has heen destroyed; the striz remaining in
parts, and elsewhere the granular layer visible.

1d. Profile of part of a head: the granular layer is seen, and in parts the
striated dermal covering also.

2. Pteraspis Banksii, Huxley and Salter.
2a. Natural cast of the interior of a cephalic buckler; natural size.

2.6. Portion of the anterior part of a cephalic buckler; natural size: the
upper striated layer has been worn away.

2c. Fragment of buckler, highly magnified ; showing the constituent layers.

2d. Eye-like marginal protuberance,—one of these is situated on each
side of the anterior projection of the buckler.

Fig. 3. Portion of a head, similar in structure to the others, but imperfect ;

natural size. Only one specimen has been found. From the grey
layer.

Fig. 4. Eurypterus pygmaeus, Salter.

4a. The head and five of the body-rings (Mus. Banks).
46, The head of another specimen (Mus. Geol. Survey).

Figs. 5 & 6. Himantopterus Banksii, Salter (Mus. Banks and Geol. Survey).

5a, 56,5 c. Heads of different individuals.
5 d, 5 e. Body-rings of different individuals.
6. Probably a caudal spine of an individual belonging to this species.

102 PROCEEDINGS OF THE GEOLOGICAL sociETy. [Dec. 5,

2. On the Last Exvevation of the Aurs; with Notices of the
Hereuts at which the Sra has left Traces of its ACTION on
their Sipes. By Daniex Suarpe, Esq., F.R.S., F.G.S. &e.

[ConTENTS. |

Introduction.
Traces of Erosion on the Sides of the Mountains.
Ist Line of Erosion.
2nd Line of Erosion.
3rd Line of Erosion.
General Results.
Lines of Water-level traceable in the Excavation of the Valleys.
Terraces of Alluvium in the Alpine Valleys.
Valleys of the Rhone and its Tributaries,
Valleys of the Rhine and its Tributaries,
Valleys of the Inn and its Tributaries.
Valleys on the Sonth of the Alps.
General Results.
Theoretical Conclusions.
Erratic Blocks.
Tables of the Altitudes of Heads of Valleys, Terraces, and Erosions.

Introduction.—In the following pages I have attempted to show,
that, after the Alps had assumed their present form, and when they
already stood as much above the surrounding lowlands as at present,
they must have been nearly submerged below the sea, out of which
their rise must have been, by a series of steps or starts of unequal
amount, separated by long intervals of time. The evidence on which
these views rest is derived from three sources; Ist, from the traces
of erosion on the sides of the mountains, ending upwards in lines of
uniform level; 2ndly, from the levels to which the vallevs have been
excavated; 3rdly, from the elevation of the terraces of alluvium in
the valleys ; and lastly, from the harmony of the results obtained
from these three sets of observations, when compared together*.

Traces of Erosion on the Sides of the Mountains.

In reading Prof. James Forbes’s interesting description of Norway,
I was much struck with his remarks on the frequent occurrence of
rugged and precipitous mountain-ranges rising, at the same elevation,
from a comparative level of gentle undulations destitute of angular
prominences, where this change of form cannot be due to different
powers of resistance in the rocks, which are of the same character
both above and below the changes. Prof. Forbes states that, “‘as a
general rule, the surfaces of erosion (whether produced by glaciers or
otherwise) havea tolerably definite superior limit, as in the Alps, only
here [in Norway] at somewhere about 1500 to 2000 feet above the

* Mr. R. Chambers has brought forward evidence, in some respects similar,
to prove that Great Britain was submerged beneath the sea during the Pleistocene
period; ‘ Ancient Sea Margins,’ 1848.

1855. ] SHARPE—ELEVATION OF THE ALPS. 103

sea, instead of 7000 or 8000, as in Switzerland.’ After referring to
an observation of M. Agassiz, that ‘the limit of the surfaces of fric-
tion coincide with the levels of ancient glaciers, above which only the
peaks of the higher mountains stood forth bare, or merely snow-
covered, but free from the abrading influence of moving ice,” and
adding some remarks too long to quote, the author concludes,—
“adopting hypothetically, then, the theory of glaciers to account for
the singular configuration of the Norwegian rocks, it fits so far well
in its different parts as to explain plausibly the phenomena; and
whether correct or not, the analogy, on a great scale, of the line of
demarcation of the rugged summits and the abraded slopes of the
Norwegian and Swiss Alps, inclines us strongly to adopt a common
theory in explaining both*.”

In rambling over the Swiss Alps with Prof. Forbes’s remarks in
my mind, one of the subjects to which my attention was directed was
the much-disputed question of the extent to which glaciers had for-
merly reached ; and it was with this object in view that I first paid
attention to the upper limit of the erosion of the mountains ; but, as
all my observations led me to limit the action of ancient glaciers to a
degree which did not allow of considering them as the agents which
had produced the surfaces of erosion described, I was driven to look
elsewhere for an explanation. The traces of ancient. glaciers seemed
to me to be confined to the valleys, and only to reach between 1000
and 3000 feet below the present glaciers}; but the traces of erosion,
up to a definite line, are seen not only on the higher snow-capped
mountains, but on detached hills in advance of the great chain, such as
the Mythen of Schwytz, and the hills which enclose the Lake of Thun,
which have their flanks rounded up to the height of 4700 or 4800
feet above the sea. For glaciers to reach to those heights would re-
quire a sheet of ice 3000 feet thick descending from the whole extent
of the Alps, and covering to nearly that height the plam between the
Alps and the Jura; a supposition once thrown out by M. Agassiz
(‘ Etudes, &c.,’ p. 304), but which found so little favour that it is
not now worth combating.

Moreover, though moving ice rounds away the projections on the
sides of the rocks with which it comes in contact, it is nowhere seen
to scoop out hollows in their sides. As soon as the surface of the
rocks has become polished, the ice can produce very little farther
effect upon them; its action tends to produce a uniform surface, not
an indented one.

The action of water next suggested itself as the cause of the phe-
nomena in question: if the sea had stood for a long period at the

* “Norway and its Glaciers visited in 1851, by James D. Forbes,’ pp. 58 & 59;
and plate 2, which represents the mountains near the Folden Fiord, in illustra-
tion of the above remarks.

+ Many of the Swiss geologists are disposed to extend the ancient glaciers much
farther ; but they build their conclusions on the evidence of erratic blocks, which
belong to another set of operations of a period preceding that of the ancient
moraines.

104 PROCEEDINGS OF THE GEOLOGICAL society. [ Dec. 5,

level of the upper limit of the erosion, it would have produced a
marked indentation round the mountains, such as was under consi-
deration ; and as the mountains gradually rose out of the waters,
they would have had their flanks worn into rounded slopes; and
occasionally again indented by another line of erosion, whenever
their elevation was arrested and the waves continued to beat for a
long period against their flanks at another level *.

I had already observed several such lines of erosion in the Alps at
different levels, and I soon met with a complete confirmation of their
marking the levels of the ocean at their respective periods, in finding
that they corresponded in height with the levels of the action of water
shown in the excavation of many valleys. The inquiry now assumed a
new interest, and I regretted that, not having seen its full importance
at the outset, I had let slip many opportunities of making observations
which would have been valuable. For, if by such observations we can
mark thesuccessive stages at which the mountainsrested on their rising
out of the ocean, we may hope to throw light on some most difficult
problems of geological inquiry connected with the elevation of moun-
tain chains: we shall see how far that elevation was sudden or gra-
dual; whether the mountains of one chain were raised up together,
or separately ; and whether the different parts of the chains were
equally elevated. I am far from undertaking to answer all these
inquiries at present: I shall be satisfied if, in calling attention to a
field of inquiry applicable to other countries as well as to the Alps,
I have illustrated the subject sufficiently to lead to a due appreciation
of its importanceyt.

* See R. Chambers, ‘Ancient Sea Margins,’ pp. 183-189, describing the Lines of
Erosion on the Eildon Hills.

+ The views of M. Agassiz ou this subject will be found in his notes ‘ On the
Glacial Theory and its recent progress,” in the Edinburgh New Phil. Journ. vol.
xxxiii. pp. 232, 233; they have also been published by M. Desor in the ‘ Biblio-
théque Univ. de Genéve’ for March and April 1841, under the title “Sur le niveau
des Roches polies et sur les conséquences qu’on peut en tirer;” and again at p. 15
of an account of an ascent of the Shreckhorn in the ‘Revue Suisse’ for June 1843.
M. Agassiz states in the first-mentioned paper that ‘‘in Switzerland there exists a
limit at about 9000 French feet (9589 English feet) above which the summits are
no longer polished, but where the rugged peaks present a very striking contrast
to the lower surfaces, which are polished or at least moutonnés. In the exterior
chains of the Alps, the polishing does not reach to a greater height than 6000 or
7000 feet (6393 or 7460 English feet). It cannot be doubted that this limit,
which is so well marked, indicates the level of the bed of ice at the epoch of its
greatest thickness.”

M. Desor informs us that on the sides of the Seidelhorn the rocks are polished
to the height of nearly 8000 feet (8524 English feet), being about 200 feet above
the present level of the Glacier of the Finsteraar ; from which he concludes that
the upper limit of the polished rocks indicates also the upper ancient limit of the
glacier. On the sides of the Schreckhorn the polished rocks rise, as you ascend
the valley, until they are lost under the snow at an elevation of nearly 9000 feet
(9589 English feet), which he regards as the highest limit of polished rocks.

M. Desor’s remarks appear to apply entirely to the polishing of the surface of
rocks by the friction of glaciers; with which subject I have nothing to do at pre-
sent. But M. Agassiz appears to confound together the superficial polishing by
glaciers and the deep erosion which has altered the forms of the mountains and

1855. ] SHARPE—ELEVATION OF THE ALPS. 105

The contrast between the rounded and the rugged portions of the
mountains is best seen in the gneiss, where its foliation dips at a high
angle. Among the stratified rocks, there is often a difficulty of di-
stinguishing the flat surfaces of the beds from those produced by
subsequent abrasion.

The accompanymg woodcuts (figs. 1 and 2), taken from drawings
which Mr. Ruskin has had the kindness to lend me, will illustrate
this feature in the form of the Swiss mountains better than any de-
scription ; and they show us also that it attracts the notice of the
artist as well as of the geologist. The first drawing (fig. 1) is a view

Fig. 1.—The Chain of Mont Blanc, as seen from the Valley of
Chamouniz.

E, E, indicate the line of erosion.

of the Chain of Mont Blanc looking up the valley of Chamounix. In
this view the definite level at which the rugged peaks all rise from
the lower rounded shoulders of the chain is well seen, that level
being at about 9000 feet above the sea. The second (fig. 2) isa
drawing of the Matterhorn, or Mont Cervin, taken from the Riffelberg,
in which the same contrast is most strongly marked. I have not ascer-
tained the exact height of the base of the Matterhorn, which is above

‘worn away large portions of their sides. Prof. Forbes, on the contrary, though
alluding hypothetically to glaciers, really describes the erosion which I ascribe to
the waves of the sea.

It will be remarked that M. Agassiz notices two lines of erosion at different
levels in different parts of the Alps.

The contrast between the rugged peaks of the Alpine mountains and the rounded
shoulders from which they rise, had previously attracted the attention of M. Hugi,
who accounts for it by dividing granite into two mineral classes,—Ist, true granite,
which forms rounded masses; and 2ndly, halb-granit, which forms rugged peaks
(‘Alpenreise,’ p. 55); but he gives no mineralogical distinction between the
rocks, and no subsequent observers have been able to detect a difference between
them. The change of outline between the upper and lower parts of the same
mountains is shown in Hugi’s plates 8, 9, 12, and 13.

106 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [| Dec. 5,

Fig. 2.—The Matterhorn, as seen from the Riffelberg.

KW

E, E, indicate the line of erosion.

9000 feet; there is a thick covering of snow round it, which con-
ceals the line of erosion and makes it appear to be higher than it
really is.

There is no distinct lower limit to the abraded or rounded portion
of the mountains, but the upper limit of the abrasion is usually well
marked by a change in the outline of the hill-sides from a moderate
to a steeper slope, similar to the indentation produced on a coast by the
waves beating against a cliff*. The nearly uniform height of this
re-entering angle produces a tolerably level line round the mountains,
which I shall speak of as the line of erosion. It is best seen when
the observer is at a distance, or, if near, is only a few hundred feet
below it, when a horizontal line may often be traced by the eye round
every one of the mountain-tops within its reach; this is nowhere
more remarkable than in the view from the top of the Splugen Pass.
‘When standing on the level of the line of erosion, it is often more
difficult for the eye to follow it; slight inequalities in the ground
which are near at hand concealing or interfering with the view. This
makes it difficult to measure the height of the erosion within 100 or
200 feet, even under favourable circumstances. But there are spots
free from this difficulty : whoever has ascended from Zermatt to the
Riffelberg must remember the distinctness with which the conical
Riffelhorn rises from the flat at the top of the rounded Riffelberg :
the line of erosion is there as well marked as at the foot of a sea-
cliff, being (by my aneroid) between 9000 and 9100 feet above
the sea.

When the observer is more than 1000 feet below the line, it will
require a practised eye to estimate its height within 500 feet; and
the result will be merely a rough guess, which will usually prove to
be below the truth. In the following statements I have pointed out
those measurements which are most to be relied on; but in general,

* Some excellent profiles of cliffs and beaches have been given by Mr. Godwin
Austen, Quart. Journ. Geol. Soc., vol. vii. pp. 118, 120, and 124. ik

1855. | SHARPE—ELEVATION OF THE ALPS. 107

I feel that my best observations may, with one or two exceptions,
be 100 or perhaps 200 feet wrong, while the worst can, I think,
never have an error exceeding 500 feet. The admission of the pro-
bability of such errors may stagger the faith of my readers, but the
want of absolute accuracy will be found to be compensated by the
number of observations which harmonize sufficiently to restore confi-
dence in them.

There are many mountains in the Alps on which I failed to trace
any distinct line of erosion: but, when we recollect how long a period
has elapsed since the ocean reached to the flanks of the Alps, during
which time the surface of the rocks has been crumbling away from
the action of the atmosphere, I think it more remarkable that the
sea-levels are still to be traced at all on their sides, than that these
traces should have been frequently obliterated.

In pointing out the various lines of erosion which I was able to
trace on the sides of the Alps, I will begin with the highest, and
describe them in order from above downwards. The heights are all
reduced to English feet.

First Line of Erosion, 9000 to 9300 feet above the sea.—In
taking a general view of Mont Blanc from the Croix de Flegére, I
estimated the line of erosion to be above 9000 feet. From the Col
de Balme, I estimated it at somewhat above 9000 feet ; and from the
Col de la Seigne, which, being higher, brought me within a distance
in which the eye may be trusted, I placed it between 8900 and 9400
feet. The average between these observations is about 9000 feet.

On the Riffelberg, a good observation already mentioned, p. 106,
fixed the line of erosion at between 9000 and 9100 feet.

The top of the Stilvio Pass, 2814 metres above the sea, is about
200 feet above the upper limit of erosion, which gives us 9000 feet
for the height of the line of erosion: this measure may be trusted, as
in ascending to above the line I had a good opportunity of noting it
with tolerable accuracy. The rocks are limestone and dolomite,
belonging to the triassic series.

In all the three districts mentioned above, the effects of the erosion
are very strongly marked on the sides of the mountains, producing a
deeply indented line round them; this indentation represents the
amount of rock which has been removed by the waves, and proves to
us the great length of time that the sea must have stood at the level
in question.

A second and less-strongly marked line of erosion may be traced
round the lower shoulders of the Mont Blanc Range, a little above
the Col de Balme: I did not find it sufficiently well defined to note
its altitude accurately ; but it probably coincides with the Second
Line which I am about to mention.

Second Line of Erosion, about 7500 feet above the sea.—This
line may be traced over a great part of the centre of Switzerland, as
strongly marked on the mountain sides as the First Line, and in-
dicating an equally long period of the action of the waves at its level.
It attracted the attention of Professor J. Forbes, and led to his

108 PROCEEDINGS OF THE GEOLOGICAL society. [VDec. 5,

remark, already quoted, that the upper limit of erosion in the Alps
was between 7000 and 8000 feet above the sea. The following are
the places where I noted it.

On crossing both the Scheideck and the Wangen Alp, the line of
erosion is well seen at about 7500 ; in both these cases this line may
be observed on the nummulitic, as well as on the older rocks.

In the ranges of the Hochwang and the Casanna,: between Chur
and Klosters, which consist entirely of flysch, a rough estimate gave
me about the same height of 7500 feet for the line of erosion; and
in the Klausen Pass, between Linththal and Altdorf, I noticed the
line at about the same height on the jurassic, nummulitic, and flysch
rocks.

From the top of the Splugen the line may be very well traced
round all the neighbouring mountains; it is about 500 feet above
the Pass, or 7500 feet above the sea: it nearly corresponds to the
upper limit of the stratified slate-rocks of the neighbourhood, the
geological age of which is undetermined. |

In the Lukmanier Pass (6338 feet) and in the Pass of the Ober-
alp from Andermatt to the head of the Rhine (6580 feet), the
erosion reached to so great a height above the Pass, that I could not
estimate its upper limit accurately : in both instances the line was
somewhat above the highest jurassic rocks.

On the sides of the upper and middle parts of the Lake of Como
only a few tips of the highest hills of gneiss rise above the line of
erosion: as the highest hardly reach 8000 feet, the line must be
about 7500 feet high.

Third Line of Erosion, about 4800 feet above the sea.—The two 3

Mythen behind the town of Schwyz, consisting of cretaceous limestone,
afford an excellent example of the contrast between the rough steep
peaks above the erosion and the rounded shoulders below: the pass
between the two hills is 4726 feet above the sea, and is a little below
the line of erosion, which may be taken at about 4800 feet.

On the sides of the Rigi (nagelfluh) and Mount Pilatus (creta-
ceous), the erosion ends at about the same height: but I did not get
any accurate measurements.

The hills on both sides of the Lake of Thun rise above a line of
erosion, which, judging from their height, must nearly correspond
with that on the Mythen.

Many of the limestone hills round the foot of the Lake of Como
have their highest points a little above a line of erosion ; as only a
few of them rise a little above 5000 feet, so this line must here nearly
correspond with that on the north flank of the Alps at 4800 feet
above the sea.

General results of the preceding observations. —I have thus
pointed out three equally distinct and level lines of erosion to be
traced on the sides of the Alps at about 9000, 7500, and 4800
English feet above the sea, marking three long periods of rest in the
elevation of this great group of mountains, at each of which only so
much of the mountains as rises above this respective line then stood

ats

1855.] SHARPE —ELEVATION OF THE ALPS. 109

out of the waters: at the earliest of these periods the Alps formed
merely a cluster of small islands, with nearly precipitous sides
dipping.at once into very deep water, and surrounded by an open
ocean, the highest being 6750 feet above the sea. At the second
period there were a few large islands, rising to above 7000 and 8000
feet, separated by narrow channels, with deeply indented shores,
surrounded by a deep sea, and forming a group somewhat resembling
the Hebrides. At the third period the group would have more
resembled the north of Scotland, forming a long narrow island, in-
dented. with deep friths, but with its highest peaks 10,000 and
11,000 feet above the sea, and therefore probably capped with
snow.

It is probable that a closer examination would find other lines of
erosion, intermediate between the three here noted; but, if they
exist, they are far less marked, and consequently less important than
the three lines here described. They may also perhaps be found
below my lowest line; but it will require great care in tracing them ;
for, as we descend below that level, the vegetation interferes more
and more with our observations, and cultivation often modifies the
ground ; besides which, the lower heights lie principally among
stratified rocks, whose forms are as much due to the horizontality or
inclination of their strata as to subsequent erosion.

As the two lower lines of erosion have been traced equally across
the eocene and all the older formations, I thimk it is evident that
these erosions took place at'a late period,—probably after all the

‘strata of Switzerland (except the drift) lay in their present positions

relatively to one another: and there are no circumstances connected
with the uppermost line to lead us to place it before the same period :
the change indicated by these observations is the elevation of the
whole country out of the sea, as has been going on for several
centuries in Sweden and Norway.

This elevation seems to have been very uniform over the whole of
Switzerland ; or, if it has been greater at one end of the country than
the other, the difference must be very trifling; my observations give
a uniform level to the lines of erosion for about ninety miles from
N. to S., and a very near approach to uniformity from E. to W.
for nearly 200 miles. And, as stated at starting, I think that the
error in their general results cannot amount to 200 feet.

The amount of degradation which the Alps have undergone during

_ the periods here referred to seems to correspond with the enormous

accumulation of rolled detritus collected on their flanks. The area
of the great valley of Switzerland between the Alps and the Jura is
not very different in extent from the area of that portion of the Alps
of which the detritus would be carried northwards. I do not know
whether any one has made an estimate of the ‘average thickness of
the deposit of rolled detritus throughout that valley, which I should
estimate at several hundred feet. This therefore shows the abstrac-
tion of the same thickness of matter from the whole of the Alps, or
of a much greater thickness from the more limited area exposed to
the reach of the waves during their elevation.
VOL. XII.— PART I. 1 I

110 PROCEEDINGS OF THE GEOLOGICAL sociETy. [Dec. 5,

In the higher valleys, both in Switzerland and in the mountainous
parts of Great Britain, I have often been struck with the great accu-
mulations of rounded blocks and pebbles in places where there were
no torrents which could be supposed to have rounded them or
brought them to their present position. I particularly noticed a very
large collection of such blocks near the top of the Splugen on ascend-
ing from the north, where there were no lateral valleys down which
they could have been brought: they lay very thick at the elevation
of about 6000 to 6500 feet, reaching nearly to the top of the Pass,
covering the sides and filling up the bottom of the valley in irregular
hillocks, without forming any regular terrace, such as we see at lower
levels. These accumulations are doubtlessly formed out of the
destruction of the beaches of these early oceans, which, owing to the
steepness of the sides of the mountains, have been carried by the
slipping of the snow and by the gradual action of the weather to the
first resting-place below the level at which they were formed.

Lines of Water-level traceable in the Excavation of Valleys.

In ascending any alpine valley, we usually find the ascent tolerably
gradual until, on reaching the head of the valley, the ascent suddenly
becomes steep, and we have to climb some winding or fatiguing path
for a considerable height ; after this we often find ourselves in an-
other upper valley, which, like the lower one, is but moderately in-
clined until we reach its head, where a second steep ascent must be
climbed on to another higher level. The valley of the Engadin is
an example of such a structure ; from Martinsbruck we ascend the
Tnn gradually to Zernetz, situated at the head of the lower Engadin,
4910 feet above the sea; we then ascend rapidly about 250 feet on
to the level of the upper Engadim; then for nearly thirty miles the
ascent is so slight as to be imperceptible to the eye, until above the
lake of Sils, at an elevation of 5900 feet, we again find a steep ascent
to the Pass of Maloggia.

More frequently we find lateral valleys at a different level from the
main valley, into which they empty themselves by a cascade: thus
the valley of Linththal rises very gently to and ends abruptly at an
elevation of 2500 feet; but, if we climb a steep zigzag path by the
side of the falls of the Fatschbach, we come about 2000 feet above
the Linth to the level valley of Urnerboden, which ends, at a height
of 4700 feet, at the precipitous ascent to the Klausen Pass.

A more familiar illustration may be found in the Valley of Cha-
mounix, which rises gently to the village of Le Tour, 4274 feet above
the sea; a little above this commences the ascent to the Col de
Balme. But the lateral valley of the Mer de Glace ends some 1700
feet higher than the Valley of Chamounix; the glacier then rises
moderately ; from its termination below the Montanvert there is a
gradual ascent to a height of above 9000 feet at the head of the
branch called the Glacier de Lechaud*. The head of the Glacier

* These heights are taken from Prof. Forbes’s ‘Travels,’ &c., chap. i. 6.

1855. | SHARPE—ELEVATION OF THE ALPS. ig

de Taléfre, in which the Jardin stands, is also more than 9000 feet
above the sea. But the ice prevents our ascertaining with any
accuracy the exact height at which the change in the steepness of
the rocks takes place.

These deep indentations at the heads of valleys are not due to the
streams which flow down them, for their action tends to equalize the
slope of their beds: they must owe their origin to the action of
waves beating for a long period against the rock. To ascertain
whether the waters producing such effects were those of lakes or of
the sea, we have only to compare the levels to which they reached in
different valleys : if the same levels were only found in lateral valleys
connected with one main valley, we might attribute their production
to the waters of a lake: but when the same levels are found in
valleys which have no connexion with one another, or which lie on
the opposite sides of mountain-chains, we must refer their excavation
to the waves of the sea.

The latter is the case with the valleys of the Alps: the head of
the valley of Urnerboden, which is connected by the Linth with the
Rhine, is 4730 feet above the sea: Haudéres at the head of the
Valley of Herens stands at 4763 feet, and Ayer at the head of the
Valley of Annivier at 4776 feet ; these two latter valleys drain into the
Rhone: the Valley of Visp on the north side of Monte Rosa ends at
Zermatt, at 5410 feet; that of Gressonay on the south of Monte
Rosa ends near La Trinité at 5455 feet above the sea. From these
and other instances, which will be given in a Table, we learn with
certainty that the final excavation of these alpine valleys to their
present levels was done by the sea. It is not at present necessary to

consider what causes produced the cracks which enabled the sea to

penetrate so deeply into the flanks of the mountains, nor what
was their condition in the earlier geological periods, as I am only
treating of those later agencies to which the valleys owe their pre-
sent forms.

Coupling the conclusion, that the sea was the agent of excavation
of the alpine valleys, with the sudden changes of level previously
mentioned at p. 110, and with the different elevations above the sea
at which we find the valleys terminate, we learn a similar result to
that which we have already obtained from observing the lines of
erosion on the mountain sides,—that the elevation of the Alps out of
the sea has taken place by numerous steps or comparative starts,
after each of which was a period of rest long enough to allow the
waves to leave a permanent record of their action; and that through-
out Switzerland the whole chain was equally elevated, or as nearly so
as this method of observation will allow us to judge of.

The measurements on which my comparisons are founded are
principally derived either from the “‘ Hypsométrie de la Suisse”’ of
my friend M. Ziegler, or from the figures on the Map of Switzerland

ublished by the Federal Government, under the direction of General

ufour ; a few are reduced from my own observations by the ane-
12

112 PROCEEDINGS OF THE GEOLOGICAL society. [Dec. 5,

roid +. The two former do not give me the heights of the heads of
the valleys, but only those of the village nearest to its head, and this
is usually rather below the level of the head of the vailey. Another
source of error arises from the valleys being always more or less
choked up at their upper ends by detritus brought down from the
mountains by the torrents, and of which we cannot see the depth.
Judging from what I could observe of such deposits, I think it likely
that they do not often exceed 200 or 300 feet in such situations.
Fortunately these two errors are in opposite directions, and therefore
tend to neutralize one another. From these and other causes I con-
sider that the altitudes here given can never be relied on within 100
feet ; but they probably are all within 200 feet of the truth.

The highest valleys which contain glaciers do not admit of so near
an approach to accuracy: we have no means of knowing the depth
of the ice of the glacier, and can therefore only form a rough guess
of the level to which the head of the valley has been excavated.

The Table No. I. (p. 123) exhibits the heights above the sea of the
heads of a few valleys which I measured, and of a number of villages
which stand close to the heads of their respective valleys or just
below a spot where the valley exhibits a sudden change of level.
Where several names occur on one line, those places are on the same
line of drainage: where the village stands considerably below the
head of the valley, it is marked thus *, to show that the height there
given is below that of the head of the valley. All the measures are
reduced to English feet.

The followig levels may be reduced from the Table No. I. by
throwing together those heights which approximate most closely.

As I have no accurate measurements of the heads of the highest
valleys, owing to their being filled with ice, they are not inserted in
the Table ; but I may repeat that the branches of the Mer de Glace
end at above 9000 feet, and probably correspond at their highest
level with the highest line of erosion observed.

1. The Piedmontese Val Ferret ends at 7660 feet: I have not the
exact height of the head of the Allée Blanche, but have reason to
believe it to be about the same. This height nearly corresponds to
that of the “ second line of erosion,” noted at 7500 feet.

t The aneroid barometer is a treacherous guide, owing to the frequency with
which the hand is displaced by a jolt, and it cannot be trusted alone: but it will
answer all the purposes of a geologist in a tour where he has frequent opportuni-
ties of comparing it with a mercury barometer, or of checking the accuracy of its
index in passing spots of which the heights are known. As there is hardly a hill
or a village in Switzerland of which the height above the sea is not published,
these opportunities are offered to the tourist several times every day; and, if he
finds that no displacement of the hand has taken place, he may rely on his inter-
mediate observations to within 10 feet. The contemporary changes of the atmo-
spheric pressure may be traced from the meteorological observations at Geneva and
at the Great Saint Bernard, which are published monthly in the “ Bibliothéque
Universelle de Genéve,’”’ and from the recorded observations of Prof. Wolf of
Berne, which, though not published, are, through that gentleman’s kindness,
equally accessible.

1855. ] SHARPE —ELEVATION OF THE ALPS. 113

2. Prérayean at the head of the Valtelline, which I did not visit,
stands at 6593 feet.

3. The valleys of the Rhone, the Engadine, and Oberhalbstein
end between 5750 and 5900 feet.

4. Many valleys end between 5300 and 5450 feet.

5. The lower Engadine ends abruptly at Zernetz at 4910 feet ;
and several others between 4750 and 4900 feet: these nearly corre-
spond to the lower line of erosion, placed at 4800 feet.

6. Between 3800 and 4400 feet there are so many heights noted,
that it is difficult to throw them into groups; but the most distinct
are at about 3900, 4100, and 4400 feet.

7. In Oberhalbstein there is a termination of the lower valley at
3600 feet.

8. Val Blegno ends above Olivone at about 2900 feet.

9. Linththal and Muottathal end between 2500 and 2600 feet.

Thus it appears that the earlier elevation of the Alps, represented
by the higher water-levels, was in great starts of 1000 feet or more
at once; that these gradually became less and less violent, until,
after rising above the well-marked line of 4800 feet, the later eleva-
tions were so gradual that the rough process by which it is here
attempted to measure them is hardly sufficient to distinguish one of
the lower levels from another.

The valleys above mentioned are excavated in rocks of every age
from the nagelfluh to the gneiss; therefore the operations here de-
scribed were all posterior to the eocene period. I am unable to say
whether they are prior or posterior to the formation of the molasse ;
but I think it probable that they were posterior, and that the only
deposit which was formed during the last elevation of the Alps was
the drift. .

Terraces of Alluvium in the Alpine Valleys.

The valleys of the Alps offer innumerable instances of terraces of
alluvial matter projecting from their sides and cut through, often to
a great depth, by the present streams. These occur in places where
it is impossible to account for their existence without going back to
causes operating under different circumstances from those which now
exist ; for the forces now at work are destroying and carrying them
away. Such terraces are common in all mountainous regions, and they
have everywhere nearly the same character, form, and constitution :
their materials consist of sand and gravel, of various degrees of coarse-
ness, mixed up with slightly worn fragments of rock, all or nearly
all belonging to the rocks to be found in the same valley, and
arranged with an irregular approach to stratification, which slopes
both down the valley and from the sides towards the middle of the
valley at angles varying from 2° to 15°, in planes usually parallel to
the surface of the terrace.

The nature of these deposits is so precisely similar to those formed
immediately below the surface of the water wherever a mountain-
stream enters a lake or a quiet arm of the sea, that this explanation

114 PROCEEDINGS OF THE GEOLOGICAL society. [Dee. 5,

of their origin is, I believe, universally admitted: but it has been so
clearly stated by Mr. Darwin, that I will quote his words ; in case of
“a river delivering during a long period detritus into a lake, the
level of which was gradually sinking from the wearing down of its
mouth, a gently sloping surface would be formed at its head. But
as the barrier was cut deeper and deeper, and the lake sank, the
stream in the part where it was once checked by meeting with the
still water would gain velocity, and hence would cut through the
beds which it had originally deposited; *”’ and again, at p. 55,—
“the waterworn materials appear to have been transported by the
present rivers, and yet they are so deposited as could not have hap-
pened without some intervening cause. The only obvious solution
is that the valley had been occupied by an expanse of gradually sub-
siding water, either of a lake or of an arm of the sea.”

Besides the matter brought down by the rivers, the terraces in the
Swiss valleys have m many instances received large additions of
materials from the falling of fragments of rock down the steep sides
of the mountains; and the outlines of these accumulations give a
strong confirmation to the above views ; under ordinary circumstances
the fragments which roll down the sides of a precipice form them-
selves, as is well known, into a slope at an angle of about 35°, which
has been named in siete ae aes Fig. 3.—Diagram to show the arrange-
“the angle of repose:”’ but in ment of the materials in the Terraces.
the lower parts of the Swiss val-
leys it is very common to observe
that the slope suddenly changes
from 35° in the upper part of the
talus to about 15° in the lower
part, as at a in the annexed dia-
gram (fig. 3); and this change
of angle takes place at a uniform
height for a considerable distance.
This is well seen on the south side of the valley of the Rhone near
Sierre, where the level at a is 1800 or 2000 feet above the sea,
and the lower slope spreads out into a series of flat hillocks more
than 200 feet above the Rhone. The change of angle of the slope
of the debris, and the uniformity of level at which the change takes
place, are strong proofs that water stood at this time up to the level
at a, and that this water had sufficient motion, either from currents
or tides, to alter the angle of subsidence of the falling debris +.

The diagram, fig. 4, gives the outline of two terraces in the Val-
telline, above Grosio ; the angles are drawn correctly, but the distance
between the two ends of the upper terrace at Sandalo and Maggione

* Darwin, “ On the Parallel Roads of Glen Roy :” Phil. Trans. 1839, p. 51.

f In Nov. 1830 Mr. James Yates communicated a paper to this Society “On
the Formation of Alluvial Deposits,” of which a short abstract is given in our
Proceedings, vol. i. p. 237: it will be found at length in the Edinburgh New Phil.
Journ. for 1831, vol. xi. p. 1. The manner in which terraces are formed in lakes
. from the materials brought down by the streams is well explained, pp. 30-39.
See also R. Chambers, ‘ Ancient Sea Margins,’ p. 51.

1855. | SHARPE—ELEVATION OF THE ALPS. 15)

Fig. 4.—Section of two Terraces of Alluvium in the Vi altelline, cut
through by the River Adda.

Sondalo.

Terrace.

Maggione.

Talus.
Gneiss.

Terrace.

y0°te is ee

Bed of the Adda.

ought to be greater; the River Adda has cut through the rubble
forming the terraces for about 300 feet, down to the rock below. We
learn from this that a body of water stood for a very long period at
the level of a, where Sandalo now stands, 2940 feet above the sea ;
and that it stood at a later time, and for a shorter period, about 200
feet lower, at the level of 0.

The terraces are so uniform in their principal features that it is
useless to give other representations of them.

I noted the heights of the principal terraces in many of the valleys,
with the view of comparing them together to determine whether .we
ought to refer them to lakes or to the sea. There is usually a village
on the broader terraces, of which the height above the sea is pub-
lished ; where this is not the case my aneroid gave me a tolerably
accurate measure of their elevation. But there is an inevitable source
of error caused by the slope of the terraces themselves, which often
amounts to 100 feet ; and thus, if we happen to compare the upper
end of a terrace in one valley with the lower end of one in another
valley, we may think the one 100 feet higher than the other, when
they are really at the same altitude: nor can this be obviated by
limiting our observations to the upper end of each terrace, as fre-
quently that has been washed away, and its traces only remain on
the sides of the vaileys. I thik, however, that 100 feet may be
taken as the limit of the errors in my statements of altitude.

In tolerably level valleys, instead of terraces we find long sloping
meadows, in which we cannot separate the deposits which may have
been formed under ancient waters from those now forming by the
action of the present rivers and of the weather. I have therefore
taken no account of these, and only mention them to show that our
not finding terraces in such valleys is no proof that waters may not
have stood in them to the same height as in those valleys in which
terraces are most frequent.

_ Terraces are also less evident in bread than in narrow valleys ;
perhaps because a given amount of materials would make less show

116 PROCEEDINGS OF THE GEOLOGICAL sociETy. [Dec. 5,

when spread out in a wide valley, than when confined in a narrow
one.

In many valleys my attention was so much fixed on other objects
that I omitted to note the occurrence of terraces, or only noted the
more striking and important ones: in every instance I omitted
many of minor importance, or of which the real character may be
doubtful ; thus the following list is very incomplete, and no negative
argument can be drawn from its omissions.

Valleys of the Rhone and its Tributaries.—Valley of the Rhone :
there are great irregular terraces above Sierre, at above 1800 feet
elevation, which appear to have been altered and cut up by subse-
quent causes. :

In the valley of Evolena there is an extensive terrace at La Loet,
3316 feet, which may be traced down the valley for nearly two
miles.

Below Vex, at 2821 feet elevation, is an extensive terrace, on
a portion of which stands a ruined castle.

In the valley of Visp I noted a terrace above S. Nicholas at
3815 feet, another below Stalden, at 2490 feet, which is seen again
below Neubruck at 2470 feet.

In Entremont, descending from the Great St. Bernard, I observed
a sloping terrace a little above Liddes at 4782 feet, and a succession
of considerable terraces between Liddes and Orsiéres, at about 4350,
4150, 4000, and 3770 feet.

Valleys of the Rhine and its Tributaries.—On the Vorder Rhine
the highest terrace is seen at St. Jacob and Tavesch at 3825 feet ; it
is very extensive, but irregular. Dissentis stands on a large terrace
at 3805 feet, which must be a continuation of the same. In
Medelserthal the highest terrace is at 8. Rocco at about 4720 feet ;
there is also one at Platta at 4658 feet, which is probably part of
the same. There is a very distinct terrace at Medels, 4422 feet.

Valley of Vals: on the descent from Vals to Ilanz, I observed
several terraces ; one at Fuors at about 3300 feet, another between
Fuors and Peiden at about 3175 feet, and a third below Peiden at
about 2930 feet; and some smaller terraces above Ilanz, which
stands at 2323 feet elevation.

The Hinter Rhine: on the descent from the Splugen towards
Coire the terraces are numerous and well defined; the following
were noted.—The highest terrace is at the village of Splugen at
4780 feet; others at Sufers at 4343 feet, Ander and Dormat at
3113 feet, Zillis at 2930 feet, between Zillis and Tussis at 2770
feet, at Tussis at 2350 feet, at Rhazuns at 2200 feet, and at Bona-
duz at 2145 feet. ae a

In Oberhalbstein there are some traces of a terrace below Muotta
at 6110 feet: a terrace at Tinzen, 4230 feet, and a very large
terrace above Am Stein, at about 3300 feet elevation. I was much
interested to find an ancient moraine resting on this last-mentioned
terrace ; both the moraine and the terrace have been cut through
by the stream, affording a section in which the position of the
moraine on the terrace of alluvium was clearly seen. Higher up

a a, a a

1855. | SHARPE—ELEVATION OF THE ALPS. D7

the same valley there is a large moraine above Marmels, which also
appears to rest on a bank of alluvial detritus; but there-is no
section seen, and the superposition is not certain*.

Terraces are numerous in the valley of Pratigau; but I have only
the elevations of one at Mezza Selva, 3444 feet, and another at
Saas, 3254 feet.

In Davos there is a long terrace at Wiesen at 4770 feet: there
are others higher up the valley of which I have not the elevations.

On the lower part of the Rhine, between Ilanz, 2323 feet, and
Coire, 1968 feet, there is a succession of terraces at short intervals.

Valleys of the Inn and its Tributaries.—The upper Engadine is
a remarkable vallev, its bottom forming a uniform alluvial plam
which only falls 750 feet in 30 miles, from the Lake of Sils to its
sudden termination above Zernetz ; the upper end of this deposit is
5900 feet above the sea. Terraces are numerous in the Lower
Engadine: at Boscia, 5464 feet, and Fettan, 5404 feet, there is a
terrace on the side of the hills more than 1000 feet above the river ;
at Tarasp, 4597 feet, is a terrace which occurs also on the opposite
side of the river at Upper Schuls ; another at Lower Schuls, 3970
feet, extends down the valley nearly to Sus ; below Sus is a terrace
on the sides of the hill at 4060 feet elevation. Others occur lower
down the valley at 3567 feet, at Strada, 3465 feet and at 3415 feet,
these last two being distinct.

On the north side of the Bernina Pass there is a long terrace at 6190
feet elevation, between Pontresina and Bernina, which is the highest
terrace which I observed in Switzerland; another occurs at Pontre-
sina, 5930 feet.

On the descent from the Stilvio into the Tyrol, the highest terrace
is about 950 feet below Trefiu at about 4230 feet elevation; and
there is another about 500 feet lower.

Valleys on the South of the Alps.—The Valtelline: Ceppina
stands at 3865 feet on a terrace of some extent; at Morignone is a
well-marked terrace at 3770 feet ; another at Mondalizza, 3120 feet ;
at Sandalo is a very extensive terrace at 2940 feet, 300 feet above
the Adda, of which a sketch is given at p. 115; and about 100 feet
below is another of less extent: an important one is seen at Tiolo,
2690 feet, and another equally important above Grosio at 2330 feet,
and at Sernio at 1700 feet. Below this I did not follow the valley,
having entered it at Tiranno from the Bernina.

On the south side of the Bernina the highest terrace is at about
5650 feet, some way below La Rosa; and there are several others, of
which I have not the elevations, between this and Posciavo, which
stands at 3323 feet. sil

In Vai Bregaglia there is a small terrace at Carrel at about 5200 feet,
and another equally small a little above Casaccia at about 5000 feet.

* M. Studer informed me that a moraine near Berne rests on a high terrace of
worn debris; and M. Rozet states that, throughout the French Alps, the ancient
moraines rest on the diluvial deposits (Bull. Soc. Géol. France, 2 série, vol. xii.
p. 246); therefore there can be no doubt that these terraces were formed before
the period of the great extension of the glaciers.

118 PROCEEDINGS OF THE GEOLOGICAL sociETy. [| Dec. 5,

On the south side of the Splugen I could find no terrace whatever ;
but all round the Lake of Como there are the remains of a terrace
of coarse gravel, some 200 or 300 feet above the lake ; and therefore
between 900 and 1000 feet above the sea.

In descending from the S. Gotthard to Bellinzona, the highest
terrace observed was at Giornico, 1234 feet; but m Val Blegno
there is a terrace a little above Olivone at 3100 feet, and another at
Agoa Rossa at about 2100 feet; and in the branch valley of
Misocco there are several terraces above Misocco, between 2500 and
3500 feet in elevation. Near Bellinzona there are several large
alluvial flats at 30 feet, 100 feet, 160 feet, 190 feet, and 230 feet
above the Lago Maggiore, which may perhaps be due to a gradual
lowering of the waters of the lake, and not belong to the class
of terraces under consideration ; but between Locarno and Bellin-
zona there is a well-marked terrace at 981 feet elevation,— that
is, 300 feet above the lake.

In Val Onsernone, which ends at the Lago Maggiore, there is
a large terrace at Intragna at 1300 feet, another some 300 or 400
feet higher, and another about 300 feet below Intragna; of the
last two I have not the exact altitudes, but the last probably corre-
sponds to the terrace observed between Locarno and Bellinzona
at 981 feet.

In Val Isone, which drains into the Lake of Lugano, the highest
terrace observed was at an elevation of above 2000 feet ; but, having
no known height near it as a point of comparison, I could not fix its
altitude accurately.

Round the Lake of Lugano there is a well-marked terrace a few
hundred feet above the lake, of which I did not measure the eleva- —
tion; here we may doubt whether to attribute this to a lowering
of the water of the lake or to a more general cause.

For more convenient comparison I have thrown these observations
together in a tabular form, see Table, No. II. p. 123.

General Results from the foregoing Observations on Terraces.—
The first point to which I wish to call attention is that there are ter-
races at the same elevation in valleys which have no connexion with
one another ; thus, in valleys opening both on the Rhime and the
Rhone there are terraces between 4770 and 4780 feet, between 4340
and 4350 feet, and between 3815 and 3825 feet. Both in the
Valtelline and in the valley of Entremont, which falls into the Rhone,
there are terraces at 3770 feet. In the Valtelline and the valleys
connected with the Rhine there are terraces at between 3110 and
3120 feet, between 2930 and 2940 feet, and between 2330 and 2350
feet.

I think these are conclusive proofs that the terraces were formed
by the sea which surrounded the Alps at these periods and entered
into all the valleys: for it is incredible that there should have
been so close an agreement of level in a number of independent
lakes, such as would be formed by closing the valleys of the Rhine,
the Rhone, and the Adda by glaciers or any other barriers.

The numerous correspondences of level in terraces which occur mm

1855. | SHARPE—ELEVATION OF THE ALPS. 119

valleys connected by a common outlet, as well as those just men-
tioned, afford a satisfactory confirmation of the general accuracy of
my altitudes. These coincidences of levels in such distant localities
also confirm the remark already made, that the elevation of the
Alps must have been uniform from Savoy to the Tyrol, no such dif-
ference appearing in the levels as would occur if one part of the chain
had been more elevated than the rest.

In Table No. III. p. 123, will be found a general comparison —

of the elevation of the various water-levels, deduced from the pre-
vious observations on the Lines of Erosion, the Heads of Valleys,
and the Terraces, which harmonize in numerous points. There are
no terraces so high as the two upper lines of erosion, but the lower
line, noted at about 4800 feet, nearly corresponds with the heights
of the heads of several valleys and of four terraces observed in dif-
ferent parts of the Alps. And the close comcidences in the elevation
of the heads of many valleys with that of terraces elsewhere are very
numerous.

The conclusion which I draw from all these observations is the
same ;—that they show the levels at which the surface of the sea
beat for long periods against the Alps as they rose out of the ocean ;
the effects produced at each level giving a sort of relative measure of
the length of time that the land remained stationary at that eleva-
tion, and the distances between them marking the steps in the pro-
gress of the elevation of the mountains. These steps appear to have
been greatest at the commencement of the elevation, and to have
gradually lessened as the mountains approached the height at which
we now find them. The periods of longest rest were undoubtedly
those marked by the lines of erosion at 9000, 7500, and 4800 feet
elevation.

There are, however, some peculiarities in the unequal distribu-
tion of terraces in different parts of the Alpine Chain which may be
thought to favour the hypothesis that they were formed in lakes; I
will state these fully, that both sides of the argument may be fairly
seen. The terraces are far more numerous in the upper valleys of
the Rhone above Sion, of the Rhine above Coire, of the Inn, and of
the Valtelline, and in all the lateral valleys which fall ito these,
than they are either in the valleys on the north of the Alps, which
open on to the great central valley of Switzerland, or in those which
run southward to the plains of Lombardy. Thus, while there are
numerous well-marked terraces on the north side of the Splugen,
I observed none on the south side more than 1000 feet above the
sea, at about which height there is a terrace around the Lake of
Como some 300 feet above the lake; and on the descent from the
S. Gotthard towards Bellinzona I noted no terrace above Giornico,
where there is a large one 1234. feet above the sea, though in the
branch valley of Misocco they occur above Misocco at more than
2500 feet elevation.

Some stanch glacialist will probably offer to explain this differ-
ence by the greater facility of forming lakes in the inner valleys by

120 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 9,

glaciers choking their mouths. But, as I know of no evidence that
such glaciers ever existed, I must look elsewhere for an explanation ;
and that which occurs to me is, that such deposits would be best
preserved in valleys occupied by still water. In a rough sea of
which the level was gradually falling, the waves would under-
mine and wash away such loose deposits, and spread them over the
base of the valley, in a less regular form. If this view be correct, it
will agree with the fact that the sheltered inner valleys of the Alps
have terraces up to very high elevations; while the outer valleys,
into which the seas on the north and south of the chain must have
beaten with violence, have terraces only in their lower and more
sheltered portions; and that some valleys on the south of the Alps,
of which the east and west direction would be a cause of shelter, are
also studded with terraces, as the Valtelline, Val Insernone, Val
Isone, Val Misocco, &c.

Whether this explanation be accepted or not, I still think the
uniformity of level observed in valleys on the opposite sides of the
mountains must outweigh all other considerations, in favour of the
conclusion that such terraces were formed in the same sea.

Another difficulty will doubtless be found in our not having dis-
covered any organic remains in the terraces of alluvium. But this
meets us equally if we suppose the terraces to have been formed in
lakes. The almost entire absence of organic remains in the drift-
deposits of Europe is a most remarkable fact, which has not yet re-
ceived a plausible explanation ; it is so general, that we must look fora
wide-spread cause, and, until that is discovered, the fact itself must
not be allowed to weigh against conclusions which can be safely
derived from evidence of another nature*.

* After this memoir was read to the Society I received the following note from
Mr. James Smith, of Jordan Hill, which leads me to hope that marine shells may
be found in the alluvial deposits of Switzerland :-—

Atheneum, Dec. 14, 1855.

My Dear Sir,—A summer’s examination of the superficial beds of gravel in
Switzerland led me to the conclusion that some of them must have been deposited
under the sea, for the following reasons :—

1. They are stratified and exhibit no appearance of disturbances, hence the
configuration of the country must have been the same as at present.

2. They are at an elevation which does not admit the supposition that they are
lacustrine.

I did not discover marine remains in situ, but the following indications of the
existence of pleistocene shells may perhaps lead to their discovery and set an
important question at rest.

In the Museum at Geneva I found in a drawer marked “ Swiss fossils” Mya
Udevallensis, a most characteristic and abundant species in the Clyde beds.

In the Museum at Berne I observed several shells with the locality “ Court”
attached to them: they had all the appearance of pleistocene shells ; I inquired for
the curator of the Museum, but as it was during the vacation of the University he
was absent. It is ten years since, and af this distance of time I do not recollect
whether I could identify any of the species.

Yours truly,
JAMES SMITH.
Daniel Sharpe, Esq.

1855. | SHARPE—ELEVATION OF THE ALPS. 121

Theoretical Conclusions.—It would be very interesting to fix the
period at which the elevation of the Alps out of the waters took
place, of which the traces of water-levels here described are
the records. To accomplish this we must find the latest formation
in which we can observe levels corresponding to those which I
have established. As the objects of my visits to the Alps confined
me principally to the higher mountains, I could not extend my
observations in the Tertiary Lowlands of Switzerland; and thus
I can only say with certainty that the elevation included the Eocene
Rocks and the elder Nagelfluh which rest on them. But I have
little doubt that the elevation took place at a much later period,
after the deposit of all the Tertiary Formations. I arrived at that
conclusion by looking at the subject from a different point of view.
Every elevation of mountains on a large scale must have left its record
im an accumulation of debris round their base. If we look back-
wards in the history of the Swiss Alps, we find the earliest accu-
mulation of this kind to be the Verrucano, a coarse conglomerate
marking the first elevation of the Swiss Alps through the then crust
of the earth. Towards the close of the Jurassic period we again
find conglomerates, some calcareous, others sandstones (which have
sometimes been confounded with the earlier Verrucano), marking
another period of great elevation. At the end of the Eocene period,
the older Nagelfluh, the enormous thickness of which is seen at the
Rigi and neighbouring mountains, pomts out the period of that
great elevation when, the central masses of the Alps being thrust
upwards for the last time through the crust of the earth, the moun-
tains received their present form, and the Secondary Rocks on their
flanks were thrown into the distorted position which they now
occupy. The alternations of the beds of gravel with the marine
and fresh water deposits of the Molasse point to a long epoch of
alternate elevation, depression, and elevation, which are probably
contemporaneous with violent movements below the great central
valley of Switzerland, on a line parallel to the axis of the Alps,
to which the Molasse and the old Nagelfluh owe their disturbed
position and their dip towards the Alps for so great a distance.

After that period the whole country must have again sunk below
the sea, and the elevation to which this present communication
refers followed at a still later period, raismg the whole region up
uniformly en masse out of the ocean without disturbing the relative
positions of its parts ; and to this movement we may naturally attri-
bute the deposits of gravel and boulders spread irregularly over the
Lowlands of Switzerland; and thus place this movement after the
conclusion of the Tertiary period.

I have already pointed out (p. 116) that the moraines which
mark the greater extension of glaciers at a former period sometimes
rest on terraces of alluvium in the valleys and on the so-called dilu-
vium of the plains, showing us that the extension of the glaciers
followed the accumulation of those deposits which I suppose to
have been formed during the elevation of the Alps out of the ocean.
An increase of altitude of the Alps of between 1500 and 2000 feet

122 PROCEEDINGS OF THE GEOLOGICAL socrETy. {| Dec. 5,

would give an extension of the glaciers sufficient to account for all
the moraines and polished and striated rocks in Switzerland. After
tracing the upward progress of the Alps during their rise of 9000
feet from their position at the first observed water-level to their
present heights, it requires but a slight stretch of the imagination to
suppose a farther elevation of 1500 or 2000 feet to account for the
earlier glaciers, followed by a subsequent sinking of the land to its
present level. But so many other causes may have produced a
change of climate, and the proofs of a glacial period in other coun-
tries are so numerous, that it seems better to look for a general
cause of a colder climate throughout Europe at the period in question,
than to limit our views to a local movement peculiar to the Alps.

Erratic Blocks.—The subjects of this paper approach too nearly
to the much-debated question of Erratic Blocks for me to leave them
entirely unmentioned. A large proportion of the rounded boulders
and gravel may have been distributed over the Lowlands of Switzer-
land. during the elevation of the Alps; for, as this elevation went
forward, every portion of the country must in its turn have been part
of the coast, and consequently acted on by the waves. This may
account for the distribution of the smaller rounded blocks at all the
lower levels.

But, if that explanation be admitted for the rounded erratics, we
have still to account for the great accumulations of large blocks, often
angular, which lie scattered here and there throughout Switzerland
above the deposits of gravel, and the presence of which on the Jura
and on the sides of the hills that enclose the valley of the Rhone has
led to so much discussion. On the Jura these blocks reach, accord-
ing to M. Charpentier, to the height of 4250 feet above the sea*.
The blocks of Monthey, so eloquently described by Prof. J. Forbes,
are stated to be at least 500 feet above the plain +, or above 1700
feet above the sea.

It will be seen by Table III. that the sea has stood for some time

round the Alps near each of these levels; thus we have the existence

of a sea demonstrated, on which ice-rafts carrying such blocks may
have floated: and it only requires a climate capable of producing
floating ice, to furnish an agent for transporting blocks of any size, of
stranding them in lines along the coast, or dropping them here and
there at the bottom of the seat. The extension of the glaciers,
caused probably by a climate colder than the present, followed soon
after the period when the sea stood at the heights mentioned, and
thus the conjectural explanations of the two succeeding phzenomena,
referring both to a colder climate, harmonize together, and save us
from the necessity of the gratuitous creations of a “Glacier of the
Rhone” ending on the side of the Jura nearly 3000 feet above the

* If, as it is probable, these are French feet, they are equal to 4528 English
feet; if Swiss feet are intended, they are equal to 4182 English feet. Not having
Charpentier’s work at hand, [ quote from the abstract of it in Edinb. New Phil.
Journ. vol. xxxiii.

t ‘Travels in the Alps,’ p. 51.

t See Sir C. Lyell’s account of the transport of blocks by the breaking up of
coast-ice now going on in the Bay of Fundy.

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Cele tinal Mi.) REM een ee po ane NC Rss Eee ent Biona 5315 ....+.

i) iEMaltelline ...:.:1sedeoes tegen.
iit :

{
!

BPPe WWEISSEATINED | o..ccossesncennces

Quart. Journ. Grou. Soc, vol. xii. Zo face p. 128.

POP ee eees isaac POOe renee eesere

Peatualbll asian iste Ree tla cio Les Plans 3822
Laubach ......|....sc00.....-.++-|Lauenen 4100

BUCTENS Oe, decal acacea tues tcace ss .| Haudéres 4763
BMETMEIET det alispcicensaictsce sci <ic|nestesswcisaecserecvecteowes Ayer 4776

PEED roan ccm tical oct aranwadea asi o|inee mbiclrsbinwmincclisiabelnomaieys Tasch 4877 vevesssenes Zermatt 5410 }...| 6110

70

BENE SDLON) cera a emcees eale Malis oace «wie a odeNeanlasaeeeioul caaslduemmuserie auwesaivaet Trinité 3455 0
EMAVISED, cdoisce lane scancdectdee sk. Macugnaga 4305 *
PEQUNGAAZA icin] Sosennessecwevce es Formazza 4143

REULOM 5 avew cll siicase die es «wewtie| dese caewe tere nnaestirtr aici. Simpeln 4626 *

7 | {5464
5900

REINS ee rite aP ee echt eis aid) Mautamnte eatee ciel eauahecubes Andermatt 4642 * | 5930
PRE VANGINA. ..c]-ecosceeccneses.0s i "1 ) 6190
|} Blegno.........

BPLPMLISOCED | Lo. c0s).cascceere.soeeenals aces seen cieeesenvscaa bainaldes vet aen swe hametanecectent S. Bernardino bg

—Tehbeaet TIN Ge REE) Ren ERE sates ott, OTe RR amr CDs Hinter Rhein 53}...| 5650?

- Oberhalbstein |Am Stein 3597|Schweiningen 4058. |........s.seseceecseseesee|eoeeseeseeneeseenees 02) 5200?

EME PAGUG Fiae mist wie weteerh gases so] uosici'ecis sas dasnamaleiateiser-
WUMNBLET lc iiecatase seem scccescee

Head of
Urnerboden

\ 4730

The altitudes marked * are below the head of their respective valley

1855.]. SHARPE—ELEVATION OF THE ALPS. . 123

Lake of Neufchatel, for which there is no other evidence than that
of the existence at this height of erratic blocks +.

Tape I1I.—General Comparison of the preceding observations.

Lines of
mrasions: Heads of Valleys. Terraces.
English feet.
9000
7500...... 7660
GOD Ds Seer ad ste A daeeii damon aadewsanactee es 6100, 6190
DIOGO, IBID, DO9D s.c2s.neecdaase cee 5900, 5930
5650 ?
GATOR GAG Veco oos salavceae suetoawnae 9464
5280%, 5257*, 5315*, 5315,) | -.
Sau NISTO woe ae eae
Wee AON Se he eae 5000?
4626*, 4642, 4642*, 4730, ‘
ee AGIGOS ATT 222-52 ce osu UE LONGUE Chir
4597
AAOO. ssri4.2 Mes ets oh Jaw saramediadepes 4422
ABODE, Ah Ge aie soci. scan anctel on am 4343,.4343, 4350
BAAD G AL Pease tee yas soso 4230, 4283
4100, 4100, 4117, 4148, 4152 ... | 4150
BODO S aoe inate act voacdonedsnheses cube 4060
3936, 3953, 3954, 3985 ......... .-. | 8970, 4000?
3730, 3770, 3770, 3815,
DOLL; GOIS, BOOM va ancsinn casks secon 3825, 3865
DOO Fen css cave ne samdectctecrieueleunes 3567
3415, 3444, 3465
5254, 3300, 3300, 3316
3100, 3113, 3113, 3120, 3175
SO, hee ee es Nae 2930, 2930, 2930, 2940
2770, 2770, 2821, 2840
DOU ett ns nis Se ecsaete eosaetaeces 2690 |
DOOR Sarees de cnk aandertvasseeenaatea ters 2490
2330, 2350, 2350
2200, 2200
2100? 2145, 2145
1650? 1700
1234, 1300
981, 1000 ?

The numbers marked ? rest on doubtful measurements.
The numbers marked x are below the truth.
The altitudes placed on the same line are supposed to belong to one water-level.

+ In corroboration of my statement of the limited extension of the real proofs
of the existence of ancient glaciers, I cannot quote a better witness than M.
Agassiz, who, after saying ‘‘On ne rencontre des traces de moraines terminales
que dans les vallées comprises dans l’intérieur des chaines des Alpes,” proceeds to
account for their disappearance beyond. (‘ Etudes sur les Glaciers,’ p. 63.) The
moraine of the Glacier of the Aar, near Berne, lately discovered (see ante, p. 117),
is, I believe, the only exception to the accuracy of this statement of M. Agassiz.
The only evidence in favour of a farther extension of glaciers is built upon the
distribution of gravel and erratic blocks, to which category, I believe, that we must
refer most of the Blockwdlle of M. Escher’s Map of the “ Verbreitungsweise der
Alpen-Fiindlinge.”

duart. Journ. Grou. Soc, vol. xii. Zo face p. 123.

Tasix I.—Altitudes of the Heads of Swiss Valleys in English Feet: see p. 112.

VALLEY.

BUTIEN tysressetss|isevereuscssiesons Trient 4316 *
PAT VG. scassaecuns a eM OUtAa (Avnas. wir |seseareeuterien meses crete Nant Bourrant 5280*|
AV AINREMMCLye | tsetevercracstsem |ieceteccssaseessssses~srcce|testansavececesenens taccurs|lCemeoumeisenieaseraieen, head 7660

MEETS ereecna yf nocenacoecocrnane Gsteig 3936
Kander... .|Kandersteg 3828
Ormont .|Les Plans 3822

ILENE, Cepce | prcoonotonssoocand Lauenen 4100

du Rhone

Foot of
IRHONMGMeses ised | Nereeeste ics seeks| scaenccsssenevereracnsoscal| cesses iecvssencs vsesvacs sacl scveeueesesonseeeee { Glacier +9756

HLEYEUS toe vssens|sesccocossssucveoe Heremenence 4152...)

AVIS Decent | al Zermatt 5410
Saas 5257 *

‘Valpelline.. Cony | Pecaaeeeutegnet int |catarvenrstcesssness*ash:|screacecrceconrersesdatecse Biona 5815 ..........+. Prérayean 6593

Gressoney ..
Anzasga .....
Formazza .
Simplon

‘ Macugnaga 4305 *
.|Formazza 4143

Simpeln 4626 *

FREUSS: sse.ssass 1h. Andermatt 4642 *
Levantina ree

Oberhalbstein |Am Stein 8597|Schweiningen 4058 |.
WEG TEC G60) boseagenccoscocond Klosters 3953 ....2....|..-...-.-
TETGACIMC Nr erens|\ssevsececgrostees|secsecsctsossccess oped
AYLI Ganon hoaonenaoeenasacod

Head of
Urnerboden } efe0

The altitudes marked * are below the head of their respective valleys.

Tasxe Il.—Adltitudes of Terraces in the Swiss Valleys in English Feet: see p- 116.

Below |1000 to} 1500to | 2000 to | 2500 to |3000 to} 3500 to |4000 tol4500 to above
VALLEY. 1000ft.|1500ft.| 2000ft. | 2500ft. | 3000ft. |3500ft.) 4000ft. |4500ft.\5000ft.l50008t,
FRRONEs sc ccccccsccess|acseceveclerssreser above
TORE ecco Oe HIDE tl adocseoeceleaceee 2821 | 3316
Visp 2490) ||... 3815
3770
Brtremont 2s cesctt tecerrstlsis-. me eee sare oa epee reread gee alneee }arse
Vorder Rhein......]....++++.[eee.sse0s SNES | hepacocogced lacceaconcecte| hosaceood 3825
Medelserthall .....-|:.-0s+-+s|sceessson|eceveesnne ee ee iy eanlesecaecheers 4422 | 4720
above 5 Hi)
TABGRTRA sccorond icoccoed bare i ll teers alld enoe } 2930 { ae
2145
FER Lien THECIE corced bronssece besseeccil heeoneerwed {2200} SHOU BHU Ih ccecsccen 4343 | 4780
2350
Oberhalbstein ...]......cc.Jeeecesees[eneees Bcboed Beppcdandosd spodanoouncs 3300 }....... ceca! C2ED looscoaoan 6110
Pratigau.
Davos ......seee000e-
2770 6
North of Splugen.|......000}....-:::[eeseeeeeeeee {zo 3930 3113 |............ 4343 | 4780
Valley Of Trafoi...|.....+...]..0.cc.02|ssceeeeessts|oecvescnsees|seccoes Do006| pnosacase 3730 | 4233
; A 3567 5464
Engadine 3970 4060 | 4597 5904
p 5930)
INO OF IBEW bs heoa5enenl onsoacod| becodac6oacd| faq0o0qn00"|acooaGaonDod| PoONNCONE| Fisagj|ONooKed boemennPe| LooOAAcd 6190
( 2690 3700
Wal tellinemmeeesets| tseeesses|secrerees 1700 2330 2840 | 3120 | 4°
3865
2940
SOOO, @ 2 BERT Ad hosoccond| hoonoG50clbooa0000ced hocondcoacedl Hoociaoescond obeooted| hosertions cool paenad6ed boasooncd 5650?
WWE SE Fe socoad becacc6a hosaobece| ooaceononed| baceoaNceece| baceooonced|6GoDeGnCd saoHoSoAncNA| hacdonee 5000?) 5200?
Val Levantina. ..| 12384
WAL ococcncel fpeonnccoe| fpoondo ze" foconaconcece! PNDE | eooosanconee 3100
Lago Maggiore ...| 981
Val Onsernone ...|1000?} 1800} 1650?

124 PROCEEDINGS OF THE GEOLOGICAL sociery. [Dec. 19,

DECEMBER 19, 1855.
The following Communications were read :—

1. Description of a Fossiu Cranium of the Musx-BurraLo
[Bubalus moschatus, Owen; Bos moschatus (Zimm. § Gmel.),
Pailus ; Bos Pallas, De Kay ; Ovibos Pallasii, H. Smith § BI.]
Srom the “LOWER-LEVEL Drirt” at MAIDENHEAD, BERKSHIRE.
By Professor Owen, F.R.S., F.G.S. &e.

THE subject of this description was discovered by the Rev. Mr.
Kingsley and John Lubbock, Esq., in a gravel-pit close to the engine-
house at the Maidenhead Railway Station: the deposit appears to be
that called ‘the lower-level drift.” The specimen was submitted to
my inspection by Mr. Lubbock in July 1855, and proved to be the
first example of the Buffalo-tribe (Budalus) which had come under
my observation from a British locality, and I most heartily wel-
comed so interesting an accession to the catalogue of British fossil
mammals. |

The specimen consisted of the cranial part of the skull, from which
one condyle of the occiput, and the tip of the left horn-core were
broken away ; but the characteristic very broad, depressed, approxi-
mated, rugged bases of the horns, covering the whole upper surface
of the cranium save a narrow median channel, and a portion of the
much extended telescopoid orbit at once showed the subgenus to
which the fossil belonged.

The bovine ruminants present, as is well known, three main
modifications of their horns and horn-cores; in one the horn is
subcylindrical at the base, which springs from the posterior angle
of the frontal; in another the base of the horn, of similar shape,
springs from the frontal in advance of the post-posterior angle; in a
third the base of the horn is more or less depressed and expanded in
breadth, so as to spring (in the adult males) from the whole or a
large proportion of the lateral part of the frontal, and im some to en-
croach uponits upper surface. To the bovine animals with the first
modification the generic name Bos has been restricted ; to those
with the second modification that of Bison is given, and the term
Bubalus is applied to the third*. The common appellations of
“QOxen,” “Bisons,” and “Buffaloes” answer to the Latin generic terms
above cited, and the Musk-buffalo seems to have been subgenerically
separated without due grounds from the other Budali, and especially
from the Cape Buffalo (Budalus caffer), under the misguiding term
Ovibos ; its peculiar affinities amongst the Ox-tribe to the Sheep
being by no means obvious: for the woolly covermg beneath the
coarser hair of the Musk-buffalo is a purely adaptive modification

* T do not here pledge myself to the soundness or strict uniformity with nature of
the threefold division of the Bovide, above cited. Intermediate modifications have
been pointed out in Indian species of Wild oxen, under the terms Bibos and Gaveus,
by the acute observer Mr. B. H. Hodgson (Illustrations of the Genera of the
Bovine, 8vo. 1841); but the three main modifications of the horns, at least as
regards their bases and origins, are those that it seems to me are chiefly of moment
in reference to the fossil skull in question.

1855. | OWEN—FOSSIL MUSK-BUFFALO. 125

for an arctic climate, like that which the extinct northern Elephant
and Rhinoceros presented.

Not long after Jeremie* and Dobbs had made known the exist-
ence of the Musk-buffalo in North America, Pallast described a
fossil skull, which he referred to the same species. This skull was
found in the arctic circle on the banks of the Ob: a second cranium,
referred to the same species, was discovered in a marsh or moor still
further north. <A third fossil skull from the mouth of the Yana,
between the Lena and Indigirska, was LEER described and
figured by M. OzeretskowskyT.

The short account by Cuvier§ of the fossil remains of the Musk-
buffalo is based upon the memoirs of the Petersburg Academicians ;
the figures given by Pallas being reproduced in the ‘ Ossemens Fos-
siles’ on a reduced scale in pl. xu. figs. 9 & 10, and those of Oze-
retskowsky in pl. xi. figs. 6 & 7 (with the horny sheaths of the horn-
cores). Cuvier leaves the question of the specific relations of these
Siberian fossils undetermined, and concludes his notice by remarking
that, as they were obtained from no great depth, nothing hinders but
that they might have come, as Pallas believed, from America across
the polar ice; since the Musk-ox has been, in that way, seen in
Greenland ||.

Sir John Richardson, in his excellent account of the fadeil bones
from Eschscholtz Bay, justly remarks that “a greater accumulation
of fossil materials is needed to determine the question”? which Pallas
and Cuvier had left undecided : and Sir John gives a description and
figure of the skeleton of a young Musk-bull, and figures of the skulls
and some other bones of the male, female and young of the same
recent species, in order to facilitate future comparisons. An extinct
species is, however, founded by the same author on a fossil vertebra
dentata under the name of Ovibos maximus.

The materials for contributing towards the solution of the question
as to the specific relations of the fossil and recent Musk-buffalo, at
present at my command, are the fossil cranium discovered at Maiden-
head,—a corresponding part of the skull of the fossil Ovibos from
Siberia, which formed part of the Museum of the late Joshua Brookes,
without the record of any more special locality,—the plaster cast of
a similar fossil, also from Siberia, brought by Sir Roderick Murchison
from Russia,—and the recent skull of an old Musk-buffalo brought
from the Arctic regions, in which the occipital region and the right
horn-core are partially mutilated, and the entire horn is preserved on
the left side.

In the form of the occipital region, in the form, proportions, and
direction of the horn-cores, especially in the extent of the rough,
flattened, horizontal tract at the upper surface of their base, the

* In Charlevoix’s ‘ Nouvelle France,’ vol. iii. p. 131, “ Beeuf musqueé. a

+ Novi Comment. Acad. Scient. Imp. Petropolit. tom. xvii. tab. xvii. figs. 1-3,
1772.

+ Mémoires de l’Acad. de Pétersb. t. iii. p. 215. pl. 6, 1809.

§ Ossemens Fossiles, 4to. tom. iv. p. 155.

|| Fossil Mammals, Zoology of H.M.S. Herald, 4to. 1852.
VOL. XII.— PART I. K

Fe ie

126 PROCEEDINGS OF THE GEOLOGICAL sociETY. [Dec. 19,

three fossils closely agree with each other, as they do likewise with
the figure of the Siberian fossil cranium given by Pallas, and repro-
duced by Cuvier in pl. xii. figs. 10 & 11 of the ‘Ossemens Fossiles*.’

The first difference between the fossils and the recent skull is the
somewhat greater extent, in the latter, of the vertical plate of bone
between the superoccipital ridge and the back part of the bases of
the horn-cores. In the English fossil the still persistent lambdoidal
or superoccipital suture crosses transversely the corresponding tract.
In the Siberian fossil and the recent cranium that suture is oblite-
rated; they are. both from older individuals ; but the tract in the
recent skull is smoother and more convex, as well as more extensive.
The value, however, of this character is diminished by the fact that,
in the cranium of the recent Musk-buffalo, a bull of between four
and five years old, figured from behind, of the natural size, in the
** Fossil Mammals of the Herald,”’ pl. ii., the tract between the super-
occipital ridge and the horn-cores is not greater than in the English
fossil, and it is equally traversed by the lambdoidal suture, showing
that that suture is retained until the animal has acquired its full
size, and up to the fifth year. Sir John Richardson gives no other
view of that recent skull, of the natural size, with the horn-cores ex-
posed. Comparing, therefore, the fossil crania with the cranium of
the old Musk-bull from Melville Island, the bases of the horn-cores,
though similar in size and rugosity, slope down at their upper sur-
face, as they extend from the median fossa outwards, more directly
and gradually, and the interval between their inferior surface and the
side of the cranium is narrower and more angular in the recent skull,
but is wider and more arched in the fossil: in this respect, however,
there appears to be a difference between the skull of the old Musk-
bull and that of the younger Musk-bull figured by Sir J. Richardson,
in which the curve of the basal part of the horn-cores rather more
resembles that in the fossil skulls.

The cranium from Maidenhead is the only one of these that has
an entire horn-core; the right one, at least, wants only a small part
of the tip.

Comparing the recent (fig. 6) and fossil (fig. 3) crania in a side
view, the horn-core in the recent is less vertically deflected, and is
bent in a slight degree more outwards and forwards at the tip. This
character, however, is not.so strongly marked in the figure of the
young Musk-bull above cited, as in the old Musk-bull before me.

The deep and narrow longitudinal groove, extending along the
middle of the upper surface of the cranium, and dividing the broad
bases of the horn-cores, is similar in, and equally characteristic of,
the fossil (fig. 2) and recent (fig. 5) crania compared. The lower
surface of the base of the horn-core is continued more directly from
the side-wall of the cranium, outwards and downwards, in the recent
cranium : in the fossil crania that part of the base of the horn-core
rises before it curves outwards, and thus the space between the zygo-
matic arch and the horn-core is greater in the fossil (fig. 1) than in the
recent (fig. 4) skull. The outer surface of the horn-core is divided from

* Tom. iv. 4to. 1823.

1855. | OWEN—FOSSIL MUSK-BUFFALO. 127

the anterior surface by a ridge, that surface forming a right angle with
the outer one: in the recent Musk-bull the anterior part of the horn-
core is convex, the outer passing insensibly into the anterior surface,
at least in the old Bull under comparison.

Figs. 1-6.—Fossil and Recent Crania of the Musk-Buffalo.

W.C.S.

ne Z } Back view of the skull of the we

Fig. 2. ; fossil
: \ Top view of the skull of the | peat r Bubalus moschatus.

fossil |

Fig. 3. t Side view of the skull of tke recent J

Fig. 6.
K 2

128 PROCEEDINGS OF THE GEOLOGICAL society. [Dec. 19,

So far as the rest of the cranial structure can be compared, there
is no notable difference between the recent and fossil crania.

The question remains, whether the degree of difference observable
in the horn-cores is to be interpreted as specific. On this point it
may be remarked that the difference in the size and proportions of
the horn-cores is much greater between the male and female of the
existing Musk-buffalo, than between the recent and fossil skulls of
the male sex. It seems unreasonable, therefore, to involve a distinct
primordial origin, or specific act of creation, to account for differ-
ences that are so much smaller than those that depend on mere
sexual modification of one and the same species.

The horns are superadded appendages to the mammalian type ;
they are not common to all Ruminantia; in many of that order
they are restricted to the male sex. Like all peripheral superaddi-
tions to typical structure, they are subject to great variety. The
influence of restricted range in space and of relative number of
individuals to a given extent of feeding-ground affects the propor-
tions of the horns in wild species, or those that in all other respects
continue to live in a state of nature. This fact is exemplified in the
Red-deer of the Highlands of Scotland. No examples of that noble
crowned antler which characterized the “‘ Hart of tyne’’ within the
historical period are now to be seen, or have been obtained for some
years back, in the Scottish deer forests. But the typical luxuriance
of antler-development is still to be met with in the red-deer existing
under more favourable circumstances and with a wider range of
pasturage, in parts of central and southern Europe and in Asia
Minor*. When to restricted range is added the more direct inter-
ference of man, as in the domestic races of ruminants, the horns are
amongst the first parts to attest the influence of those modifications
relating to food, to exercise, to exposure to the elements, and to
defence from natural enemies, resulting from domestication.

We might fairly infer, therefore, @ priori, that the progressive limi-
tation of a bovine species, to a more restricted area and more northern
latitudes, would first manifest its influence in some modification of the
horns. The observed differences, however, between the fossil and
recent Musk-buffaloes in this respect are far inferior to those which
domestication has effected in the condition of the same appendages
of the same unquestionable species of Ox and Sheep.

By the analogy of such facts, therefore, and guided by the above
train of reasoning, we are led to conclude that the ascertained differ-
ences between the fossil and recent Musk-buffaloes are not of specific
value; and that the Bubalus moschatus—with a range at present
restricted to a southern limit, defined “by a line running from the
entrance of the Welcome River into Hudson’s Bay, about the 60th
parallel of latitude in a westward and northward direction to the 66th
parallel at the north-east corner of Great Bear Lake, and from
thence in nearly the same direction to Cape Bathurst in the 71st

* Since this paper was read, Dr. Sandwith has shown me the antler of a Red-

deer (Cervus elaphus) from the Crimea, which equals in size, number of snags, and
expanse of summit, any fossil specimen I have seen.—Feb. 1856.—R. O.

1655. | | ' | OWEN—FOSSIL MUSK-BUFFALO. 129

parallel*,”’ from which line it roams in summer northwards to the

islands beyond Barrow’s Strait,—is the slightly modified descendant
of the old bubaline companion of the Mammoth and the Tichorhine
Rhinoceros ; the Musk-Buffalo then enjoying a much wider range,
both in latitude and longitude, over lands that now form three divi-
sions or continents of the northern hemisphere of the globe. There
appears to have been no degeneration in general bulk in the existing
Musk-buffaloes, and the close wool and coarser hair which clothe them
were doubtless the defensive covering of the pleistocene individuals,
as of the co-existing Elephants and Rhinoceroses.

I should wish to be understood, however, whilst offering this
interpretation of the facts and comparisons based on Messrs. Kings-
ley and Lubbock’s British fossil, not to be pronouncing absolutely
as to the specific identity of the fossil and the recent Musk-buffalo.
I am submitting merely the conclusion which, in the actual state of
zoological philosophy, seems to me to be deducible from the pre-
mises at command. It is only since the publication of the illustra-
tions of the “ Zoology of the Herald,’ in 1852, that naturalists
were made acquainted with the forms and proportions of the skeleton
of the recent Musk-buffalo+. No entire skull of the pleistocene or
fossil species has yet been obtamed; the bones of the face are
unfortunately broken away in the specimen, No. 24,591, IB, in the
British Museum, from the beach in Eschscholtz Bay, which, from
the retention of the horny case of the horns, Dr. Buckland could
not consider as fossil{. Of the forms and proportions of the bones
of the extremities in the fossil Musk-buffalo we as yet know nothing.
I do not, however, deem it probable that the parts of the skeleton
less liable to variation than the horns will be found to manifest
a greater amount of modification than those parts have presented in
the specimens of recent and fossil skulls hitherto compared. And
the extent and kind of variety observed in the horn-cores of the
recent and fossil Musk-buffalo by no means lend support to the
hypothesis that would derive all the forms of bovine animals from
one specific stock. For no influences have been yet observed so to
modify the horns of the Ox proper (Bos) as to diminish the interval
between them and the Bison’s (Bison) ; the horns of the Oxen may
wholly disappear in certain breeds, but their place of origin, or
relative position to the frontal bone, never varies. Moreover, the
three leading types of Bovide,—Bos, Bison, and Bubalus,—were
coeval in geological time, and were represented in Europe, Britain
inclusive, by the Bos primigenius, Bison priscus, and Bubalus mos-
chatus seu Pallasi.

In regard to the question of the extinction of some of these
bovine species and contemporary Herbiwora; although the argu-
ment for the fact of a diluvial cataclysm, at a recent date in geologi-
cal time, which Cuvier deduced from the discovery of the carcass of
an elephant preserved with its soft parts entire in frozen soil on the

* Sir J. Richardson, loc. cit. p. 23. + Fossil Mammals, pp. 66-87, pl. ii.

t See, however, the judicious remarks of Sir John Richardson on the conser-
vative property of frost and frozen soil in regard to this specimen. Op. cit. p. 22.

130 PROCEEDINGS OF THE GEOLOGICAL society. [Dec. 19,

coast of Siberia, and which argument Sir Charles Lyell was, I believe,
the first to invalidate, has for some years lost all its weight, and the
phenomena are now known to be explicable without any such
reference to a diluvial or other cataclysm, it may not be without
its use in diffusing true ideas of the conditions of the former exist-
ence of Elephants and Rhinoceroses in northern latitudes, to bring
that argument face to face with the facts above stated relative to the
Bubalus moschatus.

Supposing that the Musk-buffalo, like the Mammoth and Ticho-
rhine Rhinoceros, had been known only as a fossil, the deductions
from the habits and habitat of the nearest allied buffaloes, as to its
unfitness for an Arctic clime, would have been as reasonable or
plausible as was Cuvier’s in regard to the Siberian elephant. The
entire division of the bovine race, subgenerically separated as Buffaloes
(Bubalus) from the Bisons (Bison) and Oxen (Bos), inhabit, it
would have been urged, the warmer or tropical latitudes. The
species which, in the form, proportions, and direction of its horns,
makes the nearest approach to the Siberian fossil Buffalo is the
Bubalus caffer of South Africa. What speculations might not have
been indulged in as to the changes that had taken place, in the
climate of the Ob, the Lena, and the Indigirska, since the period
when the Buffaloes, whose fossil remains Pallas discovered in these
inclement parts of Siberia, lived and ranged along the banks of
those rivers! What temptations to elude the difficulties of explain-
ing such changes of temperature, by invoking, with Cuvier, the vast
and sudden diluvial wave that might have borne along the carcases
of Buffaloes as well as Elephants and Rhimoceroses, from fertile
regions to the land of lasting frost !

In the Musk-buffalo encountered by our enterprising and much-
enduring Arctic explorers in Melville Island and Baring’s Island,
we have the living exemplification of the slight and superficial modi-
fications which enable one species to find its appropriate theatre of
existence in a far different latitude from the rest of its congeners.
Ought we to have been much more surprised if some individuals—some
lingering remnants of the species—of the two-horned woolly Rhino-
ceros, or even of the equally warmly-clad Mammoth, had been met
with in the same rarely visited regions of Arctic America, deriving
their subsistence from the thick forests near the Mackenzie, or
resorting to the scattered clumps of spruce-fir that skirt the barren
grounds between the 60th and 66th parallels of north latitude ?

The conclusion from present evidence seems to be that the cir-
cumstances which have brought about the extinction, probably
gradual, of the northern Rhinoceros and Elephant have not yet
effected that of the contemporary species of Arctic Buffalo.

— = sped Sores

1855. | PRESTWICH—GRAVEL AT MAIDENHEAD. 131

TABLE OF ADMEASUREMENTS.

Fossil.
TTT a,
Pallas. Lubbock. ee ;
in. lin. in. lin. in. lin.
Breadth of the cranium between the orbital
EGC US agen salseitiaaasnneoannaciote/itaoaanneens Ag ol Ob soc LE. LO
Greatest transverse diameter of the occiput... 8 6 ... 7 6... 8 3
Vertical diameter of the occiput from the
middle of the super-occipital section to
the upper border of the foramen magnum 4 0 3 6 4 0
From the outer border of one occipital con-
dyle to that of the other...........csssscceos 6 0 5 0 6 0
Antero-posterior diameter of the base of the
MUPGHAE DLO teste ns cuca tec esesees over dolceessesese HE) a) 7 0 10 0
Length of the horn-core (following outer nerve) 0 0 ll 0 12 6
Depth of the intercornual groove ............... 0 11 0 8 0 1l
0 6 0 6 0 7

Breadth of the intercornual groove ..............

2. Note on the GRAVEL near MAIDENHEAD, in which the SKULL
of the Musk Burrato was found. By J. Prestrwicu, Esq.,
F.R.S., F.G.S.

Tue Valley of the Thames, broad and open in the tertiary area as far
as Maidenhead, there contracts into the comparatively narrow and
circuitous gorge through which the river traverses the chalk hills by
Henley, Reading, and Pangbourne. ‘To this pomt also extends an
extensive mass of ochreous gravel, stretching in a continuous and un-
interrupted sheet from the sea to Maidenhead, a distance of 50 miles,
from 2 or 3 miles to 8 or 9 miles wide, and with a thickness of from
3 topo teeter.

The great bulk of this gravel is composed of subangular chalk-
flints, derived, it may be presumed, from the destruction of portions of
the adjacent chalk-surface ; whilst, as subordinate materials, we find
a considerable number of perfectly rolled and round flint-pebbles,
derived directly, not from the chalk, but from the lower tertiary

strata and from the Bagshot sands; also a not inconsiderable number

of hard quartzose sandstone-pebbles, pebbles of white quartz, slate,
and other older rocks,-——all perfectly rounded,—and these again

derived, not directly from the rocks to which they originally belonged,

but, as far as I can judge, all, without exception, from the conglo-
merates of the new red sandstone of Worcestershireand Warwickshire.
A singular feature of this gravel is, that although the transport of this
debris of the new red sandstone must have passed over the wide band
of the oolites of the midland counties, vet but extremely few traces
of these rocks are to be found. Of the Lower Greensand and sand of
the Portland series a number of the small black pebbles belonging to

_ * Tt ranges much further westward, but forms narrower bands, or else detached
masses, and loses its distinctiveness.

132 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 19,

those beds are met with, but rolled oolitic fragments are very scarce.
They do, however, occur, and one considerable block of coral rag was
found last summer by Sir C. Lyell and myself ina gravel-pit near the
Thames between Twyford and Henley. When this gravel reposes
on the chalk it is generally mixed at its base with a large proportion
of chalk-rubble, which sometimes is concreted and forms a thin solid
base or pan to the gravel.

At various places in this gravel of the Thames Valley there have
been found from time to time numerous organic remains consisting
of land shells and bones of land animals. These it is not now my
object to allude to further, except to state that they are not found
constantly, but, on the contrary, only at distant intervals. Mr.
Trimmer long since discovered them at Brentford, and last summer
elephant remains were found in the gravel near Kingston. Mr.
Blackwell has also found them far up the Valley of the Thames, or
rather the branch Valley of the Kennet, at Aldermaston near New-
bury. But although it was apparent that the same gravel extended
over the greater part of the intermediate area, yet no organic remains
had hitherto been noticed in the central district of Windsor and
Maidenhead.

On the right-hand side of the Great Western Railway, just before
reaching the Maidenhead station, there is a large gravel-pit which I
had formerly visited, and which has of late been extensively worked
for ballast. I had never found any bones in this pit ; still the locality
appeared very favourable for further research. Therefore, when, last
summer, Mr. Lubbock informed me of his intention to spend a few
days at Maidenhead, I pointed out this spot to him, and expressed
a hope that he would examine it carefully. This he kindly undertook
to do, and, to my great gratification, returned in a few days with
the remarkable specimen of which Prof. Owen has given so able and
interesting a description. Besides the skull of this Buffalo, Mr.
Lubbock procured a few Elephant and other bones*, but in a very
imperfect state. They were all found low down in the gravel—at the
point where it becomes mixed with chalk-rubble, or on the top of the
chalk itself. I only hope that he will return there again and follow up
an investigation so well begun. }

The bones, as usual in such situations, although very friable, are
tolerably entire, or if broken are not worn. Nor does the gravel
itself afford any evidence of long-continued movement or of much
wear. If we eliminate from it the flint-pebbles derived from the ter-
tiary beds and the pebbles of the older rocks derived from the new
red sandstone, we have a residue of subangular flints which exhibit
extremely little wear—nothing like that which would result from
long-continued river or shore action,—and it is necessarily this residue
which gives us the true measure of wear and tear which the mass has
undergone. ‘To this I wish merely to allude in passing, as it is a point

* I have since visited this pit and obtained part of a tooth of the Elephant.
The workmen informed me that a considerable quantity of bones were found some
time since at the other (west) end of the pit. At the east end, where they are now
digging, they have found but very few bones,

1855. | PRESTWICH—GRAVEL AT MAIDENHEAD. 133

which has been too frequently overlooked ; it is of essential importance
in considering the drift pheenomena, but its fuller discussion I must
reserve for a future occasion.

With regard to the age of this gravel, it belongs doubtlessly to the
same period as the Kingston, Brentford, Kew, and London beds,
which I am inclined to consider as amongst the most recent of our
drift deposits, and as posterior to the period of the great Boulder Clay
of Norfolk and Suffolk; but the exact relation of these deposits is
nowhere clearly seen, and this question of relative age depends upon
a variety of collateral evidence which I hope to lay before the Society
at a future period.

In the meantime I may mention that although the boulder clay
does not approach within twenty miles* of Maidenhead, yet there is
another gravel in that district, distinct from the mammaliferous
gravel, and showing that distinctive position tolerably clearly, although
not so well as it is seen further westward.

Section of part of the Valley of the Thames, showing the relation of

the high-level and the low-level gravels. ;
5
&
Railway Station ey
near Maidenhead. = a

be
qin levell oravels soate saves saceettadendosenswewss cons 5 to 10 feet.
6. Valley-gravel, with mammalian remains......... 5 to 20 ,,
c. Mottled clays (lower tertiary).

d. Chalk.

Thus immediately from this plain of gravel there rises near the
Maidenhead station the chalk hill on which Taplow stands. . This
hill forms a ridge connected with the hills at Beaconsfield and above
Wycombe. Over these hills and extending as far as Taplow is
another gravel very similar in many respects to that in the valley, but
always on a higher level, and without organic remains. It is an older
gravel. In the same way the hills of Bagshot and Windsor Forest
to the southward of the Thames Valley are capped by older gravel.
Both these possess some peculiar and interesting features, but the
description of them I will reserve until I can bring the subject before
you in a more complete form. My object on this occasion is merely
to point out the position and general relation of the gravel in which
the very remarkable fossil, the subject of this evening’s important com-
munication by Prof. Owen, was found, and not at present to occupy

your time by any independent inquiry on the physical phenomena
considered apart.

* The nearest places to which I have yet traced it are on the Finchley Hills;
and it extends probably as far as Hendon Hill.

134 PROCEEDINGS OF THE GEOLOGICAL society. | Dec. 19,

3. On some Geological Features of the Country between the SouTu
Downs and the Sussex Coast. By P. J. Martin, Esq., F.G.S.

THE object of this paper is not so much to give a minute descrip-
tion of the district I am about to review, as to promote a discussion
amongst the members of the Society here present on some of its
phzenomena, which seem to be singularly illustrative of the super-
ficial changes that have been effected in the south of England by
dynamic forces of comparatively modern date.

The district is to be found in the ninth section of the Ordnance
Map, and extends from near Portsmouth to Shoreham, or that flat
country which is to be seen from any part of the tops of the South
Downs from Portsdown Hill eastward to the Shoreham River.

If time serve, we may perhaps be induced to extend our views as
far as Brighton. ‘The cliffs of Brighton and its raised beach have
been so often described, have given rise to so much discussion, and
so little new can be said about them, that I have in my own
mind set them down, and the beach in particular, as amongst those
specialties (like terrestrial surfaces, patches of modern, or recent,
or post-pliocene deposits with correspondent fossils) which cannot
be ignored, but which I hope some day to see brought into harmony
with the simpler actions of consentaneous elevation and denudation,
which I, and much abler geologists than myself, have endeavoured
to expound.

The first remarkable feature of this tract of country which I pro-
pose for your notice, and which brings it into the same category with
all the disturbed districts of the south-eastern part of our island, is
an anticlinal line of chalk-elevation, extending from Portsdown Hill
into the sea at or near Worthing. Portsdown is on its northern
slope; its ridge, or line of culmination, runs by Emsworth and West
Thorney to Donnington and Hunston, south of Chichester (here
much obscured by drift), and then less obscurely by Climping and
Ford to the Arun. From thence it passes between Leominster and
the hamlet of Wick, and rises suddenly on its northern slope, like
Portsdown, in another, but smaller, emimence called High Down*.
From thence, I believe, it goes out to sea and is lost, unless it ap-
proximates to the South Downs east of the Ouse, and produces the
synclinal tertiaries of Newhaven and Seaford.

This anticlinal brings up at Hunston and elsewhere along its range,
a portion of the white chalk, characterized by Marsupites, which I
regard as higher in stratigraphical position than the so-called “upper
chalk” of the south-eastern counties of England. This uppermost
chalk is soft and marly, and without flints; it is called “ free-chalk ”’
or “marl”; and is dug for manure at Stoke and Lavant. It appears
also along the base of the chalk-escarpment at Halnaker and a few
other places in West Sussex, but does not occur on the Downs, which
have lost this upper member of the chalk-series by denudation.

North and south of this chalk-elevation are two synclinals or

* These eminences were described as “ outliers by protrusion ” in Mr. Martin’s
‘Geological Memoir on a part of West Sussex,’ 1828.

1855. | MARTIN— DRIFT-DEPOSITS OF WEST SUSSEX. 135

troughs of tertiary deposits. Eastward from the Forest of Bere the
tertiaries of the northern synclinal have been much denuded, and
are mixed up with an enormous quantity of drift, to be hereafter
described. They emerge again from this drift, and appear in con-
siderable force in the high grounds between Chichester and Arundel,
in Kastergate, Walburton, and Binsted. East of the Arun, again,
they expand imto the woody districts of Angmering, Clapham, and
Castle Goring in the rear of High Down, where a great mass of
eocene gravel has long been worked out for economical purposes.
The southern synclinal is occupied by the well-known Bognor beds
and the Bracklesham eocene; and these and the London Clay, or
its equivalent, form the basis of all the flat country south of Chi-
chester, called the Manhood. I do not think that the Bracklesham
beds have any inland outcrop ;' but the London Clay is extensively
exposed in Siddlesham, Birdham, and the north part of West Witti-
ring. Wells im the last-mentioned parish have furnished me with
the geodes or septaria of the London Clay; but I have not been
able to pick up any fossils from the same. The cement-stone is also
dredged up in the adjoining part of Chichester Harbour. Wells and
excavations in the southern part of Birdham and in Earnly furnish
a fawn-coloured micaceous sand—perhaps the Thanet Sands.

This will suffice to prove that the basis of all the plain south of
Chichester is the stratified beds which assimilate to those which
occupy the valley of the Thames. A great deal of drift reigns para-
mount over all; and the most interesting part of this material is the
deposit to be found south of Siddlesham,—consisting of loam or
brick-earth, extensive beds both of rounded gravel and angular flints,
the former much predominating, with large boulders of granite and
other crystalline rocks; the whole exhibiting much of the hetero-
geneous and tumultuary character of the boulder-drifts of the eastern
counties. :

The high grounds of Selsey are entirely composed of these de-
posits. Extensive shingle-beds spread im all directions through the
eminence on which the village of Selsey stands, which eminence
rises 25 or 30 feet above the sea; and they are carried on eastward
about the church, and on into the flat called the Harbour, a branch
of Pagham Harbour, producing there a remarkable pheenomenon
called the “ Hushing Pool,’ described by the county historians as
amongst the most remarkable natural curiosities of this district*.
The boulder-drift dies out as we come north from Selsey, though
there is good reason to believe that it was once spread over all the
district, for large masses lie here and there over the parishes of Bird-
ham, Siddlesham, and Hunston, or are occasionally brought to light
by the plough t.

North of Hunston and Donnington, and of all the chalk-anti-

* It is simply the bubbling and hissing produced by the disengagement of the
air from the gravel before the incoming tide.

+ The font of Yapton Church is of granite, which, if not found on the spot,
was most probably not brought from any ey distance, as the fonts of this
country are mostly of Purbeck marble.

136 PROCEEDINGS OF THE GEOLOGICAL society. [Dec. 19.

clinal before spoken of, extensive beds of angular gravel prevail,
containing sometimes eocene pebbles, and, more especially as we
approach the Downs, forming the “supracretaceous”’ zone of drift
I have elsewhere described as mantling round the nucleus of the
Weald.

_ These drifts have been so well described by Sir R. Murchison in
his paper* on the flint-drift of Sussex, that I need not enter into
further detail respecting them. The great occasional mixture of
these angular gravels with the shingle-beds of the eocene has escaped
the notice of Sir Roderick. This mixture is very remarkable about
Boxgrove and Crocker Hill on the Chichester road, and at Halnaker,
and indeed is common to all districts where relics of the lowest ter-
tiaries are to be found.

Much stress has been laid on the colour and general appearance
of these gravels, the white being considered as of the newest order.
The flints that are found mixed up with chalk-rubble have a white
coat, and the angular gravel that is mixed up with ferruginous sand
or brick-earth is brown.

I consider these as accidental circumstances ; and, although the
gravel arising from the earliest chalk-denudations may exhibit a
browner colour and greater marks of antiquity, whilst that which
was last produced, when the denuding forces were in operation, ap-
pears to be more recent, yet there seems to be no ground for the
belief that they belong to distinct eras or other agencies than are
common to both.

[The above notice of the geology of part of Western Sussex com-
prised the written portion of the communication made by Mr. Martin,
and was preliminary to the verbal exposition of the author’s views on
the relations of the boulder-deposits of Bracklesham and the neigh-
bourhood with the older tertiary and cretaceous strata, on the one
hand, and with the superficial gravels and brick-earth on the other ;
a subject closely connected with the author’s previous researches in
the geological history of Sussex and the Wealden district t.

A paper by Mr. Martin, illustrative of this subject, was unfortu-
nately mislaid after having been read before the Geological Society
in 1840, and not found again until about 1848. The author was
subsequently enabled to publish it in the ‘ Philosophical Magazine’
(see Mr. Martin’s “ Memoir on the Anticlinal Line,” &c. 1851) with
additional observations; and, at the request of the President, who
took advantage of the opportunity to express the Society’s regret for
the temporary loss of Mr. Martin’s memoir above referred to, Mr.
Martin favoured the Meeting with a general exposition of his views
on the Wealden denudation, as far as time allowed, on the occasion
of his reading the paper now printed.

In this communication the author assigned the boulder-drift lately

* Quart. Journ. Geol. Soc. vol. vii. p. 347.
+ See Mr. P. J. Martin’s Memoir on the Anticlinal Line of the London and
Hampshire Basins (8vo, 1851) and Supplement, 1854 ; in which also his previous

writings on the subject are referred to.
‘

Jan. 9, 1856.] SORBY—TERTIARIES OF THE ISLE OF WIGHT. 137

brought to light by Mr. Godwin-Austen to an outer zone of Wealden
drift, in addition to those which he had already described as mantling
round the nucleus of the Weald ; the corresponding parts of this
zone, he thinks, are to be found in tbe valley of the Thames, and
perhaps yet to be discovered amongst the Greywethers and other
relics of the Tertiaries found on the chalk-country of Hampshire and
Wilts. The above-mentioned zone is regarded by the author as the
remains of the boulder-deposit which is spread over the tertiary
countries of this and the adjoining parts of the North of Europe,
before their continuity was disturbed by the upheaval of the great
anticlinal of the South of England.

The country immediately under review, Mr. Martin regards as a
sectional part of this great anticlinal, and not to be considered apart
from the wide geological area to which it belongs. He considers
that its phenomena of arrangement and drift belong to the epoch of
that upheaval, and betoken the agencies of powerful diluvial cur-
rents, set in motion and contemporaneously assisted by the disloca-
tions known to abound in this part of our island; and without the
aid of which no satisfactory conclusion, in the author’s opinion, can
be deduced respecting the drifts and the other phenomena of the
denudations and surface-changes here exhibited. |

JANUARY 9, 1856.
H. P. Hakewill, Esq., was elected a Fellow.
The following Communications were read es

1.:-On the Puysican Grocrapuy of the TERTIARY Estuary of
the IsLx or Wicut. By H. C. Sorsy, Esq., F.G.S.

[This Paper has been withdrawn by permission of the Council.]
(Abstract.)

In this paper were first described the currents due to the action of
the tide and stranding surface-waves in an estuary, and the
relations between them and the physical geography of the limiting
shores. These are such, that, if the direction and character of
the currents were known, the physical geography of the area
might be inferred within certain limits. After this were explained
the various structures produced by currents in strata formed
under their influence, from which the direction, velocity, cha-
racter, and depth of the currents can be ascertained. This was
followed by an account of the directions and other peculiarities of
the currents indicated in the various sandy and other strata of the
tertiary formations at numerous localities in the district under con-
sideration. From thence the author obtains data from which many
peculiarities in the physical geography of the coast-lines of the ter-
tiary land and sea in the area now occupied by Hampshire and the

_Isle of Wight can be deduced. The chief of these characters are

138 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. _[Jan. 9,

that during the tertiary period there was formed a wide estuary of a
large river, running from the west towards the east; that the land
from which the river came must have been to the north, the west,
and south-west, whilst the estuary opened into a tidal sea towards
the east ; and that at the western part of the Isle of Wight area there
existed a considerable shoal. This explains why the section of the
tertiary deposits at Alum Bay is so very different to that at White-
cliff; where there was no shoal, but a tidal channel too deep to be
affected by the action of the waves of the surface.

2. Onthe PermM1AN CHARACTER Of some of the Rep SANDSTONES
and Brecctas of the Soutu of ScoTuanp. By E. W. Binney,
Esq., F.G.S. Ina letter to Sir C. Lyi, V.P.G.S.

At the conclusion of the paper on the Permian beds, printed in our
Manchester Memoirs this last summer, I gave the following as the
greatest thicknesses of the different beds in the descending order :—

feet.
1. Red and variegated marls, with gypsum in the north, and thin beds

and nodules of limestone in the south of the district .................. 300
2. Magnesian limestone, resembling the Yorkshire deposit ..... -wscasasaeeiee 10
3. Conglomerate ............ h sshisolewe:ds does tah Aue Cadne lwp celc’s chasenea* on deem 350

4. Lower New Red Sandstone, of a soft crumbling character ; some of the
beds flaggy; the lower beds passing into red laminated marls at
WESTROUSE. oeiccnnsessiqnedenyicckseanceacndlsrocien-Ueniseeasen ane bass eee ae 500

Below these occur the red and variegated sandstone of White-
haven, which at present I do not include as Permian. In my paper
I state that I am convinced that the conglomerate, or rather breccia,
at Craigs and in the Cleuden near Dumfries are of the same geo-
logical age as the sandstones and conglomerates of Belah, Brough,
Westhouse, and Humphrey Head, and I quote Professor Harkness
on the thickness of some of those deposits.

Since the time you were in Manchester I have been down into the
South-west of Scotland, and, after looking at the country, I have
come to the conclusion that the red sandstone of Canobie on the
Esk, Lockerbie, Corncockle Muir, Dumfries Thornhill, near Sanquhar,
and Mauchline, as well as those of the West of Scotland generally,
with the exception of the Annan beds containing tracks of the Laby-
rinthodon, will have to be classed as Permian, instead of Trias as
they appear on most geological maps.

At Ballochmoyle Bridge is a fine section of the Upper Permian
sandstone of Dumfries and of a purple-coloured conglomerate, or
breccia, resembling the same deposit near Dumfries, except that the
fragments and pebbles imbedded in the cement consist of trap-rocks
instead of slates and Silurian rocks. The escarpment near the old
bridge shows the following section :—

1856. | BINNEY—PERMIAN ROCKS OF SCOTLAND. 139

Fig. 1.—Section near Ballochmoyle Bridge.

BEER EES
SFP rvs
= 2G gq Soae
Nizar Nag, SU Ne »
ae ENS S <iNo) Da

:
SS ASS

of

a. Red-coloured sandstone, false-bedded ; 60 to 70 feet.
5. Red sandstone.
c. Breccia; 30 feet.

Further up the river, a mass of amygdaloidal trap cuts off the
breccia-beds on their rise, and thus prevents their lower portions
from being seen; but about half a mile further up the stream towards
Catrine, red marls and red and purplish sandstones, of great thick-
ness, make their appearance, dipping slightly to the west. In some
of the latter there are slight traces of fossil plants and beds of ripple-
marked sandstones.

Fig. 2.—Section from the Glasgow and South-western Railway to
beyond Catrine.

Ballochmoyle Catrine Lindsay
Railway. Bridge. Cliff. Bank.
eae ey, ae)

a. Red sandstone.

6. Breccia, dipping W. at an angle of 8°.

c. Dyke of amygdaloidal trap ; running N.W.—S.E.

d. Red, purple, and variegated marls and sandstone; dipping W.

The breccia near Ballochmoyle Bridge dips due west at an angle of
8°. Some of the pieces of trap are rounded and others quite angular.
The beds are divided by thin veins of sparry matter. The cementing
paste has much the appearance of felspathic ash. After the trap-
dyke is passed, and its breadth must be near a third of a mile, the
sandstones and marls of Catrine Cliff occur. They dip very slightly
to the west. As you pass through Catrine to Lindsay Bank you
come to a great thickness of red and variegated marls and sandstones,
some of the latter being ripple-marked flags, which near Lindsay
Bank dip due west at an angle of 30°. I did not go up the river so
far as Sorn; but, from the large fragments of breccia seen in the
Water of Ayr, im the river above Lindsay Bank, I suspect that the
Ballochmoyle Bridge deposit may again occur further up the river.
All the beds about Catrine appeared to me to be very like Permian

140 PROCEEDINGS OF THE GEOLOGICAL Society. {[Jan. 23,

strata. The red sandstone at Ballochmoyle lies in wedge-shaped
masses in the conglomerate (fig. 1), like the same deposits at Belah,
Westhouse, and Flookborough (Humphrey Head).

The conglomerate and breccia, whether seen at Flookborough in
Furness, Westhouse in Yorkshire, Belah Bridge and other places in
Westmoreland, near Dumfries, at the foot of Criffel near the mouth
of the Nith, or at Ballochmoyle in Ayrshire, present the same kind of
paste or cement, resembling decomposed felspar, but the imbedded
rocks vary as the rocks of the respective districts do; thus at Flook-
borough, Westhouse, Belah, and Brough, we have limestone frag-
ments,—at Craigs and in the Cleuden, slates and Silurian rocks,—
near Criffel, granite,—and at Ballochmoyle, trap; clearly showing
that such rocks have been derived from the beds of the neighbouring
districts, and not brought from a distance.

The circumstance of the large tract of the South-west of Scotland,
hitherto coloured as Trias, proving to be Permian, must be of great
importance to the ironstone and coal districts lying near it, and will
in some instances no doubt allow such deposits to be followed under
it. In addition to this economical advantage, the change cannot
but prove highly interesting to the palzeontologist, as it will enable
him to remove all the tracks of animals found in the Corncockle
Muir, Locker Bridge, Craigs, and Greenbank quarries from. the
Trias and place them in the Permian fauna,—a position where they
will better fit, when compared with the continental deposits, than in
their old place in the Trias.

JANUARY 23, 1856.,

Richard 8. Roper, Esq., and the Rev. S. Lucas were elected
Fellows.

The following Communications were read :—-

1. On the Cryouite of Evicrox, GREENLAND.
By J. W. Tay er, Esq.

{Communicated by J. Tennant, Esq., F.G.S.]

Tue few remarks which I am about to offer relate to the mineral
Cryolite*, and the nature of the district in which it occurs; and I
propose to lay before the Society some observations which the ex-
ploration of a rich lead-vein situated in the Cryolite has afforded me
the opportunity of making.

Evigtok (which signifies in the Esquimaux language “a place
where there is plenty’) is distant about twelve miles from the Danish
settlement of Arksut, and forms a small bay in the Fiord of Arksut;

* See Thomson’s ‘ Outlines of Mineralogy,’ vol. i. p. 251 ; and Giesecke’s article
“ Greenland,” in the Edinburgh Encyclopedia, 1816.

18

56.]

TAYLER—CRYOLITE. 141

it is a semicircular space of rather low irregular ground, surrounded

¢

Fig. 1.—Horizontal Section or Ground-plan of the Cryolite at Evigtok.

>
- =
S “2 N Ne SS

ee ay:

/
{
%
i
i
i
’
1
J
'
}
!
'
'
R
N

[i

(The exposure of the Cryolite is about 300 feet in length.)
€

RC
3 AC

VOL. XII.—PART I.

1,1. Galena
t, ¢. Tin-stone.
T. Tantalite.

2. Sparry iron-ore.

ap. Arsenical pyrites, and tin.
pl, pl. Iron- and copper-pyrites, galena, and blende,

SJ, f- Fluor-spar.

g. Quartz-rock, with felspar, cryolite, and ores of
iron, tin, lead, zinc, &c.

g,g- Granitic gneiss, with quartz-veins.
sg, sg. Schistose gneiss and hornblende-schist.

xv, a. Trap-dykes.

by a ridge of mountains,
rising abruptly to the height
of about 2000 feet; making
the enclosed space appearthe
half of a deep basin about
two- miles im diameter.
Evigtok is noted in Green-
land for its abundance of
fish in the summer season ;
shoals of capelins blacken
the small bays, whilst thou-
sands of codfish swim close
to the shore in pursuit of ©
them, both of which are
taken by the natives in large
quantities. At the foot of
the mountains and on their
sides are to be found many
grouse, hares, and arctic
foxes. In the winter season
immense flocks of eider
ducks and other water-fowl
resort to this part of the
Fiord. Vegetation, such as
it is in Greenland, also pros-
pers here : a miniature forest
of Salix Arctica, about 4 feet
high, covers about a square
mile, and the Angelica,
Rumex, Taraxacum, Poten-
tilla, and other plants are
met with more abundantly
than is general in Green-
land; the spot appearing
like a garden amidst the
general barrenness of a land
buried deep in snow nine
months out of the twelve.
But Evigtok is more remark-
able as being the only place
in the world in which the
mineral cryolite has hitherto
been found.

By reference to the hori-
zontal section (fig. 1), two
trap-veins will be seen bound-
ing a space containing the
eryolite and the minerals
accompanying it. To this

L

uf a

142 PROCEEDINGS OF THE GEOLOGICAL sociETy. ([Jan. 23,

space I shall confine my remarks. The section is not drawn accu-
rately to a scale, but it is about =, inch to the fathom.

Starting from the western trap-vein, which is situated in schistose
gneiss and hornblende-schist, we find the gneiss gradually losing its
slaty structure, until in the neighbourhood of the ecryolite it becomes
granitic, and now contains numerous metallic traces ; before arriving
at the cryolite, we find a wide vein of white quartz and felspar, run-
ning about S.W.; the quartz and felspar are in very large masses
and crystals, some crystals of quartz measuring a foot in thickness.
This rock is traversed in several directions by small veins and masses
of cryolite, isolated from the larger body of that mineral, im
which, as well as in the rock, are to be found numerous crystals of a
variety of tantalite, oxide of tin, blende, molybdenum, much galena,
copper-pyrites, arsenical and iron-pyrites, and sparry iron-ore. In
this rock are many small caverns, arising from the decomposition of
the felspar, and probably also from the decomposition of the cryo-
lite, which is here porphyritic, containing crystals of felspar and
quartz. The floors of these caverns are covered with loose crystals
and fragments of felspar, and in some places kaolin, crystals of tin-
stone, and carbonate of iron. In one of these cavities is a large vein
of arsenical pyrites and purple fluor-spar; also a large vein of black
cryolite, containing copper- and iron-pyrites, and red felspar. Smaller
cavities are found when blasting, the sides of which are completely
covered with crystals of the tantalite, resembling on a large scale

Fig. 2.—Transverse Section of the Cryolite at Evigtok.
(The width of the Cryolite is about 80 feet.)

By

WZ

——/

Black Cryolite.

9,g. Gneiss. | pl, pl. Galena, copper-pyrites, blende,
¢. Sparry iron-ore. iron-pyrites, and carbonate of
g- Quartz-vein. iron scattered in cryolite.
l. Argentiferous galena. | * Fragment of cryolite was found
Ff. Purple fluor-spar. imbedded at this spot.

the crystalline cavities in amygdaloidal traps. In this quartz- and
felspar-rock there is a remarkable vein, containing soft ferruginous
clay and rolled pebbles, sparry iron-ore, and copper-pyrites. The
copper lies over the sparry iron, and runs in fine threads between the

1856. | TAYLER—CRYOLITE. 143

folia of the partly decomposed iron-ore, appearing as if it had run
into it in a state of solution. To this quartz- and felspar-rock suc-
ceeds more granitic gneiss, in which the cryolite occurs ; this gneiss
gradually loses its granitic character as it approaches the eastern
trap-vein, where it again takes on the same slaty appearance as at
the western trap-vein.

Wewill nowrefer to the transverse section of the cryolite(fig.2). The -
cryolite forms a bed or vein parallel to the strata, and is about 80 feet
thick and 300 feet long ; it dips to the south, at an angle of nearly 45°,
‘and runs nearly E. and W. In the upper wall of gneiss, about 2 feet
above its junction with the cryolite, runs a vein of sparry iron, with
the same dip as the cryolite ; and a layer of opake quartz-crystals lines
the under side of the gneiss, between the iron-ore and the cryolite:
sometimes sinking several feet into the cryolite, but never rising into
the gneiss, is a vein of argentiferous galena, containing 834 per cent.
of lead, and 45 ounces of silver in the ton of ore; this was worked
during the year 1854-5, and some good ore was extracted. The
cryolite below this vein is impregnated for a few feet with galena,
copper-pyrites, and sparry iron-ore ; but beyond, until within a few
feet from the under wall of gneiss, it is quite pure and white ; within
10 feet, however, of this under-gneiss, it again contains the same
minerals disseminated, but is here separated from the gneiss by a
vein of dark purple fluor-spar. The gneiss on both sides of the
cryolite contains much fluor-spar disseminated.

The upper part of the cryolite at its junction with the gneiss is
much decomposed, leaving many cavities, which contain loose crystals
of sparry iron. At a depth of about 10 feet from the surface, the
cryolite, although free from foreign matter, assumes a darker colour;
and at 15 feet it is nearly black, and more translucent and compact ;
and, as the deeper we sunk we found the cryolite become darker,
there is reason to believe that below this depth the mineral will be
found to be wholly black. As the white cryolite is only found at the
surface, and bears evidence of partial disintegration by having lost
some of its compactness and translucency, it is reasonable to suppose
that the cryolite was originally wholly dark-coloured or black.

When the black cryolite is heated to redness, it loses about 1 per
cent. (moisture and acid), the whole of its colour, and part of its
translucency, becoming perfectly white, like the cryolite at the sur-
face. And from this fact we may conclude that the white colour of
the cryolite at the surface has been produced by a similar cause.
I consider it probable that the trap now found at each end of
the cryolite has formerly overlain it, heating it superficially, and
rendering it white; there are at present no remains of overlying trap
between these two veins, but in this country the trap and allied rocks
disintegrate most rapidly from the effects of frost. The ecryolite itself
has considerably decreased, from this and other causes ; for I found
a piece of it imbedded in the upper gneiss, more than 8 feet above
the highest part of the cryolite, proving that it formerly stood at
that height.

In working the lead-vein, we sunk about 30 feet on the dip of the

L2

144 PROCEEDINGS OF THE GEOLOGICAL SocIETy. [Jan. 23,

cryolite; it probably extends to a great depth, and exists in great
quantity.

The fact of its solitary occurrence in this spot induces speculation
in regard to its origin. The number of minerals, mostly crystallized,
which accompany it, indicate some powerful- and long-continued
agency to have operated in a limited space. The few facts I have
stated may suggest some opinions which may elucidate the as yet ill-
understood subject of mineral veins. The cryolite has been hitherto
applied to few purposes. The Greenlanders were the first to turn it
to account, which they did in a curious manner, viz. the manufacture’
of snuff. They grind the tobacco-leaf between two pieces of cryolite,
and the snuff so prepared contains about half its weight of cryolite
powder. This snuff they prefer to any other. In Europe cryolite
has been employed to a limited extent; but the recent discovery of
‘the mode of preparing aluminium will probably render it a valuable
ore of that metal.

2. Description of Remarkable Minera VEINS.
By Prof. D. T. Anstrp, M.A., F.R.S., F.G.S.

[Tu1s Memoir was preceded by an introduction, in which the author,
after certain definitions, stated the class of facts which he considered
it desirable should be recorded by mining engineers in investigating
mineral veins, in order that their observations might be available for
scientific purposes. |

1. The Cobre (Copper) Lode of Santiago de Cuba.

As being a very exceptional and remarkable vein, and one which
possesses a remarkable geological interest, I have selected for this
memoir the great Cobre lode, and I propose to describe and, as far as
possible, explain the conditions of this vast deposit of mineral wealth.
I select it with the greater readiness, as it has not hitherto, I believe,
been the subject of scientific investigation, although known for twenty
years as the richest copper lode which has within that. period been
the object of continuous mining operations in any part of the world.

Position of the Lode. —This deposit of copper ore, opened in a hill
near the small town of El Cobre, is about eight miles W.N.W. of the
town and magnificent harbour of Santiago de Cuba, the mines being
directly connected with the harbour by a railway, which takes ad-
vantage of the valley of the Cobre River to reach the mining district.
There is a fall of about 300 feet from the plateau on which the town
is built to the sea, and the hill on which the principal crop of the
lode takes place is about 300 feet above the level of the railway.
The line of railway running nearly parallel to the principal direction
of the sierras, both along the coast and in the interior, gives some
little insight into the structure of the country, and to the facts ob-
served in the cuttings I shall have occasion to allude presently.

1856. | ANSTED—COBRE LODE. » AS

Structure of the Country.—Commencing with the plateau on
which the town is built, we find towards the south a considerable
mountain-chain, consisting of highly calcareous porphyritic rocks,
passing into and associated with basalts and a peculiar conglomerate,
while to the north, at some distance, are hard beds of limestone. I
submit a general section (diagram fig. 1) through the eastern part of
the island of Cuba, crossing the mining district, which will give a suffi- .
cient idea as to the allocation of the beds. It will there be seen that
the beds of greenstone and porphyry appear to overlie the conglome-
‘Yates, green grits, and hard limestones, and these in turn are overlaid
by newer tertiary limestones developed near the coast. For this
section I am partly indebted to M. Quintana (Government Inspector
of Mines of the district), who had crossed the island as far as Holguin
in the central plains. My own observations were confined to the
mining district and the north and south coasts.

Fig. 1.—General Section across the Eastern End of the Island of
Cuba.

(Length of Section about eighty miles.)

n
S ® ©;
s, § 23
2 1 oj 60
Ee © = BMS)
Lo 3 a N
nO 2 ‘2 wn a :
; : i
‘ '
H

Ds lie

Cobre
}--=----- Palma.

: (Gold.)
ce. Conglomerate. 7. Limestone. p. Porphyry. ss. Syenite. 4g. Granite.

The mineral veins occur in the large-grained porphyry already
alluded to, near its contact with a coarse conglomerate, both con-
glomerate and porphyry being extremely calcareous. The general
direction of the mountain-ridges and watershed, the strike of the
porphyries and conglomerates, and also the strike of the lodes, are
all approximately east and west, this being also the direction of the
south-eastern coast of the island of Cuba.

The dip of the lodes is to the south, and that of the bedded rocks
to the north, but the former are much more nearly vertical than the
latter. Towards the east the coast range is syenite, and it is not un-
likely that this syenite extends to or is repeated in the west side of the
harbour, south of the mines. Of this, however, I have no positive
proof. It is worthy of notice that the whole of the mountain-tract
forming the south-eastern extremity of Cuba, is remarkably subject to
earthquake action, two months rarely elapsing without a shock, while
towards the centre of the island and to the west no shocks are ever felt.

The surface of the ground, both in the neighbourhood of the
mines and elsewhere in this part of Cuba, is so covered with tropical
vegetation, and the ground for the most part so impracticable, that
any continuous survey is impossible, so that many observations, else-

146 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 23,

where matters of course, are here of necessity reduced to mere
inferences.

Dimensions of the Lode.—The Cobre lode, as at present known, is
limited in its crop to a distance of about a mile, but it probably
ranges further to the east. Near the eastern extremity a branch is
given off, making an angle of about 30°, and proceeding south-west.
At the bifurcation, which is well seen on the steep banks of the
Cobre River, both lode and branch are nearly vertical, and the latter is
large ; but as it proceeds it becomes irregular, and is broken up and
intersected by numerous threads and strmgs. The main lode is cut
off to the west by a cross course, after being heaved by several slides
of small amount. See fig. 3. af

Fig. 2.—General Map of the Country around Cobre.

Se:

MAESTRA
RRA
S\t
3

‘imestonc)
(Grits)

Caney,

i Cobre a ‘
: Basalt) ye CY SANTIAGO
40 os
(Borphy™
of

SIERRA

Scale of Geographical Miles.

(The arrows mark the dips.)

Although the whole extent of the lode, as known by the crop,
extends to 1800 yards or thereabouts, it is but a small part of this
that can be regarded as valuable. The whole workings on the prin-
cipal vem are limited to a linear extension of 800 yards, and the

1856. | ANSTED—COBRE LODE. 147

Fig. 3.—Map of the Mineral Field of Cobre, Island of Cuba.

LS

. NN

ca * \ = ce

ea ae

ie, ‘
a

>
—]
BAS &,

se ae X S
Uy uty: en

SN
Sym | N

E

rome

The breadth of orey ground in

Heaves and cross-courses. TI vig lode, approximately .

extreme breadth of the ground, including all the parallel rich
branches, is less than 200 yards ; so that within a narrow space of

148 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 23,

about thirty acres are crowded the whole of the “ plant”’ and buildings
of two extensive mines, and part of a third, with dressing-floors and
ore-heaps on a scale rarely seen*, as it seldom happens that so much
ore has been raised from a single group of lodes of such small extent.
The diagram fig. 3 marks the limits of the concessions, and thus
shows the small extent of surface ; but it gives no idea of the crowding
that has necessarily resulted from the form of the ground, which
is extremely broken, and in many parts precipitous. The section
fig. 4 will, however, assist in giving an idea of these peculiarities.

Fig. 4.—Section across the Mineral Field of Cobre.
(Length of Section about 1200 yards.)
a

cS
=
° n
<) ad
ee ay
Santiago as Cobre Lode. a
veins. ~~ oO [a=] Oo

y SS

Sa

f\-iniwisecnuan SUMO CONTE.
v4

C. Conglomerate. p. Porphyry.
A.B. Line of Section on the Map, fig. 3.

Contents of the Lode.—The rich part of the lode is for the most
part contamed in the precipitous hill on which the old and now
ruined church stands, and the ground here, at one time the source
of litigation amongst three companies, is now entirely undermined.
The enclosing “‘country,”’ of which the shell of this hill is composed—
the contents consisting almost entirely of veinstone, formerly largely
mixed with red ore (of which nearly a million tons have been re-
moved),—is a confused mass of material scarcely distinguishable
from a coarse breccia of the adjacent perphyries, with the exception
of some more schistose portions, and of grits met with in descend-
ing. This material, identical with that which formed the hill now
fissured, has no doubt fallen into the cavity or rent formed by some
subterranean elevatory force. The whole group of lodes may
be described as a multitude of yawning cavities, connected with
innumerable smaller crevices, having, for the most part, an east and
west extension, but crossed by other crevices of the nature of small
faults or heaves, all more or less nearly at right angles, and termi-
nated towards the west by one such cross-course, beyond which no
ore has yet been found.

Towards the east, the crevices or veins become gradually of less
importance, and pass into a vein containing but little valuable ore,
though clearly traceable for some distance at the surface. (See
map, fig. 3.)

The whole outcrop of the great lode on this hill has been so much

* At the time of my visit there were not less than 5000 tons of dressed ore
ready for shipment belonging to the Cobre mine alone.

1856. | ANSTED—COBRE LODE. 149

disturbed, and there remains so little of the original gossan to exa-
mine, that the real characteristics of the gossan and crop can only be
made out by close investigation. It would seem, however, beyond a
doubt, that the appearances must originally have been very re-
markable, consisting of an enormous breadth of ferruginous earthy
mineral, much of it of a bright vermilion colour, very soft and easily
removed, and containing, at various depths, down to sixteen or
seventeen fathoms, so large a per-centage of black oxide of copper
in a powdery state, that this mimeral alone, for a long time, was
obtained by simple digging, and sold at a low price to the original
proprietors of the Cobre mine. With the black oxide, there was,
however, a considerable quantity of red oxide, and of blue and
green carbonates, crystals of great beauty having been frequently
obtained ; whilst, in any hollow space that might exist, or be left
after superficial workings, large stalactitic masses of sulphate of
copper accumulated. As a specimen lode, however, the Cobre has
long ceased to exist, though singularly large and perfect crystals of
iron pyrites are still not unfrequently met with, and sulphates might
be found in abundance in neglected workings.

The whole of the ground to the depth above stated (sixteen
fathoms) appears to have been largely impregnated with copper ; but
down to that level, sulphurets of the ordinary kind were either not
found or were partly decomposed. This at least: appears to be the
recollection of those who saw the mine in its early stages, and it is
well known that the yield of the ore was then very high, and the
supply chiefly oxide.

Below sixteen fathoms, however, the gossan appears to have ter-
minated, passing down at once into valuable and solid sulphurets,
occupying a large breadth of some part or other of the wide space
of orey ground which was still traceable, and which ranged between
what were called the north and south lodes. A section across this
part of the lode shows it to consist of three courses of ore, the
northernmost of large size, though variable in width, underlying to
the south, and especially rich at moderate depth; the middle less
regular and less valuable, and diminishing as it goes down, though
generally traceable ; and the southernmost, smaller and less regular
than-the northern, but still a steady course of ore, rather improving
in depth, and nearly vertical. Between these, not only is the ground
generally mineralized, but pockets and bunches of rich ore have been
so often met with, that every part of the space is worth exploring,
while many bunches of ore have been found outside the walls both
of the north and south courses of ore.

Heaves and Cross Courses.—The north course of ore has been
affected by several small heaves, some of which have not reached the
south course. The north course also, about the middle of the rich
ground, has apparently possessed the largest and richest branch of
ore yet found. All the heaves and cross courses dip west, ranging a
little east of north and west of south ; and the great north course of
ore dipping south, while the south course is vertical, there would
thus appear to be a tendency in the orey parts of the lode to unite

150 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 23,

at a certain depth. Everything seems to show that the various
deposits occupy the gaping mouths of a fissure which is of moderate
dimensions below, although expanding, and containing much rich ore
near the surface.

Breadth of orey ground.—The magnitude ‘of the deposits of ore
is often so large, that a breadth of ground amounting to from twenty
to forty feet required to be removed, leaving only very small and
insufficient arches.

Timbering on the grandest scale has therefore been resorted to, to
prevent accidents; and it is not unusual to see pairs of spars, con-
sisting of trees hewn square and having a section eighteen inches
square lashed together, placed to meet at an obtuse angle midway,
and strengthened with diagonal bracings, forming a solid construc-
tion, like the vaulted roof of a cathedral. Those only who are
conversant with the difficulty of introducing such spars into the
small shafts of a mine, and handling them underground so as effec-
tually to serve for the purpose intended, and preserve the mine for
years without danger or accident, can do justice to the science and
engineering that have been brought to bear on this part of the
mining operations of the Cobre Company, and it is only a just tri-
bute to the skill and activity of the successive managers (all, I
believe, of Cornish experience) to allude to so important a part of
the ceconomy of these remarkable mines.

Mundic.—Within the various parts of the lode are found at inter-
vals, and at all depths, large quantities of mundic, or iron pyrites,
often highly crystallme. Much of this occurs between the north
and south deposits of ore; and, in addition to the masses, and de-
tached crystals, the copper pyrites are not unfrequently so completely
coated with this worthless mineral as to render it impossible to esti-
mate their value by the eye. This is the case more in the upper
than in the lower levels.

Veinstone.—The Cobre mine is open at present to the 160-fathom
level below adit ; and, although a fair proportion of reserves exists In
the lower levels, it will be readily understood by those accustomed
to mining in rich veins, that only a few arches of ground have been
allowed to remain in the upper part of the mine. The communica-

tions between the different courses of ore at the different depths, and

the cross cuts out of the lode to north and south, at various points,
as well as the appearance of the lode, where now being removed, are
all extremely interesting and instructive. The enclosing country, and
the ground between the courses of ore, appear to become more com-
pact and regular in descending, and are occasionally very hard. At
the 140-fathom level the lode becomes gypseous, considerable quan-
tities of white alabaster appearing without sensibly affecting the value
of the ore; but the veinstone a little below becomes very hard, and
in some parts of the lode the ore ceases altogether in the vicinity of
the gypsum.

At the lower levels, the heaves and cross courses appear to have
rather more influence than near the surface, at least with regard to
the quantity of ore.

1856. | ANSTED—COBRE LODE. 151

Temperature.—The temperature of the lode in the upper levels is
about 90° Fahr., both in the levels themselves, and wherever I could
place a thermometer in the rock. At ninety fathoms I noted in one
place a temperature of 96°, and in a small neglected working on the
south course of ore an exceptional temperature of 101°. At this
point, which was not without ventilation, being close to a shaft, the
heat was very sensible, but the air did not appear to be tainted with
any disagreeabie odour. I noticed, however, much iron pyrites
thereabouts. Lower down, the air becomes much cooler, and in the
130-fathom level I observed the thermometer to stand at 86° in a
small sump near a slide, and at 88° in a hole opened in the rock, not
in the orey part of the vein. In many parts of the mine, both men
and boys work entirely naked, and although, while underground, I
did not notice much difference in the temperature, as compared with
deep mines in other countries, the subsequent exhaustion was far
greater than is usual in temperate climates. The mines and district
are by no means unhealthy, although there has often been consider-
able mortality amongst the white (Cornish) hands, owing to the want
of prudence and caution whilst above ground. I was pleased to find
a cage provided in the Cobre mine to lift the miners after their
work was concluded.

Recapitulation.—I may now sum up as follows the principal re-
sults of my observations on the western or productive part of the
Cobre lode.

1. It includes three courses of ore regarded as distinct, nearly
parallel to each other in strike, but gradually approaching as they
go down, two of them unusually large and rich, and the third (the
middle) of smallest importance, the northernmost (on the foot-wall)
being chiefly affected by certain small heaves; but all the orey
ground terminated by a cross course to the west. The intervals
between the three courses of ore are occupied by a conglomerate or
breccia, consisting of fragments of decomposing porphyries and
greenstone, abounding with lime, passing into a compact whitish
green porphyry. Associated with the courses of ore, the veinstone,
and the country, are large quantities of iron pyrites, and at a certain
considerable depth the veinstone contains gypsum.

2. Regarding the three courses of ore together as parts of one
great lode, nearly 200 yards wide at its crop, this lode may be de-
scribed as dipping moderately to the south, as shown in fig. 4, p. 148,
the orey portions being chiefly near the hanging-wall and the foot-
wall, but extending occasionally and irregularly not only into bunches
and strings in the intervening veinstone, but also into the country,
both north and south of the lode. The whole of the adjacent rock
is also highly mineralized.

3. Not only the lode, but each of the principal courses of ore
appears to be well indicated at the surface by a distinct gossan, con-
sisting of spongy quartz and iron oxide of the usual kind, and
highly coloured clays and marls, immediately beneath or amongst
which have been oxides, carbonates, and sulphurets of copper. At
greater depth, the yellow ore (a sulphuret of copper and iron) en-

152 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 23,

tirely replaces the other metalliferous minerals, the proportion of
iron gradually preponderating on going down.

4. The horses, or areas of unproductive ground occurring within
the lode and between courses of ore, consist for the most part of

porphyry, identical in appearance with the rock outside the lode,

but generally mineralized with iron and copper pyrites.

5. The metalliferous deposit, obeying the form of the ground,
terminates abruptly to the west, where the hill is precipitous, and
dies away towards the east. The heaves and cross courses do not
carry ore.

The Santiago Lode.—Following the main lode from its chief deve-
lopment towards the east, its outcrop may be traced at intervals
until we reach a point where a contra lode or main branch forms a
junction with it. This junction is well seen in a natural section
formed by the river-banks, and beyond it, towards the east, the out-
crop continues remarkably strong, and possesses many points of in-
terest. The contra lode or branch makes an angle of 30° with the
main lode, and goes away to the south-west. It is seen at various
points, and after about half a mile bifurcates, and is crossed by
several small strings and subsidiary lodes, traceable in various direc-
tions, and not yet proved to be connected with each other in any
important sense. Some of these strings and lodes are of considerable
size (measuring underground from three to seven feet) and have
shown, either at the surface or at some depth, very good coppery
indications, consisting of oxides, carbonates, and rich sulphurets of
copper. The gossans of such lodes have generally led down to
bunches of unusually rich sulphuret, but no steady and continuous
deposit has yet been proved to exist, resembling that found in the
Cobre concessions. ‘The country also is here less metamorphosed,
calcareous green conglomerates replacing the porphyries, while
elvans of porphyry occur amongst the lodes. Generally speaking,
in this part of the mineral field the appearance of the lodes when
cut underground has not been so satisfactory as might have been
expected from the character of the gossans, and whilst the ore
obtained has been of the finest quality, the quantity has been too
small, and the supply too irregular, to secure a profit on the mining
operations carried on.

Besides the group of lodes cropping out to the south of the Cobre,
and connected with the Santiago lode, trials have been made on
small gossany outcrops in the valley of the Cobre, to the north of the
lode, and also in the ground to the west. Bunches of ore exist under
these crops, but no valuable deposit of copper has been found.

Metamorphism of the enclosing rock.—Having thus described the
circumstances of the Cobre lode, and its principal contra lode, it
remains for me to allude to one very important fact regarding the
enclosing and associated rocks. I have already described these as
consisting of grits and conglomerates, passing into metamorphic rocks,
which include porphyritic conglomerates, greenstone, and even basalt.
The circumstances under which these changes take place are too

remarkable to be passed over,

—=—— rrr OC

1856. | ANSTED—COBRE LODE. 153

In passing along the railway from the harbour towards the mines,
the first thing seen is a bedded greenstone-porphyry, and as the
road tends to the north of west (intersecting the strike of the beds,
which dip northwards), we come successively on newer beds. These
include, first, shales and alternating beds of basalt, partly columnar
and partly in concentric blocks of various dimensions. To these
succeed bands of grit, and rotten altered rock, after which come in
nodular sandstones and greenish grits with calcareous lumps, di-
stinctly passing into greenstone and porphyritic conglomerate. This
is the general sequence; but there is a special example near the
bifurcation of the Cobre lode, which is also deserving of notice. __

At this point the rock on the south side of the main lode and
contra lode, as seen in actual contact with the vein, of which it forms
the hanging-wall, is a fine-grained porphyry, compact and hard, and
of crystalline appearance. At the distance of a few yards, this por-
phyry is succeeded by, or passes into, a conglomerate, made up of
angular fragments, some of them of large size and of extremely
irregular composition. At no great distance, but still to the south,
and in a cutting close to the right bank of the Cobre river, a grit-
stone is seen, covered by conglomerate ; and a little further off, in
the direction of the branch, the porphyries altogether replace the
grits and conglomerates.

Lastly, In a quarry close to the hanging wall of the great lode,
and near its richest part, the green porphyritic rock is quarried for
road material; while close by, to the south, and near the branch,
the conglomerate takes its place. It is almost impossible to repre-
sent in a diagram the near approximation and complete intermixture
of the crystalline rock with the bedded conglomerate, while the
chemical characteristics of the two are sufficiently similar to justify
the conclusion that one is only a modification of the other.

There are few or no marks of direct igneous action, in the ordinary
sense of the term, with the exception of the bedded basalts, and .
other rocks of this kind.

Conclusion.—The Cobre lode is thus remarkable for its great mag-
nitude and complication, its extraordinary richness, the high degree
of mineralization of the surrounding “country,” the nature of its en-
closing rock, and the combination of metamorphic and mechanically
formed rocks, in close contact, and frequent alternation. It possesses
the ordinary characteristics of veins only in some respects, and is
in others very anomalous. It is situated in a district not much re-
sembling in any point those in which copper is usually found, and
the general geology of the surrounding country would hardly indi-
cate so rich and remarkable a deposit as that which has been proved
to exist. The study both of the phenomena of the lode and of the
surrounding rocks, would well repay a longer time than I was able
to afford; and I shall be happy if my remarks, by attracting atten-
tion, may serve to the further elucidation of the exceptional appear-
ances I have referred to.

154

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LIBRARY OF THE GEOLOGICAL SOCIETY,

From November \st, 1855, to December 31st, 1855.

I. TRANSACTIONS AND JOURNALS.
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AMERICAN Academy of Arts and Sciences, vol. ii. pages 105-184.

American Journal of Science and Arts. 2nd Ser. No. 60. Nov. 1855.
With an Index to Vols. xi. to xx.
J. Leconte—On Moseley’s paper on the descent of glaciers,
335.
B. Silliman, Jun., and J. D. Whitney.—Copper-mine at Bristol,
Connecticut, 361.
W. J. Hamilton.—Biographical Notices of E. Forbes, Franklin,
Jameson, Aikin, Stanger, and Fischer, 375.
J. Wyman.—Fossil bones from the Red Sandstone of the Con-
necticut River Valley, 394.
W. J. Taylor.—Tennantite and Buratite from Lancaster, Pa.,
Zinc Mines, 412.
E. Hitchcock.—Shark-remains from the coal-formation of Illinois,

and. bones and tracks from the Connecticut River sandstone,
416.

American Philosophical Society, Proceedings, vol. vi. Nos. 51, 52,
1854.

Art-Union of London, Report of Council, for 1855.
——————, Almanack for 1856.
—_— ——., Prospectus for 1856.

Athenzeum Journal, for November and December, 1855. From C.
W. Dilke, Esq., F.G.S.

DONATIONS. 155

Bengal Asiatic Society, Journal. New Series, No. 74. 1855, No. 4.
H. Piddington.—Analysis of coal from Cherra Punji, 283.
S. Hislop.—The age of the coal-strata in Western Bengal and
Central India, 347.

Boston Society of Natural History, Proceedings, vol. iv., pages 385—
415 (1854).
E. Daniels.—Geology and Mineralogy of Wisconsin, 387.
S. Kneeland.—Reef at Pernambuco, Brazil, 390.
Dr. Gorrie.—Changes of level of the Coast of West Florida,
391.
C. T. Jackson.—Geology of North Carolina, Georgia, and Ten-
nessee, 397.
— Copper Mines in Polk County, Tennessee, 399.

———., Proceedings, vol. v. pp. 1-176 (1854, 55).
W. B. Rogers.—Fossils and age of the coal-districts of North
Carolina, Virginia, &c., 14.
H. D. Rogers.—Epoch of the Elephas primigenius, 22.
Dr. Pickermg.—Boulders on hills near Salem, 24.
T. Bouvé.—Slabs with Ornithichnites, 29.
W. B. Rogers.—Natural coke in the oolitie coal-region near Rich-
mond, Virginia, 53.
C. T. Jackson.—New mine of gold, silver, lead, and copper,
Bridgewater, Vermont, 62.
Sir J. Richardson.—The Mastodon and the fossil Elephant, 82,
107.
J. Wyman.—Batrachian footprints, 84.
J. C. Warren.—Zeuglodon, 91.
—— Insect tracks? on Connecticut sandstone, 105.
see Ursus spelzeus, 108.
C. T. Jackson.—Analysis of Allophane, 120.
Dr. Shaw and A. A. Hayes.—Coal-mines at Staitsville, Ohio,
124, 154.
I. A. Lapham.—Teeth of Mastodon giganteus, 133.
A. Perrey, and others.—The frequency of earthquakes in relation
to the ote age, and the changes of the Earth’s surface,
&e. 136.
J. C. Warren.—Teeth of Mastodon giganteus, 146.
A. A. Hayes.—Saline incrustations of the “ Mauvaises Terres ”’
of Kansas, 150.
Analysis of a fossilized egg from the Guano Islands, :
165. |

Canadian Institute, the Canadian Journal, September 1855.
Fr. Kuhlman.—Artificial stone, 333.

Earthquake in France, 336.

—— Carbonate of iron veins in Somersetshire, 341.

, October 1855.

Hogan, Harris, and Lillie.—Canada and its resources, 350.
A. D. Bache.—Earthquake-waves, 355.

Guyot and Agassiz.—Frozen wells and ice-caves, 355.
James Hall and Agassiz.—Graptolites, 356.

James Hall.—Geology of Nebraska, 357.

W. Blake.—Sandworn granite, 357.

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156 DONATIONS.

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Civil Engineer’s and Architect’s Journal, November 1855.
Water-supply, 391.
Artificial stone, 393.
Well-waters of Liverpool and London, 407.

——__——, No. 261, December 1855.
H. C. Sorby. —Structure of limestones, 410.
Paterson.—Cultivation of sand-hills, 411.
Serpentine of the Lizard, 424.
Artificial stone, 424, 426.

Ethnological Society of London, Regulations, 1855.
, List of Members, 1855.

France, Société géologique de, Bulletin, 2 Sér. vol. xu. feuil. 33-43.
1855.
EK. Gueymard.—Note sur des gites de nickel dans le département
de l’Isére, 515.
J. Omboni.—Série des terrains sédimentaires de la Lombardie
(PL XID) 5 517.
Elie de Beaumont.— Extrait de son mémoire intitulé: Faits pour
servir 4 Vhistoire des montagnes de Oisans, et de celui de
M. de Charpentier sur les environs de Bex, 534.
Laugel.—Résumé des études de M. Studer sur les Alpes de
l’Oisans, 570.
Albert Gaudry. —Résumé des travaux qui ont été entrepris sur
les terrains anthraciféres des Alpes de la France et de la
Savoie (Pl. XIV.), 580.
A. Sismonda.—Note sur des fossiles trouvés par lui au col des
Encombres (Savoie), 631.
Albert Gaudry.—Résumé des analyses faites par lui des mémoires
sur les terrains anthraciféres des Alpes (Bulletin, 2de série,
t. xu. p. 580 et suiv.), 636.
Table alphabétique des localités des Alpes savoyardes,
suisses et francaises qui ont été plus spécialement soumises
a observation des géologues, 642.
Elie de Beaumont.—Remarques au sujet de la carte Pl. XIV.
(contours de la region anthracifére des See occidentales),

670.
‘Franklin Institute, Journal. 3rd Series. Vol. xxx. No. 4. October

1855.
Fr. Kuhlman.—Artificial stone, 221.

3rd Series. Vol. xxx. No. 5. November

1855.

Geographical and Commercial Gazette. (Edited by an Association
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January, 1855.

E. Emmons.—The mountain-system of the State of New York, 4.
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Snow and snow-mountains, 18.
Declivity of rivers, 20.
Californian gold produce, 20.

Glasgow, Philosophical Society, Proceedings. Vol.i. For 1841-

44,

1844.
T. Thomson.—Some new minerals, 61.
~~ New Zealand minerals, 105.

W. Gourlie.—Fossil plants in the Glasgow Geological Museum,
105 (plate).

W. Murray.—Section of the Lanarkshire Coal-field, 113.

G. Gardner.—Extensive chalk-depesit in Northern Brazil, 146.

T. Thomson.—Coal-gas, 165.

R. D. Thomson.—Antarctic minerals, 207.

Boyd.—Analysis of sulphur from Sicily, 208.

———. Vol.u. For 1844-48. 1848.
James Smith.—Island of Lewis, 1.
R. D. Thomson.—Analyses of some minerals, 97.
L. D. B. Gordon.—Temperature of the earth, 140.
J. Brown.—Analysis of a slag, 163.
R. A. Couper.—Chemical composition of pottery, 171.
J. Brown.—Analysis of molybdate of lead, 180.
T. Thomson.—Geology and climate of Nice, 192.
J. Bryce.—Geology of the island of Bute, 198.
E. T. Wood and T. Coutts.—Analysis of Titwood mineral-water,
261.

——. Vol. ii. No. 1. 1848-49.

Fi Bryce.—Structure of Staffa and the Giant’s Causeway, 19.

Altered dolomites of the island of Bute, 20.

W. Ferguson.—The geology of part of Buchan, Aberdeenshire,
and the occurrence there of chalk-flints and greensand, 33.

————. Vol.ii. No. 2. 1849-50.
‘ Bryce.—The parallel roads of Lochaber, 99.
Geology of Roseneath and neighbourhood, 113.

Vol. i. No. 3. 1850-51.
T. Thomson. —Biographical notice of Dr. Wollaston, 135.
W. Ferguson.—Marme deposit with shells in Glasgow, 147.

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Ji ames Napier.—Mineral veins and water-worn stones, 231.
R. M. Murray.—Water of the Dead Sea, 242.

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W. Crum.—Biographical notice of Dr. T. Thomson, 250.

T. Anderson.—The Natro-Boro-Calcite, or Tiza, of Iquique,
293.

J. Napier.—Sandstones used for building, 313.

Journal de Imprimerie et de la Librairie en Belgique. 2° Année.
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Linnean Society of London, List of Fellows. 1855.
_ VOL. XIT.—PART. I. M

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Linnean Society of London. Annual Address, by Prof. T. Bell.
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Proceedings. Nos. 58*-66. June 1854 to June 1855.
Goppert.—Remarks on fossil palms, 352.
Obituary notices of H. T. De la Beche, E. Forbes, G. B. Green-
ough, G. B. Sowerby, J. E. Winterbottom, and others, 406.

at, Transactions.. Vol: xxin Part4i 855,

Literary Gazette, for November and December, 1855. From L.
Reeve, Esq., F.G.S.
Notices of Meetings.

London, Edinburgh, and Dublin Philosophical Magazine, 4th Series.
No. 68, December 1855. From R. Taylor, Esq., F.G.S.
J. A. Galbraith.—Felspars of the granites of the Dublin and
Wicklow mountains, 420.
R. P. Greg.—The lunar origin of aerolites, 429.
H. J. Brooke.—New ore of silver, 436.

Manchester Literary and Philosophical Society, Memoirs. 2nd Series.
Voloi. -“Vs05:

; Volos aSis:
W. Martin.—On Rotten-stone, 313.

J. Gough.—On an ebbing and flowing well at Giggleswick, York-
shire, 354.

—-——. ——. Voli. 1819.
J. Otley.— Account of the floating island in Derwent Lake, Kes-
wick, 64.
. B. Logmire.—On the flexibility of all mineral substances ;
and the cause of creeps and seats in old coal-mines, 161.

. Otley.—Account of the blacklead-mine in Borrowdale, Cum-
berland, 168.

2: Volfiv. «1824.

. ——. Vol.v. 1831.

. Otley.—On the floating island of Derwent Lake, 19.

. Dalton.—Observations, chiefly chemical, on the rock-strata in
Manchester and its vicinity, 148.

. Otley.—On a floating island at Newbury Port, U.S., 226.

ee | Vol ino
Vol. viii. 1848.

W. C. Williamson.—On some microscopical objects found in the
mud of the Levant, and other deposits (plates), 1.

E. W. Binney.—On the origin of coal, 148.

On the drift-deposits of Manchester and its neigh-
bourhood (plate), 195.

R, A. Smith.—On water from peat and soil, 377.

T. Ransome.—Analysis of a saline spring in a lead-mine near
Keswick, 399.

E. W. Sas laa the geology of Low Furness, Lancashire,
423.

——

Cay

Cy

DONATIONS. 159

Manchester Literary and Philosophical Society. Memoirs. 2nd
Series. Vol. xii. 1855.

KE. W. Bimney.—On the origin of ironstones, 31.

J. Dickenson.—Statisties of the Collieries of Lancashire, Cheshire,
and N. Wales, 71.

E. Peey- .—On the Permian beds of the N. W. of England,
Ze

J. Harland.—Classified Index to the Memoirs (old and new
series), 284.

Mittheilungen aus Justus Perthes’ geographischer Anstalt tiber neue
Erfosschungen auf dem Gesammtgebiete der Geographie von Dr.
A. Petermann, 1855, vi.
J. Marcou.— Ueber die geologie der Veremigten Staaten und der
Englischen provinzen von Nord-Amerika, 149 (map).
Physikalisch-geographische Skizze vom Herzogthum Coburg,
160 (map).
Geographical notices, 163 ; geographical books, 171.

New Orleans. Academy of Sciences. Constitution and Bye-Laws.
1854.

. Proceedings. Vol. i. No. 1.

Forshey. —Artificial stone, 10.

Riddell.—Native iron, 10.

Mineral-waters, 32.

Apparatus for ascertainmg the temperature in ar-
tesian wells, 54.

Walker.—Soils of Texas, 66.

New York University, of the State of. Eighth Annual Report of the
Regents of, on the condition of the State Cabimet of Natural
History, &e. 1855.

Philadelphia. Academy of Natural Sciences, Journal. New Series.
Vol. im. Part 1... 1855.
J. C. Norwood and H. Pratten.—Notice of the Producti and
Chonetes found in the Western States and territories, 5, 23
(2 plates).

—_———_—. ————-.. Proceedings. Vol.i. 1843. (Nos. 1-25,
28-33, and Index.)

Bailey.—Fossil foraminifera from the cretaceous marls on the
Upper Missouri, and on silicitied wood found near Frederick-
burg, Va., 75

A. D. Chaloner.— Rhombic formations in anthracite, 4.

—— Galena from Mexico, 14.
— Supposed trilobite from Pottsville, Pa., 193.
Fossil bones from Missouri, 321.
A. ome .—Geology of vicinity of New Albany, Indiana, 18,

J. A. Clay.—Some magnesian minerals from Europe, 39, 193.
T. A. Conrad.—New species of tertiary shells from Maryland,
28.
— Silurian and devonian systems of the U. S., &c.,
142, 143.
M 2

160 DONATIONS.

Philadelphia. Academy of Natural Sciences, Journal. Proceedings.
Vol. i. (continued).

T. A. Conrad.—New species of miocene and eocene fossils of
U.S., 305.

New genus of trilobites ; new species of silurian and
tertiary fossils; Trenton limestone; and lead-bearing lime-
stone of Wisconsin, 323.

J. H. Couper.—Strata, in which fossil bones and shells were
found at the Brunswick Canal, 216.

G. R. Gliddon.—Boulder-formations in Egypt, 172.

W. R. Johnson.—Crystalline form in anthracite and bitumimous
coal, 7, 73.

Mechanical structure of coal. 9.

—_— Analysis of coal from Chih, 21.

Coal of South Wales, and some Pennsylvanian anthra-

cites, 40.

Anthracite from Rhode Island, 118.

=== Spontaneous combustion of coal, 140.

—- . Analysis of some coals from Europe and the U. S.,
156.

a Analysis of natural coke from Virginia, 223.

S. G. Morton.—New species of cretaceous shells, 106, 132.

D. D. Owen.—Fossil trees from Indiana, 270.

J. B. Quinby.—Eastern ridges of the Andes, 82.

oa Spontaneous combustion of coal, 121.
E. Ravenel.—Two new fossil Scutellz from S. Carolina,
H. D. Rogers.—Rhombs in anthracite, 7.

— Age of Richmond coal-formation, 142.

— Earthquakes, 181.

—. Posidonomya minuta, 250.

—_—— Geology of St. Petersburgh, 256.

——. ——. Vol. i. 1846. (Nos. 2, 4, 6,
8, 9, 10, and Index.)
T. A. Conrad.—New fossil shells, 173.
R. W. Gibbes.—Fossil teeth from greensand of S. Carolina, 254.
Gilpin.—Cetacean bone from Delaware, 166.
E. Harris.—Geology of the Upper Missouri, 235.
W. R. Johnson.—Properties of certain coals, 8.
= Different varieties of plumbago, 74.
—— Rocks from the White Mountains, 89.
—— Spontaneous combustion of coal, 163.
—— Analysis of the alluvium of the Nile, 318.
A. T. King:—Fossil footmarks, 175, 299.
S. G. Morton.—Fossil Crocodile from New Jersey, 82.
—— Mosasaurus from New Jersey, 132.
E. Ravenel.—Eocene fossils from S. Carolina, 96.
Reid.—Analysis of sulphur springs, in the State of New York,
120

He D- Rogers.— Oolitic rock from Florida, 210.

——. ————. Proceedings. Vol. ili. 1848. (Nos. 1-3,
8, 10;

T. A. Conrad.—New species of fossil shells and corals (plate),
19)

DONATIONS. 161

Philadelphia. Academy of Natural Sciences, Journal. Proceedings.

Ge 1h)

os

asia

Vol. i. (continued).
T. A. Conrad.—Kocene formation, 105.
—— Eocene fossils from Vicksburg, Miss., 280.
J. W. Dawson.—Gypsum of Nova Scotia, 272.
M. M. Dickeson.—Fossil bones from Natchez, 106.
a Alligator-tracks and Ornithichnites, 109.
R. W. Gibbes.— Fossil squalide, 41, 266.
E. Hallowell.—Fossil bones, 130.
E. Harris.— Difference of level between the waters of the Gulf of
Mexico and of the Atlantic, 34.
W. R. Johnson.—On drift, 109.
— Fossil bones from Berks Co. Penns., 318.
J. Leidv.—Fossil rumimant, Poébrother1um Wilsoni, 322.
-—— Fossil horse of America (plate), 262, 328.
Locke.—Fossil Asterias from Cincinnati, (figure), 32.
R. Owen.—Fossil bones from the excavation of the Brunswick
Canal, Georgia, 93.
M. Tuomey.—Cranium of Zeuglodon, 151.

Vol. ivy. 1850. (Nos. 2, 3,

ere oe
e

L. Agassiz.—Fossil crocodile of New Jersey, 169.
—_—— Dorudon serratus, 4.
S. Ashmead.—Calcareous spar from Rossie leadmines, 6.
R. W. Gibbes.—Dorudon serratus, 57.
S. S. Haldemar.— Fibrous lava from the Hawaiian islands, 5.
J. Leidy.—Fossil pachyderm, Merycodoidon Culbertsonui, 47.
—— Fossil Tapirus americanus, 180.
H. D. Rogers.—- Formation of mountain-ridges, 145.

—_—___—_——_.. Vol. v. 1852. (No. 12.)
ik Lea.—Obituary notice of R. C. Taylor, 290.
—— Wavye-theory of earthquakes, 261.
J. Leidy.—Fossil bones from Big Bone Lick, Kentucky, 140.
ed Fossil Ruminants from Nebmsna. 237.
—— Oreodon robustum, 276.
——- Palzotherium Proutii, 170.
—— Fossil tortoise from Nebraska, 172, 173.
—— Rhinoceros occidentalis, 119, 276.
= Fossils from Nebraska, 278.
a Fossil Balzna, 308.
—— Fossil reptilian and mammalian remains, 325.
— Fossils from the greensand of New Jersey.
oe Fossil rhinoceros from Nebraska, 331. —
—_—— Crocodilus antiquus from the miocene formation of
Virginia, 307.
T. F. Moss.—Carpolite from Arkansas, 59.
D. D. Owen.— Fossils from the “ Mauvaises Terres’ of Missouri,
66, 328.

———. Vol. vi. 1854. (Nos. 7-1]
and Index. ).
T. A. Conrad. —Tertiary strata of St. Domingo and of Vicksburg,
Miss., 198.
ae Fossil shells, 199, 320.

162 DONATIONS.

Philadelphia. Academy of Natural Sciences, Journal. Proceedings.
Vol. vi. (continued).
F, A. Genth.— Minerals accompanying gold in California, 113.
—— Rhodophyllite, 121.
— Iridosmine, platinum, &c. from California, 209.
—— New variety of grey copper, 296.
oe Owenite, 297.
F. V. Greene.—Chemical investigation of fossil mammalian re-
mains, 292.
J. Hayes.—Tooth of fossil Tapir, 53.
if a of human feet on sandstone from Illinois,
106.

a Shells from the drift near Philadelphia, 106.
Eschara Claibornensis (figures), 109.
J. Leidy.—Fossil vertebra from Onachita, La., 52.
—— Fossil tortoises from Nebraska, 59.
—— Extinct species of Ox, 71, 117.
—-— Fossil tooth of Tapir, 106.
—— Fossil Edentata of N. America, 117.
— Fossil Rhinoceros of Nebraska, 2.
— Fossil Turtle from Nebraska, 34.
—_—— Fossil Delphinus from Virginia, 35.
—— Fossil crocodilian reptile from New Jersey, 35.
—_—— Various fossil teeth, 241.
—_— Fossil remains from Natchez, Miss., 303.
—— Extinct Cetacea from the greensand of New Jersey,
and from S. Carolina and Virginia, 377.
——— Fossil Mammalia and Chelonia from the ‘“‘ Mauyaises
Terres’ of Nebraska, 392.
--— Fossil Saurian from Prince Edward’s Island, 404.
D. D. Owen.—Prints of human feet in limestone, 106.
—— New mineral from California, 108.
—— Fusulina limestone and Teutenmergel, 118.
oa Geological map of Wisconsin, &c., 189.
—— A magnesian earth, 379.
C. M. tinmtigsigaric ye of lead from Phoenixville, Pa., 55,
119.
—— Tron crystallized from slag, 434.

—. Vol. vii. Nos. 2-7. (March

oe ee eee eee

1854—Jan. 1855.)

T. A. Conrad.—Nomenclature of tertiary shells, 29.
—- New Conularia, 31.
J. W. Dawson.—Fossil Coniferous wood from Prince Edward’s
Island, 62.
A. T. King.—Fossil trees in coal-rocks, Pennsylvania, 64.
Fossil fruit in coal-rocks, Pennsylvania, 66.
Leconte.—New fossil Pachyderm from Virginia, 69.
H. Miller.—Mosaic history of geology, 69.
J. Leidy.—Brimosaurus grandis and Cimoliasaurus magnus
(plate), 72.
a Identity of Harlanus Americanus and Bos latifrons,
9

89.
— New fossil mammalia, 90.
— Dinictis felina from Nebraska, 127.

DONATIONS. ‘ 163

Philadelphia. Academy of Natural Sciences, Journal. Proceedings.
Vol. vu. (continued).
J. Leidy.—Synopsis of the extinct mammalia from the eocene of
Nebraska, 156.
J. Evans & B. F. Shumard.—New tertiary shells and Cypris from
Nebraska, 164.
M. Tuomey.—New cretaceous fossils from the Southern States,
167.
J. Leidy.—Camelops Kansanus, 172.
—— Fossil bones from the Ohio River, Indiana.
Bootherium and Ovibos, and recent and fossil species
of American Ox, 209.
F. A. Onth.—Identity of Herrerite and Smithsonite, 232.
C. M. Wetherill.—Gold near Reading, U.S., 233.
T. A. Conrad.—Eocene deposits of Jackson, Mississippi, and
new species of fossil shells and corals, 257.
— New species of cretaceous and tertiary fossils, 265.
aa New cretaceous fossils from Texas, 268.

Photographic Society, Journal. Nos. 36,37. 1855.

Royal College of Surgeons of England, Descriptive and Illustrated
Catalogue of the Histological Series contained in the Museum.
Vol. ii. Structure of the Skeleton of Vertebrate Animals. 1855.

Royal Irish Academy, Proceedings. Vol. vi. Part 2, for 1854-55.

J. H. Galbraith.—On the potash and soda in the Dublin and
Wicklow granites, 134.

Downing.—On the draining of the Haarlem Lake, 173.

S. Hanghton.—On the mica of the Dublin, Wicklow, and Carlow
granites, 176.

S. Haughton & R. Griffith.—On the granites of Leinster, 230.

R. T. Forster.—On the molecular formation of crystals, 240.

? fi Wol. xxune) Part vi, ° PBD5.
Raya Society, Proceedings. Vol. vii. No. 16.

Smithsonian Institution, Eighth Annual Report of the Board of
Regents. 1854.

Ninth Annual Report of the Board of Regents. 1855.

J. Froebel.—On the physical geography of the North American
continent, 272.

C.T. Jackson, J. Locke, Jno. Foster, J. D. Whitney, & D. D.Owen.

—On rocks and minerals from Michigan, &c., *338.

————. Report on the Constructions of Catalogue of Libraries,
and of a General Catalogue. 1853.

Smithsonian Contributions to Knowledge. Vol. vi.
1836. ~

Statistical Society of London, Journal. Vol. xviii. Part 4.
December 1855.
J. Strong.—Coal and iron trade of the West of Scotland, 330.
H. R. Lack.—Minimg resources of France, 345.

164 ; DONATIONS.

Il. GEOLOGICAL CONTENTS OF PERIODICALS
PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 2nd Ser. vol. xvi. No. 96.
December 1855.
T. Davidson.—On the Brachiopoda (with a plate), 429.
Notice of the Histological Catalogue of the Royal College of
Surgeons Museum, 454.
R. Owen. .—On the bones of the leg of Dinornis and Palapteryx,
460
Leonhard and Bronn’s Neues Jahrbuch fiir Min. — Geol. und
Petref. Jahrgang 1855, fiinftes Heft.
KE, Zschau.—Bemerkungen tiber das Vorkommen der phosphor-
sauren Yttererde in den Gang-artigen Graniten des Norits
auf Hitteroe in Norwegen, 513.
QO. Dieffenbach.— Ueber den Mineral-Reichthum der Vereinten-
Staaten von Nord-Amerika, 527.
——. — Vorkommen von Chrom-Erzen und ihre Verbreitung
in den Vereinten-Staaten, 533.
Fr. A. Romer.—Graptolithen am Harze (plate), 540.
Letters; Notices of Books, Mmeralogy, Geology, and Fossils.

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.

Names of Donors in Italics.

Archiac, A.d. Résumé d’un Essai sur la Géologie des Corbiéres.

Baker, J.G. The Flowermg Plants and Ferns of Great Britain: an
attempt to classify them according to their Geognostic Relations.

Barlow, P. W. On some peculiar features of the Water-bearing
Strata of the Lower Basin.

Belcher, Sir E. 'The last of the Arctic Voyages. 2 vols.

Bell, T. Woree Carcinologicee. I. A Monograph of the Leuco-
siadee.

Catullo, T. Memoria intorno ad una nuova Classificazione delle
Calcarie Rosse Ammonitiche delle Alpi Venete.

Davidson, T. A few remarks on the Brachiopoda.

De la Condamine, H. M. On the Geology of the neighbourhood of
Blackheath. From T. Rupert Jones, Esq., F.G.S.

Drian, A. Note sur une Roche Pyroxénique du Département du
Rhone.

Gregg, R. P. An Essay on Meteorites.

Harkness, R. On a Deposit containing Subfossil Diatomacez, in
Dumtriesshire.

DONATIONS. 165

Harkness, R. On the Geology of the Dingle Promontory.

Harkness, R., & J. Blyth. On the Cleavage of the Devonians of the
South-west of Ireland.

Hornes, M. Ueber die Gasteropoden und Acephalen der Hallstatter
Schichten.

Jewett, C.C. Report on the Construction of Catalogues of Libra-
ries. From the Smithsonian Institution.

Jones, T. Rupert. Notes on Paleozoic Bivalved Entomostraca; —
Nos. | & 2: Beyrichia.

Lea, I. Fossil Footmarks on the Red Sandstone of Pottsville. Fol.

Leidy, J. On Bathygnathus borealis.

Meyer, H.von. Zur Fauna der Vorwelt. Zweite Abth. 1855.

Observations et Résumés des Observations recueillies en 1852-54,
dans le Bassin de la Sadne, par les soins de la Commission
Hydromeétrique de Lyon.

Observations météorologiques faites 4 Lyon, 1851-53.

Peters, K.F. Schildkrotenreste aus den Oesterreichischen Tertiar-
Ablagerungen.

Report of the Commissioner of Patents for 1855. Part 1.

Siluria: histoire des roches les plus anciennes, par Sir R. I. Mur-
chison. From M. A. Favre.

Suess, EH. Ueber die Brachiopoden der Hallstatter Schichten.

Trask, J. B. Report of the Geology of the Coast Mountains and
part ef the Sierra Nevada.

Trimmer, W. K. An account of some organic remains found near
Brentford. From J. Trimmer, Esq., F.G.S.

Verneuil, E. de, de Beaumont et Dufrénoy. Rapport sur une Mé-
moire de M. Jules Marcou, relatif 4 la Classification des Chaines
de Montagnes d’une partie de l’ Amérique du Nord.

Verneuil, E. de, et H. Coliomb. Note a loccasion de deux coupes
Géologiques Générales faites a travers Espagne, du Nord au
Sud et de Est a POuest.

Verneuil, E. de, K. Collomb et de Loriére. Notes pour accompagner
le Tableau Orographique d’une partie de l Espagne.

Verneuil, E. de, E. Collomb et de Loriére. Note sur les Progrés de
la Géologie en Espagne, 1854.

Wailes, L.C. Report on the Agriculture and Geology of Mississippi.

Wetherill, C. M. Report on the Iron and Coal of Pennsylvania.
From the Smithsonian Institution.

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THE.

QUARTERLY JOURNAL

OF

THE GHOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

FEBRUARY 6, 1856.

The Rev. Thomas Wiltshire was elected a Fellow.
The following communications were read :—

1. Notice of some RatseD BEacuHEs in ARGYLLSHIRE.
By Commander E. J. Beprorp, R.N.

[In Letters to Admiral Sir F. Beaufort, communicated by Sir R. I. Murchison,
V.P.G.S.*]

Surveying Service, Lochgilphead,
August 21st, 1851.
Since my last report of progress I have made a more minute ex-
amination of the ‘raised beaches”’ which I therein alluded to. I
have directed my observations to two in the locality of Lunga Island,
a sketch + of each of which I enclose. ‘‘ No. 1” is at the head of
a deep bay in Lunga proper; “‘ No. 2”’ is situated about the centre
of the north isle of the group, or North Fullah. Guided by your

* This portion of the Communication was read before the Society on June 13,
1855; and an abstract of it was published in the Quart. Journ. Geol. Soc. vol. xi.
p. 549.

+ These sketches and others afterwards referred to are deposited in the Society’s
Library.

VOL. XII.—PART I. N

168 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 6,

suggestions, I carefully levelled each for ascertaining their present
altitude above high water mark, and for determining their horizontal
position. The former gave respectively 40 feet 11 inches and 40 feet
4 inches ; but, allowing for some little difference in the high water
mark, I have given the mean as the altitude of each. The latter
(No. 2) I found to be a plane, perfectly horizontal. The deposit is
composed entirely of water-worn stones, of various sizes, from + cwt.
to a pebble, and of the same character as the solid neighbouring
rocks, without fossils, shells, or wood ; which, however, is not sur-
prising, as few shells are to be found on the shore; and they, ex-
posed to a heavy sea, would become pulverized and difficult to trace ;
and wood is seldom met with. The shingle of No. 1 is covered by
about 6 inches of a mossy soil; that of No. 2 is nearly exposed, and
in places as clean as the daily-washed beach; and, whereas the first
is but a short distance from and parallel to the present shore, exposed
to the same direction of swell and exhibiting the same effects, that of
the latter alone has the general character of a beach, as the present
margin of the isle in the direction of the longest fetch is now low,
broken, and rocky.
Lochgilphead,
August 29th, 185].

Having been detained in Kerrera Sound, I was led by information
to search for a deposit with fossils, which I was fortunate in finding ;
and, on levelling it, found it to be within 1 inch of the same height
as the raised beaches before referred to. The base of the deposit
being 39 feet 10 inches, the band about 1 foot in thickness=40 feet
10 inches ;—40 feet 11 inches being the elevation given (or rather
found) of the beach on Lunga.

The deposit contains fossils having the same appearance as shells
now to be constantly seen thrown up by the sea and lodged in the
cavities of rocks.

[In a letter to the Secretary of the Geological Society. ]
Admiralty Survey, Oban,
October 31st, 1855.

I beg herewith to forward a tracmg of part of the West Coast of
Jura which exhibits the most remarkable raised beaches of the
district ; they can also be traced nearly to the northern extreme of
the island; and there is a conspicuous one to the south. Upon the
Isles of Colonsay and Oronsay they are equally distinctly marked ;
the bare shingle being exposed at the medium level of about 40 feet.
I was not on the survey of Islay, but should think they would be
traceable there also.

These beaches are remarkable under several considerations. First,
their uniform level, although separated many miles apart, as between
Loch Tarbert and Lunga eighteen miles, between Lunga and Kerrera
fifteen miles ;—secondly, their uniform horizontal position ;—thirdly,
the vast extent of exposed shingle, from the polished pebble the size
of a pigeon’s egg to the rough stone of near a hundredweight, covering
many acres of land ;—and fourthly, their undisturbed state, exhibit-

1856. | MOGGRIDGE—SWANSEA DOCKS. 169

ing every undulation, basin, and channel as when formed ages since
by the thundering ocean-wave. With regard to the period and
method of their formation, I must leave the subject to more ex-
perienced heads than mine,—egratified should the correct notice and
illustration of them afford interesting matter for discussion to the
members of the Geological Society.

2. On the Section exposed in the Excavation of the SWANSEA
Docks. By M. Mocerines, Esq.

[Communicated by Sir Roderick Murchison, V.P.G.S.]

ANCIENT legends which point out different courses for the Swansea
and Neath Rivers from those which they at present take, induced
me to watch the progress of the excavations made for the Swansea
Docks from their commencement. Of my success in tracing the old
bed of one if not both of those streams I need not here speak,—the
geological features are those to which I would draw attention.

The Swansea Docks consist of a ‘‘ half-tide-’? and a floating-basin.
They are situated on the brink of the sea, which lies to the S.E.,
while the N.E. boundary is the harbour through which flows the
river Tawe. ‘The entrance is from the harbour into the half-tide
basin; and thence, through a large lock, vessels will pass into the
main dock. ‘The greater part of the stuff which has been removed
consists of gravel and rolled stones, many of which have been
transported full twenty miles.

The sections exposed varied greatly m different parts of the cuttings,
but the best and most regular occurred at the N.E. end of the main
docks exhibiting (August, 1853) :—

1. Made ground, sand, and loose gravel of variable thickness
from 20 feet to 6 feet.

. Peat, with leaves, trees, &c., 2 feet.

. Blue marine clay, 8 feet 6 inches.

. Peat of rather greater density than No. 2, 10 inches.
. Blue marine clay, 4 feet 1 inch.

. Peat with trees, 3 feet 1 inch.

. Brown clay and gravel, not penetrated.

The bottom of the dock is 244 feet below high water and 44 feet
above low water at ordinary spring tides.

I have said “‘ marine clay,”’ because I found imbedded in it Scro-
bicularia piperata, a sea-shell still living on these coasts and burrow-
ing in a similar clay now forming in some of our estuaries. The
valves of this shell are dispersed in pairs throughout the whole of the
clay, but abound most in the upper portion of each stratum.

As to the peat, I have been met with the remark, that it might
have been brought together by submarine currents, and that there-
fore the alternation of sea and land was not proved. To this I
answer that in very many cases roots still attached to plants which
constitute a portion of the peat descend into and ramify among the
clay, proving that those plants lived and died where ei are,

N

STD Or & GO DO

170 PROCEEDINGS OF THE GEOLOGICAL society. ([Feb. 6,

Thus then we have three beds of peat (2, 4, and 6), separated by
two strata of marine clay (3 and 5).

In another place, four of peat and four of clay were exposed, but
I chose the spot above referred to because the formations were hori-
zontal, more regular, and easily measured. In the peat we find the
oak, beech, birch, alder, hazel, and crab-tree still easily identified.
The bark of the birch is little changed, that of the other trees has
lost much of its character.

I have not met with any of the Coniferee; but reeds and grasses
abound. In the peat I could find nothing besides the vegetables
composing it; the same plants occurring in the different beds, but
less distinct as they became more distant from the surface.

The gravel (No. 1) in the dock-section, has, I think, been brought
down from the very large accumulation of that material at Landore,
13 mile N., where water has cut through a deep deposit which
appears to me to be an ancient moraine.

The origin or parent source of the gravel must be sought in the
sandstones of the coal-measures, which have contributed the largest
portion; the millstone-grit 20 miles N., next in abundance; the
limestone 21 miles N., pieces of which are rare; and the Old Red
Sandstone, 22 miles N., nearly as frequent as the muillstone-grit.
The size generally ranges from small gravel up to large shingle; but
boulders have occurred, some large enough to require blasting: one
of these was limestone.

AppENDIx.—On the Sunken Portion of Swansea Bay.

According to the ancient legends before referred to, Swansea Bay
was once land, the sea-boundary running from the Mumble Point to
near Aberavon, a distance of 7 miles. The present high-water line
runs far into the land, there being on an average 3 miles between the
actual and the traditionary limit of the sea, more than half of which
is dry at the low-water of average spring tides. The western portion
is said to have been covered by a forest called Silverwood. It is
also stated that the Neath River joined the Swansea River near
Swansea, and that their waters flowed out to the sea close to the
Munnble Rocks.

How much of the legends may be true, we will not stop to inquire ;
but in the dock-cutting, I found the beds of two rivers and their
junction, while the stool and root of many a noble tree covered at
every high tide tell of the ancient forest.

The peat and clay extend along the shore 4 miles to the W. and
2 miles to the KE. of Swansea; further on towards the Neath River
the sand has accumulated to such an extent that I can only infer
their continuity from the water being thrown out with considerable
regularity, as if by the out: crop of those impervious beds, and at the
same level.

I know not how far these formations extend inland, but the upper-
most is traceable from the shore for distances varying from a —
yards to more than a mile (at Crumlyn Bog).

1856. | HAUGHTON—GRANITES OF IRELAND. 171

I ought perhaps to add that to the west of the Mumbles, we find
a raised beach, while the contents of the caves show that the contour
of the coast must have been very different in the days of the extinct
quadrupeds to that which we at present see.

3. Notice of the Recent Ervetion of Mauna Loa, m Hawatt.
By W. Miter, ee H.M. Consul-general for the Sandwich
Islands.

[Forwarded from the Foreign Office by order of Lord Clarendon. ]
(Abstract.)

Tue late volcanic eruption* in the Sandwich Islands broke out in
August last, near the summit of Mauna Loa, which is 14,000 feet
high and sixty miles from Hilo, Byron’s Bay, in Hawaii.

The stream of lava, having a breadth of from two to three miles,
continued to flow in a north-east direction until the end of October,
when the lava-current, after having traversed a great part of the
dense forest, appeared to have been checked in its progress at about
ten miles from the town of Hilo.

4, EXPERIMENTAL RESEARCHES on the GRANITES of IRELAND.
By the Rev. Samuen Haveuton, M.A., F.G.S., Professor of
Geoiogy in the University of Dublin.

PART I.—On tue GRANITES OF THE SOUTH-EAST OF Ee teas

Introduction.
I. Granites of the Main Chain.
Elementary Minerals.
Accidental Minerals.
Chemical Composition of the Granites.
Mineral Composition of the Granites.
Il. Isolated Granites of Wicklow and Wexford.
First or Western Group of Isolated Granites.
Second Group of Isolated Granites.
Third Group of Isolated Granites.
Fourth Group of Isolated Granites.
Type-Granites of the South-east of Ireland.

The granitic rocks of Leinster, or South-east of Ireland, occur in
the counties of Dublin, Carlow, Kilkenny, Wicklow, and Wexford,
and may be divided physically into two distinct groups (see Map,
fig. 1, p. 172) :—

ee The main chain of granite-hills, extending from Booterstown,
county Dublin, to Poulmonnty, in the south of the county of Carlow,
within five miles of New Ross. This granite-chain is unbroken
throughout its extent, and has a length of sixty-eight miles, and a
breadth varying from eight to fifteen miles.

2. Besides the main chain there are about twenty isolated granitic

* For detailed notices of this eruption of Mauna Loa, by Messrs. Coan and
Dana, see Silliman’s American Journal of Science and Arts, vol. xxi. January and
March, 1856.

[ Feb. 6,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

172

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1856. | HAUGHTON—GRANITES OF IRELAND. 173

districts in the counties of Wicklow and Wexford, forming small
islands, as it were, of granite, which have penetrated and broken
through the Silurian slate of those counties. The general axis of
each of these granitic outbursts is parallel to that of the main chain ;
these secondary granitic rocks are found at intervals for a distance of
forty-three miles, from Ballinaclash, county Wicklow, to Camaross
Hill, county Wexford.

I propose to give a short mineralogical sketch of these two groups
of granitic rocks, which, considered as groups, are distinguished from
each other by well-marked chemical differences, not hitherto observed.

I. GRANITES OF THE Main CHAIN.

Elementary Minerals composing the Granite of the Main Chain.

The granite of the main chain varies less than might be supposed
from its great extent, and specimens from the southern end of the
chain might easily be mistaken for northern specimens. This simi-
larity of appearance arises from the prevalence of the same consti-
tuent minerals, blended together in not very dissimilar proportions.
The elementary minerals, which may be seen distinctly crystallized
in the granite of this whole range, are
1. Quartz. :
2. Orthoclase. :
3. Silvery grey biaxial mica. :
4. Black mica.

1. Quartz.—The quartz of this district is grey transparent, and
presents no variety of colour or appearance ; smoky quartz is, so
far as I am aware, unknown in this range, although so abundant in
the Mourne granites. The mean specific gravity of the quartz, taken
from the granite of distant localities, is = 2°645.

2. Orthoclase.—The feldspar of the granite of the main chain is
invariably white and opaque, and occasionally crystallizes out from
the mass in large crystals ; these crystals were examined from seven
different localities by Professor Galbraith of Trinity College, and
found to be, without exception, pure Orthoclase. I here subjoin, in
a tabular form, the results of his examination of this mineral in the

granite-range.

Taste I.—dnalyses of Feldspars.

ly 2. | 3. | 4, 5. | 6. ¥ ‘Average.

i ee |

SiHica) ne. ssskenae 64:00 | 65-40| 65-44} 65°05| 64:19; 63-60| 64:48! 64:59
Alumina.......... 18-11] 17-71] 18°36 | 17:72} 18°39) 18°84] 19°04} 18-31
DUE, capes eene el eee ehh soc 0:30) O25 eeOgoy 2. |... 0:25
Magnesia ...... WMA EL eeccs. | Speen 034; 0-40] 1:02) 058
Potash ......006 12:73) 10-68) 12°34) 13°42] 11°39; 14:33} 10-74) 12-23
Soda ......---00- 3°00} 3:26) 2°73) 2°75) 2°95; 192] 2:64) 2-75

Loss by ignition) 0°55) 069} 052] 036] 058 060} 0°78] 0:58

Total ..........:.{ 98:96] 99-51 {100-19 | 99:53 98:54 | 99°69 | 98°70} 9929

174 PROCEEDINGS OF THE GEOLOGICAL SociIETY. _ [Feb, 6,

No. ]. Quarries of Dalkey, county Dublin ......... Specific gravity =2°540
No. 2. Three Rock Mountain, county Dublin ...... 55 » =2:562
No. 3. Lough Bray, county Dublin .................. on » =2:554
No. 4. Lough Dan, county Wicklow ............... a » 2559
No. 5. Glenmacanass, county Wicklow ............ ss. » =2'553
No. 6. Glendalough, county Wicklow .............0 B; » 2-453
No. 7. Glenmalure, county Wicklow ............... xp ~ =2ato

These feldspars, crystallographically considered, were found to be
monoclinic, or of the fifth crystalline system of Rose. The analyses
of the granites of the main chain, which will be given subsequently,
prove that the constituent feldspar of the granite differs from the
large crystals of the mass, in containing somewhat more soda. It
might be supposed that this arises from the admixture of other
varieties of feldspar, m addition to Orthoelase ; but a careful exami-
nation of the district has failed to prove the existence of any other
variety of the feldspar-family in distinct crystals. In this respect
the granites of the south-eastern district differ remarkably from the
granites of Mourne, which contain distinct crystals of both Ortho-
clase and Albite, both which feldspars may be distinguished by the
practised eye, in every hand-specimen of granite from that district.
No Albite, so far as I am aware, or other feldspar than Orthoclase,
has ever been found in the Leinster granites.

The mineralogical formula of the Orthoclase of the Leinster
granites may be deduced from the last column of Table 1. ; dividing
by the atomic weights, we find for the numbers of atoms :—

Siheat ee. wo F404). 153°) 3404. See
Alumina...... 0°356") .\2..2 (0 356 ae
Lime 7) eS. 0:009

Magnesia .... 0°029

Potash 222002 26076 0387 .... 1
Soda... 220) (O0B ayy

from which results the well-known formula
RO, SiO, + Al,O,, 3810,.

3. Grey Silvery Mica.—The grey mica of the distriet under con-
sideration is frequently of considerable dimensions, sometimes at-
taining a diameter of between 2 and 3 inches; and even in the mass
of the granite it is occasionally very variable in size, large plates
being sometimes mixed with plates not exceeding one-tenth of an
inch in diameter. This mica is trimetric, occuring in either flat right
rhombic prisms, or in hexagonal plates, formed from the former by
the replacement of the acute angles; the angles of the prisms in all
the specimens which I have had an opportunity of examining are 120°
and 60°, and the plane of the optic axes was invariably found to
contain the greater diagonal of the rhomb, joining the acute angles.
Of the angles between the optic axes recorded in my note-book, I
subjoin the following :—

1856.] HAUGHTON—GRANITES OF IRELAND. 175

1. Three Rock Mica ...... Do, 8
2. Glendalough Mica ...... 70 4
3. Mount Leinster Mica.... 72 18
4, Lough Dan Mica ...... 70 O
5. Glenmalure Miea ...... 67 11

Chemically considered, this mica is the Margarodite of mineralogists,
and is very constant in its composition, as appears from the following
analyses :—

TaB Le II.—Analyses of Grey Mica.

1. 2. 3. Average.
INCA gescc- sen gavaee 44:71 44°64 43°47 44:27
Alumina sds 31:13 | 30°18 | 381-42 30°91
Peroxide of iron..| 4°69 6°35 4-79 5:27
WING) S ovisiices ene LOO We ck: 1:38 0°82
Magnesia ..-...... 0-90 0°72 113 0:92
Rotasht ctecr.s64 oa). 12-40 10°71 1-01
SOMA, es scaccesscases ME ZT Te. 33 1:44 0:90
Loss by ignition...} 6°22 5°32 5:43 5°66

99-92 99°61 99°77 99°76

No.-1. Glendalough Valley, county Wicklow ......... Specific gravity =2°793

No. 2. Mount Leinster, county Carlow ............++.
No. 8. Three Rock Mountain, county Dublin......... 5 ep Maer er

Dividing the last column of the foregomg Table by the respective
atomic weights of the constituents, we find the following :—

UES eth LS MOOR I: 8 ay DS
Alumna: een) 0-601 :

Peroxide of iron .. te Se | aay 4
Hamre Garis Agi s+ 2b 0-029)

Magnesia........ 0°046 :
Potash 42.2 06. 300s 2 08284 US ss NSE eae
POH aa Use. NA 0°029 ;
Water vs 8c Sis O2629; 2232102029 lose 2

From the foregoing figures may be inferred the formula,
| RO, Si0,+ 2{R,0., $10,} + 2HO,

which coincides with the received mineralogical constitution of
Margarodite.

4. Black Mei aces the mica already described, black mica
in small grains presents itself in the granite of several parts of
Leinster ; it is never present in great quantity, but appears to be
distinct from the grey silvery mica, as it can be separated from it to
a considerable extent by levigation, proving that it has a different
‘specific gravity. I have never been able to procure it in sufficient
quantity for examination, either chemical or optical. It is sometimes
found, as in the granite of the Three Rock Mountain, county Dublin,

176 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

in small specks or grains imbedded in the larger plates of grey silvery
mica ; in such cases, it impairs but does not destroy the transparency
of the latter; and it is worthy of remark, that the mica of this
mountain, which contains specks of black mica, has a smaller angle
between its optical axes than the pure silvery mica of the other
districts.

Accidental Minerals found in the Granite of the Main Chain.

The following list contains the names of all the accidental mine-
rals of the Leister granite, with which I am acquainted. I have
excluded from it the minerals found im the metallic lodes which
occasionally traverse the granite and the neighbouring metamorphic
slate, as at Glendalough and Glenmalure.

1. Schorl (black and dark green).
. Beryl.

. Apatite.

. Killinite *.

. Garnet (in small crystals).

. Fluor Spar (cubic).
Spodumene.

NID OA ODD

Chemical Composition of the Granites of the Main Chain.

The following analyses show the composition of the granite, taken
from localities distant from each other, in the extreme cases, by
upwards of sixty miles. There is a striking similarity in all the con-
stituents, considering that they are derived from rock-analyses,
and this remarkable uniformity of composition is a proof of the great
scale on which the fusion took place which gave rise to the Lemster
range of granites. The range in per-centage of silica is less than
four per cent., varying from 70°28 to 74°24; the small quantities of
iron, lime, and magnesia are remarkable, when taken in conjunction
with the uniform fact, that the soda falls short of the potash; as we
shall show that in the granites in which soda predominates over pot-
ash, as a general rule, there is a larger quantity of iron, lime, and
magnesia than in the granites here described.

* The title of Killinite to be considered a distinct mineral has been disputed ;
some mineralogists being disposed to consider it as an altered form of Spodumene.
It is a rare mineral, and has been hitherto only found at Killiney, near Dublin.
Its exact chemical composition has been recently satisfactorily determined by
Professor Galbraith, who considers its mineralogical formula to be well represented
by the following relative number of atoms :—

SUCA neces 4 Protoxides...1
Alumina ...2 WWAtEr ocx... 3

Giving for mineralogical formula
RO, Si03;+2A1,03, 38i0;+3 HO.

Professor Galbraith’s discussion of this interesting question is published in the
sixth volume of the Journal of the Geological Society of Dublin.

1856. | HAUGHTON—GRANITES OF IRELAND. 77,

Tasie II].—Analyses of Granites.

1 2 3. 4 5

SIEGE) Se eae 70°38 | 73:00 | 70:28 | 70°32 74:24
PLLA <5. os cana 12°64 13°64 16°44 16°12 13°64
Peroxide of iron...| 3°16 2°44 2-60 3°20 1-40
PME te sisteccaa seals 2°84 1°84 2°04 1:34 1-48

Magnesia ......... 0:53 OF. tie eta elite ei
POCASILS s,.. ctessoes ss 5:90 4-21 5°79 4-65 3°95
Soda) Mretes sass 3°13 3°53 2°82 3°39 2-72
Loss by ignition...} 1°16 20 eee ie 0:96 1:20
Motalsasacscgscses 99:74 | 99:97 | 99-97 99:98 98-63
6 7 8 9 Average

SUITE. Sunk ..tce. dees 70°82 73°24 | 73:20 | 73:28 | 72:084
ATuprina 6.05 - .is5s 14:08 15°45 15°48 | 12°64 | 14-459
Peroxide of iron...| 3°47 1:60 1:72 2:00 | 2-399
IME ecoec selene same 4 * 2°65 0:99 0:96 1:72 1-762
Magnesia ......+.- Ose M recede Viet sade aly cece: 0-105
Potash’ s..c0.50 00 4°64 4:59 4-80 4:70 | 4-803
Sadar Hck owedaslyns 2°31 3:08 3°18 2:97 | 3014
Loss by ignition...) 1°39 AZO iho vacsebs 1:04 | 0-906
AL GE ANS insicesy- +5 99:67 | 100-15 99:34 | 98:35 | 99:532

No. 1. Dalkey Quarries; specific gravity = 2°647; a fine-grained granite, con-
taining both black and grey mica. This granite has been used in the
construction of Kingstown Harbour. 3

No. 2. Fox Rock, county Dublin; specific gravity = 2°638; a coarse-grained
granite, striking fire when struck with a hammer, and showing abundant
grey quartz.

No. 3. Three Rock Mountain, county Dublin, Woodside Quarry; specific gravity
=2°652; a coarse-grained granite, containing rhomboidal and hexa-
gonal plates of grey mica, speckled with grains of black mica.

No.4. Three Rock Mountain, county Dublin; fine-grained granite, with occa-
sional large plates of speckled mica, which appears to be characteristic
of the granite of this mountain.

No. 5. Enniskerry, county Wicklow; specific gravity = 2°633; a rather coarse-
grained granite, containing veins of black schorl.

No. 6. Ballyknocken, county Wicklow; specific gravity = 2°636 ; a fine-grained
durable granite, considered to be the best building-stone near Dublin.
The quarries are situated beyond Blessington, county Wicklow.

No. 7. Kilballyhugh, county Carlow; specific gravity = 2°616; a fine-grained
granite and a good building-stone ; it contains no trace of black mica.

No. 8. Blackstairs Mountain, county Wexford; specific gravity = 2°622; a
medium-grained granite from Kiltealy, on the Wexford slope of Black-
stairs Mountain.

No. 9. Ballyleigh, county Wexford; specific gravity = 2°627; a fine-grained
granite, from near Poulmounty Bridge, at the extreme southern bound-
ary of the main granite chain.

The mean specific gravity of the specimens examined is 2°634.

a

178 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 6,

Mineralogical Composition of the Granites.

Various methods have been suggested for ascertaining the relative
proportions of simple minerals, entering into the composition of com-
pound rocks, such as granites. In Table III. I have given the
ultimate chemical analysis of the rock ; in this section I propose to
determine the physical or mineralogical analysis of the granites under
consideration.

Of the different methods in which the per-centage of elementary
minerals in a given rock may be found, the following appears to be
more simple and accurate than the methods hitherto in use, which
are based either on specific gravities or on measurements of surfaces
of crystals in polished specimens of the rock.

Let the rock be assumed to be composed of a number of minerals
whose mineralogical formula is known, and also their per-centage
composition, and let the atoms of silica, peroxides, and protoxides in
the rock be ascertained from the ultimate analysis of the rock, and
denoted by a, (6, y; it is possible thus to obtain three equations
from which the per-centage of elementary minerals, supposed to be
not greater in number than three, may be ascertained.

If the elementary minerals exceed three in number, this method
will fail to give a determinate solution, and will lead to an equation
of condition, from which certain properties of the rock may be
deduced, although its exact composition cannot be ascertained.

This reasoning will be made quite clear by its application to the
granites under discussion.

Dividing the numbers in Table III. by their respective atomic
weights, and adding together the isomorphous protoxides and per-
oxides, I find

TasLe [V.—Atoms of Granitic Constituents.

iV 2. 3. 4. 5.
DIICR i ceuseene one ae 1:530 1-587 1:528 1-529 1-613
ELORIDEN parcisesers 0:286 0:296 0:352 0:353 0-282

Protoxides ...... seal OB5S 0:274 0°287 0:256 0-226

6. ic 8. 9. | Average.
DIMER nosierseseccens 1:540 1-592 1:587 1593 1:567
P€rORiges): :..650.5% 0317 0:321 0°322 0-271 0311
Protoxides.......... 0282 0232 0238 0°257 0-267

Assuming the granite to be a ternary compound of quartz, marga-
rodite-mica, and a feldspar rich in silica, we know that the minera-
logical formule of these minerals are :

Quartz = 810,

Margarodite = RO, SiO, + 2{R,0.,, SiO,$ + 2HO
Feldspar = RO,Si0,;+ R,O,, 3 SiO.

1856. | HAUGHTON—GRANITES OF IRELAND. 179

It follows from these expressions, and from the definitions given
of a, (, y, that, if Q, F, M denote the number of atoms of quartz,
feldspar, and mica respectively contained in the granite,

a = Q+4F+ 3M
B =F +2M sa ene ego ee

Substituting in these equations for a, 3, y their numerical values
from the last column of Table IV., we find

1-567 = @ + 4E + 3M
0°267 =] FE we

From these equations, we find easily

M = 0-044
f= 0:223
Q = 0°543.

These numbers express the atomic quotients of mica, feldspar,
and quartz existing in the granite, and if m, f, q denote the atomic
weights of these minerals, then 7

The per-centage of mica = M x m
is feldspar = F x f >.
99 quartz =Q xq

(2).

And consequently, if our hypothesis be correct, the following
equation must be satisfied :—

99°53 = Mm.t+-Ef+Qg . -~ 2. «. (3).

The left-hand side of the equation being taken from the last
column of Table III.

But here a difficulty presents itself; we know the atomic weight
of quartz, but not of margarodite or feldspar, unless we assume the
per-centage composition of these minerals, or in other words assume
the composition of the constituent minerals of the granite.

I shall assume the composition of the grey mica from Table II.,
from which and the subsequent list of atomic quotients, we may
calculate the atomic weight of the grey mica of the granite as
follows :—

The mineralogical formula of margarodite is in atoms = 3 silica
+ 2 peroxides + 1 protoxide + 2 water. The atomic weights of
silica and water are known, and are 46 and 9 respectively ; there-
fore, if z and y denote the atomic weights of the peroxides and pro-
toxides respectively, we have }

Atomic weight of mica = 3 x 464+ 2a+y+2x9. |

180 PROCEEDINGS OF THE GEOLOGICAL society. _ [Feb. 6,

But the values of z and y are found by the relations

36°18 = 0°667 x a (4)
13°65 = 0°338 x y ar i

The left-hand numbers being the per-centages of peroxides and
protoxides respectively ; and the right-hand numerical coefficients
denoting the atomic quotients of peroxides and protoxides respect-
ively ; from these equations we find the values of 2 and y to be 54
and 40. And finally

Atomic weight of mica = 304.
Assuming this atomic weight for the grey mica, we find from
equation (2) the quartz and mica per-centages directly, and the per-

centage of feldspar from equation (3) by difference.
Hence we obtain :

Mineralogical Analysis of Granite.

Mica aide ted fsce 1337
Peldspartpanbse. in 61:18
Cartas Lee eee tte: 24°98

99°53

Having ascertained the proportions of quartz, margarodite, mica,
and feldspar which form this granite, we can ascertain with precision
the composition of the feldspar of the granite, and at the same time
verify the entire calculation as follows. Adopting the mineralogical
analysis of the granite already found, and the average composition of
the mica, we can form the following Table, which assigns to each
mineral its own share of each constituent of the granite; the feld-
spar column being found by difference.

TaBLe V.
Quartz. | Mica. | Feldspar.| Granite.
Dihigaiisciten sth ead 24:98 3°93 41:18 72-09
Alumina ......... —_ 4:14 10°32 14:46
Peroxide of iron} — 0:70 1:70 2-40
|B) 1s (ie ea — 0:16 1-60 1-76

— 0-10 _— 0:10
— 1-47 3°33 4:80
— 0°12 2°89 301
— 0°75 0-16 0-91

24:98 13°37 61°18 99°53

If the preceding calculations be correct in theory, the feldspar
column must give us a true feldspar rich in silica; which is verified
as follows. Raising the proportions of the feldspar column to per-
centages, we find—

—

eee eee

i

tt I

1856. | - HAUGHTON—GRANITES OF IRELAND. 181

Caleulated Composition of Granite-Feldspar.

Per cent. Atoms.
Sie we 67°30) 02). RAGA e464 7; 4
Avumina. 2: kOkg ae eel 0°364 ..1
Peroxide of iron 2°87 ....0°036f °° i
HEE oe. hoe 2°60 .... 0°093 ]
Magnesia .. a eA Sea
Pouch |... 543....G11g
OCaiitsh, Siscane 47 RO 2)

Loss by ignition 0°24

100-00

This is a genuine tersilicated feldspar; from which fact we may
draw the conclusion, that our original hypothesis as to the granite is
admissible, viz. that it is composed of quartz, margarodite-mica, and
tersilicated feldspar; if other minerals enter into its average compo-
sition, they must do so to such a slight extent as practically to have
no influence on the composition of the granitic mass. On comparing
the calculated feldspar just determined with the average feldspar of
Table I. the following interesting difference may be observed ; that
the feldspar of the main body of the granite contains more soda, and
lime replacing potash, than the crystals of feldspar, whose compo-
sition is given in that Table. It would appear from this fact, that in
cooling from a molten condition, the large crystals of feldspar, in
assuming their crystalline state, had appropriated to themselves more
than their share of potash. It is possible, inasmuch as the typical
orthoclase of the fifth system contains a large proportion of potash,
that the excess of potash may be an essential condition for the forma-
tion of such large and distinct crystals. In fact, in a molten mass,
like that under consideration, if no alkali were present besides potash,
all the crystals of feldspar would belong to the monoclinic system ;
and if the only alkali present were soda, all the feldspar crystals
would be found in the triclinic system. There must therefore be
some intermediate mixture of potash and soda for which the crystals
of feldspar are, as it were, undecided in which system to crystallize ;
or, in other words, the feldspar will remain in a confused crystalline
mass, as in the body of the granite, while the large crystals which
occur take their character from the predominant alkali, and consist,
as in the case before us, exclusively of orthoclase crystals, of typical
composition, in the monoclinic system.

Il. IsoLaAtED GRANITES.

The isolated granites of Wicklow and Wexford are shown on the
Map, fig. 1, p. 172; they appear in theform of isolated detached ranges
A, B, C, having an elongated form, running N.N.E. and S.S.W., or
parallel to the axis of the main chain. The granites composing these
detached hills are frequently associated with and penetrated by dykes
of greenstone and other forms of trap-rocks. Mineralogically they
are distinguished by the presence of black mica, chlorite, dark-green
mica, and hornblende. These minerals do not enter into the compo-

182 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

sition of all the isolated granites, which present greater differences ot
mineral constitution than occur in the main chain. Topographically
considered on the large scale, it has been suggested to me by Dr.
Griffith, who is well acquainted with this district, that we may refer
the isolated granites to four parallel broken chains, as follows :—

1. From the north-east of Rathdrum, A, passing south-west
through Ballinaclash, to the village of Aughrim, in the county of
Wicklow.

2. From Croghan Kinshela, B, south-west to Conna Hill, in the
county of Wexford.

3. From the south of Oulart, county Wexford, C, through Ballin-
amuddagh to Camarus Hill, midway between Wexford and New Ross.

4. The extreme south-east of Ireland, at Carnsore, D, extending
to the Saltee Islands, in the same general direction as the other
outbursts.

First, or Western Group of Isolated Granites.

The granites of this district extend in a broken manner from near
Rathdrum to Aughrim, a distance of ten miles north-east and south-
west, and attain in Cushbawn Hill an altitude of 1318 feet. In the
northern part of this chain, the granite contains red feldspar and
black mica, at West Acton; but the general character of the granite
is best exhibited in Cushbawn Hill, which is composed of a fine-
grained granite, contaiming grey quartz, white feldspar, and minute
particles of grey and dark-green mica. An average specimen from
this hill, selected with care, gave the following analysis :—

Granite of First Isolated Group.
Specific gravity =2°671.
Per cent. Atoms.

DUCA se rie nds dene Mk 70532... .21b 29
ASI rani He. te sees te 11°24 ok
Peroxide ot ironies. a37e .h 4:80 (/* 3 0-278
dames 43 2x3 Hea ABE 3°01)
Masnesiah hie jan geciss. Dee ;
Potashux¢ Satie bsisgal PaTat F oo
Sodaic+ x ob eee Sine ee 3°39
Carbonate of lime........ 1°34
Loss by ignition. 2: 2.2... 1°62

98°72

The carbonate of lime in this granite is present accidentally, and
has been introduced by infiltration from the limestone-gravel of the
drift which covers the district. On comparing the preceding analysis
with the average granite of Table III. we may observe the following
differences :—

1. In the granite of Cushbawn there is an increase of peroxide of
iron replacing alumina, and attended with an increase of specific gravity.

2. The quantity of lime and soda is increased, so as to invert the
relative proportions of potash and soda, rendering the granite of
Cushbawn a soda-granite, and showing that it has proceeded from

1856. | HAUGHTON—GRANITES OF IRELAND. 183

an igneous focus, different from that of the main chain, and one con-
taining more soda and lime. Neglecting the small quantity of mica
which enters into the composition of this granite, it may be repre-
sented by the mineralogical analysis following :—

Orang ee) os soe eye ee 17-4 per cent.
Beldspaigies se 2. c\-0 oe S260) 7
100-0

Comparing this result with the mineralogical analysis of the main
chain, we observe a deficiency of quartz and an increase of basic earths.

Second Group of Isolated Granites.

The second group of isolated granites consists of Croghan Kin-
shela, rising to a height of 1985 feet, and Conna Hill. The line
joining these hills is N.N.E. and 8.8.W., and the greatest length
of the granitic outburst may be stated at six miles. The granite of
Croghan Kinshela rises through and alters the slate of the district,
converting it in a great degree into hornblendic and chloritic meta-
morphic slate. On the northern slope of Croghan Kinshela are
Situated the famous gold-mines of Wicklow, which consist of stream-
gold brought down from some undiscovered source in the mountains
by the floods of winter; they are still occasionally wrought by the

- neighbouring peasantry, when other employment is wanting in the

district. ‘The granite of Croghan Kinshela differs from all other
granites I have seen in the south-east of Ireland in its mineralogical
composition. It is, on the whole, a binary compound of quartz and
albite, containing variable quantities of chlorite, which is sometimes
nearly wanting, at other times present in considerable quantities. It
is to be observed, that the quartz occurs in small rounded granules
in the rock. The following analysis of a specimen, as free from
chlorite as could be procured, will give a good idea of the nature of
this rock.
Granite of Croghan Kinshela.
Specific gravity =2°629.

Per cent. Atoms.
SELTTER Wy bea liees eae S0:240 1-744
Alumina 12724
Peroxide of iron .... 0°72{ °° 0°247
Mine: Oo AG.) As. rate
Magnesia, . 2%. .2-.'. trace : 7
_ECOISG | 9 ee rae empress 2 O-213
Pee ted eee a i ae 5°58
100°07

From the foregoing analysis we can infer the following mineralo-
gical analysis of the granite of Croghan Kinshela.

Quartz <5... = 38 per cent.
Atbite: 2... —=02 is
100

VOL. XII.—PART I. O

184 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. _ [Feb. 6,

This is evidently a granite suz generis, eminently siliceous, and
containing a minimum of bases. It possesses a brilliant white colour,
except where stained by the patches of chlorite. ‘This lustrous white
colour is due to the presence of the feldspar, which is exclusively
albite. If it were not for the chlorite, which appears to take the
place of mica, rendering this rock a genuine ternary compound, we
might consider it as an albitic Pegmatite; but since it contains a
mineral so closely allied to the mica-family as chlorite, I believe it is
fairly entitled to rank as a variety of the extensive family of granites.

On comparing the composition of this remarkable granite with the
granites already discussed, we may draw the following inferences :—

1. That it is eminently a soda-granite.

2. That the addition of soda to the igneous source from which it
is derived, has not been accompanied by the corresponding addition
of lime and iron, which was remarkable in the Cushbawn granite.

3. That this increase in soda has been accompanied by a remark-
able increase in the quantity of free silex, existing as quartz in the
rock.

4. From the rounded appearance of the quartz-granules, I should
be disposed to infer that their angles were rounded off by fusion,
consequent on the addition of the powerful base soda, which acted as
a flux on the siliceous rock.

Third Group of Isolated Granites.

The third chain of isolated granites commences a little to the
south-west of the village of Oulart in the county of Wexford, and
extends, at intervals for fifteen miles south-west, to Camorus Hill.

Mineralogically considered, these granites are composed of grey
quartz, white feldspar (passing occasionally into yellowish and pink
feldspar), and black mica, the latter mineral being probably some-
times accompanied by hornblende.

I subjoin the analyses of two specimens, which may be taken as
typical of the district.

Granite of Third Isolated Group.

No. 1. | No. 2. | Average.| Atoms.

TLIC Scivtincitg toence ten amemoitenn 66°60 68°56 67°58 |...1°469

PUAN A soc wemesvnsmescower ent 13°26 14°44 13°85 0-346

Peroxide of 1r0n -is...h-sses- 7°32 5:04 6:18

BAITED se cia s/asina nin gia ovens eee 3°36 3°85 3°60

NIGENERIA dec dwaebosestesdenes 1:22 0:43 0:82

i) Se ee ices 231 | 2-78 | 955 | £9385

Re taneous oe evivwseebuce nts 3°60 3°36 3°48

Loss by ignition ............ 2:34 1:00 1:67
Totals...... 100-01 99-46 99°73

No. 1.—A fine-grained granite from Ballymotymore, containing black mica ;
specific gravity = 2°659. ma’

No. 2.—A coarse-grained granite from Ballinamuddagh, containing distinct
and large plates of black mica, of =3,th inch in breadth; specific gravity =2°670.

1856. | HAUGHTON—GRANITES OF IRELAND. 185.

It is not possible to obtain the mineralogical analysis of these
granites without assuming the composition of the black mica, which
has never been determined. If we assume, provisionally, that the
formula of the black mica is the same as that of the gray mica (as
seems probable from the manner in which it replaces it, isomor-
phously, in the crystals of the Three Rock Mountain), we can obtain
the relative atoms of quartz, feldspar, and mica in this granite from
equations (1) ;

1:469=Q44F+4+3M
0346S F 2M ee, a oe EY
0:335= F+ M.
From which we readily obtain as atoms of quartz, feldspar, and
mica :—

Q=—0:°140
F=0°324
M=0:011.

The per-centage mineral composition of the rock cannot be de-
duced from these figures without assuming the ultimate analysis of
either the mica or feldspar, both of which are unknown; but we can
readily assign the limits of error. Let us suppose the mica to con-
tain no alumina. In this case its peroxides are iron, and therefore
the atomic weight of the mineral is 356. If the mica contains no
iron, its peroxides are all alumina, and its atomic weight will be 299.
These are the extreme atomic weights of margarodite-mica, possible
on the supposition that its protoxides remain as in Table II. Multi-
plying the preceding numbers by M, we find,—

Major per-centage of mica...... 356 x 0:011=3°'91
Minor per-centage of mica...... 299 x 0:011=3°29.

Assuming the mean of these as the per-centage of mica, and deter-
mining the quartz as before, and the feldspar by difference, we ob-
tain the following

Mineralogical Analysis.
Cyiartz. sine nore = 9:44
Heldspar 4s-2).459.4-—59 09
i ae SR = 3°60

99°73

In the Cushbawn, or first group of isolated granites, the quartz
was diminished from 25 to 17 per cent. of the entire rock, as com-
pared with the granite of the main chain ; in the granites of the third
group of isolated granites, we observe a further reduction of quartz
to 6 per cent. ;

This third group of granites agrees with the first, and differs from
the main chain in the following particulars :—

Ist. The diminution in per-centage of silex.
-. 2nd. The increase in iron and lime.
3rd. The preponderance of soda over potash.
02

186 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 6,

4th. The increase in specific gravity ; the mean specific gravity of
the two specimens being =2°665.

In addition to the foregoing peculiarities common to both groups
of granites, it may be remarked that the change of character, as
respeets the iron and lime, is carried further in the third isolated
group than in the first.

Fourth Group ofeIsolated Granites.

In the extreme south-eastern corner of Ireland an outburst of
granite occurs, at Carnsore, which appears to be continued to a con-
siderable distance under the sea in an E.N.E. and W.S.W. direction.
This granite consists principally of grey quartz and reddish-pink
feldspar, associated with which in many specimens are green mica,
and apparently a variety of hornblende. I selected for examination
a specimen consisting almost exclusively of quartz and feldspar, con-
taining a few specks of dark-green mica, but no trace of hornblende.
This appears to be the prevailing character of the rock; the horn-
blende, when it does occur, appears to be very irregularly distributed.

The specific gravity of the specimen examined by me was found
to be 2°636.

Analysis of Carnsore Granite.

Per cent. Atoms.
reuse Bie Cia Pca Anas? Bl 2 (| aie Maria MER S|
Alumina... 24... D7 2 ee oe i 0-276
Peroxide of iron. . B 862s 02 0048 ir =
Limiter Le ex OTD ke ORO
Magnesia ...... trace
Potash. ooo a B77, is wpa, OP LOL > eae Ue
SOU sete set. o06 2... 02098

Loss by ignition.. 0°95
98°30

The most cursory examination of this analysis, compared with the
average granite of the main chain in Table III., serves to show that
we have recovered in Carnsore the original type of potash-granite
from which we set out in the main chain. To render this important
fact more evident, I shall enter into some further calculations.

It is plain from the atomic quotients that the quantity of mica
present is triflmg in amount, and that the rock may be regarded as
’ composed of quartz and feldspar in the following proportions :—

Quartz.......... =21°50
Peldspar ..cceis =78'b0
100-00

From this analysis we can calculate readily the theoretical composi-
tion of the feldspar of the Carnsore granite :—

1856. | HAUGHTON—GRANITES OF IRELAND. 187

Calculated Feldspar of Carnsore Granite.

Alumnae” 222-4 14292
Peroxide Of Iron. 4°93

eames eons 3°30
Magnesiac. .) 10-6 ===
1 ELC ol pei ig 6:07
BOs sae. eye 3°90
Loss byignition.... 1°20

100-00

From the analysis of the granite and its calculated feldspar, the
following inferences may be drawn :—

Ist. The Carnsore granite, as respects its ultimate analysis, is ab-
solutely identical with the average granite of the main chain, in the
constituents, silica, lime, magnesia, potash, and soda.

2nd. In the Carnsore granite, peroxide of iron to some extent
replaces the alumina, giving to the feldspar its reddish-pink colour.

3nd. The free quartz in the Carnsore granite is nearly equal in
amount to that of the main chain.

Type-Granites of the South-east of Ireland.

From the preceding facts, the following inferences appear to me to
follow :—

Ist. In the south-east of Ireland, the granites may be classified by
the preponderance of potash over soda, or vice versd.

2nd. The granites of the main chain and of Carnsore, are potash-
granites. |

3rd. The granites of the intermediate groups are soda-granites,
and are reducible to two types :—

a. The Croghan Kinshela granite ;
6. The soda-granite proper.

The former of these is exceptional, and of rare occurrence; the latter
is common, and reappears in the County Down and County Armagh
granites. |

4th. The potash- and soda-granites, properly so called, or type-
granites, differ from each other in a regular manner, in respect to
the other constituents, as well as in respect to the alkalies; the most
striking differences being the deficiency of silica in the soda-granites,
this deficiency being made up by the addition of peroxide of iron
and lime; and the increase in specific gravity of the soda-granites.

Nore.—At the Meeting of the Geological Society at which this
paper was read, I was requested to state whether there was any
geological evidence of difference of age between the potash- and soda-
granites of Leister. I know of no conclusive evidence on this point ;
but the age of the potash-granites is known within certain limits; it
is subsequent in time to the Silurian rocks of Wicklow and Wexford,

188 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 6,

supposed to lie on the geological horizon of the Lingula-beds of Wales;
and it is older than the calp-deposits of the carboniferous limestone
of the county Dublin, as is proved by the latter, as at Crumlin,
county Dublin, containing angular fragments of the granite of the
potash-type in question.

The soda-granites of Wicklow and Wexford also are subsequent to
the same Silurian rocks of these counties, as they convert the latter,
when in contact with them, into hornblende- and mica-slate, and
exhibit the usual phenomena of metamorphic action, such as the
development of minerals.—S. H.

Trinity College, Dublin, March 3, 1856.

PART I].—On tHe Granites oF THE NORTH-EAST OF
. TRELAND.

Introduction.

I. Granite of the Mourne District. .
Elementary Minerals.
Accidental Minerals.
Composition of the Mourne Granite.

II. Granites of the Carlingford District.
Description of the Igneous Rocks of Carlingford.
Composition of the Granites.

Composition of the Syenites.

III. Granites of the Newry District.
Potash-Granites.
Soda-Granites.

The granite-rocks of the north-east of Ireland are mostly collected
into a limited district on the borders of the counties of Down, Louth,
and Armagh. This district contains all the granites of the north-
east of Ireland, with the exception of a small outburst near Cushun-
dun in the county Antrim, of which separate mention will be made.
The granitic district of the north-east of Ireland admits of sub-
division into three natural groups.

lst. The granite-district of Mourne; which consists of a nearly

circular mass of granite, having a diameter of about nine miles, lying
to the north of Carlingford Bay.
_ 2nd. The granite-district of Carlingford, which is also nearly
circular, having a diameter of nearly five miles, and lying to the south
of Carlingford Bay. In this district, in addition to the granite proper,
there is much hornblende-rock and syenite, with varieties of green-
stone, the exact relations of which to the granite have never been
precisely ascertained.

3rd. The granite-district of Newry, extending from Slieve Croob,

~on the north-east, in a south-westerly direction to Forkhill and
Jonesborough, a distance of twenty-eight miles, and having an
average breadth of six miles.

I. GRANITE OF THE Mourne District.

Elementary Minerals composing the Granite of the Mourne District.

The granite of the Mourne mountains is very fine-grained, and
contains numerous vughs or cavities, which are lined with distinct

1856.] . HAUGHTON—GRANITES OF IRELAND. 189

crystals of the minerals composing the granite and also with some
rare accidental minerals, from the occurrence of which the Mourne
district has become well known to mineral-collectors. The granite
of this district has been described by some writers as a pegmatite,
but the distinction between this variety of granite and ordinary fine-
grained granites does not appear of sufficient importance to be worthy
of a separate name. Whether the Mourne rocks be called granite or
pegmatite, they consist essentially of four distinct and well-marked
minerals.

Quartz.

. Orthoclase.

. Albite.

Green Mica.

1. Quartz.—The quartz of the Mourne granite is of a brown
smoky colour, and occurs in hexagonal crystals lining the numerous
cavities of the rock.

2. Orthoclase.—The orthoclase of the Mourne granite occurs in
large opaque white crystals, and is interesting to the crystallographer
from the number of measurable faces which it presents ; it is fre-
quently found, in company with quartz-crystals, albite, green mica, |
and some of the accidental minerals, lining the surfaces of cavities.

In order to ascertain its average composition, I have examined

specimens from different localities, and in one instance determined

with care its crystallographic constants, which differ slightly from

those recorded from other localities. I should add, that the crystals

of orthoclase from the Mourne mountains are sometimes, but erro-

neously, confounded with the albite of the same district, in consequence |
of their brilliant, though opaque white colour.

The following Table contains the results of my analyses of ortho-
clase.

A oo boo

Tasie 1.—dnalyses of Orthoclase.

A. 2. 3. Mean.

SLICE each a Se 66°32 | 66°33 | 66-10 66°25
Alumina.........00 17°56 17°47 17-01 17°35
DTG Wao acceaea ware 1:36 115 1-26 1:25
Magnesia ......... OTL sli watten heameioes 0:05
Potash 9 ......2c0s0: 10°60 12:10 10-95 1]-22
SiD02) ee Re aR eae 2°33 2°67 4:14 3°05
loss by ienition...{ 0790 |. one. Vi cescne 0:30
Tatale soc. scccs- 99°24 99°72 99:46 99°47

No. 1. Orthoclase from Slieve Kevita, north-west of Slieve Donard, Mourne moun-
tains, in monoclinic system. Specific gravity =2°490.

No. 2. Orthoclase from Slieve Corragh, Mourne mountains, occurring in beautiful
crystals, lining cavities in the granite. Specific gravity =2°415.

No. 3. Opalescent translucent orthoclase, or moonstone, from Slieve Corragh;
occurs in large crystals. Specific gravity =2°557.

From the preceding analyses. it is plain that this feldspar is an
orthoclase ; and its mean specific gravity is 2°487, being somewhat

190 PROCEEDINGS OF THE GEOLOGICAL SocIETY. [Feb. 6,

less than the’ specific gravity of the orthoclase of the Leinster
granites,

The following angles of No. 2 were measured with great care and
gave the following results ; using Miller’s notation :—

(001) (010)= 90 0
(001) (110)= 68 5
(001) (110)= 68 5
(110) (110)=118 46
(111) (001)=(111) (110)=124 2

From these data we can easily calculate the following crystallographic
constants :—

Angle between a and e = 64° 18).
Ratiolof O40idsciscxnt « == 1S be
Ratio'’of ¢ t0°@s< 56. sc. =0°8358.

Besides the faces already mentioned, many crystals exhibit face
having the notation (101) and (102); the angles of which giv
results consistent with the above constants.

Albite.—The albite of the Mourne granite is found in twin crystals
incrusting the interstices of the orthoclase and quartz in the cavitie:
of the rock, and may also be traced by its translucent appearance u.
the body of the rock itself in small quantities.

It is distinctly triclinic, and a specimen from Slieve Corragh, on
being submitted to analysis, gave the following results :—

Analysis of Albite.

Per cent. Atoms.
UIC wines 08'S] ain 99
Alumima..;.° 19°23 ...3.. O0°375
Paime © <0 121)
Magnesia .. 0°24 :
Potash .... 1°56 Y. ie

Soda eh 2 98°71 g

99°92
From the preceding analysis it is evident that this is a pure albite,
having the usual formula of a tersilicated feldspar,
RO, Si0,+ Al,O., 38103.

The following angles were measured between three of its planes,
two of which (viz. (010) and (001)) are planes of cleavage :—

(010) (001)=86 52
(010) (101)=54 53
(001) (101) =92 37.

Green Mica.—The mica of the Mourne mountains occurs in small
quantities through the mass of the granite and in larger crystals

~

1856. | HAUGHTON—GRANITES OF IRELAND. 191

accompanying the quartz, orthoclase, and albite, which line the
cavities.

It is of a dark-green colour, nearly opaque, and crystallized in
regular hexagonal plates, all the angles of the hexagon being 120°.
A specimen from Slieve Corragh was found to have the following
composition :—

Analysis of Green Mica.

Per cent. Atoms.

SMG. cca os AS a2 Ne OGAE es D

Ahumima,, oo. ss 19:00 i

Peroxide of iron... oe ar cilia ioe

Witten eet ties. sy ST}

Masnesia’....7. .'. 0°54 ‘eae

HeOeaSH cas sce 5. O77 | pene a

NOGA tee eee OOO

Wass*by inition..." 4°30)" 32.2 0477... 2
99°14

From this analysis, it appears that the composition of this mica is

closely represented by the formula

2(RO, Si0,)+3(R,0;, SiO,) + 2HO.

The green colour of the mineral is due to the large quantity of iron
replacing alumina. On comparing the formula just given with that

obtained for the mica of the Leinster granites, it is plain that they

both come under the general formula of the mica-family, viz.,
p(RO, Si0,) + ¢(R,0,, Si0,) +7HO,
p> % 7, having different integer values, and the value of 7 being
sometimes cypher, as in the formula for muscovite.
Accidental Minerals of the Mourne Granite.

A number of beautiful specimens of occasional minerals are found
in the cavities of the granite of this district, especially in the granite

of Sleve Bingian and Slieve Corragh. I have endeavoured to render

the following list as complete as possible.

1. Beryl.

2. Chrysoberyl.

3. Fluor-spar (octahedral).
4. Topaz.

5. Peridot.

These minerals occur in the cavities of the granite, accompanied
by hexahedral crystals of smoky quartz, crystals of orthoclase, albite,
and green mica. The fluor-spar, which is very rare both in the
Mourne and Leinster granites, is found octahedral in Mourne and
cubic in Leinster, a curious difference, which probably arises from
some unknown difference in the conditions of cooling of the granite
masses in the two localities.

192 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 6,

Composition of the Mourne Granite.

The Mourne granite is very fine-grained, and would be called
elvan in Cornwall; it contains distinctly quartz, orthoclase (both the
opaque variety and the translucent kind known as moonstone), albite,
and green mica. An average specimen from Slieve Corragh gave
the following results :—

Composition of Granite.
Specific gravity =2°595.

PEt eae a EOE SOR Re ae 75°00
PASTUGTIMUAREL ach ite te abou 2% aM 13°24
Peroxide lof won? i. ae oe 2-52
hire) eee eas ROMs mie RS 0°69
WER NOS TAN 2% vesersiale sreveis sie —
Potasly (0. Posi ee ee ASS3
SOGda os cee tases a aes
Loss byignition....... a aio
99°65

A comparison of this analysis with the average analysis of the
potash-granites of Leinster shows a striking similarity m all the
constituents excepting the quartz, which is three per cent. greater in
the Mourne granite; this excess of silica bemg accompanied with a
falling off in the lime and magnesia. Neglecting the small quantity
of mica in this granite, its mmeralogical composition may be consi-
dered as—

Quartz, per. asia eet dur tant 28°0 per cent.
Orthoclase 22. is oes 44°2
Ailbitet?, OEE pate 27°8

100:0

II. GRANITES OF THE CARLINGFORD DISTRICT.

Description of the Igneous Rocks of Carlingford District.

The granitic and other igneous rocks of the district south of Car-
lingford Bay, although only occupying a circular area of about five
miles in diameter, present to the geologist a variety and complication
which is at first perplexing. Although I propose to confine my atten-
tion to the granitic rocks of the district, yet it.is necessary to give a
summary of all the igneous rocks, and a statement of what is known
of their relative ages.

Igneous Rocks of Carlingford.

. Medium-grained granite: quartz, feldspar, green mica.
Fine-grained granite: quartz, feldspar, hornblende.

. Syenite : hornblende and anorthite.

. Hornblende-rock.

.. Amygdaloidal or pockmarked greenstone.

Fine-grained grey dolerite.

a ae

1856. | HAUGHTON—GRANITES OF IRELAND. 193

The following geological relations were observed by me to exist
among these rocks. The two varieties of granite pass into each
other, as may be seen in Slieve na glogh, of which the base is com-
posed of No.1, and the upper parts of No.2. At the summit of
this hill, the fine-grained granite, No. 2, is observed to pierce the
pockmarked greenstone, No. 5, in numerous veins.

At Grange Irish, the granite, No. 2, penetrates the lower beds of
carboniferous limestone, which there rest upon the granite; at the
junction of the granite and limestone the limestone is converted into
a bluish sugary marble, containing garnets, and the granite is con-
verted into the remarkable syenite, No. 3, composed of anorthite and
hornblende.

The summit of Carlingford Mountains is composed of the syenite
No. 3 and the hornblende-rock No. 4, passmg imto each other; the
hornblende-rock, however, being penetrated with numerous veins of
fine-grained syenite.

_The metamorphic mica-slate, of the Silurian age, which rests on
the north slope of Carlingford Mountain, is penetrated by dykes of
the pockmarked greenstone No.5; and the slates, carboniferous
limestone, and pockmarked greenstone are all penetrated by thin
dykes of the grey dolerite No. 6.

Judging from the variety and interlacing of the igneous rocks of
this district, there can be little doubt that it once formed the active
focus and vent of a most extensive volcanic outburst.

If we suppose all the amygdaloidal or pockmarked greenstone
to be of the same, or nearly the same age, it must be considered as
post-silurian, and the oldest igneous rock in the district. The two
granites, the syenites, and the hornblende-rock must be considered as
probably of the same age and post-carboniferous ; as it will be shown
that the granite is converted by the metamorphic action of the lime-
stone into the syenite in a particular locality; and it is highly pro-
bable that the whole of the syenite of the district owes its origin to
the limestone penetrated by the eruption of granite. The grey
dolerite has been observed to penetrate all the other rocks, excepting
the granite ; and it is probably of the same age as the latter. My
attention was first directed to this district by Dr. Griffith, who in-
formed me that it contained post-carboniferous granite. Mr. Grif-
fith considers the granite of Carlingford district, and also a granite
found near the top of Slieve Gullion in the Newry district, to be
newer than the granites of Mourne and Newry. It presents certain
structural differences which distinguish it from the granites of those
districts*. Having described—so far as they are known to me—
the geological relations of the granitiform rocks of this district, I
shall now proceed to the mineralogical investigation of these rocks,
which is full of interest.

Composition of the Granites.

There are two varieties of granite in this district, one composed of

* See Journal of the Geological Society of Dublin, vol. ii. p. 113.

194 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 6,
quartz, feldspar, and green mica, and the other, fine-grained, of

quartz, feldspar, and hornblende.

First Variety of Carlingford Granite.
Specific gravity =2°593.
Per cent. Atoms.

Silicn) wisest Beis 70°48) =... 1°532
Alumina, (nee rat 14°24 ;
Peroxide of iron .... eos ee
Lie .3, eat Seeley}
Mapmesian. 2c. eon 0°40 et
Potash: .23 5 od. SG —
Sodas A Een! weet 3°66

Loss by ignition .... 1°59

99°83
This granite was taken from the base of Slieve na glogh, is medium-
grained, and resembles the usual specimens of Dublin granites,
excepting that its mica is green and not grey silvery. Assuming,.
however, that the mica is margarodite, we easily deduce the following
equations, from which its mineralogical composition may be inferred.

1°532=Q+4F+3M,

0°323—= F+2M,
0-231 F+ M.
From these data we infer—
M=0:042
F =0-339

If we assume the atomic weight of mica as before to be 304, we
can obtain the mineral composition of the rock; in this calculation
the mica is slightly in defect, because there is more iron in this mica
than in the mica from which the number 304 is inferred.

Mineralogical Composition of the Granite of the First Variety.

QUUBTEZ on a es 20°70 per cent.
Peltspat «ec 66°37
Mica... ase we

99°83

From the preceding diseussion we are entitled to draw the in-
ference that the first variety of granite of Carlingford is a potash-
granite, and has a mineral composition very like that of the main
chain of Leinster.

The second variety of granite is very fine-grained, but distinctly
composed of quartz, white feldspar, and hornblende, without any
mica; and the first and second varieties of granite pass into each
other. I shall show, that although physically, and mineralogically,
these two varieties of granite are so distinct, yet chemically they are

1856. | HAUGHTON—GRANITES OF IRELAND. 195

closely allied; a fact which explains the passage of one into the
other; and also shows the necessity for some more certain criterion
of the true character of an igneous rock than either its physical
aspect or its mineralogical character, as both these may vary within
wide limits, although the ultimate analysis of the rock has changed
but little.

Second Variety of Carlingford Granite.
Specific gravity =2°632.

Sil T(r eget Cle eo VATS i oredog
lumina, sate. 2. | F264 ee O24
Protoxide of iron.... 4°76 )
SIT en aes Jee 1°80
Macuesia $2 2!0s 2 F.°) 0°63 >....0°441
POLash sth. on eye 22% 5°47
GMa ae et ts 3°03 J

99°74

The preceding granite was taken from Grange Irish, from the
» main body of granite, within ten yards of the point where the granite
penetrates the carboniferous limestone in dykes, and is converted
into a crystalline syenite. I have considered its iron as protoxide,
for, as there is no mica, and the feldspar is a pure white, the iron
must belong to the hornblende, and therefore must be protoxide.
If we suppose the alkalies and alumina to belong exclusively to
the feldspar, and consider the hornblende to be of the form

RO, SiO,, :
we have from the preceding numbers a
1552 =Q+4F +H |

0:246 = F
0:441 = F+H;
from which we obtain
P=. 0°373
T= O21.95:

If we calculate the atomic weight of the hornblende, referring to
it the iron and lime, we find it to be 79; from which we may infer
the composition of the granite to be as follows :—

Mineralogical Composition of the Granite of the Second Variety.

EE oo. ons = os 17°16 per cent.
Belispar ... :..:, 67-18
Hornblende ...... 15°40

99-74

This is a potash-granite, similar in composition to the first variety,

196 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 6,

containing about the same quantity of feldspar, but differing in the
other minerals. In fact, it would be easy to assign the conditions
under which the first or second variety of granite would be formed,
which consist of similar elements, but of different minerals.

Composition of the Syenites.

The syenites of Carlingford, which are coarse-grained and fine-
grained, and occasionally pass into pure hornblende-rock, are com-
posed of two minerals, anorthite and hornblende. As this is the
first time that anorthite is noticed as a British mineral, it may be
useful to discuss its chemico-mineralogical formula.

Carlingford Anorthite.

Per cent. Atoms.
Silica... 2. Dut 4b 87, Fy 0:90 7. aie
Alumaita.). dna OA (ah Ajo) OO 76.8 eee
Lime>. 22s. obasdee 17a
Magnesia ...... fey ose eee
99°25

The formula deducible from this composition is
2RO, S8i0, + 2{Al1,0., Si0,}.
It is plain that this feldspar is the anorthite of Vesuvius and
Hecla, and is identical with the anorthite of Java, of Columbia, and

of meteoric stones. It is essentially a volcanic mineral and is the
most basic of all the feldspar-family, as it contains disilicate of lime.

It is completely decomposed by muriatic acid, and is harder than

ordinary feldspar, striking fire under the hammer freely.

At Grange Irish, this mineral is formed by the addition of carbo-
niferous limestone to the fused granite of the second variety already
described.

I shall now describe the hornblende which forms part of the
syenites.

Carlingford Hornblende.

Specific gravity = 2-923.

Per cent. Atoms.
Sultea. bolas. | ames ee 50°72 .
Aiding ee oe aera
Protoxide of iron.... 18°61
Dime: 03.5 630 eG ore 1248
Midenesia \. 22 oe 2°40 J
Loss by ignition .... 1°52

99°57

From the preceding analysis, uniting, as Rammelsberg does, the
alumina with the silica, we obtain

RO; {SiO,, Al,0,};

——

1856. | HAUGHTON—GRANITES OF IRELAND. 197

a formula which is frequently found for the hornblende containing
alumina.

The syenites of Carlingford are composed of variable proportions
of the anorthite and hornblende just described; and a remarkable
instance of the formation of this syenite from granite occurs at
Grange Irish. The granite No. 2 there pierces the carboniferous
limestone in dykes, and in the dykes is converted into a Coarse-
grained syenite, composed of anorthite and hornblende, in no way
distinguishable, physically or chemically, from the syenites of Car-
lingford Mountain.

The metamorphic reaction of the granite and limestone upon each
other is strikingly shown at this pomt; the limestone being con-
verted from an earthy bluish-brown stone into a crystalline marble
of a light bluish-white colour, and having garnets developed in
many places; on the other hand, the granite is converted from a
ternary compound of quartz, orthoclase, and hornblende, into a
binary compound of anorthite and hornblende, of the following com-
position :—

Granite converted into Syenite, from Grange Irish.

Specific gravity =2°757.

Per cent. Atoms.
ee OY at ew dss ATS ol 030
Almansa 64s. 222 23°50 2. Obad
Protoxide of iron.... = 7°23)
Aime RU OE OMA OF 715
MnemesIA..... 2. <'s)2'- 1:48
100°23

Specific gravity of average specimen of medium-grained syenite
from Carlingford Mountain = 2°877.

From the preceding analysis we can show that this rock is a
binary compound of anorthite and hornblende. From the formula
for anorthite already given, and assuming hornblende to be a simple
silicate of protoxides, as shown from the analysis of the hornblende
of this district, we have, denoting by A and H the number of atoms
of anorthite and hornblende in the rock,—

1:033 = 3A + aH
0:555 = 2A + (1—2) H
0-715 = 2A +H.

In these equations, x denotes the proportion of silica, considered
as atomic quotient, which enters into the composition of each atom
of hornblende. .

Adding together the first two equations so as to eliminate x, and
solving from this sum and the third equation, we find

1588 =5A4+H
0-715 = 2A + H,

198 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 6,

from which we deduce
A = 0°291
H ='0°135.
Referring to the analysis of the anorthite, it is easy to see that its
atomic weight is
AO XG +54 x Qe 27x, 2,

or exactly 295; from which, multiplying by the value of A just
found, we have, finding the hornblende by difference,—

Mineralogical Composition of altered Granite.

Anorthite = 85°84
Hornblende = 14°16

100:00

On comparing this result with that obtained in page 195 from
the granite before it is metamorphosed, it is interesting to observe
that the total quantity of hornblende remains almost unaltered, and
that the effect of the addition of the limestone to the melted granite
has been to convert the quartz and orthoclase into anorthite. In
this operation, the alkalies of the orthoclase have disappeared ; the
lime, being a more fixed base at high temperatures, has altogether
displaced the alkalies ; showing on a grand scale, in the great labora-
tory of Nature, an experiment, which is in daily use on a small scale
by chemists, for the determination of the amount of alkaline consti-
tuents in an earthy mineral.

III. Granites or THE Newry District.

The Newry district of granite extends, as already described, N.E.
and S.W. about thirty miles, from Slieve Croob to Forkhill. My
examination of the granites of this chain is incomplete, but interest-
ing, so far as it has extended, as proving in this district the existence
of the two types of potash- and soda-granite, which I have established
in the granites of the south-east of Ireland.

Taking a nearly N.S. line through Newry, from Goragh Wood on
the north, through the Wellington Inn on the south to Jones-
borough, I have obtained the following results: that on this line
there is soda-granite to the north of Newry, and potash-granite to
the south; I am not prepared to say that the potash- and soda-
granites are confined to the limits here indicated, nor do I know
the relations between them; but I hope shortly to be in a position
to state more precisely the exact connexion between these two varie-
ties of granite in this district.

Potash-Granites of the Newry District.

To the south of Newry much of the granite has the character of
the medium-grained granite No. 1 of the Carlingford district, of

2 en —

vs

a a i

| " 88a6.] HAUGHTON—GRANITES OF IRELAND. 199

which it is in all probability a continuation, as shown in the accom-
panying map of parts of Down and Armagh, fig. 2. It is composed

Fig. 2.—Map of the Ulster Granites.

ZV
CRAZE

LI hj

ti

4
ie ; Potash-Granite.
N

ooo :
| 0 0° £ of Soda-Granite.
8 (2) 5) fe)

. of quartz, white feldspar, and green mica, and resembles in its phy-
| sical and mineralogical character the granite at the base of Slieve na
/ glogh. This resemblance is not confined to its external character,
but exists as to its chemical composition, as is shown by the following
analysis of the average granite, near Wellington Inn. In the cutting
of the Belfast Junction Railway near this place, numerous trap-dykes
are seen penetrating the granite, and may be traced for a considerable
distance in the small quarries of the neighbourhood.

YHA Silurian Slate.

Carboniferous
Limestone.

Wellington Inn Granite.
Quartz, Orthoclase, Green Mica.

Specific gravity =2°615.

Per cent. Atoms.
Sires ot ee TIC2ay ee 1°549
Alumina. 2. 22: 14°36 ;
Peroxide of iron. - seal 0-321
Dimes ye. ss 6k 1°48
Magnesia ...... 0°64 :
Potash: af. 4°09 0°273
Oat cle 8 3°13
Loss by ignition.. 1°50

99°80

If we assume, as in the discussion of the corresponding granite of
VOL. XII.—PART I. P

’

200 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

Slieve na glogh, that the green mica is margarodite, we readily find
by the principles so often explained:—

Q=0°505
F=0-225
M=0:048

From which we deduce—

Mineralogical Composition of Wellington Inn Granite.

Quartz...... 23°23 per cent.
Feldspar.... 61:98
Mica”. 4." 14°59

99°80

Whether we consider the physical aspect, the mineralogical cha-
racter, or the chemical composition of this granite, it is strikingly
like the granite of the base of Slieve na glogh, with which I have no
hesitation in identifymg it. Combining both together, we find :—

Mineralogical Composition of Potash-Granite.
Quartz, Orthoclase, and Green Mica, South of Newry.

Quartz...... 21°96 per cent.
Feldspar.... 64°17
AY GT ce eee ere 13°67

99:80

In the granite of Jonesborough, at the southern extremity of our
section, large crystals of white opaque orthoclase are found, of which
the following is the composition :—

Jonesborough Orthoclase.
Specific gravity = 2°546.

Per cent. Atoms.
SEH = cee ae 64:20. ow 1°40
Alumina) s . pele 0:37
Peroxide of iron.. ‘trace
ae ee 1:00
Magnesia... °. 3: 0°18
Potash’. 32 =e rel ea uae
Soda . 1°89

100:07

This analysis shows the feldspar to be a pure orthoclase.

The potash-granite, composed of quartz, white feldspar, and green
mica, common to the South Newry and Carlingford districts, pre-
sents a remarkable similarity in mineral composition to the potash-
granites of Leinster. The only question as to which any doubt
remains is as to whether the green mica is a margarodite, in which

—— = —————————— —

eee e.._|_xg_—ee—ewee —————— rere eee

1856. | HAUGHTON—GRANITES OF IRELAND. 201

peroxide of iron replaces alumina to a considerable extent, or not ;
I have been unable to determine this point by direct experiment,
either chemically or optically, from the difficulty of procuring a
sufficient quantity of pure mica for examination.

If the green mica be not the margarodite of the Leinster granites,
but similar in composition to the green mica of the Mourne Moun-
tains already described, we shall then have, taking the mean of the
atoms of the Wellington Inn and Slieve na glogh granites :—

1:°540=Q+4F+4+5M

07322 F+3M
i 0-277= F+2M.
Solving these equations, for Q, F, M, we find :—
F=0°187
M=0:045

In calculating per-centages from these results, we must use the
atomic weight of the mica found from the analysis of green mica in
page 191, which is found to be 508 instead of 304. Hence we ob-
tain finally :—

Potash-Granite of Newry and Carlingford.

Quartz. 2: 26°08 per cent.
Feldspar.... 50°76
Green mica.. 22°86

99°70

It is worthy of remark, and confirms the preceding view of this
eranite, that, if we suppose the peroxide of iron of the granite (which
is 3°54 per cent.) to belong exclusively to a mica similar to the green
mica of Mourne, we shall obtain 20°07 per cent. of mica in the gra-
nite; a result which is sufficiently near the per-centage just given.

I have neticed as a curious fact that the mica of the potash-
granites of Mourne’and Carlingford is the green mica, without any
transparent grey mica, and that the mica of the soda-granites of
Newry is a jet-black mica, identical in appearance with the black
mica which is found in the soda-granites of Oulart and Wexford ;
and that this black mica, both m Newry and Wexford, is unaccom-
panied by any of the grey margarodite of Leinster.

Soda-Granites of the Newry District.

As I have not as yet satisfied myself as to the true mineralogical
character of the type of granites to which I propose to apply the
term “‘ Soda-Granites,”’ I shall here confine my attention exclusively
to their chemical composition, which is sufficient to identify them
with the soda-granites of Wicklow and Wexford. The soda-granites
of the Newry district are characterized by the presence of black
mica, of the exact composition of which I have no means of forming

an opinion at present.
BZ

202 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

Soda-Granites of the Newry District.

Mean. | Atoms.

—————— | [tee

Silicagiys..beaests tee . . 63°34 1377

Alumina 15:28 ;
Peroxide of iron 6°88 fo ae
Lime cece bccn were : 4:34
Magnesia 2°48 f
Potash 2°67 ye
SOGA, sess. Jac Seseean ; : 368

Loss by ignition 1:01

99-82 | 99-68 |

No. 1.—Coarse-grained granite, from Newry Quarry, intersected by trap-dykes
and veins of fine-grained pink granite ; consists of quartz, white feldspar, passing
into pale pink, and black mica.

Specific gravity =2°695.

No. 2.—Coarse-grained granite, from Goragh Wood Station ; composed of quartz,
white feldspar, and black mica.

Specific gravity =2°731.

A comparison of these results with the granites of the third
isolated group of Leinster, shows a remarkable similarity, and the
column of atoms proves that this granite cannot consist of quartz,
tersilicated feldspar, and common mica.

The soda-granites of Newry agree with the soda-granites of
Leinster in the reduced per-centage of silica, in the increase of iron,
lime, and magnesia, and in the preponderance of soda over potash.

I hope, on a future occasion, to be in a condition to complete this
account of the Newry granites.

Frepruary 15, 1856.

Annual General Meeting.
[For Reports and Address see the beginning of this volume. |

Fesruary 20, 1856.
W. Howland Roberts, M.D., was elected a Fellow.

The following Communications were read :—

—

1856. | POOLE—VISIT TO THE DEAD SEA. 203

1. Notice of a Visit to the Deap Sra. By H. Poors, Esq.
[Forwarded from the Foreign Office by order of Lord Clarendon. |
[ Abstract. |

Mr. Poo te went to this district to look for nitre, which was reported
to occur there; but he met with none, and found reason to suppose
that the report was unfounded. The same word in Arabic means
‘‘ bitter or rock salt,’ as well as “‘nitre,’’ hence possibly the erro-
neous information. Further, the cave (at Usdum) in which the nitre
was said to have occurred is called ‘‘the cave of the Gun-men,”
not from the Arabs getting their nitre there for gunpowder, but as
the spot from which they watch for the crossing of the hostile tribes
across the plain.

Mr. Poole and Mr. E. Mashallam spent nearly two days at Usdum,

going to several caves (in which fine stalactites of salt occur), climb-
ing nearly to the top of the mountain, and walking about the shore,
but in no instance could they find a deposit or even a sample of nitre.
Mr. Finn, H.M. Consul at Jerusalem, also informed Mr. Poole that
he had never seen any ; nor had the Sheik Aboo Daook and his men.
The Arabs generally make their own nitre by boiling the dung of
goats; others scrape it off old walls or limestone-caves, but never in
any large quantity.
_ The Arabs charge 60 piastres or 10 shillings for a camel-load of
salt, about 500 lbs., delivered in Jerusalem, and the purchaser pays
the Turkish government 15 piastres more for duty. Each camel
will make about twenty-four trips in a year, thus carrying altogether
12,000 lbs. a year.

From Usdum Mr. Poole proceeded to El Lisan (the Peninsula),
and travelled all round it. The ridge of high land is highly im-
pregnated with sulphur; but the nodules of native sulphur are very
rare.

At the present time it would be almost impossible to do anything
on El Lisan, for the road between it and Usdum is open to the
attacks of four independent tribes of Bedouins, including the Sultan
of Kerak, over whom the Turkish government has no control.

Previously to visiting Usdum, Mr. Poole made a trip to the
northern end of the Dead Sea. At Nebi Mousa (half-way from
Jerusalem to the Dead Sea), there is a quantity of bituminous shale
or ‘‘ blind coal,” from which ornaments are cut; and a thick bed of
soil highly impregnated with sulphur occurs there. Nothing but
saline incrustations were found on the north shore of the Dead Sea.

The author exhibited to the Meeting a series of the specimens of
sulphur, sulphurous earths, salt, and other minerals from the vicinity
of the Dead Sea, together with recent natural-history specimens,
volcanic and other rock-specimens, and some tertiary and cretaceous
fossils* from the district visited.

* For descriptions and figures of a series of fossils from this and other districts
in Palestine, see Conrad’s ‘ Appendix to Lieut. Lynch’s Official Report of the U.S.
Expedition to explore the Dead Sea and the River Jordan.’ 4to. Baltimore,
1852.—Ep.

204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

2. On the Arrinitiss of the LARGE EXTINCT Birp (GASTORNIS
PARISIENSIS, Hébert), indicated by a Fossil Femur and Tibia
discovered in the Lowrst Kocenr Formation near Parts.

By Prof. Owen, F.R.S., F.G.S., &c.
[Puate III.]

Peruars no part of the progress of Paleeontology, since the demise,
in 1832, of the founder of that science, has been more striking and
unexpected than that which relates to the discovery and restoration
of giant members of the feathered Class.

First indicated by the foot-prints in the New Red Sandstones of
the valley of the Connecticut, described by Hitchcock, in 1836* ;
next demonstrated by the evidence of the bones themselves from the
recent deposits in New Zealand, in 1839+ and 18431; afterwards
exemplified by the great eggs and associated fragments of skeleton
discovered in alluvial banks of streams in Madagascar, in 1851§; the
list of extinct giant birds has lastly been recruited by the fossil
remains of a species, at least as large as an Ostrich, from the Eocene
conglomerate || at Meudon near Paris, which lies between the plastic
clay and the surface of the chalk.

It is this last example of extinct Birds, discovered in the early
part of the year 1855, which is the subject of the present com-
munication. Associated, as I have been, with the work of recon-
structing gigantic species of that class, I received immediate
notice of the discovery by M. Gaston Planté and M. Hebert of
the fossil bones which indicated the large bird in question,
in letters from scientific friends at Paris, and more especially from
the accomplished ornithologist, Prince Charles Lucien Bonaparte,
then occupied in completing his admirable and celebrated summary
of the:genera and species of Birds, by a record of all the known
fossil kinds. :

On my arrival in Paris on the service of the Jury of the Universal
Exhibition of 1855, the specimens themselves, consisting of an almost
entire tibia (Pl. III. figs. 1 a & 14) and the shaft of a femur, were
brought to the Institut, by MM. Hébert and Lartet, to be shown to
me; and, on my expressing the wish to carry out a series of com-
parisons with the answerable bones in other birds, accurate and
beautifully prepared coloured casts of the fossils were most liberally.
and kindly made and presented to me before my return to London,
with the desire that I would endeavour to arrive at some definite
conclusion as to the nature and affinities of the bird to which the
fossils belonged. In the meanwhile the opinions of M. Hebert,

* In the American Journal of Science and Arts, January 1836, vol. xxix.

+ Zoological Transactions, vol. iii. p. 29. t Ib. vol. iii. p. 235.

§ Isidore Geoffroy St. Hilaire, in Comptes Rendus de l’Académie des Sciences,
Paris, January 27, 1851.

| Particularly described by D’Orbigny, in the Bulletin de la Société Géologique
de France, lére série, vol. vii. p. 280.

4 The uppermost cretaceous stratum called caleaire pisolithique.

eee

1856. ] OWEN—GASTORNIS PARISIENSIS. 205

Director of the Scientific Instruction at the ‘Ecole Normale supé-
rieure,’ of M. Lartet, the well-known and accomplished Palzeontologist
of the tertiary formationsin middle and southern France, and of Prof.
Valenciennes were briefly recorded in the notice of the discovery of
the tibia, communicated to the Institut, in March, 1855*. In the
month of June in the same year M. Hébert communicated to the
Academy of Sciences, his discovery of the femur, at about 3 métres
of horizontal distance from the spot, and in the same formation,
where the tibia had been previously found by M. Gaston Planté.

The femur is the shaft of that bone of the left limb, with both
articular ends broken away: it measures 11} inches in length, and
2 inches by 1 inch 9 lines in the two diameters of its middle part.
The entire femur of a large male Ostrich measures 13 inches in
length; and 2 inches by 1 inch 5 lines in the two diameters of its
middle part.

The tibia also has its proximal end broken away and its distal
condyles mutilated : its length, when entire, would be 1 foot 7 inches :
it 18 1 inch 9 lines by 1 inch 6 lines in the diameters of the middle
of the shaft. The tibia of a large male Ostrich measures’ 1 foot
114 inches in length; the diameters of the middle of the shaft being
1 inch 6 lines by 1 inch 3 lines.

The femur of the Parisian eocene bird, for which the name
Gastornis Parisiensis has been proposed, has a rounder and thicker
shaft in proportion to its length than in the Ostrich, and the tibia
is shorter and thicker than in the Ostrich; whence, as M. Hébert
rightly infers, the Gastornis was a proportionally heavier bird than
the Ostrich. In the size and proportions of the two above-specified
bones of the leg it closely corresponds with the species of Dinornis
which I have called Dinornis caswarinus (figs. 2a &26). As the
conclusions, in reference to the more immediate affinities of the Gast-
ornis, to which the above-cited able naturalists and paleontologists
of Paris have arrived, were founded almost exclusively on the cha-
racters presented by the lower or distal end of the tibia, I shall pre-
mise a brief summary of the leading modifications of that part of the
skeleton in the different orders of the class of Birds.

Characters of Birds’ Tibie.—The tibia is a well-marked and
characteristic bone in birds. At the proximal end the intercondyloid
convexity is more marked than the entocondyloid concavity, which
is the principal articular surface there developed: next may be
noticed the strong rotular process dividing into the procnemial and
ectocnemial ridges. Below and behind these is the usually short
fibular ridge, marking the outer side of the proximal third or fourth
part of the shaft. The distal end of the tibia resembles that of a
mammalian femur, with the back of the two condyles turned forwards.
All these characters, common to birds in general, distinguish this

* Compte Rendu, Mars 12, 1855.

tT First so named and defined in my memoir on the Dinornis of June 1846,
Zool. Trans. vol. iii. p. 323; these ridges are not developed in the Hornbill
(Buceros).

206 PROCEEDINGS OF THE GEOLOGICAL society. ([Feb. 20,

bone from that of all other known existing animals: save as regards
the proximal end, they are sufficiently evident in the tibia of the
Gastornis, and permit no manner of doubt as to the class of animals
to which that bone belongs. There is, however, a great range of
variety in some of these, and of other less constant, characters of the
birds’ tibia.

In comparing the distal end of the tibia, attention must be paid to
the following points :—Relative breadth and depth of that end:
Relative size and shape of the anterior productions of the condyles,
fig. 2, a, 6, and of the mterspace between them : Configuration of the
rest of the trochlear surface, fig. 2, a, d: Presence or absence of a
bridge, e, completing a canal, f, for the exterior tendon of the toes
on the fore-part of the distal end of the tibia: Direction, position,
and size of the bridge: Position and aspect of its lower outlet, g ;
Entocondyloid, h, and ectocondyloid, 2, surfaces,—or those that are
found on the inner side of the inner condyle, a, and the outer side
of the outer condyle, 6.

The distal end of the tibia varies in its degree of expansion as
compared with the shaft, in the relative prominence and thickness of
the condyles, in the width and depth of the intercondyloid space, and
especially in modifications of the anterior surface above that space.

This surface is traversed by the ‘ extensor communis’ tendon of the.

toes, and here the tendon, in all young birds, is strongly bound down
by a more or less oblique or transverse ligament, which in most
species becomes ossified before full growth is attamed: it then forms
the ‘bridge’ or ‘supra-tendinal bridge,’ e. The existing Struthio-
nide, viz. the Ostrich, Rhea, Emeu, and Cassowary, are exceptions,
also the Hornbills and Parrots: in them the ligament retains its nature
throughout life.

Order RApPTORES seu ACCIPITRES.

In the Sea Eagle (Haliaétus albicilla) the breadth of the condyles
exceeds the depth*; the anterior convexities each equal the inter-
condyloid depression: the posterior trochlear space is broad and
oblique. The bridge is broad, median, and very oblique from above
downwards and outwards. Below the bridge a thin transverse rising
bounds the intercondyloid depression above. There is a shallow de-
pression at the sides of the distal end, above each condyle; an
obtuse tubercle projects from the middle of the mner concavity.
The inner side of the shaft is thinner than the outer one, which is
contrary to the proportions of the part in most birds.

In the Vulture (Sarcoramphus papa, fig. 3) the depth and breadth
of the condyles are nearly equal ; the imner one is smaller than the
outer ; the bridge lies to the inner side of the mid-line, and is more
nearly transverse than in the Eagle. A small fossa is defined by a
transverse ridge at the intercondyloid space: the tuberosity in the
depression above the inner condyle is less developed. The posterior

* By depth I mean the fore-and-aft, or antero-posterior diameter.

> emmiees~

-
a ee eee -

-~ ee a

1856. | OWEN—GASTORNIS PARISIENSIS. 207

trochlear surface is narrow and slightly concave. The fibula is not
anchylosed to the tibia in the Vulture.

Order INSESSORES.

In the Raven (Corvus coraz, fig. 4) the breadth and depth of the
_ condyles are nearly equal: the condyles are of the same size, and are
equally prominent behind ; the intercondyloid space is wider than
either condyle; there is a depression in it, bounded above by a
transverse ridge. The bridge is broad, median, and nearly transverse ;
the canal is rather oblique. The posterior condyloid surface is
divided by a median longitudinal rising. The sides are slightly con-
cave: there is a low protuberance in the inner one.

The Crow (Corvus corone) shows but a feeble rudiment of the
ridge at the narrow posterior condyloid surface : the anterior inter-
condyloid space equals each condyle: the depression in it is well
marked: the bridge is broader than in the Raven. The tubercle in
the shallow entocondyloid surface is minute.

In the tibia of the Hornbill (Buceros), the pro- and ecto-cnemial
ridges are rudimentary. At the lower end of the bone the breadth of
the condyles exceeds their depth : the inner condyle is longer, broader,
more prominent posteriorly, but not anteriorly, than the outer one.
The intercondyloid space equals the outer condyle: the depression in
that space is deep, and well-defined by the superior transverse bar :
above this the narrow ligamentous bridge remains unossified. Poste-
riorly the condyles are divided by a deep and narrow longitudinal
groove ; the sides are slightly concave.

Order SCANSORES.

In the Parrot (Psittacus) the breadth of the condyles exceeds the
depth : the intercondyloid space is rather broader than either condyle,
and retains its depth and breadth from the fore to the back part of
the trochleee. The intercondyloid fossa is a transverse groove at the
lowest part of the space. The bridge is unossified.

In the Woodpecker (Picus viridis) the procnemial ridge extends
down the inner side of the proximal third of the shaft. The breadth of
the condyles a little exceeds their depth: the intercondyloid space is
broader than each condyle, which are equal in degree of convexity
and prominence anteriorly: the condyles contract to.mere ridges
behind. Here the space is divided by a low median longitudinal
rising. The intercondyloid fossa is broad and deep. The bridge is
broad ; its lower outlet forms a small foramen.

Family CotumMBID2.

In the Crown-Pigeon (Lophyrus coronatus, fig. 5) the depth of the
inner condyle exceeds the breadth of that end of the tibia. The
anterior convexities of the condyles are subequal, the inner one being
rather more prominent. The intercondyloid space is of the breadth

208 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

of each condyle. The posterior trochlear surface is very slightly
concave transversely. The sides of the condyles are almost flat.
The bridge is broad, transverse, submedian: the canal is narrow,
with the lower outlet oblique and close to the inner condyle.

Order GALLINZ.

In the Curassow (Crax Alector) the breadth and depth of the
condyles are equal; their anterior convexities slope gradually to the
intercondyloid space, which has a small well-marked pit at its lower
part; the sides of the condyles are very shallow, the outer ligamentous
tubercle is slightly marked. The bridge is a little to the inner side
of the mid-line, and is very broad, subtransverse; with the lower
outlet oblique, and close above the inner condyle. .

In the Cock (Phasianus gallus) the condyloid convexities are
more distinct, or relieved from the intercondyloid space, than in the
Curassow (Craz), and the fossa in that space is less marked :—in
other respects the same characters prevail.

In the Turkey (Meleagris gallopavo, fig. 6) the relative breadth
of the distal end of the tibia is rather greater; it has a relatively
narrower bridge and a wider canal than in the Cock ; the bridge is
rather nearer the mid-line; external to the bridge is a low tubercle,
just above the outer condyle : a narrow and shallow canal divides the
bridge from the tubercle; the fossa, at the bottom of the intercon-
dyloid space, is well-marked. In other respects the tibia of the
Turkey closely resembles that of the Cock.

Order GRALLZE.

In the Bustard (Otis tarda, fig. 7) the breadth and depth of the
distal end are subequal: the condyles slope to a very narrow inter-
space: they are equal, but the innermost is most prominent, and
most convex. The bridge, on the imner half of the bone, is broad,
subtransverse, supporting a transverse ridge, which bounds above the
cavity into which the lower outlet of the canal opens. The posterior
part of the trochlear surface is deeper, its borders being more pro-
duced and sharper than in the Turkey and other Galline. The
ectocondyloid surface is slightly concave, with a median tubercle ;
the entocondyloid surface is more concave, with a larger tubercle
near the anterior end of the inner condyle. The groove leading to
the bridge has a ridge on the inner side, but none on the outer side
of the bone.

In the Adjutant Crane (Ciconia argala) the depth exceeds the
breadth of the lower end of the tibia more than in any other bird :
the condyles are equal; the interspace is very short and narrow;
that space is represented by the deep cavity formed by the tubercle
and ridge developed from the bridge above, and by the oblique con-
verging upper borders of the condyles below. The bridge is very
broad, internal; the lower outlet is round, looks obliquely down-
wards and forwards, and opens into the supracondyloid concavity two

ee indie

1856.] _ OWEN—GASTORNIS PARISIENSIS. 209

lines above the inner condyle. The lower and hinder trochlear space
is concave transversely ; the lateral surfaces are slightly concave.

In the Seres Crane (Grus Antigone, figs. 8 a, 86) the breadth
and depth of the condyles are equal. The intercondyloid space
(answering to the supercondyloid in the Argala) exceeds in breadth
either condyle ; of these the inner one is the shorter in vertical extent,
and is the more convex and prominent one: the outer and vertically
longer condyle slopes gradually to the wide mid-space, which shows
no special pit or depression. The canal leading to the bridge is
broad, but is defined by a well-marked ridge on each side; the
bridge is to the inner side of the mid-line, is very broad, transverse,
with a transversely-oblong lower outlet pretty close to the mner
condyle, looking directly forwards. ‘The chief peculiarity is a
tubercle, external to this aperture. The lower border of the outlet
defines, with the tubercle, or bounds above, the shallow intercondyloid
or supra-condyloid space; but there is no special depression. The
posterior condyloid space is deeper than in the Gallina, especially
towards the inner side, the bounding ridge of which is well-marked :
the under surface is flattened. The outer side of the condyle shows
a middle low tubercular ridge ; the inner side is rather more concave,
with a rising near the base of the anterior prominent part of the
condyle.

In the Common Stork (Grus nigra) the breadth of the condyles
anteriorly rather exceeds their depth. The trochlear space is rather
flattened at its under surface ; and in all the other modifications the
correspondence with the Grus Antigone is close. The fore part of
the trochlea is more remarkable for the tubercle external to the
bridge than for the depth of the depression (intercondyloid or super-
condyloid space) below the bridge.

In the Heron (Ardea cinerea) the depth a little exceeds the
breadth of the condyles: the intercondyloid space is twice the width
of the inner condyle, which is rather narrower than the outer one:
the bridge is broad, oblique, internal : the lower outlet is transversely
oval ; immediately above the inner part of the intercondyloid space,
which is shallow and has no special depression. There is no tubercle
or ridge upon the bridge; the posterior trochlear surface is concave
transversely.

In the Spoonbill (Platalea leucorodia) the depth of the condyles
exceeds the breadth. The intercondyloid space is deep, and is wider
than either condyle, which are narrow and prominent: the trochlear
surface is flattened below, and is shallow behind. The bridge is near
the inner border, and is broad and transverse : a low ridge is continued
from it outwards, which forms the upper boundary of the shallow
super- or inter-condyloid space: there is a slight special depression
in this space just below the outlet of the bridge. The ectocondyloid
surface is almost flat: the entocondyloid one has the tubercle for
the attachment of the lateral ligament.

- In the Hematopus the breadth of the distal end of the tibia
exceeds the depth. The intercondyloid space equals the outer and
exceeds the inner condyle: the outer one slopes more gradually to it :

210 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

the rest cf the trochlear surface is a little concave transversely, with
a feeble median rising behind. The bridge is to the left of the mid-
line, short, and transverse: the lower outlet is above the imner
side of the intercondyloid space: its lower border bounds above the
shallow cavity at the upper part of, and continuous with, that space.
There is a short ridge on the outer side of the bridge: the ecto- and
ento-condyloid surfaces are as in Grus.

The distal end of the tibia of the Woodcock (Scolopax rusticola)
closely conforms to that of the Oyster-catcher. The trochlea is a
little flatter below, and the inner condyle is relatively smaller and
more prominent: the lower border of the bridged canal, and a ridge
continued outwards from it, define the shallow intercondyloid cavity
above.

In the Gallinule (Gallinula chloropus, fig. 9) the bridge is broad,
transverse and submedian: the lower outlet is large, and opens
above the intercondyloid space, in which no particular cavity is
defined. The canal leading to the bridge is broad, deep, and bounded
by a ridge on each side. The inner condyle is much narrower than
the outer one: the trochlear space is not flattened below ; it is
narrow and. concave behind.

In the Notornis, or large short-winged Coot of New Zealand,
figs. 10a, 106, the breadth rather exceeds the depth of the con-
dyles: the intercondyloid space is more than twice the breadth of
either condyle. The bridge is of moderate breadth, transverse and
median in position: its lower outlet is a transverse ellipse, looking
forwards, just above the wide and shallow intercondyloid space: the
canal leading to the bridge is wide and deep, with a boundary ridge
on each side: the under and back parts of the trochlear surface are
broader and flatter than in the Gallinule. The narrow inner con-
dyle is very prominent. ,

The Aptornis (figs. 11 a, 11 6) chiefiy differs from the Notornis
in the less median position of the bridge, and the less depressed sur-
face external to it: also in the much shallower canal leading to it,
which has no external boundary ridge; the intercondyloid space,
though wide and shallow, is less so relatively than in the Nofornis :
in other respects the tibize of this and the foregomg New Zealand
birds resemble each other at the lower end.

Order CurRsoRES.

In the Apteryx (fig. 12) the breadth and depth of the condyles
are equal: the inner one is the more prominent ; the intercondyloid
space is rather narrower than either condyle. The bridge—some-
times unossified—is internal; external to it the surface of the bone
is moderately convex, and divided by a transverse linear groove from
the intercondyloid space, in which is no special depression. The
hinder trochlear space is slightly concave transversely.

In Dinornis (figs. 2a, 2 6) the breadth and depth of the condyles
are equal: the outer condyle (4) is the broader, the inner one (a) is
the more prominent ; their articular surfaces are so continuous as to

—

1856. | OWEN—GASTORNIS PARISIENSIS. 211

leave no space answering to the intercondyloid one in Aptornis,
Notornis, &c.; but the continuous surfaces form a ridge which
bounds below the supracondyloid space, the same being bounded
above by the ridge extending outwards from the supratendinal
bridge, e. This is nearer the inner side of the bone, is subtransverse,
rather narrow, with a widely elliptical lower outlet opening above
the inner condyle: the canal (/) leading to the bridge has an internal
boundary ridge : a shallow longitudinal groove divides the outer side
of the bridge from a tuberosity above the outer condyle. The under
and hinder parts of the trochlear surface are concave transversely.

In the Ostrich (Struthio camelus) the breadth and depth of the
condyles are equal: they are less produced anteriorly than in other
birds, and their articular surfaces are so continuous as to leave no
well-defined intercondyloid space; that surface projects in a trans-
verse concave line some way in advance of the supracondyloid space,
which is marked by a submedian transverse ridge or broad tubercle,
external to which is a rounded depression. There is no supratendinal
bridge or groove. The under trochlear surface is broad and slightly
concave from side to side; posteriorly it is deepened by the develop-
ment of its borders, of which the inner one is the sharpest and most
suddenly produced. This surface is traversed by a slight median
longitudinal rismg. The ectocondyloid surface is concave, and has a
pit fitting the end of a finger. The entocondyloid surface shows a
deep pit near its anterior part, whence a wide groove curves back-
wards, becoming broader and shallower to the posterior part of the
condyle. The distal condyles expand more suddenly beyond the
shaft than in most birds.

Order NATATORES.

In the Swan (Cygnus ferus) the breadth and depth of the con-
dyles are equal: the intercondyloid space, fig. 13, a, exceeds either con-
dyle: it has a very shallow transverse fossa. The bridge, e, of mode-
rate breadth, is median, transverse, and straight ; it spans a wide and
deep canal, the lower aperture of which looks forwards and opens
immediately above the intercondyloid space. The canal leading to
the bridge has no lateral sharp ridge: the mner border is most
developed and is rounded.. The under and hinder trochlear surface
is very slightly concave transversely. Both ecto- and ento-condyloid
surfaces are flat.

I have received from the brick-earth at Grays, in Essex, the lower
end of a fossil tibia (figs. 13 a, 13 6) corresponding precisely in the
modifications of its distal end with those of the Cygnus ferus: it is
very little larger than the tibia of the Wild Swan, and may be of the
same species. The bone had undergone the same change as the bones of
the Elephas primigenius, Rhinoceros tichorhinus, &c., from the same
formation.

The above characters are very closely repeated in the Goose
(Anser palustris) : the bridge is broader in proportion to the size of
the canal. The under surface of the trochlea has a feeble median

|

212 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

prominence, as in the Swan. The inner border of the canal above
the bridge is more defined than in the Swan.

In the Falkland Island Goose, the tendinal canal is more oblique
and its lower outlet more to the mner side than in the Common
Goose.

In the Pelican (Pelecanus onocrotalus), the lower end of the tibia
is less expanded than in the dnatide and most extinct birds: the
breadth and depth are equal. The intercondyloid space is wider than
either condyle, which are alike. The bridge is median, but narrow
and oblique; spanning a wide and deep canal, the lower outlet of
which looks forward, opening immediately above the intercondyloid
space. The posterior trochlear surface is nearly flat transversely,
and has a low and broad median rising.

The Great Gull (Larus marinus), with the breadth and depth of
the expanded lower end of the tibia equal, has a wide intercondyloid
space ; the inner condyle is more prominent, and is shorter than the
outer one: the posterior trochlear surface is concave across. The
bridge is submedian, narrow, descending rather obliquely from the

inner to the outer side; spanning a wide canal, with the lower outlet

above the intercondyloid space, and separated from it by a feeble
narrow ridge. The canal leading to the bridge is broad, and is
bounded on each side by a short sharp ridge.

In the Albatros (Diomedea exulans, fig. 14), the breadth, depth,
and prominence of the condyles are equal; but neither of them is
so broad as the intercondyloid space. The bridge is submedian,
transverse, broad, with the lower outlet of the wide canal transversely
elliptical and large, looking directly forwards, just above the imner
half of the intercondyloid space, and situated relatively lower down
than in the Swan. The trochlear articular surface is not produced
forwards in advance of the intercondyloid space, nor does that space
show any fossa or depression.

In the Alca torda, the breadth a little exceeds the depth of the
condyles, These are subequal, with a wide intercondyloid space: the
posterior trochlear surface is very slightly concave across, and with a
feeble median rismg. The bridge is submedian and broad: the
inner ridge of the canal leading to it is most developed, the lower
outlet is transversely elliptical and just above the intercondyloid
space. The ectocondyloid surface is flat: the entocondyloid one is
subconcave, with a median tubercle.

In the Grebe (Colymbus glacialis)—so remarkable for the modi-
fication of the proximal end of the tibia,—the distal end of the bone
deviates little from the usual natatory type. The wide intercondy-
loid space is deeper, the narrow convex condyles being more pro-
duced than in the Albatros and Anatide. The posterior trochlear
surface has a well-marked outer ridge, and a feeble median rising.
The bridge is median, transverse, very narrow in the middle, spanning
a very deep and wide canal, the large lower aperture of which looks
directly forwards, opens just above the intercondyloid space, and has
a thin sharp lower transverse border. The canal leading to the
bridge occupies almost the whole of the breadth of the bone.

1856. | OWEN—GASTORNIS PARISIENSIS. 213

Comparison. — Having premised the foregoing remarks on the
modifications of the distal end of the tibia in some existing examples
of every order of birds, I proceed to apply this knowledge to the
elucidation of the nature of the fossil tibia of the Gastornis dis-
covered in the lowest eocene beds in the vicinity of Paris. |

In this fossil, fig. 1, the distal end is much mutilated : the anterior
projecting convexities of both condyles are broken away, and both
the under and posterior trochlear surfaces are to a certain extent
wanting: a small tract of the original smooth articular surface remains
there, and a smaller portion is left on the broken outer condyle.
The proportion of breadth to depth of this end of the bone is,
therefore, indeterminable in the sole example discovered. It would
seem as if the anterior intercondyloid or supercondyloid surface had
been divided from the articular surface by as abrupt a transverse bar
as in the Ostrich, Dinornis, and certain Gralle; and the under sur-
face appears to have had a similar extent and contour of surface to
that in the Gruide: it seems to have been broader and flatter than
in the Dinornis. Posteriorly the trochlea is relatively as broad as in
the Galline, and is broader than in the Gralle. The rough frac-
tured base of the inner condyle shows that the intercondyloid space
was relatively narrower than in the Anatide, and most other water-
birds. The supratendinal bridge is more median in position than in
most of the Gralle ; though not more so than in the Gallinule and
Oyster-catcher. This median position, though common in the Nata-
tores, is not peculiar to them. The Curlew, Notornis, Raven, Eagle,
and the Crown Pigeon have a similar position of the bridge.

The direction of the bridge appears to have been nearly transverse ;
but much of it is broken away. The canal leading to it is bounded by
a well-marked ridge internally, but seems to want an outer boundary :
the aspect of the lower opening is obliquely forwards and downwards,
as in the Galline and some Gralle; not directly forwards, as in
most Natatores. As to the distance of that opening from the lower
surface of the trochlea, it is not relatively greater than in the Turkey,
the Cock, the Gallinule, and the Anatide. The depression beneath
that outlet in the fossil, if it be natural, is a peculiarity I do not find
in any Wading-bird. The depression above the articular trochlear
surface in the Bustard, e.g.,is one intowhich the tendinous canal opens,
and is chiefly due to the transverse ridge developed from the bridge
spanning the canal. In the Argala it is due to the strong tubercle
similarly developed above the outlet of the canal; in the Grus to a
similar tubercle projecting forwards external to the outlet.

The Curlew (Numenius arcuata, fig. 15) and Oyster-catcher
(Hematopus) show a more shallow depression below the outlet.
The smooth surface of the middle of the depression on the outer side
of the condyle appears to indicate its concavity, but the border is too
much broken away to enable one to judge of its original depth.

The relative breadth of the posterior part of the trochlear surface
agrees with that in the Turkey and the Swan; but the borders are
here, also, too much broken away to enable one-to determine its

214 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

original degree of concavity: the margins were, however, evidently
more developed than in the Swan.

The general proportions of the fossil tibia from the Paris eocene,
fig. 1, are most like those of the Dinornis casuarinus, fig. 2: the size
is nearly the same. The differences at the distal end are seen in the
more median position of the supratendinal bridge, e, in the Gastornis;
it is close to the inner side in the Dinornis ; in the absence of the
depression below the outlet in the Dinornis ; in the greater posterior
breadth of the trochlea in Gastornis; and in a greater antero-poste-
rior diameter of the inner side of the shaft. The shallow groove and
low tuberosity external to the canal are present in both these extinct
birds.

From the tibia of the Solitaire (Pezophaps), that of the Gastornis
differs in the more median position of the bridge, and in the depres-
sion below the bridge: in other respects it makes*a close approxima-
tion to that extinct bird.

The Aptornis further differs from the Gastornis in the wider inter-
condyloid space, and in the narrower and (probably) more prominent
inner condyle ; but the mutilated state of that part in the Parisian
fossil prevents a decided opinion on this point.

The Noéornis resembles the Gastornis in the median position of
the bridge, but differs in the absence of the depression below it, in
the aspect and shape of the lower outlet, in the wider intercondyloid
space and narrower inner condyle, and in the well-developed outer
boundary of the canal leading to the bridge.

Conclusion.—Having made the foregoing observations and com-
parisons of the tibize of recent and fossil birds with that of the Gas¢-
ornis, as much as possible independently of any preconception or bias
from previous opinions published as to the nature and affinities of that
bird, I propose to review those opinions, commencing with the remarks
of M. le Prof. Hébert, who has given a very accurate description of the
fossilin question. After rightly pointing out the gradual increase of
the transverse over the antero-posterior diameter of the bone as the
lower fourth of the shaft approaches the condyles, he remarks :-—
“‘ Cet aplatissement du tibia est trés remarquable et constitue un bon
caractére distinctif*.’’ It offers a marked difference as compared
with the tibia of the large species of Crane (Ciconia), Stork (Grus),
Bustard (Otis), and most Waders, and also from the Galline and
the Natatores, especially in the development of the ridge or angle
between the fore and outer surfaces of the bone leading to the outer
condyle. The Eagle shows something like this, which is due to the
anchylosed lower point of the fibula, which forms the corresponding
ridge ; the lower third of the tibia in all the great Aquiline birds is
proportionally more compressed from before backwards ; but the inner
side is by no means so thick antero-posteriorly. The correspondence,
however, between the Gastornis and the Dinornis casuarinus in the
general form and proportions of the lower end of the tibia is very

* Compte Rendu de l’Académie des Sciences, Mars 12, 1855, p.579.

1856. | OWEN—GASTORNIS PARISIENSIS. 215

close ; and the same may be said with regard to the Aptornis and
Notornis. The outer ridge is not developed in the Pezophaps. The
fibular crest, supposing it to be entire in the fossil, is not so strongly
developed as in the Swan, the Pelican, and other Natatores, or as in
the Ciconia, Otis, Notornis, and other Gralle; the proportions of
that ridge in the Turkey and other Galline most resemble those in
Gastornis. . |

As to the form and extent of the inferior trochlear articular surface,
nothing precise can be affirmed of its much-mutilated condition in
the fossil: the development of the boundary margins and prominent
condyles in perfectly preserved tibie of Dinornis, Palapteryz,
Aptornis, &c. has so much surpassed any indications given by the
first-received mutilated bones of those extinct birds, that due caution
has been impressed upon me in regard to inferences from abraded
bases of such promirfences of their natural state. Far from inferring
a flattened surface on the non-articular sides of the condyles of the
Gastornis*, the rugged broken peripheral tract surrounding the
small portion of the natural surface intimates the concavity which
one would find there were the borders of those lateral surfaces
perfect.

The Dinornis, Pezophaps, Notornis, Platalea, Crax, Turkey, and
Common Fowl have the lateral surfaces in question as flat as in the
Lamethrostres, or as it is possible for them to have been in the
Gastornis. No especial affinity of the Paris fossil to any tribe of
aquatic birds can be inferred from the external or lateral surfaces of
the condyles. The greater prominence of the upper and fore part of
that surface of the inner condyle (“ malléole interne,” Hébert) is a
character common to most birds of every order: a strong lateral
ligament is attached to that prominence.

Interesting unquestionably is the median position of the supraten-
dinal bridge in Gastornis+, and it would satisfactorily indicate its
affinities to the Swan and Goose, were not the same bridge equally
medianly situated in the Gallinule, the Notornis, the Raven, some
Accipitrine birds, &. Amongst the Galline, also, the Turkey so
nearly resembles the Gastornis in the position of the bridge, and so
much more closely resembles it than does the Swan or Goose in the
low tuberosity external to the bridge above the base of the outer
condyle, and in the shaliow groove dividing that tuberosity from the
bridge, that I should infer an affinity of the Gastornis to the Gall-
nacea from the characters of the bridge, rather than to the Lamelli-
rostres. That very inclination of the canal to the inner side, and
the position of the lower outlet to the left of the median plane, in the
Gastornis, while it is a departure from the anserine type, is an ap-
proximation to the Gallinaceous and Dinornithic structures. The
lower outlet of the tendinous canal, while it is relatively higher in

* “ Les deux condyles portent latéralement en dehors une facette plane, comme
chez les Palmipédes lamellirostres, et non-excavée comme cela a lieu chez
l’autruche et les autres courenrs.”—TIb. p. 579.

t “L’arcade ossense est située 4 peu prés dans la partie médiane de la face
antérieure, comme dans le cygne et l’oie.””—1b. p. 580.

VOL. XII.—PART I. Q

_ /
~

216 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

Gastornis than in the Lamellirostres, does not appear to me to have
been more above the level of the trochlear surface than in the
Aptornis, Pezophaps, Dinornis, or the Gallinacea. I believe, indeed,
that, if the prominent anterior parts of the condyles had been pre-
served in the Gastornis, the appearance of the high position of the
bridge would have been much modified. The aspect, or plane, of the
lower outlet offers a useful character of comparison, and it appears
to me that it can be judged of in the Parisian fossil. The border of
the outlet is sufficiently entire to show that its upper and inner part
was most prominent, causing the outlet to look a little downwards as
well as forwards, or in some degree into the supra-condyloid cavity
below the canal. Now in the Lamellirostres, and in the Diomedea
and other Longipennate Palmipeds, the corresponding foramen looks
directly forwards: its plane is vertical, or, if inclined therefrom, it is
by the greater projection of the lower border. ‘This foramen being
relatively lower in the Albatros than in the Swan, makes the Albatros
depart further from Gastornis.

In the aspect of the lower outlet of the tendinous canal, the Gas¢-
ornis more resembles the known large wading and land birds and
the Dinornithide, than it does any aquatic bird; this character
appears not to have been taken into consideration in previous com-
parisons of the Gastornis. The fossa beneath the canal, bounded
below by the projecting border of the intercondyloid trochlear
surface, is a character which, though not precisely repeated, as to
the form, proportion, and position of that fossa, in any of the
Grallatores, finds its nearest correspondence in the usually larger
cavity at the corresponding part of the tibia in most birds of
that order: and I concur with MM. Hebert and Lartet in deeming
the fossa in question to indicate more directly an affinity of the
Gastornis to the Grallatorial order, than any other character
which the fossil bone presents. The anterior border of the trochlear
surface presents a similar projection in the Dinornis ; it bounds a
cavity below, which has its upper boundary in the ridge continued
transversely above the bridge, and into which the lower outlet of the
canal opens, as in the Bustard. The Swan, the Albatros, and other
Palmipeds show no trace of this anterior prominence of the trochlear

border ; nor can any more trace be seen of a fossa below the ten-.

dinous canal in the Albatros, than in the Swan or Goose. The
proportions of the tibia—its thickness, e. g., in proportion to its
length—would plainly show, however, that the Parisian eocene bird
had more robust and shorter legs than in the typical waders ; and
probably was, as in other birds of like dimensions, better adapted
for terrestrial life. The result of the numerous comparisons which I
have made lead me entirely to concur in the final conclusion of
M. Hebert, viz. that the Gastornis belongs to a genus of birds
distinct from all previously known.

|

cs
Sines

1856. | OWEN—RED CRAG MAMMALS. - RMEZ

DESCRIPTION OF PLATE III.

Fig. la. The fossil tibia of the Gastornis parisiensis, nat. size.

Fig. 16. The lower articular surface of the same bone.

Fig. 2a. The lower end of the tibia of the Dinornis casuarinus, nat. size.
Fig. 24. The lower articular surface of the same bone.

Fig. 3. The lower end of the tibia of the Vulture (Sarcoramphus papa).

Fig. 4. Jb. ib. ib. Raven (Corvus corax).

Fig. 5. 20. ib. ib. Crown Pigeon (Lophyrus corona‘us).
Fig. 6. 6. ib. ib. Turkey (Meleagris gallopavo).

Migs t., La * tb. ib. Bustard (Otis tarda).

Fig. 8a. Ib. ib. (65.5% Seres Crane (Grus Antigone).

Fig. 8. The lower articular surface of the same bone.

Fig. 9. . The lower end of the tibia of the Gallinule (Gallinula chloropus).

Fig. 10a. Ib. * ib. ab. Notornis Manteli.

Fig. 104. The lower articular surface of the same bone.

Fig. lla. The lower end of the tibia of the Aptornis otidiformis.

Fig. 116. The lower articular surface of the same bone.

Fig. 12. The lower end of the tibia of the Apteryx australis.

Fig. 13a. Ib. - ib, ib. of a Swan (Cygnus ferus?): fossil, from a
pleistocene formation.

Fig. 135. The lower articular surface of the same bone.

Fig. 14. The lower end of the tibia of the Albatros (Diomedea exulans).

Fig. 15. The lower end of the tibia of the Curlew (Numenius arcuata).

3. Description of some MamMauiaNn Fossixs from the Rep Crac
of SurFoLK. By Prof. Owen, F.R.S., F.G.S.

SincE my description of the mammalian fossils of the Red Crag,
collected by Sir Charles Lyell at Newbourn, Suffolk, in 1840*, and
the publication of the ‘ History of British Fossil Mammalia,’ in which
these and subsequently discovered Cetacean Crag fossils were figured,
I have visited several localities where the Red Crag is worked for
phosphatic nodules, in Suffolk, and have myself collected, and have
received from other collectors, numerous specimens of mammalian
remains, from the Red Crag, of which I have selected the following
as most worthy of being described. |

Genus Rhinoceros.

There is some difficulty in determining the species of Rhinoceros
by detached fossil molar teeth—the only recognizable parts of the
genus that I have yet obtained from the Red Crag of Suffolk.

Most of the detached molars of Rhinoceros from this formation
appear by their size, want of roots, and indications of absorbent action
at the base of the crown, to have belonged to the deciduous series of
teeth, and to have been shed by young individuals; and the milk-
teeth are less characteristic even than the permanent ones, as indeed
most structures of the immature period of life partake more of the
general and less of a special character than those of the adult. There
are, however, specimens of the permanent teeth sufficiently cha-

* Annals and Magazine of Natural History, vol. iv. 1840, p. 186.
Q 2-

CHy7; of Gaon

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(Compared with the Tibue of other Birds)

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218 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

racteristic and well-preserved to determine their relations to the like
evidences of extinct Rhinoceroses previously discovered in England.
The most characteristic examples of these teeth from the Red Crag
are figured for the present communication*, and, having previously
studied and endeavoured to demonstrate the differences between the
upper molars of the Rhinoceros tichorhinus aud those of the RAi-
noceros leptorhinus in my ‘ British Fossil Mammalia,’ figs. 122, 125,
and 126 (Rh. tichorhinus), fig. 141 (RA. leptorhinus), I have been,
in some degree, prepared to deduce satisfactory evidence of the
nature of the molars of the Rhinoceros from the Red Crag.

Baron Cuvier+, Prof. Kaupt, Dr. Buckland, and Prof. Jaeger §

have given the laudable example of figuring such fossil. teeth of the
natural size: all who are reduced, as in the present case, to mere
teeth for the determination of species must regret that the authors
of the excellent ‘ Zoologie et Paléontologie Frangaises||,’ and of the
‘Nouvelles Etudes sur les Rhinoceros Fossiles{,’ should not have
followed that example: for, reduced figures of objects rarely exceed-
ing two or three inches in natural size cannot afford satisfactory
means of comparison, and the loss to science is greater than such
saving of expense or space can compensate for.

In the upper molar (fig. 1, probably the third of the right side)
from a ‘Red Crag’ or ‘ Coprolite’ pit, at Wolverston, Suffolk, the
contour of the outer side of the tooth, d, d', d'', more resembles that of
the older pliocene and miocene Rhinoceroses (RA. megarhinus, Christol,
Rh. Schleiermacheri, Kaup), than that of the pleistocene Rh. ticho-
rhinus or Rh. leptorhinus ; the vertical ridge d! is relatively more
produced and is nearer the antero-external angle of the crown, d, than
in the Rh. tichorhinus, in which the outer border of the crown is
more undulated. From the ridge d', the outer border of the crag-
tooth has extended to the hinder angle of the tooth, d", in a nearly
straight line; a part of the enamel near that angle has been,

unluckily, broken away, but the body of dentine seems there to be

entire, whence one may refer the resemblance of the contour of that
border to that of the fourth and fifth upper molars of the Rhinoceros
megarhinus, figured (half nat. size) by M. Christol, in the ‘ Annales
des Sciences Naturelles,’ tom. iv. 2nd sér. pl. 2. figs. 3°, 4°, 5°.

In that species of Rhinoceros the second, third, and fourth molars
(premolars) are distinguished from the three following molars (true
molars) by a basal ridge extending along the inner side of the tooth,
and continued along a part of both the anterior and posterior sides of
the tooth. The present crag-fossil shows the same basal ridge, f£, f,
commencing at the inner half of the anterior side of the crown,
sweeping across the whole imner side, and gradually ascending to

* The woodcuts illustrative of the Teeth, Bones, and Antlers described in this
communication will be found at pages 231-236.

+ Ossemens Fossiles, tom. ii. pls. 6, 13, 1822.

+ Ossemens Fossiles de Darmstadt, 4to et fol. 1833.

§ Fossilen Saugethiere Wurtembergs, fol. 1839.

|| Gervais, 4to, 1852-54.

q Duvernoy, in the ‘Archives du Muséum d’Histoire Nat.,’ tom. vii.

A Ne ee

1856. | OWEN—RED CRAG MAMMALS. 219

terminate near the entry of the posterior valley a, where, however, it
has been worn away by pressure against the adjoining tooth. There
is no evidence of such a ridge in any of the upper molars of the
Rhinoceros tichorhinus. In the excellent figures of the upper
molars of the Rhinoceros Schleiermacheri, of the natural size, given
by Prof. Kaup*, the third and fourth molars exhibit a similar basal
ridge to that in the Rhinoceros megarhinus, and in the crag-tooth,
fig. 1.

oi the greater depth and width of the entry to the internal (6) and
posterior (a) valleys, the crag-tooth resembles the pliocene and
miocene Rhinoceroses above-cited, and differs from the pleistocene
Rhinoceros tichorhinus ; im which, owing to the entry of the corre-
sponding valleys being relatively shallower, and those valleys deepening
more as they penetrate the crown, they are sooner converted into pits
circumscribed by islands of enamel, as shown in the teeth, figs. 1, 2,
& 4, pl. 6, and in figs. 1 & 6, pl. 13, of the ‘ Ossemens Fossiles’ of
Cuvier, in the paper by Dr. Buckland in the ‘ Philosophical Trans-
actions’ for 1822, pl. 21. fig. 3, and in my ‘British Fossil Mam-
malia,’ figs. 122 & 126.

The internal valley, 4, is bilobed in the Rhinoceros tichorhinus,
or bends back so abruptly at its termination, that that termination
becomes insulated by attrition from the rest of the valley, as in some
of the figures above-cited ; such a change does not take place in the
Rhinoceros megarhinus and Rh. Schleiermacheri; in the latter the
end of the valley 4 slightly expands, and sometimes it is festooned by
small processes of enamel and dentine re-entering it, as 1s shown in
the crag-tooth, fig. 1, 6, and in the penultimate upper molar of the
Rhinoceros Schleiermacheri, figured in tab. 9. fig. 5, of Prof. Kaup’s
excellent work above quoted.

Prof. Christol does not represent this structure in any of the
molars of his Rhinoceros megarhinus ; but in the sixth (penultimate
or second true) molar, attributed by M. Gervais to the same species,
and figured, of half the natural size, in the ‘ Paléontologie Frangaise,’
pl. 2. fig. 5, the same modification of the end of the valley, 4, re-
appears, as is shown in the corresponding tooth of the Rhinoceros
Schleiermachert. From these differences I conclude that the fossil
tooth from the Red Crag of Wolverston does not belong to the
species of Rhinoceros (Rh. tichorhinus) which is associated in our
pleistocene gravels, drifts, and bone-caves with the Hlephas primi-
genius, but that it belongs to a species much more nearly allied to,
if not identical with, either the Rhinoceros megarhinus of the older
pliocene formations, near Montpellier, or the Rhinoceros Schleterma-
chert of the miocene formations near Darmstadt.

The second example of the upper molar of a Rhinoceros, from
the Red Crag of Suffolk, fig. 2, is also from the right side; but
the outer third of the crown is broken away together with the
base of the tooth. It is worn down more deeply than the preceding
molar, the valley 4 being insulated, and the valley a connected by an
isthmus of little more than a line in breadth with the outer wall of

* Op. cit. tab. 11. fig. 5.

———_ NE ———————E———E————eE——————EEEYYE. =,’

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220 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

enamel. The amount of attrition to which this tooth has been sub-
ject is about the same as that of the teeth of the Rhinoceros ticho-
rhinus figured by Cuvier in the ‘Ossemens Fossiles,’ tom. ii. pl. 6.
figs. 1 & 2. But, whereas it is the shorter posterior valley which is
still uninsulated in the crag-tooth (fig. 2), the long internal valley is
the one which retains the narrow continuity of enamel in the molar
teeth figured by Cuvier ; moreover, these teeth show the third island
due to the separation of the hinder divison of the expanding and bi-
furcating valley 4, in the Rhinoceros tichorhinus, whilst no trace of
the third enamel-island exists in the crag-molar in question. This
molar, moreover, shows a well-developed internal basal ridge, f, com-
mencing, as in the foregoing crag-tooth, fig. 1, near the middle of the
anterior surface, and rising as it extends along to the inner surface
to terminate at the postero-internal angle of the crown.

From the above characters it may be concluded that the portion of
the upper molar, fig. 2, from the crag-pit near Felixstow, Suffolk,
does not belong to the Rhinoceros tichorhinus, but to a species more
nearly allied to, if not identical with, either the Rhinoceros mega-
rhinus or the Rhinoceros Schlevermachert.

The third example of the upper molar of Rhinoceros, from the
Suffolk Red Crag, fig. 3, is from the left side, and had been but
little used in mastication,—not more, for example, than the tooth
of the Rhinoceros leptorhinus, from the Clacton pleistocene, fig. 141,
p. 373, of my ‘History of British Fossil Mammals,’ and to about
the same extent as the premolar teeth of the Rhinoceros Schleier-
macheri, figured by Prof. Kaup in tab, 11. fig. 7, of his most useful
[llustrations of the Fossils of Darmstadt. In the disposition of the
enamel-folds, the present crag-tooth so closely accords with the upper
molars of the miocene Rhinoceros (RA. Schletermacheri), that I am
strongly inclined to regard it as belonging to that species ; I have not,
however, had the opportunity of comparing it with an upper molar
of the Rhinoceros megarhinus in the same stage of attrition.

The valley, 6, as in the Rhinoceros Schleiermacheri, after pene-
trating along a line parallel with the anterior border, two-thirds
across the crown, suddenly bends backwards at a right angle; the
commencement of the valley is very wide and deep. The posterior
valley a is triangular, and in form and place closely resembles that
in the Rhinoceros Schletermachert. The position of the longitudinal
ridge d! accords with that in the crag-tooth, fig. 1, and with that in
the upper molars of both Rhinoceros Schleiermacheri and Rh. mega-
rhinus. 'The basal ridge f extends as far along the fore part of the
crown as in the Rh. Schleiermacheri, and it is continued, as in some
premolars of that species, around the inner side of the lobe ec. The
basal ridge is confined to the fore part of the crown in the Rhinoceros
leptorhinus,

In all the characters in which the present crag-molar resembles
those of the Rhinoceros Schletermacheri it differs from those of the
Rh. tichorhinus.

The lower molar teeth of Rhinoceros from the Suffolk Crag are
more numerous than the upper ones. Unfortunately they are less

1856. | / OWEN—RED CRAG MAMMALS. 221

characteristic of species. I have figured three of the best-marked
specimens,

If the teeth in the lower jaw of the Rhinoceros Schleiermachert
figured by Kaup in tab. 11. fig. 8, op. cit., be compared with the
figures of the lower molar teeth of the Rhinoceros tichorhinus given
by Cuvier in pl. 6. fig. 7 and pl. 13. fig. 3, op. czé., and by Buckland
in pl. 21. fig. 5, op. cit., it will be seen that the tract of dentine
exposed by moderate abrasion in the hinder lobe of the tooth is more
angular in the miocene Rhinoceros, and more gradually bent in the
pleistocene one.

If the figure of the lower molar of the Rhinoceros from the Red
Crag at Sutton, fig. 4, be compared with that of a probably answerable
molar, only a little more worn, of the Rhinoceros tichorhinus in the
‘History of British Fossil Mammals,’ fig. 127, p. 337, the same
difference will be recognized, together with the difference in the
thickness of the enamel, the greater thickness of which characterizes
all the teeth of the Rhinoceros tichorhinus as contrasted with those of
the Rhinoceros megarhinus and Rhinoceros Schletermacheri*, Ihave
no hesitation, therefore, in affirming that the crag-tooth, fig. 4, does
not belong to the Rhinoceros tichorhinus ; although, in the absence
of means of comparing it with the lower molars of the pliocene and
miocene Rhinoceroses hitherto defined, I cannot positively refer it to
any of those species. There is a short oblique, basal ridge at the
outer and anterior angle of the tooth, and a short rudimentary one
at the back part of the crown.

Fig. 5 is a lower molar from the left side of the lower jaw of a
Rhinoceros, from the Red Crag at Felixstow; it is more worn than
the preceding, but repeats all its characters of resemblance to the
lower molars of the Rh. Schlecermacheri, and of difference from those
of the Rh. tichorhinus.

The crown of aright lower molar of a Rhinoceros, from the Red
Crag at Sutton, fig. 6 a, 6, c, of which the summit of the anterior
lobe had only just begun to be abraded, shows the anterior oblique
basal ridge continued, of less thickness, along the fore part of the
anterior lobe, where it describes a curve convex upwards, fig. 6 6;
there is a shorter and thicker curved basal ridge, behind, fig. 6 ec.

The small lower molar from the right side of the jaw of a Rhi-
noceros, fig. 7, found im a erag-pit at Sutton, corresponds in size
and general form with the second molar of the Rhznoceros Schleier-
macheri figured in tab. 12. fig. 11, of Prof. Kaup’s work above cited.

The above-described specimens of fossil teeth of Rhinoceros, from
the crag-pits of Suffolk, afford satisfactory evidence of the remains of
a species distinct from the common Tichorhine Rhinoceros and
from the Leptorhine Rhinoceros of the pleistocene era, and more
nearly allied to, if not identical with, either a species of Rhznoceros,

* The figure of the lower molars of the Rhinoceros megarhinus, given by
Christol in the Annales des Sciences Nat. vol. iv. 2nd ser. pl. 2. fig. 1, and by
Gervais, in pl. 30. fig. 1. of the Paléontologie Frangaise, as well as that of the
Rhinoceros pleuroceros, in pl. 8 of the Archives du Muséum, tom. vii., are too
much reduced to be of use in this comparison. ;

222 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb, 20,

viz. Rh. megarhinus, from the older pliocene, or with one, viz. Rh.
Schleiermacheri, from the miocene tertiary formations.

Genus Tapirus.

At the period of the publication of my ‘ History of British Fossil
Mammals,’ 1845, no remains referable to the genus T'apirus had come
under my notice from any British locality ; the Tapiroid family was
represented only by species of Coryphodon and Lophiodon.

The existence of a true Tapir in tertiary strata was first made
known by Prof. Kaup, in the miocene deposits at Eppelsheim; an
almost entire under jaw and part of an upper jaw, with the charac-
teristic teeth of both, are described and figured, tab. 6. op. cit.,
under the name of Tapirus priscus... Remains of a Tapir have also
been discovered in both miocene and old pliocene strata in Auvergne
and other paits of France: -these fossils M. de Blainville thought
not to be specifically distinct from the Tapirus priscus of Kaup.
They are assigned, in Gervais’ ‘ Paléontologie Frangaise,’ to a species
named Tapirus arvernensis (from the Puy-de-Dome), to a Tapirus
minor (from the pliocene sands of Montpellier), and to a Tapirus
Poirieri (from the miocene deposits of the Bourbonnais).

It may seem hazardous to affirm the existence of a British fossil
Tapir from a single tooth, and that a lower one; but the molar tooth
figured, fig. 8, from the crag-pit of Sutton, from which the upper
molars of the Rhinoceros so near to, if not identical with, the RAz-
noceros Schleiermacheri were obtained, bears a closer resemblance to
a newly risen and unworn molar of the lower jaw of the Tapzrus
priscus, Kaup, than to any other recent or fossil tooth with which I
have been able to compare it. There are the same two principal
transverse ridges, the same low basal ridge at the fore and back
parts of the crown, the same slight concavity of that side of the
principal ridge which is directed upwards ;—the closest agreement,
in fact, both as to form and size, prevails. I am, therefore, led to
expect that the former existence of a British Tapir, probably not
distinguishable from the Tapirus priscus, Kaup, will be confirmed
by subsequent discoveries of the more characteristic upper teeth, in
the Suffolk crag-pits.

[Since the above paragraph was in type, I have had the desired
opportunity of comparing an upper molar tooth (fig. 9) from the Red
Crag of Suffolk, now in the British Museum, with those of the Tapirus

priscus, Kaup, and the comparison has afforded the anticipated
confirmation.—R. O., July 1856. ]

Genus Sus.

Since my first determination of a fossil of the genus Sus in the Red
Crag of Suffolk*, viz. the external incisor of the lower jaw (p. 428,
fig. 173, Brit. Foss. Mamm.), several molar teeth of the Hog genus
have been obtained from that formation, and some of them in the

* Annals of Natural History, vol. iv. 1840, p. 185.

i eee ui siti | Taner

1856. ] OWEN—RED CRAG MAMMALS. 223

usual mineralized state of its characteristic fossils. Of these I
have figured the last upper molar tooth of the left side, fig. 10,
from the Red Crag at Sutton. It differs from the corresponding
tooth in the Sus scrofa by the shorter antero-posterior diameter
as compared with the transverse diameter of the crown, the latter
dimension at the fore part of the tooth being the same as in the
corresponding tooth of an ordinary wild boar; but the crown of
the fossil tooth wants one-fifth of the length of the grinding surface -
in the corresponding tooth of the recent species (Sus scrofa). Prof. .
Kaup has described (p. 11) and figured (tab. 9. fig. 3, op. cet.) an
almost precisely corresponding tooth to that represented in fig. 9;
and, for the species of Hog represented by portions of jaws with
similar teeth he proposes the name of Sus paleocherus; founding
the specific difference chiefly on the same differences in the proportions
of the molar teeth which are illustrated by the crag-fossil under con-
sideration. To those who will compare the figure of this fossil, fig. 9,
with the figure above citedfrom Kaup’s excellent work, there need
not be more said in favour of referring the crag-tooth to the same
extinct species of Hog (Sus paleocherus) from the miocene forma-
tion near Eppelsheim.

Fig. 11 represents a portion of the crown of a molar of apparently
a larger species of Sus, from the Red Crag at Ramsholt, Suffolk ; it
probably belongs to the same species as the Sus antiquus, Kaup,
founded on fossils from the miocene sands at Eppelsheim.

Genus Equus.

Molar teeth, from both upper and lower jaws, of a large species of
Equus, occur in the Red Crag, and in the usual condition of the
fossils of that formation. The disposition of the enamel on the
grinding surface of one of these molars from the upper jaw, fig. 12, 6,
resembles that of the tooth from the Oreston cavern, referred to
the species called Equus plicidens in the ‘ Brit. Foss. Mamm.’ p. 393,
fig. 153. It is of large size, and presents the heavy, mineralized,
deeply stained characters of the true Red-crag fossils.

Similarly fossilized teeth of a smaller species of Equus, probably
of the subgenus Hzpparion, have likewise come under my notice from
the Red-crag of Suffolk.

Genus Mastodon.

The specimens of teeth and portions of teeth of Mastodon, from
the crag-pits of Suffolk, are not distinguishable specifically from those
referred to the Mastodon angustidens (Mastodon longirostris, Kaup)
from the fluvio-marine crag of Norfolk, in my ‘ History of British
Fossil Mammals,’ pp. 276-284. In the Ipswich Museum there is a
considerable proportion of the crown of a molar corresponding with
the fourth of the upper jaw in Kaup’s Mastodon longirostris ; also
a well-preserved atlas vertebra of, apparently, the same species of
Mastodon.

”
224 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

Family Cervide.

In the miocene strata near Darmstadt the remains of a peculiar form
of small Deer, with pedunculated antlers like those of the Muntijac,
but with the typical mumber of molars, 7—7, at least in the upper
jaw, have been found, on which remains Prof. Kaup has founded his
genus Dorcatherium. With this were associated other and somewhat
larger species of Deer, represented by more or less mutilated antlers,
which Prof. Kaup refers to his species Cervus dicranocerus (tab. 24.
figs. 3, 3e, op. cit.). In this species the beam of the antler rises
from one to two inches above the burr without sending off any brow-
snag, but at that distance it sends obliquely forward a branch so large,
that the beam seems here to bifurcate, the anterior division being,
however, rather the smallest and shortest.

I have received the bases of similar antlers, which had been shed,
from different Red-crag pits of Suffolk, some corresponding in size
with, others larger than, the largest of the specimens figured by
Kaup*; none of these specimens, however, have either branch of the
beam entire.

Dicranoceros (Subgeneric division of Cervus).

The specimen (fig. 14) from a crag-pit near Sutton, Suffolk, is
the base of a shed autler of a species of Deer, identical with, or nearly
allied to—certainly belonging to the same section in the Deer tribe as—
the Cervus dicranocerus of Kaup. The absorbed basal surface is
slightly convex, subcircular, 1 inch in long diameter ; the base of the
antler extends from 2 to 3 lines beyond it : in one half of the cireum-
ference, the base is continued with a mere convex bend into the ascend-
ing beam; in the other half it projects outward, at first slightly,
then more prominently, forming a ridge or “ burr,” which extends
4 lines from the margin of the absorbed surface. The proportion
of the absorbed, and formerly adhering, part of the base to the non-
adherent part of the base indicates that the antler was supported by
a persistent bony process of the frontal, or by a pedicle, as in the
Cervus anocerus, Kaup (probably identical with the Dorcatherium,
Kaup), and in the existing Muntjac. The beam is 2 inches in length
before it divides ; and it is more extensively and deeply excavated on
one side (the excavation widening to the division) than on the other.
The antler is marked by longitudinal grooves and a few low ridges,
but is equally devoid, with the Darmstadt specimens, of any of the
tubercles which characterize the antlers of the Roe. The length
from the base to the broken end of the main branch is 3 inches
3 lmes; the circumference of the beam above the base is 3 inches
5 lines.

From the same Red-crag pit, I have received a left lower true
molar, fig..15, with proportions of the lobes and their crescents more
resembling those of Cervus than of other genera of Ruminantia,—in
the greater angular production e. g. of the outér crescents, e, e, and the
greater proportion of dentine between the apex of the triangle and

* Kaup, Description d’Ossemens Fossiles de Mammiferes de Darmstadt, 4to
1839, tab. 24. figs. 3, dc.

1856. ] OWEN—RED CRAG MAMMALS. 225

the base formed by the enamel-islands. There is a low accessory
tubercle at the bottom of the cleft between the two outer crescents*.

A second specimen of antler, from a crag-pit near Felixstow, is larger
than the foregoing, but offers the same characteristics. The beam is
rather shorter in proportion to its girth above the burr; it is 2 inches
long and 4 inches in girth; but it shows the same convexity at the
side next the burr and the same concavity on the opposite side. It has
been a shed antler; the slightly convex, absorbed surface bears the ©
same proportion to the entire base of the antler as in fig. 14; the
burr, in like manner, is limited to, or chiefly developed from, one
half of the circumference of the base, where it has projected from 3°
to 4 lines beyond the line of attachment.

Assuming one and perhaps the chief use of the burr to be to defend
the subjacent skin from abrasion, in actions of the antlers when they
are strongly rubbed from above downwards against a hard body—
and were it not for such projecting ledge, such actions might peel off
the skin where it abruptly terminates at the circumference of the basal
adhesion of the antler to the skull,—I infer, from the partial de-
velopment of the burr in the Dicranoceros of the Red-crag, that the
pedicle supporting the antler was so oblique as to render such defence
necessary only on one—probably the anterior and outer—side of the
antler.

M, Gervais has figured, pl. 7. fig. 1. op. cit., a shed antler of a Deer
having the same short, simply bifurcated form as the C. dicrano-
cerus of the Eppelsheim miocene and the Suffolk crag. It is rather
more slender in proportion to its length; the burr, according to the
figure, shows the same partial development from one-half of the basal
circumference. ‘The fossil is from the lower pliocene (marine sands
and blue and yellow marls) of Montpellier. The accomplished French
naturalist refers this bifurcate antler to the Cervus australis of
M. de Serres.

Similar bifurcated antlers, probably not materially differing from
the foregoing, or from the Cervus dicranocerus of Kaup, except in
having been found attached to their supporting bony pedicles, form
the type of the subgenus “‘ Dicroceros”’ of M. Lartet, and occur in
the miocene erences molasse at Sansan, Gers.

The largest portion of antler of the Cervus dicranocerus which I
have, as yet, received from the Suffolk crag-pits, is 4 inches in
length, and the preserved part of the main branch of this antler is
continued in a more direct line from the base than is either of the
divisions of the best-preserved antler figured by Kaup, tab. 24.
fig. 3c, op. cit. The example of the Cervus dicranocerus, from a
crag-pit near Ipswich, Suffolk, fig. 16, sends off the smaller or sub-
sidiary fork a little nearer the base than in the smaller specimens ;
the base, however, shows well the same characteristic partial develop-
ment of the burr, a, a, asin the other fossils. The circumference of the
antler, above the burr, is 4 inches 9 lines; the breadth of the burr is

from 5 to 6 lines, being proportionally more than its vertical thickness,

* See the figures of the modifications of homologous similar molars in my
‘ Odontography,’ pl. 134. figs. 1-8, fig. 5 being that of the Cervus megaceros.

226 PROCEEDINGS OF THE GEOLOGICAL Society. [Feb. 20,

as compared with the burr in the Cervus elaphus. The length of the
beam to its bifurcation is only 2 inches.

The individual variations in size and proportion which the crag-
specimens of fossilized and more or less rolled antlers of the Cervus
dicranocerus have presented are not greater than those observed in
antlers of different individuals and of different ages of the Fallow or
Red Deer.

Fig. 17 a, b, are views of an upper molar, of probably the Cervus
dicranocerus, from the same crag-pit as the foregoing antler.

Megaceros (Subgenus of Cervus).

A very interesting evidence of the Deer-tribe from the Red Crag
of Suffolk is the base of the left antler (fig. 18), which had been shed,
of a deer as large as the Megaceros hibernicus or of the Strongyloceros
speleus*,

In the relative size and position, immediately above the burr, of
the origin of the brow-snag, in the absence of a second snag at the
distance above the brow-snag where such second snag arises in the
Strongyloceros speleus, in the commencing flatness of one side, and
expansion, of the beam at the broken end, eleven inches from the burr,
this crag-fossil resembles the corresponding part of the antler of the
Great Irish Deer (Megaceros hibernicus). The circumference of the
burr is 11 inches. In colour and ponderosity this remarkable fossil
agrees with the ordinary fossils of the Red Crag.

I have had similar evidence of the Megaceros from the RE en
brick-earth of Essex, but equally agreeing in colour and mineral
characters with the fossil bones of the Mammalia usually occurring
in that formation.

Order CARNIVORA.

Of this order I have received clear evidences of the genera
Ursus, Felis, and Canis from the Red Crag. Some more or less
imperfect and waterworn canine teeth indicate other genera, as Phoca,
and apparently a species of the family Viverride, but do not yield
safe ground for a decided reference. I therefore limit my present
notice to those molar teeth which satisfactorily determine, at least,
genera of the Carnivora.

Genus Felis.

This genus is represented by a lower sectorial or carnassial tooth
resembling in size and other characters that of the Felts pardoides
of the ‘ Brit. Foss. Mamm.’ p. 169, fig. 66. The specimen, from a
Red-crag pit, five miles from Newbourn, consists of the crown and
base of the fangs, most of which are worn away, of the lower car-
nassial or sectorial molar, fig. 19. The two compressed triangular,
trenchant, and pointed lobes of the crown have the same near equality
of size, as in the corresponding fossil from Newbourn f.

* History of Brit. Fossil Mammals, p. 469, figs. 193, 194.
+ Ib. p. 169, fig. 66.

_—

1856. ] OWEN—-RED CRAG MAMMALS. 227

As the strata of the Red Crag at that village, from which the
mammalian fossils originally determined by me* were obtained,
were traversed by vertical fissures, Sir Charles Lyell in his descrip-
tion of the formation remarks :—‘‘ It might be suggested, that the
mammalian relic was possibly derived from the contents of one of
the fissures, the filling of which was an event certainly posterior, and
perhaps long subsequent, to the era of the deposition of the crag+.”’

The subsequent discovery of a feline carnassial tooth of the same
size, and apparently species, as that ofthe Felis pardoides, adds
satisfactorily to the high probability—founded upon the original
feline tooth having undergone the same process of trituration and im-
pregnation with colouring matter as the associated bone and teeth of
fishes known to be from the regular strata of the Red Crag—that the
Felis pardoides is a fossil of that period. The Felis antediluviana
of Kaup, from the miocene sand at Eppelsheim, and the Felis par-
dinensis of Croizet and Jobert, from the miocene strata of Auvergne,
correspond in size with the Felis pardotdes of the Red Crag of
Suffolk.

The lower sectorial tooth, fig. 20, deviates from the feline type,
and approaches that of the carnassial in the Glutton, Hyzena, and
Grison; but with a minor development of the hinder tubercle, and
a major development of the outer cingulum. I suspect that we have,
in this tooth, an mdication of an extinct osculant genus, linking on
the true Felines to the Hyzena or Musteline family. It closely re-
sembles one of the teeth of the Miocene Carnivora to which the
generic names Hy@enodon and Pterodon have been given.

Genus Canis.

Three views (fig. 21) of a left upper carnassial tooth of a spe-
cies of Canis, agreeing in size and shape with that of the Wolf
(Canis Lupus), give an outside view, c; a, an inside view ; and 6, a
view of the fore part of the tooth, from which the two fangs,
outer and inner, of that part ascend. I am unable to detect any
character by which I could positively distinguish this tooth from that
of the existing Wolf, or of the species found in our bone-caves and _
pleistocene deposits. The specimen presents the usual characters of
the crag-fossils, and was obtained from a crag-pit near Woodbridge.
A portion of the lower jaw of a species of Canis from the same pit
is figured at fig. 22, a, 6.

Genus Ursus.

The Ursine genus is represented by an antepenultimate grinder cf

the right side, upper jaw, of a Bear, somewhat smaller than the

corresponding tooth of the Ursus speleus. The fossil im question
was obtained by Mr. Colchester from the Red Crag at Newbourn,
near Woodbridge, Suffolk. The specimen is now in the collection of
the Rev. Edward Moore, of Bealings, near Woodbridge.

* Ann. of Nat. Hist. vol. iv. 1840, p. 185. + 1b: i 186:

228 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

Order CETACEA.

By far the greatest proportion of the mammalian fossils from the
Red Crag belong to this order. In reference to the largest speci-
mens, I have little to add to the description of the fossils on which
were founded the species of Balena (Balenodon’) affinis, Bal. de-
finita, Bal. gibbosa, and Bal. emarginata, in the ‘ Hist. of British
Fossil Mammals’ (pp. 526-542). Mr. James Carter of Cambridge
submitted to me, July 1850, two pairs of Cetotolites from Sutton,
differing from the Bal. emarginata in the thicker and squarer form
of the greater end of the tympanic bone. The Rev. R. K. Cobbold
has showed me a series of silicified fragments of Balena gibbosa, and
cetacean ribs, collected from the Red Crag in the parish of Sutton,
where it is separated from Felixstow by the River Deben.

The front part of the atlas of a cetaceous animal, which must have
been from 30 to 40 feet in length, was obtained by the Rev. Prof.
Henslow, in 1855, from the Red Crag at Woodbridge, Suffolk.

Waterworn teeth, corresponding in size and form to the singular
teeth from the marine miocene deposits of the ‘‘ Département de la
Drome,”’ figured by Gervais, in pl. 20 of his ‘ Paléontologie
Frangaise,’ under the name of Hoplocetus crassidens, have been
discovered in the Red Crag of Suffolk, and transmitted for my
inspection.

Teeth corresponding in character with those of the Grampus (Pho-
cena Orca) have also reached me from the Red Crag. One speci-
men, from a crag-pit at Bawdsey, with a less expanded fang than
ordinary, is figured at fig. 23.

Petro-tympanic bones of a species of Delphinide, about the size of
the Grampus, and some of a smaller species, have been obtained from
the Red Crag.

Portions of a long, slender, gradually attenuated, edentulous, upper
jaw have been transmitted to me, by Mr. Edwards of Bunhill Row,
from the Red Crag near Woodbridge, Suffolk: the specimen, fig. 24,
from the Red-crag at Felixstow, was submitted to me by Mr. G.
Ransome. They belong to that family of Delphinide of which the
genus Ziphius is the type, and very closely resemble the species
from the crag of Antwerp described by Cuvier* under the name of
Ziphius longirostris, now forming the genus Dioplodon of Gervais.
The original fossil from Antwerp appears to have been in a similar
mineralized condition to those from our own Red Crag. Cuvier
describes it as being “ petrified and very heavy.” MM. Gervais and
Van Beneden distinguish the Antwerp Crag fossil im question from
the true Ziphius longirostris, Cuvier, under the name of Dioplodon
Becanii. They believe it to have come from a ‘ molasse’ formation.
There is not enough of the upper jaw preserved in the Suffolk Crag
fossils to enable me with certainty to pronounce on their specific
identity with, but I have no doubt of their belonging to the same
genus as, the Antwerp fossil. They are equally edentulous in respect
of the upper jaw.

* Ossemens Fossiles, tom. v. (1823), p. 356, pl. 27. figs. 9 and 10.
+ “Elle semble provenir d’un terrain de molasse,” Pal. Frang. p. 155.

———

1856. | OWEN—RED CRAG MAMMALS, 229

The following extinct species of Delphinus are given by M. Gervais
in the ‘ Paléontologie Francaise’ :—

D. pseudodelphis, from the miocene molasse at Vendargues ;

D. Dationum, from the miocene formation at Dax; and

D. Renovi, from the miocene molasse of the Département de Orne.
M. Pictet refers the formation in which were found the fossil Ziphius
longirostris of Cuvier (Dioplodon, Gervais) to the marine molasse
of the miocene period. 3

Conclusion.—F rom the foregoing details it will be seen that the re-
searches now applied during fifteen years to the mammalian fossils of
the Red Crag of Suffolk have led to the very interesting result, that the
majority of them are identical, or closely correspond, with miocene
forms of Mammalia, and especially with those from the Eppelsheim
locality, described by Prof. Kaup. In Suffolk, as in Darmstadt,
we find the Mastodon longirostris, Rhinoceros Schleiermacheri,
Tapirus priscus, Sus paleocherus, and Cervus dicranocerus, associated
together, in the same formation ; and, with these miocene forms of
extinct Mammalia in the Red Crag, we have, likewise, a Cetacean
which most closely resembles a miocene species of that order, pre-
viously recognized in the crag or molasse of the continent. At the
same time there are, as e.g. in the Megaceros, specimens of newer
pliocene or pleistocene forms of Mammalia mingled with the older
tertiary species ; whilst on the other hand eocene forms of fish, as
e.g. Edaphodon, with Myliobatide and eocene Crustacea, have been
obtained from the Red-crag pits. |

As, however, several of the. Mammalia which occur in miocene
formations are also found in the older pliocene deposits in parts of
France, it would be rash, perhaps, to pronounce positively on the
miocene age of any of the above-cited crag-fossils; but it is certain
that the majority of those mammalian fossils, and by far the greatest
proportion of individual specimens, belong to an older tertiary period
than the Mammalia of the newer pliocene drifts, gravels, brick-
earths, and bone-caves.

DESCRIPTION OF THE FIGURES.

Fig 1. Grinding surface of right upper molar (probably the third) of the Rhino-
ceros Schleiermacheri? (From a Crag-pit, Wolverton, Suffolk ;
communicated by W. C. Maclean, Esq., Collector of Customs at
Woodbridge.)

Fig. 2. Grinding surface of the inner portion of the crown of a right upper molar
of the Rhinoceros Schleiermacheri? (From a Crag-pit, Felixstow ;
communicated by George Ransome, Esq.)

Fig. 3. Grinding surface of’a left upper molar of the Rhinoceros Schleiermacheri?
(From a Crag-pit, Felixstow; communicated by W. C. Maclean, Esq.)

In these upper molars are marked—a the hinder valley, 4 the inner or
front valley, c the inner end of the front lobe, ec’ the inner end of the back
lobe, d the front angle, d’ the ridge, d” the back angle of the outer sur-
face, f the cingulum or basal ridge.

Fig. 4. Grinding surface of a right lower molar of the Rhinoceros Schleiermacheri?
(From a Crag-pit, Sutton ; communicated by W. C. Maclean, Esq.)

230 PROCEEDINGS OF THE GEOLOGICAL society. [Feb. 20,

Fig. 5. Grinding surface of a left lower molar of the Rhinoceros Schleiermacheri ?

(From a Crag-pit, Felixstow; communicated by G. Ransome, Esq.)

In these lower molars are marked—a the outer side of the front lobe,

b the outer side of the back lobe, ¢ the front ridge, d the mid ridge, e the
back ridge, of the grinding surface, f the front valley, g the back valley.

Fig. 6a. Grinding surface of unworn crown of a right lower molar of the Rhino-
ceros Schleiermacheri? (From a Crag-pit, Sutton ; communicated
by George Ransome, Esq.)

Fig. 64. Anterior surface of the same.

Fig. 6 c. Posterior surface of the same.

Fig. 7. Grinding surface of second lower molar, right side, of the Rhinoceros
Schleiermacheri? (From a Crag-pit, Sutton; communicated by
W. C. Maclean, Esq.)

Fig. 8a. Grinding surface of a lower molar tooth of the Tapirus priscus, Kaup.
8 5. Side view of the same. (From a Crag-pit, Sutton; communi-
cated by W. C. Maclean, Esa.)

Fig. 9. Upper molar of Tapirus priscus. (From a Crag-pit, Suffolk: British
Museum.)

Fig. 10. Grinding surface of the last left upper molar of the oe paleocherus.
(From a Crag-pit at Sutton; communicated by W. C. Maclean, Esq.)

Fig. 11. Part of a molar.tooth of the Sus antiquus? (From a Crag-pit at Rams-
holt ; communicated by W. C. Maclean, Esq.)

Fig. 12 a. An upper molar of the Eguus plicidens? (From a Crag-pit at Bawd-
sey; communicated by Sir Charles Lyell.)

Fig. 12. Polished section of the grinding surface of the same tooth.

Fig. 13, a,. A much-worn lower molar of a species of Equus : a, grinding sur-
face; 6, side view. (From the Fluvio-marine Crag at Norwich ;
communicated by W. C. Maclean, Esq.)

Fig. 14,a,. Portion of a shed antler of the Cervus dicranocerus; 6, base of the
same. (From a Crag-pit, Sutton; communicated by George Ran-
some, Esq.)

Fig. 15. Grinding surface of a lower molar of the Cervus dicranocerus? (From a

Crag-pit, Sutton; communicated by Ed. Acton, Esq.)

Fig. 16. Oblique basal view of a portion of a shed antler of a larger individual of
the Cervus dicranocerus. (From a Crag-pit near Ipswich; com-
municated by George Ransome, Esq.)

Fig. 17 a, side view, 17 4, grinding surface, of an upper molar of the Cervus
dicranocerus ? (From the same pit ; communicated by George Ran-
some, Esq.)

Fig. 19. The lower carnassial tooth of the Felis pardoides. (From a Crag-pit,
Newbourn; communicated by W. C. Maclean, Esq.)

Fig. 20. The lower carnassial tooth of a Carnivore, allied to Hyenodon and Péero-
don. (From a Crag-pit, Woodbridge ; communicated by Ed. Acton,
Esq.

Fig. 21. The left upper carnassial tooth of a species of Canis: c, outer fae. a,
inner side; 4, fore-part. -(From a Crag-pit, Woodbridge ; ; com-
municated by Ed. Acton, Esq.)

Fig. 22, a,b. Two views of a portion of the lower jaw of a species of Canis. (From
a Crag-pit, Woodbridge ; communicated by Ed. Acton, Esq.) i)

Fig. 23. The tooth of a Grampus (Phocena, sp. ind.). (From a Crag- -pit, Bawd-
sey ; communicated by W. C. Maclean, Esq.)

Fig. 24. Portion ‘of the upper jaw of the Ziphius (Dioplodon, Gervais). a, Section
of the smaller end of ditto. (From a Crag-pit, Felixstow ; commu-
nicated by George Ransome, Esq.)

All the foregoing figures are of the natural size.

Fig. 18. The base of the antler of the Megaceros hibernicus, one-third the natural

size: a, the surface from which the brow-antler had been broken
off. (From a Crag-pit at Felixstow ; communicated by George Ran-
some, Esq.)

1856. | OWEN—RED CRAG MAMMALS.

Hie. 1,

Mammalian Remains from the Red Crag.

VOL. XII.—PART i.

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232

Mammalian Remains from the Red Crag.

OWEN—RED CRAG MAMMALS. 233

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1856. | RUBIDGE—SOUTH AFRICA. 227

Marca 5, 1856.

J. W. Tayler, Esq., W. H. Groser, Esq., H. B. Medlicott, Esq.,
H. G. Bowen, Esq., T. J. Smith, Esq., T. Moffat, M.D., W. Mat-
thews, jun., Esq., were elected Fellows. Prof. Bunsen, of Heidelberg,
was elected a Foreign Member.

The following communications were read :—

1. Notes on the GEoLoGy of some parts of Sourw AFRICA.
By R. N. Rusipes, M.B.

(In a letter* to Sir Roderick Murchison, F.G.S.)
[ Abstract. ]

Dr. RusipGe first referred to the occurrence of gold at Smithfield
in the Orange River Sovereignty, as detailed in his letter of May
1854, published in the Society’s Journal, vol. xi. p. 1 ; and stated that
several pieces of gold had since been found at the spot described in
the letter referred to. Besides being found in the alluvium there,
gold was met with in a quartz-vein in the trap traversing the strati-
fied rock,—in other quartz associated with the trap, —and in a mass
of limestone enclosed in the trap-dyke ;—but none in the stratified
rock itself (which belongs to the Dicynodon or Karoo Series).

Dr. Rubidge next alluded to the fossil plants which he there found
in the strata; some of these he referred with doubt to Calamites.
Six years ago, also, the author found numerous vegetable remains
(some of which were possibly referable to Lepidodendron) at Jackal’s
Kop+, on the eastern side of the Stormberg Range, in the same for-
mation as that of the Drakensberg and Smithfield ; and Calamite-like
plants in the western part of the Zuurbergen. The author remarked
that the plant-remains above referred to much resembled those col-
lected by Mr. Bain at the Ecca Heights in rocks of the Karoo Series.
Dr. Rubidge had also found*bones of the Dicynodon near the Caledon
River and at Halse’s farm six miles from Smithfield.

From various observations by himself and others, the author had
been enabled to recognize the existence of the Dicynodon or Karoo
rocks in the Drakensberg, at Harriesmith, at Winburg, and even at
Megaliesberg ; and Dr. Sutherland lately described the same rocks
as occurring in Natal, where they are rich in coalf.

The amygdaloid rock which supplies the agate-gravel of the Orange,
Caledon, Kroai, and Vaal Rivers appears to exist in the ‘‘ Mont des
Sources”’ in the Drakensberg, as an unworn specimen was found in
the Eland River (a tributary of the Vaal), not more than twelve miles
from its source.

* Dated Namaqualand, April 16, 1855.

+ Some of these plants were sent to Col. Portlock by Dr. Rubidge, and were
exhibited to the Meeting of the British Association in 1851, together with some
jurassic fossils from Sunday River. The plant-remains comprised specimens of
Pecopteris and other ferns, with Zamia.—Ep.

t Quart. Journ. Geol. Soc. vol. xi. p. 465.

VOL. XII.—PART I. s

238 PROCEEDINGS OF THE GEOLOGICAL society. [ Mar. 5,

Lastly, Dr. Rubidge supplied some remarks on the geology of the
copper-district of Namaqualand and bordering countries. Granitic
rocks of several varieties occur, together with gneiss, mica-schist, and
tale-schist. The gneiss strikes 5° to 20° 8. of W., and dips alter-
nately N. and S.; one dip continuing for many miles. On the hills
the gneiss and schists are covered by horizontal sandstones, which
appear to be the same as the sandstone of Table Mountain, and con-
tinuous with it.

The copper is found in fissures of the gneiss, where the latter is
locally disturbed in its dip, the strike remaining unaltered ; that is,
along anticlinal and synclinal folds or axes; also in fissures extending
nearly in the direction of the magnetic meridian, and in crevices
between masses of rock, with no veinstone or gangue: the oxides
and silicates often appear to be infiltered into the rock-mass. The
ores most common are red and black oxides, green and blue silicates,
purple and yellow sulphurets, and a few carbonates. Granitic rocks
are often found in the axes above referred to.

2. On the Lowest SEDIMENTARY Rocks of the Sout of Scot-
LAND. By R. Harkness, Esq., F.G.S., Professor of Geology
and Mineralogy, Queen’s College, Cork.

It is stated in Sir Roderick Murchison’s ‘ Siluria,’ page 151, on my
authority, that the axis of the Silurians of the South of Scotland
ranges in the direction of the Dryfe Water. In order to satisfy my-
self as to the exact position of this axis, and of the deposits with
which it is more immediately associated, I examined in detail, during
last summer, that portion of the county of Dumfries where this axis
occurs. Its position in the adjoining county of Roxburgh is laid
down by Professor Nicol as near the course of the River Teviot*.
West from Hawick, however, it appears to leave this stream, and
follows nearly the direction of the Borthwick Water.

In the high mountainous district which separates Roxburghshire
from Dumfriesshire, the exact position of the axis is difficult to de-
termine owing to the want of good sections, and from the thick cover-
ing of soil which here invests the mountains. Even in the course of
the River Esk, in Dumfriesshire, which intersects the country almost
at right angles to the strike of the strata (and in which, on looking
at the map, we should naturally expect to find good sections, and
the axis well exhibited), the solid rock is not well exposed in con-
sequence of the gravelly nature of the bed of this river. Yet through
the whole course of this stream, from Skipper’s Bridge, about a mile
south of Langholm, where the Silurians first make their appearance,
to near Eskdale-muir Bridge, wherever we have the strata exposed,
these possess (when not perpendicular) the prevailing south dips
which mark the deposits forming the Silurians on the south side of
the axis.

* «Siluria,’ page 152.

1856. | HARKNESS—LOWEST ROCKS OF ESKDALE.

At Eskdale-muir Bridge we have
evidence of proximity to the axis,
for here north dips begin to mani-
fest themselves.

There is a small burn which
joins the Esk, a little to the south
of Eskdale-muir Bridge, from the
east, called the Rennel Burn; and
in the course of this we have the
axis well developed (see fig. 1) ;
and here it consists of hard purple
grits intersected by veins of calc-
spar. From this locality it takes
a W.S.W. route; and, crossing
the Esk, we have it displayed near
the road which connects Hskdale
with Annandale; and, running
nearly parallel to this road, through
the farm of Twiglees, it enters the
parish of Hutton, and is here well
seen in the course of the Dryfe
Water about half a mile above Bor-
land Bridge. In this locality it is
seen in the form of an anticlinal
axis consisting of purple grits, like
those seen in Rennel Burn, and
having also the calc-spar veins
traversing them.

In a small burn to the west, the
Shaw Burn, a short distance from
the Dryfe, the axis also makes its
appearance, and here it seems to
run in the direction of Shaw House.
In the other small burns, to the
westward, we have S8.S.E. dips
obtaining, which indicate strata
occupying a position on the south
side of the axis; but at a quarry
situated a short distance N.E. of
Newbiggin House, the N. N. W.
dips occur, pointing out strata on
the north side of the axis. In the
course of the Auchenrodden Burn,
in the parish of Applegarth, we
have evidence that the axis crosses
the higher portion of this stream ;
and here it makes its last appear-
ance on the eastern side of Annan-
dale; the areaoccupied by the Corn-
cockle-muir sandstone coming on
immediately to the westward.

‘SQUOPSOUII] PUL S}IIS SHOIaJIUOGIeD ‘p

‘(sIxy) 873 ofdimg *?

‘(avLINyIg) Souojspues pur soreys ofdind-ystppaa puw Ard “4styos ajovqUy “9

*PLPE-1[20D s1qouuey *4P
*(Z19JUNG_) SsoWOJspURS poy ‘a

Rennel Burn.

------ Westerkirk.

*yooi-de1y, ‘2

---- Boykin Crag.

eneee Hollows Bridge.

k .---~— Rowan Burn.

‘apopysyy fo worsag—* | “ST

240) PROCEEDINGS OF THE GEOLOGICAL society. {[{ Mar. 5,

With reference to the appearance of the axis on the opposite side
of the sandstone area, owing to the thick deposits of clay and gravel
which cover up both the red sandstone and the Silurians on the west
side of the valley of the Annan and the east flanks of the Tinwald
Hills, we lose sight of these deposits until we reach a spot called
Blaweary in the parish of Lochmaben ; and at this locality N.N.W.
dips show themselves, leading to the inference that the axis is to the
S.S.W. from this. In the course of the Bellridding Burn, in the
parish of Torthorwald, on the south side of the high-road, we meet
with both N.N.W. and S.S.E. dips, indicating a proximity to the
axis; and in the same parish, in the course of the Peartree Burn, the
same circumstances are exhibited; and here too the purple grits,
which constitute the axis, are also seen. From this locality west-
ward we lose all traces of both the axis and the Silurians themselves ;
but the former appears to strike in the direction of the syenitic
mountain Criffel in Kirkcudbrightshire.

The course of the axis, as traced in Dumfriesshire, agrees with
that laid down by Professor Nicol in Roxburghshire, and supports
the inference that it has a E.N.E. and W.S.W. route through the
Silurians of the South of Scotland.

The lithological nature of the strata composing the axis seems to
be the same throughout, consisting of purple grits which have great
resemblance to some of the bottom-rocks of the Longmynd.

With regard to the strata which lie conformable to the axis on
both sides, they consist of thin-bedded greywacke sandstones, having
grey and purplish red shales interstratified with them. The pur-
plish-red shales are much more abundant in these lower portions of
the Silurians than in the strata more immediately connected with
the superior anthracitic and graptolitic shales; and their presence
serves to mark a low zone in the Silurians of the South of Scotland.

Although the strata most intimately connected with the axis oc-
cupy a considerable breadth of country on both sides of this axis,
there is reason to conclude that these beds do not attain any great
thickness, but that they owe their wide area to frequent repetitions
in consequence of flexures ; these flexures on the north side having
oblique curves towards the north, and the reverse occurring on the
south side of the axis; in consequence of which we have almost uni-
form N.N.W. dips on one side and 8.S.E. dips on the other. This,
however, is not universally the case; for in the course of the Lamb-
ridden Burn in the parish of Torthorwald, on the north side of the
axis, both a N. anda S. dip obtain, in consequence of curving in
the strata, but the usual N.N.W. inclination soon succeeds. Like
circumstances are seen on the south side of the axis in the same
parish, at the farm of Barleiuth ; and a similar occurrence may be
seen in Eskdale on the farm of Billholm.

The occurrence of flexures among these deposits is also exhibited
by the irregular angles of inclination, as well as by the comparatively
uniform characters of the repeated strata.

There is another circumstance which tends to corroborate the in-
ference that the beds immediately contiguous to the axis have been

1856. | HARKNESS—LOWEST ROCKS OF ESKDALE. 241

repeated several times both on the north and south side,—and this
is the aspect which the deposits of a shaly nature present, which is
of such a character as would result from the violent twisting of them
and their associated strata. Many of the shaly beds in Eskdale are
rarely capable of being divided along the lamine of bedding, but
have a broken-up appearance, the small fragments having a rhom-
boidal form ; and at one locality in this portion of Dumfriesshire,
namely Boykin Crag in the parish of Westerkirk, we have these
shaly deposits so far changed (the result of pressure in consequence
of oblique curving of the deposits) that the argillaceous beds here
are possessed of a decided slaty cleavage, this being the only locality
among the Silurians of the South of Scotland where this form of
structure occurs, so far as I am aware of. So rare is this form of
structure in the mountainous districts of the South of Scotland, that
Prof. Sedgwick* cites the district as affording proof against cleavage
resulting from lateral pressure,—an opinion in which I was disposed
to agree ; but more minute examination of the country, and a more
enlarged experience of the nature and features of this structure, as it
is manifested in the Devonians of the South-west of Ireland, have
induced me to adopt an opposite conclusion.

The great mass of the strata which make up the Silurians of this
part of Scotland are of an arenaceous nature; a composition which
is not so susceptible of being impressed with cleavage as argillaceous
deposits ; and they have not been subjected to the same amount of
flexuring as those small areas which are more intimately connected
with the axis, and which it is the object of this communication to
describe ; therefore it is in these latter, which abound in argillaceous
beds, that we have that rearrangement of particles which seems to
result from lateral pressure in consequence of the oblique flexuring
of strata.

The deposits which compose the beds lying on the bottom-rocks
of the South of Scotland present some circumstances which afford
considerable insight into the physical conditions under which these
were formed. The alternations of thin-bedded sandstones and shales
indicate that these strata resulted from comparatively shallow water ;
and the abundance of ripple-markings corroborates this inference.
In one locality, on the south side of the axis, at Binks in Roxburgh-
shire, about three miles N.E. from Mosspaul Inn, the ripple-marked
surfaces of the sandstones are well seen, as well as the alternations
of the thin argillaceous and arenaceous beds. Here also we meet
with evidence of another character, which, considering the extremely
low position of these sedimentary rocks, is of an important nature.

Some of the thin beds forming the deposits in this locality con-
sist of alternating layers of very fine sedimentary matter, associated
with coarser layers; deposits which have originally been fine and
coarse mud. On the faces of the beds which are composed of the
former, in one instance, we have distinct traces of desiccation-cracks,

* Brit. Paleoz. Fossils, page xxxvi, nofe.

242 PROCEEDINGS OF THE GEOLOGICAL sociETy. [ Mar. 5,

in the state of fine lines emanating from several centres, and joining
together in the usual manner of cracks in sun-dried mud.

The features which mark this occurrence, and also the laminz in
which it is seen, distinctly point out the deposition of mud in a lo-
cality where littoral conditions prevailed ; and where the subsequent
exposure of this fine mud to solar influence caused it to shrmk : these
very ancient desiccation-cracks afford us the earliest direct evidence
which we possess of land above the surface of the waters of the
palzeozoic sea.

In the deposits which occur at Binks, and also in similar beds on
the north side of the axis in the Tinwald range of hills, there are
found pitted hollow markings on the surfaces of the strata ; and, on
splitting one of the thin beds in which these markings are seen, the
latter are found frequeutly to extend through the thickness of the
stratum. At first sight they appear to have been formed by marine
worms in their burrowings ; but, as they decrease both in diameter
and distinctness as we proceed downwards, they could not have re-
sulted from such a cause. On examining the base of a stratum where
these markings are seen, they are found to occur in the form of
small, somewhat circular hollows, all tailing away in one direction.

These markings, from their nature and the mode of their occur-
rence, seem to have arisen from the influence of very slight currents,
which, meeting with some small impediment, probably in the form of a
grain of sand, washed a small hollow in the side offered to the flow of
the water ; and during the deposition of the mud forming the strata
these hollows continued to increase in size, until they assumed some-
what of the form of the burrows of Annelids.

In these low strata we possess proofs of currents in the form of
ripple-markings, also in the gentle drifting of the mud which eonsti-
tutes these beds ; and the lithological nature of the deposits indicates
that they have had their origin in shoaling water ; and, even at this
remote geological time, we see evidence of a muddy shore in the
presence of the sun-cracks which fissure the lamine of the fine shales
of these beds, belonging to a series of strata which are among the
most ancient of the paleeozoic division of sedimentary deposits.

Nor are these beds altogether devoid of such evidence as shows
the existence of animal life during the period when they were being
formed. At the locality already alluded to as affording distinct
proofs of the operation of causes such as now prevail in shallow
water, we find the surfaces of some of the strata marked by the
meandering tracks of Annelids ; showing the existence of this form
of animal hfe im this locality at a very early period. These annelid-.
tracks are not, however, the only circumstances which indicate the
occurrence of animal life; for-we have a track also of another kind,
and such as seems to have had its origin in the wanderings of an-
other tribe of animals, viz. Crustaceans. This track consists of a
central line and two lateral series of markings (see fig. 2). The cen-
tral line appears to have been formed by either a keel-like projection
on the lower portion of the animal, or to have originated from the

1856. | HARKNESS—LOWEST ROCKS OF ESKDALE. 243

tail being dragged along the ground. On each side of this central
lime we have a regular series of other lines, of a more complex nature,
arranged almost at right angles to the cen- |. 5

tral line; these are about the one-fifth of Fig. 2.—Impression on
an inch in length, and the nearest of these “@ suaface of the
lines to the central one is at about the di- A4gstone at Binks,
stance of its length, viz. one-fifth of an inch. Roxburghshire. (Na-
These lateral lines, which are somewhat tural size.) .
broken, and arranged at nearly right angles f ;

to the centre one, are broader and deeper at Teed ye
their extremities ; and outside of them there ws
is seen, slightly before each, a small pitted ~~ || 7
hole about the size of a pin’s head. These 4¢---e att i
lateral linear impressions appear to have been — Pain
produced by legs, and the holes near their "ee a
extremities seem to have arisen from joints, ¢------- « | 2 @
while the small hole in front looks like the “se f 7
markings caused by the tip of the leg. If * ez PO. wigs
these markings have resulted from Crusta- Cee
ceans, they afford us proof of the very early e _
existence of Crustaceans with feet. d--P 9 re
[Note on the Fossil Track from Binks, ices pate
by Mr. Salter.—We may apply to this im- < $
print—which through Mr. Harkness’s kind- oe eo °

%

ness I have had full opportunity of study-
ing—the name of Protichnites scoticus. ; }

The imposition of this generic name does not in any way imply
that the creature which made the track was generically identical
with those which produced the tracks in the Potsdam sandstone,
and which Professor Owen has so well described *. On the con-
trary, there are some differences of importance, indicating, as I think,
that a single pair only of members (in addition to the median ridge
of the body) were employed in making the impression ; whilst in the
Canadian tracks there were (according to Prof. Owen) certainly three,
four, or five pairs ; or, if (as appears to me most probable) each im-
pression was made by its own independent limb, seven or eight pairs
of such members may be supposed to have existed.

The inner and double imprints, aa, are all so closely like each
other, and so much of the same size, as to indicate that the same in-
strument produced them in succession ; and the smaller indents, c,
are not so unlike but that they might have been also impressed by
the tip of the same weapon in different positions. They were pro-

' bably made (assuming that the creature was a Crustacean, as is most

likely) by the basal joint or joints of a bent limb, or swimming
foot ; while the single indents, 6 4, not always present, might be made
by the tip of the same limb during each stroke. These strokes appear
to have been given at first at a greater distance from the central line
or track (e) than the latter ones, which have gradually converged

* Quart. Journ. Geol. Soc. vol. viii. p. 214.

244 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 5,

towards it, as if from want of muscular power, and to have been then
renewed again with fresh vigour * ; and a corresponding difference is
observable in the strength of the median track, as if the body had
been elevated and depressed at intervals.

We have only traces of three of these successive, and, so to speak,
spasmodic attempts at progression in what was probably very shallow
water, scarcely deep enough to float the animal. In the lower or
first group there are six pairs of larger imprints, gradually coming
nearer to the central line, and somewhat closer also to each other ;—
then a small one, c, which may have been a point of rest, much nearer
to the groove than the others: the eighth pair suddenly starts out
again, and with a breadth equal to those of the first set, and four, or
probably five strokes of this series were given before the line of pro-
gression, having swerved a little from the original direction, was re-
newed again, somewhat to the left, at, where we have only the central
groove and a single pair of imprints, the rest being lust.

The whole would be consistent with the action of a single pair of
_ swimming limbs, and the impression of a poimted or ridged sternal

portion, but does not, I think, favour the supposition of a long body
with a pointed caudal segment, such as Hymenocaris or Eurypterus
possessed.—J. W. SALTER. |

At Binks also there are seen on the strata some branching bodies,
which from their indeterminate form must at present be referred to
that division which includes most indistinct organic bodies, viz.
Fucoids.

Organic remains are not, however, restricted to this locality amon
these very low strata of the Lower Silurians of the South of Scotland.
Fossils are found in the reddish-purple shales, which have been al-
ready alluded to as occurring, along with the thin grey shales and thin-
bedded greywacke-sandstone (as developed in the parish of Apple-
garth at Upper Cleugh Burn, on the south side of the axis). These
fossils consist of Protovirgularia, which was first discovered in this
spot last year by my friend Sir William Jardine, and also some small
branching bodies, which appear to bifurcate dichotomously, and have
somewhat the character of branching Graptolites of the genus Didy-
mograpsus. ‘These were met with by the late Prof. E. Forbes and
myself, in the same reddish-purple shale which affords Protovirgu-
laria, in the autumn of 1854. ‘They are, however, too indefinite to
admit of their being assigned to any known forms.

Graptolites also occur on the south side of the axis at Dalton
Rocks in the parish of Dalton, Dumfriesshire ; and these, from their
relative breadths, seem to belong to two species. They are, how-
ever, in too imperfect a state to allow of their being referred to any '
particular species. They are met with in a shaly bed, associated with
greywacke-sandstone very distinctly rippled ; deposits very different
from those which contain these fossils elsewhere in Dumfriesshire.

On the south side of the axis, in this county, we have no traces

* Or it may be, as kindly suggested to me by Prof. Owen, that the body was

elevated by the successive strokes, and the feet consequently touched the ground
nearer to the central line.—J. W.S.

1856. | HARKNESS—LOWEST ROCKS OF ESKDALE. 245

of the anthracites and the graptolitic shales which are connected
with them; and it would appear that no strata occupying so high
a position are developed on this side of the axis in this district. I
have hitherto been led to the conclusion, that the beds of Griestone,
Peeblesshire, and what I regard as their equivalents in Kirkcudbright-
shire, the Barlae flags, occupy a higher position than the anthracite
shales and their accompanying graptolite beds; but, when we take
ito consideration the flexures to which the Lower Silurians of the
South of Scotland have been subjected, and the consequent repetition
of the same strata, it is by no means improbable that the Griestone
graptolite-flags, and the Barlae deposits affording these fossils along
with Fucoids, are inferior in position to the anthracitic shales ; and
perhaps they may be the Scottish representatives of the fucoidal
sandstones which underlie the graptolite-beds of Sweden and Nor-
way *. There is one circumstance which serves to support this
inference as to the inferior position of the Griestone and Barlae flags,
which is based on fossil evidence,—this is the occurrence of the
hitherto almost purely Scotch fossil, the Protovirgularia, in these
beds and in the low-lying reddish-purple shales which are found
near the axis. Theanthracite and graptolite schists, which abound
in fossils, have as yet never afforded the genus Protovirgularia in
Scotland, and its appearance in the low beds would tend to the con-
clusion that it is a fossil characteristic of a low zone among the
Lower Silurians of the South of Scotland.

Formerly I was disposed to consider the several parallel bands of
anthracite-shales as the result of faults: I now consider that they are
the products of flexures,—a cause assigned for their occurrence by
Sir Roderick Murchison t,—which would also account for these beds
sometimes lying above, and at other times below, the flaggy beds of
Griestone and Barlae.

The inferior position of these latter strata is also supported by the
occurrence in them of a species of Olenus, which I found in these
deposits last summer at Corfarding, in Penpont parish, Dumfries-
shire.

Hitherto the lowest beds in the Lower Silurians of Scotland which
have furnished animal remains are the graptolite and anthracite
schists and the flagey beds of Griestone and Barlae, and their equi-
valents.

The position of the strata more immediately referred to in this
memoir is lower than either of the deposits just mentioned, and in
them we have the earliest traces of animal life which have been de-
tected in Scotland, and these may be looked upon as amongst the
earliest records which we possess of organized existences.

* ¢ Siluria,’ page 318.

+ This form has been met with associated with the “larger Nereites”’ in Thii-
ringerwald ; see Sir R. J. Murchison and Prof. Morris’s Memoir on the Paleozoic
Rocks of Thiiringerwald, Quart. Journ. Geol. Soc. vol. xi. p. 413.

+ Quart. Journ. Geol. Soc. vol. vii. p. 163.

246 PROCEEDINGS OF THE GEOLOGICAL Society. [Mar. 5,

3. On Fossit RemMAtns in the CAMBRIAN Rocks of the LONGMYND
and Nortu Waters. By J. W. Satter, Esq., F.G.S., of the
Geological Survey of Great Britain.

[Puate IV.]

Tue occurrence of any organism in those ancient sediments which
have been so often called Azoic is of sufficient interest for an account
of it to be laid before the Society. We have hitherto been acquainted
with but one genus—and that doubtfully an animal or a plant—in
the oldest Cambrian schists of Ireland. No fossils from rocks of
this age have been recorded from England except the forms which I
now describe, and of which a brief notice was sent to the last meeting
of the British Association. They are a new Sea-weed, or Zoophyte,
traces of marine worms, and a Crustacean of the Trilobite group.

When, a few years back, I crossed the Longmynd with Prof.
Ramsay and Mr. Aveline, the unaltered and flat-bedded sandstones
which abound on the eastern side, and which are quite unaffected by
cleavage, appeared most promising for fossil remains, if any organisms
existed at the time when these rocks were deposited. Some of these
beds were ripple-marked, and the sandstones and flaggy beds of
greenish-grey stone were evidently not deposits from very deep water.
I hoped, therefore, that at least Oldhamia or Fucoids might be
found in them, if not more highly organized fossils; and in the
summer of the past year, I was able to devote three or four weeks
to the search.

A Fucoid, or at least one of those doubtful fossils we are in
the habit of calling such, had been found by myself a few years
back in the Cambrian grits near Bangor. It may be briefly described
here. |

Chondrites, sp.
The fossil alluded to is far too imperfect for any exact description to

be given of it; yet, as it is the only species known in these old rocks, it
should be noticed.

It occurs as elongated and nodular branches, generally 4 of an imch thick,
but of variable size, upon the surface of a coarse sandstone, the cleavage
of which interferes much with the shape of the fossil. It is even possible
that these apparent branches may have been produced by the crossing of
separate tubes, arfd that the whole may be due to large Annelides, the filled-
up burrows of which have a great resemblance to Fucoids, and are often
mistaken for them.

Loc. Moel-y-ci, a mountain near Bangor (1850).—J. W. 8.

That there may be no doubt about the geological position of the
fossils about to be described, it is as well to say that they occur in
nearly vertical beds of hard flag-like sandstone, which run along
the strike of the Longmynd at about 15 mile EK. from the principal
ridge; and they form part of a series of bluish-grey sandstones,
alternating with purplish slaty beds, which all lie delow the conglo-
merates and red sandstones of the Portway, and above the thick series
of dark-olive schists which are seen so well at Church Stretton, All
Stretton, &c., and which are the lowest portion of the Longmynd

1856. ] SALTER—LONGMYND FOSSILS. 247

series. See Section, fig. 1. The
fossiliferous beds, therefore, are
fairly packed in with strata which
are not only distinct in mineral
character from any of the Llandeilo
flags or Lingula-beds to the west
of them, but are unlike the upper
portions even of the Longmynd
rocks themselves.

The transverse valleys or “ gut-
ters’ on the east side of the moun-
tain afford excellent sections. Of
these, the brooks at All Stretton,
Church Stretton, Little Stretton,
Minton, and Batch are the principal ;
and along these rivulets the follow-
ing succession may be everywhere
observed, in ascending order*.

1. Dark-olive schists, with very
rare lines of crystalline limestone.
Church Stretton, All Stretton, Bro-
cards Castle, &c.

2. Harder beds, often rippled,
some felspathic, alternating with
thin courses of dark-greenish shale.
All Stretton Quarries, the Burway,
and Minton.

3. A thick series of hard and
greenish sandstones, generally very
fine-grained, except near the top
where they are flaggy, rippled, and
micaceous, and contain the fossils
hereafter noticed. These sand-
stones form the hills of Synold’s
Coppice and Bodbury Ring, are seen
at the Carding Mill, the Devil’s
Mouth, Winter Hill, and the ridge
between Round Hill and Callow
Hill, and have been traced as far as
the Packet Stone, above Minton.

4. Red slates and harder beds.
Conspicuous above the Carding Mill,
Church Stretton, W. of Yearling
Hill, Little Stretton.

5. Alternating grey and red slaty
beds and sandstones.

6. Hard grey beds like No. 3.
Light-spout Waterfall, above Church
Stretton.

d, Pentamerus-limestone.

f. Wenlock limestone.
e. Wenlock shale,
c. Conglomerate.

} Bala and Llandeilo beds.

h. Variegated fossiliferous sandstone.

Fig. 1.—Section of the Eastern Slope of the Longmynd, near Church Stretton.
g. Conglomerate.

(Reduced from the Horizontal Sections, Sheet 34, of the Geological Survey of Great Britain.)

} Longmynd rocks.

6. Hard shales.
a. Hard sandstone,

—s_.

. pl. 32. fig. 1.

—

* See also Silurian System, 1839, chap. xxi. p. 255, and p. 717

ee oe

248 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 5,

7. Alternating reddish and grey slates and sandstones succeed.

8. And these are overlaid by red sandstones, which form a band
three miles broad, extending from the Portway about three and a half
miles to the westward, chiefly vertical, or with a westerly high dip ;
they include thick bands of conglomerate ; the principal band is 120
feet thick*.

It is only in the grey sandstones, No. 3, that the fossils were found,
and these sandstones are so interstratified with the red shales, alter-
nating with them and dipping in the same direction, that it is im-
possible to regard them as anything but a part of the Longmynd
series, and rather low down in it.

The olive shales, Nos. 1 and 2, were searched vainly for any fossils,
and the greater portion of the next series, No. 3, which forms the
first considerable ridge, is of too fine and homogeneous a texture to
promise much. At the upper part, however, the beds are coarser
and more flag-like, and show considerable variations of surface.

Organic Remains+.—On the beds last mentioned, at the Carding
Mill, Church Stretton Brook, are numerous double impressions, not
a line long, but covering in quantities the surface of the slabs (Pl. IV.
fig. 1). They are elongated in one direction, and appear nearly
always parallel to each other,—a circumstance that at first suggests
their being merely mechanical marks, such as minute ripples or
ridges. But, when closely examined, they are found to be regular
in size, constantly double, and distinctly of two kinds, viz. one set
consisting of strongly impressed holes, as if recently made,—and.
others faint, as if subsequently effaced. I do not know anything to
which these markings can be properly referred, unless it be the holes
of marine worms, something like the Lob-worm of our own coasts.
It will be remembered that Mr. Binneyf first described such mark-
ings as the burrows of Annelides: they occurred in the flaggy sand-
stones of the lower division of the Lancashire coal-field; and he had
ample reason for believing his conjecture to be a correct one, by
finding the holes connected by a loop-like tube beneath the surface.

We may call ours, from analogy with these,

ARENICOLA pipyMA. PI. IV. fig. la, 1 6.

A. fodinis didymis, minutis, approximatis, ellipticis, sepissime
parallelis.

The most remarkable point, indeed, about these markings, whether
the deep, or the obliterated ones, is their parallelism. They never
deviate more than a degree or two from it; and, that this is not due
to lateral pressure, is clear from the fact that the position of the

* This conglomerate, recently cut through by the new road to Ratlinghope, is
of a very soft texture, easily worn away, and therefore not conspicuous except
in brook- or road-sections. Quartz-rock is its chief constituent; syenite is very
rare.

+ The fossils described in this paper are in the Museum of the Geological
Survey.

~ Mem. Lit. Phil. Soc. Manchester, 2nd Ser. vol. x. p. 191, pl. 1. fig. 2.

aE

1856. | SALTER—LONGMYND FOSSILS. 249

pairs of holes themselves is always the same, and a line connecting
them would be at right angles to their long diameter.

The only reason I can assign for this arrangement is, that it may
have been determined by the current, which in the direction of the
dotted lines might keep the holes clear from sediment, but in a
contrary direction might tend to choke them. I do not know enough
of the habits of the recent worms to explain it more fully.

Localities. Carding Mill, Stretton, in beds No. 3, north end of
Callow Hill, Little Stretton, and other places ; very common.

Annelide tubes. PI. IV. fig. 2.

Besides the above, which may be doubtfully referred to Worms,
there are occasional tracks of the Worm itself, in the form of shallow
furrows on the surfaces. Only a couple of these tracks, preserved
because of their greater sharpness, are represented in Pl. IV. fig. 2.
But on the surfaces of the slabs I saw several undulating impressed
lines, which I could refer to nothing else than the trails of such
creatures.

Locality. Callow Hill.

The most interesting, however, of these few fossils is one which I
cannot consider doubtful as belonging to a Trilobite, though differing
from any species yet described, and probably referable to quite a new
genus. I call it

PaLzZopycE Ramsayi. PI. IV. fig. 3.

We have three or four specimens, the best of which is represented
in Pl. IV. fig. 3. It is 22 inches broad, and 2 of an inch long. Its
forward edge is slightly curved downwards in the middle, but is
otherwise nearly straight, and has an angular ridge running along its
whole length just within the margin. The outer angles are rounded
off, and the sides are a little oblique, and appear as if they had been
produced, for the basal edge which follows the same line as the front
nee is a little curved downwards as it runs to meet the side

atc).

The centre is occupied by a parabolic axis, obscurely defined by
furrows. It is $ an inch broad, or nearly one-fourth of the whole
width, and appears to extend nearly to the basal edge. In another
specimen, however, it is shorter, and leaves a space 2 lines broad ;
but in this specimen the segment itself is somewhat broader and the
base more strongly ridged ; it may be the cephalic shield.

At first, indeed, all the specimens (four or five have been collected)
were supposed to be the heads of a new trilobite; and the axis (a)
was taken for the glabella. But the rounded outer corners (6, 6) in
the figured specimen negative this idea; the straight base and the
apparent production of the posterior angle, c, remind us most nearly,
among primordial fossils, of the new genus Dikelocephalus, proposed

250 PROCEEDINGS OF THE GEOLOGICAL society. | Mar. 5,

by Dale Owen* for the oldest known Trilobites of America, which
were found in the Potsdam sandstone of St. Croix, Minnesota.

The far more transverse form of our fossils, and the entire want
of annulation on the axis or side-lobes, are sufficient to indicate a
distinct genus; and I dedicate the species to Prof. Ramsay, who has
done so much to clear up the history of the Longmynd.

Locality. Ridge north of Callow Hill, Little Stretton. This fossil
occurs with the next described. .

Marks of PL aN figs.

There are numerous hollows on the surfaces of the beds, which
greatly resemble the impressions of Rain-drops. But they are less
regular, less equal in size, and, although generally oval and lying in
the same direction, have no ridge thrown up in front of them. It is
impossible, however, to say they have not been caused by primeval
rain; and Sir Charles Lyell, who examined them, was much struck
by their resemblance to those he has figured and described.

Across the same surfaces run very frequently raised thread-like
lines (PI. IV. fig. 4, a) in the same direction as the longer diameter of
the spots. Sometimes these lines are simply parallel, at others they
are branched, at others interrupted and fading off. But they are
sufficiently parallel and uniform in their direction over the bed to
make it probable that they are lines of mineral structure, rather than
anything organic, and I believe, too, that the drop-like hollows may
be due to gaseous bubbles, or to the decomposition of small concre-
tions, rather than that they indicate the marks of ancient showers.

Locality.—Carding Mill, in the base of the red or purple sand-
stone (No. 4). |

Ripple Marks (with thin mud-coating?). PI. IV. figs. 5 & 6.

The surfaces of very many of the beds are, as above noticed, co-
vered with ripple- or current-marks ; this is particularly well seen
about the small Waterfall called Light-spout, above Church Stretton.

Dark grey micaceous flags are there easily split into thin layers;
and on these the ripple-hollows are generally stained with a thin film
of protoxide of iron. Numerous radiating furrows, in the form of
very fine branched lines, run from the margin toward the centre of
these hollows or across them; the smaller ones near the edge run-
ning into the larger, just as brooks run into rivers. The lines are
always impressed on the upper surface of the bed (7. e. in the faces
dipping westward ), so far as this could be ascertained, and are ele-
vated threads on the casts of these hollows upon the lower surfaces ;
the edge of the hollow (PI. IV. fig. 5) being concave or convex in
each respective case. These ripple-marks have suffered, of course,
all the contortions of the beds; and hence are puckered (c), flat-

' * Report of Geol. Survey of Wisconsin, Iowa, and Minnesota. Philad. 1852,
p: 573, pl. 1.

TXT. PLIV.

0

JD.C. Sowerby lth.

Quart.Journ Geol Soc V

Ford & West imp.
FOSSILS FROM THE LONCMYND.

a

Oh
a iaf'8

;
RH
aa

*)
“fl

marin."

ee Le

1856. | SALTER-—-LONGMYND FOSSILS. 251

tened (a), folded (4), and very often obliterated. All these various
conditions are represented in one figure (woodcut, fig. 2), which
thus gives an average idea of the appearance of the markings when
perfect. The furrows themselves either slightly impress a plain sur-
face, as at a; or run between convex ridges, as at c, when they are
closer and more branched.

Fig. 2.—Diagram of the restored form of peculiar Ripple-marks on -
the Surfaces of the Flagstones near Church Stretton.

All these circumstances and the great irregularity of outlime con-
vinced me, after careful search, that these were not fucoidal impres-
sions*, but mechanical markings produced by the minute drainage of
the surfaces when the water retired; and hence that they afford
proofs of quiet littoral action.

Had the surface been merely sand, however fine, it is probable
that no such marks would have been produced, but that simple per-
colation would have taken place. But if a thin film of ochreous mud,
now a mere stain, were deposited on the surface, or washed into the
ripple-hollows, such a surface, being more retentive, might show the
tracks of the minute runnels of water as they flowed towards the
lowest part of the hollow before they were absorbed.

This seems but a slender datum on which to found a belief of the
proximity of land in these old Cambrian deposits. Their arenaceous
character, however, and the conglomerates which occur a little higher
up in the series, are better indications.

The conglomerates themselves, 120 feet thick to the W. of the
Portway, are well deserving study. They are chiefly round pebbles
of quartz-rock and vein-quartz ; but there is an occasional stray pebble
of syenite among them, as well as a great deal of felspathic matter de-
rived no doubt from the degradation of still older volcanic shores.

* Such as those described under the name of Dedalus by Marie Rouault, Bull.
Soc. Géol. France, 2de Sér., 1850, vol. vii. p. 736.

252 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 19,

Marcu 19, 1856.

Capt. W. S. Sherwill, the Rev. H. H. Wood, and D. T. Evans, Esq.,

were elected Fellows.
The following communications were read :—

1. On some Oncanic Remains from the BoNE-BED at the base of
the Lias at Lyme Reeis. By the Rev. Mr. Dennis. Com-
municated by Sir C. Lyexz, V.P.G.S.

[This Paper was withdrawn by the Author by permission of the Council.]
(Abstract.) ;

In this communication the author drew attention to some peculiar
bones and teeth from the Bone-bed which occurs between the Trias
and the Lias. Mr. Dennis considered that some of these fossils
presented mammalian structure under the microscope. Among the
specimens from the Lyme Regis bone-bed, Prof. Owen determined
the remains of Lepidotus and Saurichthys, and also of a fish, Pla-
codus, which had not previously been recognized among British
fossils.

2. On the VALENCIENNES Coat-Basin. By MM. Decouste and
Laurent, Civil Engineers.

[In a letter to, and communicated by, A. Tylor, Esq., F.G.S.]
(Prate Y.)

WE are enabled to give you some particulars relative to the works in
the coal-basin of the Departments of the “‘ Nord”’ and the “ Pas de
Calais,”’ on the prolongation of the Belgian coal-basin of Mons. At
the end of the last century, France in the north possessed only the
mines of Anzin, which were first worked in 1716. This state of
things lasted until 1832, when the workings had only extended to
Denain. In 1839, the concessions of Douchy, Bruille, Vicoigne,
Aniche, Azincourt, and Thivencelles were made. The works of re-
search went on until 1841, at which period the adventurers, discou-
raged by the numerous fruitless attempts made in the supposed direc-
tion of the basin—towards Arras, abandoned them. Six years later,
the works undertaken towards the north-west of Douai, in the direc-
tion of the present concessions of the ‘‘ Pas de Calais,” indicated the
true direction of the coal-basin, and up to 1854 numerous trial-
sinkings, of which many passed through the coal, led to the esta-
blishment of nine new concessions. A tenth on the border of the
basin is in progress. Two more also have been made this year, one
to the north of Douai, the other to the north of Bethune, above
Choques, where it is supposed that the bands of dry coal (faisceau
maigre) end, the coal-basin beyond this place becoming narrower,
and representing only the seams of caking-coal in all the concessions

- 1856.] DEGOUSEE AND LAURENT—N. FRENCH COAL-FIELD. 253

to the west. Many works have, moreover, been undertaken in the
course of the last three years in search of a widening of the basin by
the series of the seams of caking-coal, and of an extension of the
dry-coal-band, which disappears at Choques. With the exception of
those made by the “ Vendin Company,” these sinkings have as yet
given only negative results.

In all the smkings which have been made from Valenciennes to
the furthest of these researches, the Chalk forms the “head” (mort
terrain) with a varying thickness. As far as Aire the Chalk alone
forms the rock which has to be passed through before reaching the
Coal, from which it is separated by a bed of green sand from 1 to 3
metres in thickness, known under the name of ‘‘tourtia.”” On the
north of Aire it is, in addition, covered up by tertiary deposits,
alternations of sands and clays, with a thickness in places of 100 to
150 metres, and which render it necessary to line the sinkings as
the work advances. This formation is found even in Belgium, at St.
Ghislain, near Mons, with a thickness of 60 metres.

The average thickness of the overlying beds is 140 metres. It
seldom exceeds 180 metres, and was found to be only 85 metres at
Marles, near Bethune. It is near this town that the depth to the
base of the Chalk is the greatest ; the sinkings which have been con-
ducted on the south gave a result at a smaller depth.

Nearly 2,000,000 fr. have been expended by various companies,
all formed of private persons, in more than 150 sinkings, and nume-
rous workings have resulted, which have increased beyond all ex-
pression the wealth of these two Departments, have opened up a por-
tion of the coal-field of France, and enriched, on a grand scale, the
fortunate adventurers.

The small basin of Fiennes and Hardinghen, near Guines, is inde-
pendent of this large one; it is a coal-deposit in the Mountain
Limestone, and has been worked for some time past for local con-
sumption ; the coal is found at a slight depth, but the quantity of
water renders the workings both difficult and expensive.

Similar works are progressing in the Dep. of the Moselle, where
they are tracing the prolongation of the Sarrebruck basin, beneath
the New Red Sandstone. Eight companies have already met with
the coal between 200 and 300 metres in depth, and are applying for
concessions. It is in this quarter and in the Dép. du Nord that the
principal search is now being made, and where we have the greatest
number of establishments.

As to the explorations between Douai and Valenciennes, where
only shafts, and perhaps a few sinkings for the study of the ground,
have been made, we are unable to give you such information as we
have with respect to the new companies, whose recent works present
much more interest.

Herewith we send you a tracing, according to scale, of the works
done to the west of Valenciennes, together with an indication of the
concessions which have been obtained in the ‘“‘ Département du Nord”’
and the “ Pas de Calais,”’ as also the names of the villages where the
most important sinkings have been made. (See Plate V.) We have

VOL. XI1.—PART I. T

254 PROCEEDINGS OF THE GEOLOGICAL society. [{ Mar. 19,

marked with a red line all those places where the sinkings have hit
the Coal or the ‘ coal-measures”’; with a green line those where
the Mountain Limestone is reached, and with a blue line those where
the sinkings are in the Silurian formation. We have indicated the
extent of the several concessions, and have marked, by two red lines,
the limits, as they are at present approximatively known, of the coal-
basin of the “ Pas de Calais.” Lastly, we give you separately the
number of the sinkings which we know have been made by various
companies in the course of the last few years.
Paris, December 26th, 1855.

Note.—Several errors in the names of places occur in Plate V. MM. Degousée
and Ch. Laurent, having seen a copy of the lithographed Map, which was pre-
pared from the tracing forwarded to Mr. Tylor, have kindly transmitted another
sketch-map (containing several new features of interest), with the local names
very distinctly written. The following isa list of the more important errata :—

For Marquises_ _read Marguise. For Harnes read Hasnes.

— Hardinghem — Hardinghen. — Sollan — Sallau.

— Nottinghen — Lottinghen. — Baches — Raches.

— Fouquenottes — Foucquexolle. — Eupin — Erchin.

— Vizernes — Wizernes. — Marchicourt — Emerchicourt.
— Ellinghem — Eblinghem. — Menchicourt — Monchecourt.
— Lapagnoy — Lapuignoy. — Auiche — Aniche.

— Gounay — Gesnay. — Rilloy — Tilloy.

— Bally-grenay — Bully-grenay. — Auzin — Anzin.

— Anhay — Annay. —Ep.

3. On the Sanpstones and Brecctias of the Sout of Scor-
LAND* of an age subsequent to the Carboniferous Period.
By R. Harkness, Esq., F.G.S., Professor of Geology and Mine-
ralogy, Queen’s College, Cork.

In a memoir “on the New Red Sandstone of the Southern Portion of
the Vale of the Nith,” published in vol. vi. of the Quart. Journ. Geol.
Soc. (p. 389), I have given in detail the names of the localities where
sections of these strata are exposed, also their dip at the several lo-
calities, and the connexion which exists between the different depo-
sits composing what is termed the “‘ New red sandstone”’ in this
neighbourhood.

In describing the area occupied by this sandstone, I have been in
error in supposing that, in the locality under notice, there is a con-
nexion between the sandstone-beds of the Vale of the Nith and those
of that portion of the Vale of the Annan in which the Corncockle-
muir strata occur. A more perfect examination of the Dumfriesshire
sandstones induces me to believe that there are five, if not seven distinct
areas occupied by these deposits; and that the beds which appear in
these several districts have an intimate connexion with each other,
and are, for the most part, referable to the same geological age.

* See also Mr. E. W. Binney’s paper “On the Permian Character of some of
the Red Sandstones and Breccias of the South of Scotland,” Quart. Journ. Geol.
Soc., No. 46, p. 138.—Ep.

ir
7
pill

es)

Quart Journ. Geol. Soe. No\.XM\P1.V.

16) Cravelines List of Concessions andi Borings continued

List of Concessions and: Borwngs
Superficial | Number = =
‘ Mirea | ofBorings Gee Dilhep i
‘ Order} Companies Concessvons yee ee, 2 | Fresnes -Midi Thivencelles 9 | ar
i Kilenuira|Heetares.| Coal | Negative 4
- = ee [ree = Concession granted. \ Escaupont , “ 10 .
Vieux: Condi ( Nori) 39 | 62 3 | Crespin-3 ™ Marty |) Crespin F 2B | 42 é
1 | Auur Fresnes 20. 73 Marly +, 33 I .
| Se Saulve i 22 é Chatcaw UAbbaye 9°| 6 x
Odometx . 3 16 e 4 | Vicoigne Bruille b a .
«Hamas 2 9 Z
ae Raismes 45 20 Vicoigne as Thi 20 *
PP Guiness ‘ a Hasnon - W | 88 Neeux (Fis de Calais) 65 | 28 \(Neux)8!
- Auzn , WS | 52 ' 5 | Douchy Douchy (Nord). 34 19
‘ Ss Denan : 13 VW ’ 6 | Awiche Auiche W8 | 52 C
* Ss + 7 | Arincourt Azneourt 8 | 70
Sy (oa & | Lascarpe UE scarpelle | Nerd & Passe (ninss) | 47 a 8 1
SSE 9 | Dourges Dourges (Pus de Calais) 37 | 87 6
. soonest Cassel: i “4 rs
= z : co) ee W | Courridres Courritres di? 45 | 97 | 6 1
+ . Ze sis : iit || Hom hop : oo | 37 \ 6 2 é
= Sa oe : 2 | Bethune Grenay 57 | 6 | 6 1
Dot Omer ; ‘ 13 | Bruay Bruay : i eee Le 1
: WA | Killers Marlis : | sa hee 3
ERM OTS Ellinghon ; KN 5 ert j
. ) Boulogne - Département x ¢ 5 15 | Ames & Ferfay Ferfay r = = 6
‘ fr Gitaxebrouck Sad : 3 ‘mae 16 | Auchy-au- Bois Auchy elise ||o3 4
Coe ES eae . 17: \ Lys Supérieure - x = 2 3 Concession upplird for
Nord i é s
O48 / \ 18 | Vendin -les-Buhune er |e al bo
Hargisouphern % |
os a > 19'| Douaistene = = 3
a Nord f 20| Fiennes &Hardinghem\ Picines & Hardinghem = = Omeesston qrantal
Oure Francois = a]
cle Thefquaitne eee al
as ire . gr
Dede $ ix
Cees @sVenane cre &

Coyceque iN C y HS es
e) CY 44, Manche if Ci \ oe
z OLERE f ;
Desi ye teetene MéBernanchon 7
fii) . 18 i 4
Flishin i 7 SC cillers aK
= Gronicham. {

\ ‘Tournay 5
Obdingher
Se Mara . z pe
/ } C rf < ee aa — oe e = . : : :
Feuquirai poy, ; , : \ ct.
Chinas pun : eas ‘ .
18 Te SS ee
; *Labussilee + Vermales ; y
Bruay + — Uaillecourt Byam iiGas 2 ,
a cS *Mazingurber / we: : TS
> Courcitres a: — 7 Mons «
ea oun 7 y .
~ *Grenay | | ney :
——s * Ballygrenay | / 10 Sats Aievin Malmaison : : : 6 S
e x Noulelle tn TOMS eterno FF x Sa,
: eh | : = Warendin x
—— 7 = Sottan | Fr ;
Billy” Mop feet PAuby 8 i u = =
DISTRICT SE he ae
; T, Lins me / ; :

. ; 4

Ss Pas de Calais /
REFERENCE. : uy)

<n [The outlines and particulars of the Concessions and Mining [

Borings at Places underlined this ——-————~ reach Mountain Limestone. have bandervul from MM Laurent und Degouste, Ingérarurs \

y

(Concession Concession Auxin

Car

d Naiche

| + Ratsmes
Lerrhicourt « Auiche
— :
_... Silurian Rock . des Sondagis, Haris ( Some of dus Geological information has .

already been published by Mle Viconite D'drehuae.) The \
outlined areas of the Carboniferous and Doonan rocks have

buen traced in. from MER. Godwin -Austen’s MS Maps]

U ee ee ge Coal - reassures

Ravay
Expostires of Devonian Rocks.

CM. Coal Measures

LC. Lower Carbonifirous }
ML. Mountarn Limestone. y Fhoey
U.M.L. Upper Mountain Limestone.
L.ML Lower Mountacn Limestone 4 5, Nord
a 7 2 ores
D.L. Devonian Limestone jt 2 PRG C02) :
te Scale in French Leagues f
AD aera i Berlaimone«
M.D. Middle Devoraan
L.D. Lower Devonian
ilowutr ex) (ete So z! 3 Myriamitres BL :
Seale in Kilomatres 2), Gunbrac

e Landrecies:

Maibuuge »

ad oe
a) its ul i <
ee

Sint

rae
ie

i:
yp htin Ay ey a.

*Newee \84

me

1856. | HARKNESS—-PERMIAN ROCKS OF SCOTLAND. 299

Topography of the Sandstone areas.—To commence with the
eastern side of the county, we have, occupying theS.E. extremity, a
portion of the great deposit of sandstone which covers so large a sur-
face of Cumberland. This has the usual aspect of the deposits in the
latter county ; and, if we regard the sandstone of the country around
Carlisle as Triassic, we have no alternative but to adopt the same
nomenclature for this portion of the Dumfriesshire sandstones.

This area, commencing on the Solway Frith, in the parish of Cum-
mertrees, and running in an E.N.E direction to the Liddle at Can-
nobie, I regard as Trias, and newer than the deposits to be more fully
alluded to.

In the Vale of the Annan, about six miles to the north of the above-
mentioned area, the country is occupied by another area of sandstone,
to which the name of the ‘‘ Corncockle area’? may be applied. Whe-
ther this can be connected with the deposits which occur on the east
side of the River Annan, to the south and north of Moffat, is doubt-
ful ; and I am at present disposed to consider that in the higher por-
tion of the Vale of the Annan there are three distinct areas, viz. the
Corncockle,—the one which is seen in the form of a breccia in the
streams immediately to the KE. of Moffat, and to the S.E. at Bellcraig
Linn, in the state of both sandstone and breccia,—and the third, filling
up the head of the Annan in the district called the ‘ Marquis of
Annandale’s Beef-tub.”’

To the N.W. of the north-western extremity of the Corncockle
area, beyond several ridges of Lower Silurian mountains, there is
found another spot where the sandstone presents itself, viz. to the
S. of the farmhouse of Mitchell-Slack, in the course of the Capple
Water. The area occupied by this is very small, probably not ex-
ceeding half a mile, if so much, in diameter ; and the beds here have
a brecciated character.

Westward from this last, we have another patch, of considerable
size, occupying the east side of the Nith, from the Drumlanrig tunnel
on the Glasgow and South-western Railway, to near Blackwood,
having more than six miles in a N. and 8. direction; and exceeding
two miles in its greatest breadth.

To the south of this the ‘‘ Dumfries area’’ appears, which has
been already described. If the higher portion of the Vale of the
Annan contains three areas of sandstone, we have scattered over the
face of Dumfriesshire seven distinct patches of this substance ; and
these areas are well and widely separated from each other. If the
higher portion of the Vale of the Annan contains only one patch,
then we have five areas occurring under like circumstances.

Each of these several areas, with the exception of the one regarded
as Trias, and the one which appears in the course of the Glasgow
and South-western Railway immediately south of the tunnel (which
may be termed the “Thornhill area’’), has so far as can be deter-
mined Lower Silurian rocks for its margin. The other two are sur-
rounded by Carboniferous rocks.

Sandstones and breccias of an age posterior to the Carboniferous
are not confined in the South of Scotland to Dumfriesshire; we

T2

256 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 19,

meet with deposits having the same characters, and apparently be-
longing to the same age, at and about Mauchline in Ayrshire ; and,
if we add this to the number, it gives us either six or eight patches
of sandstones, covering several widely remote areas in the South of
Scotland.

Physical Geology of the Sandstone-areas.—Besides the question
as to the geological age of these patches, their position and isolation
are matters of some importance, and there are certain circumstances
connected with the physical geology of these strata which render
them interesting.

As the Dumfries area has been already described, any matters of
detail connected with this may be found in the memoir already
alluded to. There are, however, certam phenomena or physical
characters which are not there mentioned, and which should be
noticed.

Corncockle Sandstone-area.—To commence with the Corncockle
area,—this presents us with sandstones and breccias, but they have not ~
the same relative arrangement as deposits of this nature have in the
district around Dumfries. In the latter area we have a considerable
thickness of sandstones, forming the lower portion of the deposits ;
these are succeeded by thick breccias (Craigs breccias) ; and above
all we have sandstones, which are not extensively developed (Castle-
dikes sandstone). In the Corncockle area there appear to be no equi-
valents of the breccias, nor the higher-lying sandstones ; and the same
remark, so far as I can ascertain, applies to all the other areas both
in Dumfriesshire and Ayrshire. Breccias do occur in the other areas,
but not under such circumstances as are presented in the Dumfries
district.

In the most southern portion of the Corncockle area, at Dalton
Hook, we have breccias exposed ; and these possess some features
which are peculiar in Dumfriesshire. Here they were formerly
wrought for lime; the calcareous matter occurring in the form of
angular fragments of Carboniferous Limestone, characterized by the
usual fossils: these angular fragments are associated with others de-
rived from the Lower Silurians. Both the Carboniferous and the
Lower Silurian formations are met with at about a quarter of a mile
from the spot where this breccia has been worked. In this locality
the strata dip N.N.W., at a slight angle.

Breccias of a somewhat similar nature are seen in the course of
the Water of Milk, about two miles east from Dalton Hook; and at
the northern end of the Lockerby railway-cutting the breccia also
makes its appearance ; but here the fragments seem to be exclusively
of Lower Silurian origin, and the inclination is more towards the west.
Beds of sandstone are met with in the course of the Dryffe Water ;
and in the small burn which runs from the N.E. near Nether Cleugh
station, on the Caledonian Railway, beds of a similar nature are like-
wise found. In the course of the Upper-Cleugh Burn, immediately
as the newer beds come in contact with the Lower Silurians, the
former assume a brecciated character, like the deposit which is seen
at the north end of the Lockerby Cutting ; but at Upper Cleugh the

1856.] | HARKNESS—PERMIAN ROCKS OF SCOTLAND. 257

matrix is of a softer nature. In the Ryecastle Burn, about two miles
from Nether Cleugh station, where the two formations come in con-
tact, the newer is found resting on the older, and consisting of sand-
stones, which dip toward the W.S.W. Here, at the junction of
the two formations, breccias do not make their appearance.

At the north-eastern extremity of the Corncockle area the sand-
stones are well exposed. They occur in the course of the Annan at
Johnston Bridge, and have a south inclination ; and when we go west
from this, we find them well developed in the course of the Kinnel
Burn, about half a mile below St. Ann’s Bridge. See Section, fig. 1.
In this neighbourhood the best section of the sandstones and breccias
is seen which this area affords.

Fig. 1.—WSection in the course of the Kinnel Water, Parish of
Johnstone, Dumfriesshire.

ANIA
- cy \\\

\ AY
\\ \\ \\\ A \\\\
AY \\\ AA \ \
AY

c. False-bedded sandstones. 6. Breccias and sandstones. a. Silurian rocks.

A short distance above the foot-bridge over the Kinnel, near Eliza-
town, the Lower Silurians are seen with the sandstones almost in
contact. These latter consist of thin beds of red sandstone, false-
bedded, associated with breccias, the latter abounding to a greater
extent than the former. The total thickness of these strata exceeds
100 feet; and they have above them deposits of false-bedded red
sandstone, devoid of breccias ; the whole dipping south at an angle
of about 30°. Red sandstones of the same character occur in the course
of the Mollin Burn. They are seen also on the road leading from the
Moffat Road to Courance, and have a S.E. inclination. They also
present themselves in the Burrans Burn, with a S.S.E.dip. And at
the western extremity of this area the conglomerate occurs immedi-
ately under Kirkmichael Manse, abutting against the Lower Silu-
rians*. To the south-east of this locality, immediately below the
Water of Ae bridge, the sandstone likewise occurs; it is flaggy, and
dips N.N.E. ; and near Trailflat, in the course of the Ae, it is also
seen. From this last locality, 1am not aware that the sandstones or
breccias are anywhere exhibited until we reach Rammerscales; and
here we have the strata dipping north ; and at Smallholm the sand-
stone was formerly worked to a small extent, but the quarry is now
filled up. Here likewise the northern dip obtained.

In the interior of this area the sandstone is well seen at Corncockle
quarry, Templand Village quarry, Red Hall, and Lochbrow ; the two
latter quarries being now abandoned. In none of these four localities
are the breccias seen; but the sandstones of the two quarries now

* See Section, Quart. Journ. Geol. Soc. vol. xi. p. 469.

258 PROCEEDINGS OF THE GEOLOGICAL sociEeTy. | Mar. 19,

wrought, viz. Corncockle and Templand, differ materially from each
other. The former consists of very regularly bedded red sandstone,
easily worked ; the latter of a hard red flag, coarser than the Corn-
cockle beds, and remarkably durable. I know of no red sandstone
which at all approaches the Templand flags in respect of hardness.
In these two localities the strata dip to the W., at an angle exceed-
img 30°; and, as Templand lies a short distance to the S.W. of Corn-
cockle, the beds which occur at this spot occupy a higher position
than the Corncockle sandstone.

I learn from Sir William Jardine, that, like the Corncockle strata,
the deposits which occur at Templand afford fossil footsteps.

There are some circumstances in connexion with the Corncockle
area which are matters of interest. One of these is the directions of
the inclinations of the strata in the several localities where the sand-
stones and breccias are exposed.

Whenever we find the newer and the older formations near each
other, the former in all cases dips from the latter. On the eastern
margins of the area we have a westerly dip, on the western an
easterly dip, on the northern a southerly, and on the southern a
northerly dip ; and in the intermediate positions the same circum-
Stances occur.

Had the area been circular, we should have had the dips converging
to a central point ; but, as the form of the area is irregular, we have
an approximation to this mode of arrangement. The Lower Silurian
margins do not appear to present any evidence of the operation of
those causes which have given to the sandstones and breccias their
inclination ; for we have either a continuous N.N.W. or a continuous
S.S.E. dip occurring all through the Silurians of Dumfriesshire.
The cause of this peculiar mode of arrangement in the Corncockle
area seems to have been local; and I can attribute it to no other
circumstance than a subsidence in a small area, which has dragged
down the strata towards it in all directions, and so produced a series
of inclinations which always dip from the older formation.

Another circumstance of interest is the sequence of the deposits
which form the sandstones and breccias. As concerns the latter,
we have seen that it only occurs in certain spots along the margins of
the area. When we have higher beds, these are seen to be false-
bedded sandstones, as in the Kinnel Section ; and in no case do we
meet with any thick deposits of sandstone beneath the breccias, as is
the case with the breccias of the Craigs in the Dumfries area. The
mode of occurrence of the breccias would therefore lead to the in-
ference, that these are the lowest deposits,—that they are succeeded by
a series of sandstones to which those wrought at Corncockle appertam,
—and that the highest beds consist of the hard flags of Templand. We
have therefore three groups,—Ist, and lowest, breccias, with sand-
stones, more than 100 feet thick ; 2nd, sandstones, the thickness of
which has. not been ascertained, but which must be considerably
thicker than the breccias ; and 3rd, hard flags, the thickness of which
is not determined, but is probably less than that of the breccias.

The age of these several strata is also a matter of great interest ;

1856.] |§HARKNESS—PERMIAN ROCKS OF SCOTLAND. 259

but this at present we are hardly in a position to discuss. At one
time I was disposed to regard them as triassic, resting the conclusion
on the character of the sandstones and the nature of the footprints
found on them.

With regard to the latter, which are principally Ghelonians I find
these differ in the relative length of the toes from those which occur
in the Trias sandstones of Western Point, Runcorn, Cheshire ; and,
as Chelonians have existed during several geological epochs, too great
importance may be attached to impressions of this Order. Under these
circumstances, therefore, the triassic age of these strata is doubtful.

Sandstone-areas of the upper part of the Annan.—With regard to
the two areas which occupy the east side of the River Annan, to the
north of the Corncockle area, these consist of breccias with false-
bedded sandstone ; and beds of these characters are best seen in the
Bell-Craig Linn, about four miles 8.S.E. of Moffat. They appear to
appertain to the lower strata of the more southern patch; and the
inferior-lyig conglomerates are well seen in the course of the Well
Burn, from below Heathery Haugh to above Arch-bank. In the
most northern area, the sandstone is well exposed at Newton; and
this is probably the lower portion of the false-bedded sandstone which
rests upon the breccias, as seen in the course of the Kinnel Burn.
It is on the eastern margin of these two areas that we have the beds
exposed ; and here they are seen dipping from the Silurians. The
western extremity of these patches is not seen, as the low ground is
occupied by drift, and by gravel deposited by the River Annan.
Where we have the newer strata exposed, they manifest themselves
under the same circumstances as in the more southern area, viz.
dipping away from the older deposits.

Sandstone-area of Mitchell-Slack.—As regards the little patch in
the course of the Capple Water, below the farm-house of Mitchell- .
Slack, this is so small that little can be made of it, except that, from
its brecciated vature, it appears to have affinity to the lower portion
of the Corncockle series. It has a southerly inclination, dipping
from the high hills which lie to the north. Its area cannot be made
out owing to the drift which covers it, except in the spot before
alluded to. This patch is, however, so closely surrounded on all
sides by Lower Silurians, that the area occupied by it must be very
small. Such a small isolated patch, surrounded on all sides by
Silurian hills from 1000 to 2000 feet high, is a matter of considerable
interest in connexion with physical geology.

Thornhill Sandstone-area.—The sandstone-area on the east side of
the River Nith, around Thornhill, and occupying the lower portions
of the parishes of Morton and Closeburn, is of considerable importance
as concerns size; and its being, for the most part, surrounded by
Carboniferous rocks renders this area different in its boundaries from
the patches before-described.

We have better sections exposed here than in some of the other
localities occupied by sandstones and breccias; and we can derive
some information from this area which the others do not afford.

The ‘spot where we have the best sections of the strata of the

260 PROCEEDINGS OF THE GEOLOGICAL society. [ Mar. 19,

Thornhill area is in the course of the Creechope Burn, at Creechope
Linn, the scene of the retreat of Balfour of Burley in ‘Old Mor-
tality.” Here a small rapid streamlet has cut itself a deep channel
among soft sandstones, leaving steep cliffs on either side. At the
entrance of the Linn, a short distance above where the Creechope
joins the Cample Burn, we have purplish flagstones, which belong to
the Carboniferous age, dipping at N. 4°S.E. at an angle of 15°; and
the same flagstones are seen in the bed of the stream higher up the
Linn, at a spot called the Sutor’s Seat. The deposits, which at this
spot occur immediately above the Carboniferous flagstones, cannot
be seen owing to debris; but at about 9 feet above the flagstones
purple clays make their appearance, with cream-coloured spots,
devoid of lamination, and fracturing very irregularly. These have a
thickness of about 6 feet; and above them are seen the soft red sand-
stones, attaining a considerable thickness, and very much false-bedded.
See Section, fig. 2. In the purple clays I was unable to detect any

Fig. 2.—Section at Sutor’s Seat, Creechope Linn, near Thornhill,
Dumfriesshire.

. False-bedded sandstones.
. Purple clays.

. Not seen.

. Carboniferous grits.

aera &

fossils. The sandstones extend through the whole of the Linn, and
present the same false-bedded aspect, so much so that their apparent
directions and dips are not to be depended on. At Gatelaw Bridge,
about a mile north from Creechope Linn, the sandstone is extensively
worked ; and is here also false-bedded, but not to the same extent as
at the latter locality. Where the inclination is regular the dip is
N.N.W., at an angle of 15°; and at a short distance, higher up the
Cample Water, breccias are seen, which seem to underlie the sand-
stone of Gatelaw Bridge. Columnar basalt, with layers of amygdaloid,
occurs further to the east than the breccias, and has furnished the
latter with a considerable portion of their contents.

1856. | HARKNESS—PERMIAN ROCKS OF SCOTLAND. 261

In the course of the Glasgow and South-western Railway, we
have the sandstones exposed twice in the cutting between the Thorn-
hill and Carron Bridge Stations, and one of these exposures presents
a troughing of the beds. North of Carron Bridge Station, in the
cutting at the south entrance of the Drumlanrig tunnel, we have the
sandstones and accompanying strata well exposed. The beds here
dip south, at an angle of about 12°; and besides sandstones we have
breccias of an interesting character. The south end of the tunnel
consists of amygdaloidal trap ; and on the south side of this we have
the breccias composed of fragments of the igneous rocks in great
abundance ; and these, with the associated sandstones, dip from the
amygdaloids. See Section, fig. 3. At the north end of the tunnel,

Fig. 3.—Section at the South Entrance of Drumlanrig Tunnel,
Carron Bridge Station, Dumfriesshire.

6. Sandstones and Breccias.
a, Trap-rock.

we have variegated Carboniferous grits, dipping 8.S.E., at an angle
of 25°; and through these grits the igneous rock has burst.

The occurrence of igneous rocks here, and the relations which
these bear to the Carboniferous beds, as well as their connexion
with the newer sandstone strata, are subjects of interest, as we are
enabled, to some extent, to derive information concerning the age of
the latter; and this is more important as we shall find in another
district the sandstones and breccias occurring under like circumstances.
The relations which exist between these several rocks show that the
outbursts of trap were anterior to the deposition of the sandstones and
breccias ; and this does not appear to be a mere local occurrence, but
tends to support the inference that the Coal-fields of the centre of
Scotland had not only been deposited, but had been subjected to all
those violent disturbances, and outbursts of igneous matter, which
are so prevalent among them, before the deposition of the sandstones
and breccias. .

as in the other areas of sandstone which are found in Drumfries-
shire, we have no proofs that the causes which disturbed them have
affected the Silurians surrounding this area; but the intermediate
Carboniferous strata partake to a great extent of the influences of
the forces which have disturbed the newer formation. From the
appearance of the breccias in the lower portion of these deposits, I
am. disposed to consider them as the equivalents of the lower and
middle portion of the Corncockle series.

262 PROCEEDINGS OF THE GEOLOGICAL sociEeTy. [Mar. 19,

Sandstone-area of Mauchline, Ayrshire—We have now to leave
Dumfriesshire and go to near the centre of the adjoining county
Ayrshire. In this district, around Mauchline, there is another patch
of red sandstone and breccias exhibited. About a quarter of a mile
to the south of the Mauchline Station this sandstone is worked. It
possesses all the features which characterize the false-bedded sand-
stones above the breccias in the several Dumfriesshire areas, and
seems to be of considerable thickness. About half a mile further
south, at Ballochmoyle, in the course of the Water of Ayr, we have
a beautiful section exhibiting these sandstones and the strata upon
which they repose.

Immediately above the bridge over the Railway the red sandstones
dip N. 50° W., at an angle of 15°; and as we go up the Water of
Ayr, from newer to older beds, we see a great change taking place
in the nature of the deposits.

The lowest strata of the sandstones are soft, and rest upon a thick
series of breccias, which in appearance are like those at the south
entrance of the Drumlanrig tunnel, and consist of angular fragments
of amygdaloid, in the cavities of which are nests of zeolitic minerals.
In the highest portions of these breccias there are thin beds of a
siliceous limestone, of a purplish colour, but in these I found no
organic remains. See Section, fig. 4. In going up the stream, from

Fig. 4.—Section near Ballochmoyle, Water of Ayr, Ayrshire.

c. False-bedded sandstones.
5, b. Impure limestone.
a, a. Breccia.

the higher to the lower beds of the breccia, we come upon a trap-
dike which cuts off the beds, and from which the fragments entering
into the composition of the breccias have been obtained ; and on the
eastern side of the dike we have Carboniferous grits, similar to those
which surround the sandstones of the Thornhill area.

The association of the several rocks here is intimately connected
with what is seen at the entrance of the Drumlanrig tunnel, the only
difference being that at Ballochmoyle we have a more perfect section

1856.] |§ HARKNESS—PERMIAN ROCKS OF SCOTLAND. 263

presented to us. As regards the thickness of the sandstones, there
are more than 200 feet exposed in the Water of Ayr; and the por-
tion of the breccias which is seen must be nearly 50 feet in thickness.
The newer strata here exposed appear to me to be most probably the
representatives of the low breccias and overlying sandstones of the
typical area, Corncockle.

Sandstone-area of Dumfries.—We have now to return to’the area
already described*,—the Dumfries area; not for the purpose of
alluding to it in detail, but to endeavour to find out its relation to the
several patches which have been noticed. In the memoir referred to,
the Locharbrigs quarries are noticed (doc. cit. p. 391). These are
the quarries which are nearest to the Corncockle quarry ; and some
of the strata seen in them are identical with those at the latter
locality, afford the same chelonian footsteps, and have even the same
angle of dip and direction. Like the Corncockle strata, they have
no breccias covering them, and any person examining the two localities
would arrive at the conclusion that they are the same, not only in
nature, but position. We have in the Dumfries area no exposures
of the beds which are subjacent to these sandstones, and consequently
the breccias which support these are not seen.

If the sandstones of the Corncockle quarry and the Locharbrigs
strata are the same (which I believe to be the case), then we become
possessed of a clue which enables us to judge of the connexion ex-
isting between the other beds of the Dumfries patch and those already
alluded to.

The Craigs quarry, south-east from Dumfries, is in the line of the
strike of the Locharbrigs sandstones. It is similar in its nature, and
it affords the same footprints. As we go from Locharbrigs to this
quarry, the breccias come on, and are well seen occupying a position
above the sandstone at Craigs (see Section, fig. 5, p. 264); and, conse-
quently, we have in some portions of the Dumfries area certain breccias
which have no equivalents occupying the same relative positions in
any of the other Dumfriesshire areas, nor in that of Mauchline in
Ayrshire.

These higher breccias differ from the lower ones in their nature ;—
they have fewer beds of sandstone interstratified in them, and they
are much harder in their composition than the inferior breccias.

It is by no means improbable that the hard flagstones of Temp-
land quarry, which overlie the beds of Corncockle quarry, may be
the equivalents of the lower portion of the Craigs breccias, which
are fully described in the memoir above referred tof. If such be
the case, and if the sandstones of Locharbrigs, Craigs, and other
localities in the Dumfries area be the equivalents of the beds at
the Corncockle quarry, then it follows that the sandstones and
breccias newer than the Carboniferous formation can be divided into
four distinct groups ;—1st, and lowest, breccias and sandstones, best
seen in the course of the Kinnel Water and at Ballochmoyle in Ayr-
shire ; 2nd, sandstones, for the most part false-bedded, well seen in

* Quart. Journ. Geol. Soc. vol. vi. p. 389.
t Loc. cit. p. 394.

264 PROCEEDINGS OF THE GEOLOGICAL SOcIETY. [ Mar. 19,

the Corncockle area, the Thornhill district, at Mauchline, and in the
neighbourhood of Dumfries ; 3rd, hard thick breccias, best seen at
the Craigs, Dumfries; and 4th, thin-bedded sandstone, only slightly
developed ; occurring at Castledikes, Dumfries, above the breccias*.
The Dumfries area presents, so far as can be seen, the same phy-
sical geology as the other patches; it appears to dip from the higher
hills, and forms a trough through which the River Nith flows.

Since my memoir on the New Red Sandstone of the southern
portion of the Vale of the Nith was written, there has been another
quarry opened immediately under the south-eastern end of the
Maiden-Bower Craigs. See Section, fig.5. Among the sandstones of

Fig. 5.—WSection near Dumfries, from Lochar Moss (S.E.) to the
River Nith (N.L.).

Georgetown Maiden’s Bower
S.E. Craig. Mid. Craig. Craig. N.W.
a , Castledikes
ES Ss sandstone.

Cc ---------

eee eenwne-=- &

Fault. Fault.

e. Castledikes sandstone. 5. Flaggy beds with footprints.
d. Breccias. a. False-bedded sandstones.
c. False-bedded sandstones.

this quarry, which occupy a higher position than those in which the
footsteps occur, there are seen features which, so far as I am aware,
are peculiar to this spot. The lithological characters of some of the
strata here show their intimate connexion with the overlying breccias,
since some of the beds have fine breccias mixed up among them. On
the surfaces of a few of the higher of these sandstones we have
singular markings, which, at first sight, are so remarkable that there
is a difficulty in knowing what to make of them. They consist of
sunken impressions on the upper faces of the beds. These markings
are in some cases somewhat rhomboidal in form, with sharp angles.
In other cases they have a rib-like appearance ; sometimes they are
sinuous, and at other times they are cylindrical ; and might be taken
for either portions of stems of trees, or fragments of large Orthocerata.
I was at one time disposed to regard them as the result of a peculiar
mode of rippling, such as would arise from the action of a small rill
over a muddy beach; but the angular character of some of the
markings is hostile to this opinion ; and the cylindricai form which
they sometimes present is also opposed to this idea. I am indebted
to my friend Sir William Jardine for the correct explanation as to

* Loe. cit. p.. 396.

1856. | HARKNESS—PERMIAN ROCKS OF SCOTLAND. 265

the nature of these smgular markings; some of the most beautiful
having been sent to him and being now in his possession. They are
a unique form of desiccation-cracks, produced on mud which, in con-
sequence of exposure to solar rays after the cracking, has curled up
at the edges in some instances; and this curling has sometimes pro-
ceeded so far as to cause the mud to assume almost the form of a
hollow cylinder, into which the sand has been afterwards poured ;
and in consequence we have the stem-like forms which occur in these
sandstones. Sir W. Jardine informs me that he has seen modifica-
tions of the same circumstances which produced these singular
markings take place on the banks of the River Annan among the
muds which have been deposited during freshets.

These markings are not the only impressions which the sandstones
of the Maiden-Bower afford. We frequently find on the upper sur-
faces of the strata pitted hollows ; and we have natural casts of these
on the under side of the overlying beds. On an average, the length
of these impressions is about 3 of an inch, and their breadth about
32 of an inch, so that they have a form approaching to oval. The
have a deeper impression on one end than the other, which gradually
thins out ; and these deeper impressions are all in the same direction
on one surface. I was at first inclined to regard them as resulting
from rain-drops; but they are larger and more irregular than the
pittings produced by either rain or hail; and Sir Charles Lyell, who
had an opportunity of examining this quarry with me, suggested that
they might be caused by the splashing of spray driven almost hori-
zontally on a muddy shore. Their elongated form shows that the
force causing them had a less perpendicular direction than rain, and
spray driven by the wind from the sea appears to have been their
origin *.

If the smgular markings already alluded to be the result of desic-
cation, and if these irregular oval markings owe their occurrence to
spray, then we have on these ancient shores proofs of a hot sun’s
rays falling on a muddy beach, and proofs of the lashings of the sea
by a violent wind which drove the tops of the foam-crested waves in
the form of spray on this old beach.

Isolation of the Sandstone-areas.—The isolated position of the
several sandstone-areas is a subject which next presents itself. Look-
ing at these patches on the map, and knowing that some of them are
surrounded by lofty mountains, it will at once be perceived that they
could not have been deposited singly in the several areas which they
occupy.

The intimate connexion which exists in the lithological characters
of the series of beds forming these patches, shows that they have had
a much more intimate union than they now possess; and all the
circumstances lead to the inference that they are the relics of a large
mass of sandstones and breccias which at one time covered a great
portion of the South of Scotland ; and which has been to a very great
extent removed from the surface of the upturned Silurians by denuda-

* Original sketches of these markings and of the desiccation-cracks are deposited
in the Society’s Library.—Ep.

266 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Mar. 19,

tion. At what period this denudation took place we have no means
of determining ; but a considerable amount of destruction must have
occurred during the pleistocene period ; for the beds which represent
this formation in some portions of the South of Scotland consist
almost exclusively of sand and gravel, the former of which has been
derived from the abraded sandstone, whilst in the latter we have
sometimes fragments of the higher breccia. It is, however, on the
whole probable that the sandstones and their accompanying strata
had suffered a great amount of denudation at a period antecedent to
the glacial epoch.

Previously to this denudation, it would appear that there existed
over an area which is now exclusively occupied by Silurians and Car-
boniferous rocks, thick deposits of a newer age, having their lower
beds composed of breccias and intercalated sandstones ; above which
were red sandstones greatly false-bedded; succeeded by hard breccias ;
the only remains of which in Scotland are to be found in the neigh-
bourhood of Dumfries, and thin-bedded sandstones, of which only
slight traces now remain. The preservation of the isolated patches
seems to have resulted from subsidences which have dragged down
into hollows these newer strata, the harder Silurians on their margins
protecting them from total destruction.

Age of the Sandstones and Breccias.—With respect to the age of
the sandstones and breccias of the South of Scotland newer than the
Carboniferous formation,—wehave as yet obtained from them no fossils
which will enable us to co-ordinate them with deposits of a like
nature elsewhere. Such evidence of the existence of animals as they
possess is not capable of affording us much assistance, since the foot-
steps obtained from the sandy strata seem to be unique among sedi-
mentary deposits ; therefore no definite conclusions can be drawn
from them. We are consequently under the necessity of adopting
lithological evidence in this matter. Red sandstones similar in all
respects to those described are common to many parts of the Trias
of England; but we do not find these red sandstones succeeded by
thick beds of breccia, as is the case with those under consideration.
Breccias are rare among the Trias, while conglomerates abound in
some of the middle and lower beds. We have, however, no conglo-
merates in the Scotch red sandstones; the absence of conglomerates
and the presence of breccias show that the lithological characters
of the strata will not support the conclusion that these deposits are
of the Triassic age.

We are therefore under the necessity of comparing them with
another formation which affords red sandstones. In the Permian
series we have sandstones which bear resemblance to those of the
South of Scotland. Here likewise we have breccias ; and Mr. Binney
has shown * that in the neighbourhood of Brough and Kirkby Stephen,
in Westmoreland, the associations and composition of the strata
closely resemble those of the deposits in the neighbourhood of
Dumfries, so much so, that he concludes the deposits of Westmore-

* Memoirs of the Literary and Philosophical Society of Manchester, vol. xii.
p. 257 & p. 267.

1856. | HARKNESS—PERMIAN ROCKS OF SCOTLAND. 267

land and the Craigs near Dumfries to be of the same age. Sir Charles
Lyell and myself had an opportunity of examining the Westmoreland
strata above referred to, and can acquiesce in the conclusions con-
cerning relative position and mineral character. Sir Roderick Mur-
chison had some years before adopted the opinion of the Permian
age of the Dumfries series*, and was the first to announce this view.
Mr. Binney also, when he accompanied me several years ago to the
Craigs, seemed disposed to question the Triassic age of the strata there |
exposed ; and on this occasion, when we visited the quarry at Green
Mill in the parish of Caerlaverock, where beds similar to those of the
Craigs quarry, and occupying the same position, are worked, he was
the first to detect footprints. These impressions he stated were
different from any found by him in the Trias of Cheshire.

Resting the conclusions therefore on the mineral evidence, it would
appear that the sandstones which have hitherto generally been re-
garded as of Triassic age must be referred to the Permian; and
probably the only portion of Triassic sandstone which occurs in the
South of Scotland is that extending from Cumberland into the south-
east of Dumfriesshire, the association of the strata of which is entirely
different from that in the several areas described.

The existence of animal life, in the form of Reptiles, during the
period of the deposition of these Permian beds must have been
abundant, since we meet with numerous impressions caused by Che-
lonians, Lizards, and Batrachians, which walked over the shores of
the Permian Sea when its sandstones were sandy beaches with mud-
patches scattered over them.

* Quart. Journ. Geol. Soc. vol. vii. p. 163.

268

DONATIONS
TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY,

From January \st, to March 31st, 1856.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

AMERICAN Journal of Sciences and Arts. 2nd Ser. Vol. xxi. No. 61.
January 1856. From Prof. Silliman, For. Mem. G.S.

A. D. Bacher.—Earthquake-waves on the American coast, 37.
E. Hitchecock.—New Fossil Fish and Footmarks, 96.
T. Coan.—Kilauea, 100.

Mauna Loa, 139.

Rose.—Aluminium, 129.

Macgowan.—Farthquake in Japan, 144.

Coal in Chima, 145.

J. Wyman.—Rain-drop-markings (recent), 145.

J. W. Bailey.—Diatomaceous deposits, 115.

Fall of Meteoric Stones, 146.

Koch.—Zeuglodon, 146.

Notices of Books, &c.

Arts, Society of, Nos. for January—March, 1856.
Assurance Magazine. No. 22. Jan. 1856. Vol. vi. pt. 2.
No. 23. April4856. Vol. vi. pt. 3.

Atheneeum Journal for January, February, and March 1856. From
W. Dilke, Esq., F.G.S.
Notices of Meetings.

Basel, Verhandlungen der Naturforschenden Gesellschaft in. Zweites
Heft. 1855.
A. Miiller—Einige Pseudomorphosen vom Teufelsgrund im
Miinsterthal, 1. B., 283.

DONATIONS. 269:

Basel, Verhandlungen der Naturforschenden Gesellschaft in. Zweites -
Heft. 1855 (continued).
H. M. Vondermiihll.—Colestin bei Frohburg, 295.
P. Merian.—St. Cassian-formation in Vorarlberg und dem nérd-
lichen Tyrol, 304.
—— Ueber verschiedene Petrefacten aus der Stockhorn-
kette, den italianischen Alpen und der Umgegend von Lu-
gano, 314.
Zahn von Ursus speleus von Massmiinster, 320.

Bengal Asiatic Society, Journal. New Series, No. 75. 1855, No.5;
No. 76. 1855, No. 6.

Berlin. Zeitschrift der Deutschen geologischen Gesellschaft. Vol.
vii. Part 2. 1855.

Proceedings of the Society and Letters, 297.

Bornemann.—Die mikroscopische Fauna des Septarienthones von
Hermsdorf bei Berlin, 307. (10 plates.)

Von Pfuel.—Lagerungsverhaltnisse einige Braunkohlenflotze bei
Jahnsfelde und Marxdorf westlich und siidwestlich von
Miuncheberg, 372. |

Ferd. Roemer.—Das altere Gebirge in der Gegend von Aachen,
erlautert durch die Vergleichung mit den Verhaltnissen im
ectee Belgien, nach Beobachtungen im Herbste 1853,

77.

F. A. Fallon.—Die durch die Chemnitzer Eisenbahn im Granulit
bei Waldheim aufgeschlossenen Serpentinparzellen, 399.
(plate.)

Th: tbe —Der Zechstein der Fiirstenthums Reuss-Gera, 406.
(2 plates.)

Q. Maschke.—Vorlaufige Mittheilungen iiber Kieselsaiurehydrat
und die Bildungsweise des Opals und Quarzes, 438.

————.. Part 3. 1855.

Proceedings of the Society and Letters, 445.

R. Hensel.—Beitrage ziir Kenntniss fossiler Saugethiere : Insek-
tenfresser und Nagethiere der Diluvialformation, 458 (plate).

Von Strombeck.—Ueber das geologische Alter von Belemnitella
mucronata und B. quadrata, 502.

H. C. Deville-—Ueber die Eruption des Vesuvs vom 1 Mai, 1855,
dll.

L. Richter.—Aus dem thiiringischen Zechstein, 526 (plate).

Ferd. Roemer.—Bemerkungen iiber die Kreidebildung der Gegend
von Aachen, gegriindet auf Beobachtungen im Jahre 1853,

34.

Bologna. Nuovi Annali delle Scienze Naturali. Ser.3. Tomo ix.
Fasc. 1-6. 1854.
Scarabelli—Conglomerato calcare gessifacto, 71.
Bianconi.—Se il mare abbia in tempi antichi occupato le pianure
e colli d’ Italia, di Grecia, dell’ Asia Minore, ete., 208.

Tomo x. Fase. 7-10. 1854.
Senoner.—Revista degli studi di Mineralogia, Geologia e Paleon-
tologia nella Monarchia Austriaca, 190.
Scarabelli.—Descrizione nella Carta geologica della Provincia di
Ravenna, 211 (with map).
VOL. XII.—PART I. U

270 DONATIONS.

Bonn and Breslau. Academiee Cees. Leop.-Carol. Nature Curio-
sorum Nova Acta. Vol. xxiv. Supplement. 1854.

Vol. xxv. Part 3. 1855.
Von Gorup-Besanez.—Chemische Untersuchungen der Mineral-

quellen zu Steben in der Langenau im Baierischen Voigt-
lande, 1.

Concours de Académie Impériale Léopoldo-Caroline
des Naturalistes de Breslau, proposé par le Prince Anatole de
Démidoff, Membre de |’Académie sous le surnom de Franklin,
a Voccasion de |’ Anniversaire du jour de naissance de S. M.
lImpératrice Mére Alexandra de Russie, le 13 Juillet (n. s.)
1856. Publié le 1° Juillet 1855.

Chemical Society, Quarterly Journal. Vol. vii. No. 4. Jan. 1856.
Titles of Chemical [and Mineralogical and Metallurgical] papers
contained in British and Foreign Journals for 1855, 309.

Cherbourg, Société Impériale des Sciences Naturelles de, Mémoires.
Vol. u. 1854.
J. Lesdos.—Sur divers minéraux existant dans les granites de la
cote de l’est de Cherbourg, 93.

Exploration géologique 4 Martinvast, disposition du
sol de la Montagne de Le Hure, 111.
Sur quelques roches Siluriennes du nord du départe-
ment de la Manche, 373.
Sur quelques minéraux trouvés 4 Cherbourg, 379.

Besnou.— Examen d’un nouveau minerai de mercure (sublimé
corrosif natif), 41, 207.

Civil Engineer and Architect’s Journal. Vol. xix. No. 262. Jan.
1856.
J. Neville-—Water-supply of Drogheda, 22.
E. Hopkins.— Vertical structure of rocks and gold-bearing rocks,
28.
No. 263. February 1856.

No. 264. March 1856.
R. Rawlinson.—Sewerage, Drainage, and Water-supply of South-
port, Smethwick, Camborne, and Ulverstone, 86.
Hutchinson’s artificial stone, 92.
H. Robinson.—The River Thames, 95.

Critic, the. For January, February, March, 1856.

France. Congrés scientifique de France qui s’ouvrira au Puy le 10
Septembre 1855. Programme, &c.

Congrés des délégués des Societés savantes des Départe-
ments. Septieme session. 24 Mars, 1856. Invitation.

. Bulletin de la Société Géologique de France. Deux. Sér.
Vol. xii. Feuill. 43-51. 1855.
Michelotti.—Sur divers fossiles recueillis aux caves dites de Saint-
Lazare, prés de la Havane (Ile de Cuba), 676.
Adolphe Roemer.— Découverte de Graptolites dans la Vallée de
l’Innerste, prés de Lauthenthal, dans le Harz, 685.

DONATIONS. 271

France. Bulletin de la Société Géologique de. Deux. Sér. Vol. xii.
(continued).

D’Hombres-Firmas.—Note sur la Terebratula diphya, 686.

Marcel de Serres.—Lettre relative 4 une note de M. Coquand sur
les terrains permiens des environs de Lodéve, 688.

Ami Boué.—Lettre sur divers sujets, 689.

G. Cotteau.—Notice sur l’age des couches inférieures et moyennes
de l’étage corallien du Département de l’Yonne, 695.

Note sur un nouveau genre d’Kchinide fossile :
Genre Desorella, 710.

Jules Beaudoum.—Note sur la composition des terraims de l’ar-
rondissement de Chatillon-sur-Seine (Céte d’Or), 716.
Triger.—Sur les terrains Jurassiques d’Angleterre dans les envi-

rons de Weymouth (Ile de Portland), 723.
J. Delanotie.—Sur la formation des silex, 732.
Ore eer sur la géologie de I’Ile Majorque (Pl. XV.),
34.

Duchassaing.—Observations sur les formations modernes de I’Ile
de la Guadeloupe, 753.

Ed. Hébert.—Note sur le terrain tertiaire moyen du Nord de
?Europe (Pl. XVI.), 760.

E. Bayle.—Observations sur la structure des coquilles des Hippu-
rites, suivies de quelques remarques sur les Radiolites (Pl.
XVII., XVIII. et XIX.), 772.

A. Sismonda.—Lettre 4 M. Ele de Beaumont sur le terrain
Nummulitique, 807.

Jules Marcou.—Notes géologiques sur le pays compris entre
Preston, sur la Riviére Rouge, et El Paso, sur le Rio Grande
del Norte, 808.

Résumé explicatif d’une carte géologique des

Etats Unis et des provinces Anglaises de ’Amérique du

Nord (Pl. XX. et XXI.), 813.
Vol. xin. Feuill. 1-2. 1855.

Helmersen.—Lettre 4 Sir R. Murchison sur divers sujets, 13.
Lardy.—Notice nécrologique sur Jean de Charpentier, 17.
Sir R. I. Murchison.—Recherches géologiques dans le nord de

l’Ecosse, 21.
Découverte de couches Siluriennes 4 Les-

mahago (Ecosse), 23.
E. Bayle.—Notice sur le Listriodon splendens et quelques autres
mammiféres découverts dans la molasse Miocene de la
Chaux-de-Fonds (Suisse), 24.
Ville-—Notice sur les gites d’émeraudes de la haute Vallée de
PHarrach (Algérie), 30.

Frankfurt. Abhandlungen, herausgegeben von der Senckenbergis-

chen Naturforschenden Gesellschaft. Vol. 1. part 2. 1855.
Fr. Scharff.—Aus der Naturgeschichte der Krystalle, 258 (with
photographie plate).

Hanau. Jahresbericht der Wetterauer Gesellschaft fiir die gesammte
Naturkunde zu, tiber die Gesellschaftjahre von August 1853 bis
dahin 1855.

R. Ludwig.—Ueber den Zusammenhang der Tertiarformation in
Mederhessen, Oberhessen, der Wetterau und an dem Rheine,
1 (with map). :
U

272 DONATIONS.

Hanau. Jahresbericht (continued).

R. Ludwig.—Verzeichniss der in der Wetterau aufgefundenen
Tertiarverstemerungen, nach der Schichten der Formation
geordnet, 62.

G. Theobald.—Die hohe Strasse, 83.

Th. Liebe.—Vorlaufige Notizen tber die Beimengungen der
Zechsteinkalke und ihre Beziehungen zur Farbung derselben,
127:

Lancashire and Cheshire Historic Society, Proceedings. 1848-9.

Hume.—Mineral springs at Leasowe, 105.

1849-50.

J. Dawson.— Analysis of Leasowe Water.
1850-51.
1851-52.
1852-53.
1853-54.

J. Rosson.—Porcelain-manufacture in Liverpool, 76.

. 1854-55.
Hi. Atherton.—Manufacture of Cobalt, 40.
J. Mayer.—Liverpool Pottery, 178.

Leeds Philosophical and Literary Society, Annual Reports, 1853-4,

1854-5.

Linnean Society, Journal of the Proceedings. Vol.i. No.1. March 1,
1856.

Literarium, the, or Educational Gazette. Vol.ii. No. 33. March 26,
1856.

Preparation of Aluminium, 525.

Literary Gazette for January, February, and March 1856. From
L. Reeve, Esq., F.G.S.
Notices of Meetings.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xi. No. 69. January 1856. From R. Taylor, Esq., F.G.S.
H. C. Sorby.—Structure and slaty cleavage of the Devonian
limestones, 20.
H. Poole.—Coal in Asia Minor, 79.
Godwin-Austen.—Newer Tertiaries of Sussex coast, 79.
J. Prestwich.—Boring through the Chalk at London, 81.
‘Sir R. I. Murchison.—Silurian rocks at Lesmahago, 82.
J. W. Salter.—New Silurian Crustacea, 83.
R. W. Banks.—Tilestones of Kington, 84.
D. Sharpe.—Elevation of the Alps, 85.
Kreil.—New Seismometer, 87.

—. No. 70. February 1856.

oi; Spiller.—Analyses of Babylonian cylinder and amulet, 107.

Wohler and Atkinson.—Analysis of Meteorites pis Transyl-
vania, 141.

DONATIONS. 273

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xi. February 1856 (continued).

H. C. Deville.-—On the density of quartz, corundum, metals, &c.,
after fusion and rapid cooling, 144.

H. C. Sorby.—On the physical geography of the Tertiary estuary
of the Isle of Wight, 163.

E. W. Binney.—On the probable Permian character of the Red
Sandstone of the South of Scotland, 164.

No. 71. March 1856.
. C. Nicholson and D. 8S. Price.—Sulphur in iron, 169.

E

E. Davy.—Peat-charcoal, 172.
R. P. Greg.—Rhodomite, 196.
R
R.

. W. Pearson.—Bismuth, 204.
Owen.—Fossil Bubalus moschatus, found at Maidenhead, 237.

J. Prestwich.—Gravels at Maidenhead, 237.
P. J. Martin.—Gravels of Sussex, 238.
J. EK. Bedford.—Raised beaches of Argyllshire, 238.
M. Mogeridge.—Peat-deposits at Swansea, 239.
W. Miller.—Eruption of Mauna Loa, 239.
S. Haughton.— Granites of Ireland, 239.
O. Fisher. —Earthquake in Switzerland, 240.

- No. 72. April 1856.

H. M. Witt.—Chemical examination of waters from near Mount
Ararat, 257.

Heddle.—On galactite and natrolite, O72.

O. Fisher.—On the Purbeck strata of Dorset, 307.

H. Poole.—Visit to the Dead Sea, 311.

R. Owen.—On Gastornis parisiensis, 311.

On mammalian remains from the Crag, 312.

R. Rubidge.—On the geology of parts of South Africa, 312.

R. Harkness.—On the lowest sedimentary rocks of South Scot-
land, 313.

J. W. Salter.—On Fossils from the Longmynd, 314.

Madrid. Real Academia de Ciencias de Madrid, Memorias. 1? Serie.
Ciencias exactas. Tomoi. Parte 1*. 1853.
A. Terrero.—Memoria sobre la Forma mas conveniente de los
Triangolos Geodésicos, 77.

5 . 3 Ser. (Cienc. nat.) Tomo i. Parte 3. 1854.

Lopez, D. P. P. y.—Memoria geognéstico-agricola sobre la Pro-
vincia de Asturias, 5.

Garcés, D. J. D. y.—Discurso sobre los diferentes métodos de
ensayar y afinar los metales preciosos y sus allaciones mas
usuales, 143.

Bayo, J. E. del.—Ensayo de una descripeion general de la estrue-
tura geoldgica del terreno de Espafia en la Peninsula : seccion
oF 16K.

——_——-. ——_——.. Resumen de las Actas, en el ano académico
de 1851 4 1852, leido en la session del dia 8 de Octubre, por el
secretario perpetuo Dr. Don M. Lorente. 1853.

1852 a 1853. 1854.

———_-. —————.. Programma para la adjudicacion de premios
en el ano 1856. }

274
Oxford.

Paris.

DONATIONS.

Ashmolean Society, Proceedings. 1855. No. 33.
Maskelyne.—The Koh-i-noor Diamond, 59.
Daubeny.—Amount of phosphoric acid in rocks, 73, 78.
Phillips.—Changes of physical geography on the coast of York-
shire in late geological periods, 80.
Daubeny. —Aluminium, 838.

Ecole des Mines. Annales des Mines. Tome vi. 6™ livr.

de 1854.

Lan.—Description des gites métalliféres de la Lozére et des Cé-
vennes occidentales, 401.

Damour.—Notice sur la perowskite de Zermatt, espéce minérale,
512.

H. Dubois.—De la présence de l’iridium dans l’or de la Californie,
518.

E. Rivot.—Extraits de chimie (travaux de 1853 et 1854), 523.

De Sénarmont.—Extraits de miméralogie, 562.

Découverte de lignite 4 Nossi-Bé et sur la cdte occidentale de
Madagascar, 570.

G. B. Greenough.—Sur la géologie de l’Inde (traduit par M. Elie
de Beaumont), 577.

Sur le lignite de Cadibona, 579.

Découverte de lignite prés de Candie, 580.

Importation et exportation du cuivre, de l’étam, du zine et du
plomb en Angleterre pendant Vannée 1854, 581.

Tome vi. 1" livr. de 1855.

Lan.—Histoire et description des mines et fonderies de plomb,
argent et cuivre de la Lozére, 1.

Juhos.—Note sur le traitement métallurgique des minerais de
cuivre gris dans l’usine Stephanhiitte (Haute-Hongrie), 53.

Rapports officiels adressés au gouvernement anglais par les in-
specteurs des houilléres, 61.

E. de Fourcy.—Anciennes carriéres de Paris, 69.

E. wes .—Voyage au lac Supérieur (Etats-Unis d’Amérique),
173

Tome vii. 2° livr. de 1855.

E. Rivot.—Voyage au lac Supérieur (Etats-Unis d’Amérique),
(suite et fin), 245.

J. Marcou.—Esquisse d’une classification de chaines de mon-
tagnes d’une partie de l’Amérique du Nord, 329.

Lan.—Histoire et description des mines et fonderies de plomb,
argent et cuivre de la Lozére (suite et fin), 351.

Pennsylvania. Franklin Institute of, Journal. 3rd Ser. Vol. xxx.
No. 6. Dec. 1855.

R. F. Brower.—Iron in Africa, 394.
Fremy.—Extraction of metals from ore of platinum, 412.
Utilization of slag, 416.

Vol. xxxi. January 1856. No. 1.

‘athens, a7, 65.
W. Beatson.—Sodium, 39.
Statistics of copper and zinc, 69.

—-——_—. ————-. ————.. February 1856. No. 2.

H. Mackworth’s “metra” for geologists and miners, 75.
H. Farrar.—Eruption of Vesuvius in 1850, 120.

275
Feb.

DONATIONS.
Pennsylvania. Franklin Institute of, Journal. Vol. xxxi.
_ 1856 (continued).
Edwards.—Titaniferous iron on the Mersey, 121.
Artificial stone, 132.

—_——. ———. March 1856. No. 3.
Canal through the Isthmus of Suez (plate), 150.

H. Moseley.—On the descent of glaciers, 211.
Photographic Society, Journal. No. 38.

Puy, Société d’Agriculture, Sciences, Arts et Commerce du Puy,
Annales. Vol. xviii. for 1853.

Repertorio Italiano per la storia naturale. Repertorium Italicum com-
plectens Zoologiam, Mineralogiam, Geologiam et Palzontolo-
giam, cura J. J. Bianconi. Anno 1853. Fasc. 1.

Notices of papers and books on Mineralogy, Geology, and Pale-
ontology, by

[Mineralogy |—
Scacchi, 96.

[Geology ]|—
Pitiot, 3.
Lanza, 8.
Meneghini, 29.
Ponzi, 31.

Cornalia, Chiozza, 33. Palmieri, Scacchi, 79.

Scarabelli, 51.
Gorini, 57.
Malacarne, 67.
Lombardini, 68.
Cesaroni, 75.

Fase. 2.

Tornabene, 89.
Lanza, 94.

[ Paleontology |—

Massalongo, 7, 55, 76.
Costa, 93.

N otices of papers and books on Mineralogy, Geology, and Pale-

ontology, by

{Mineralogy |—
Seacchi, 30, 31.
Lanza, 32.

[Geology |—

Pitiot, 2.

' Lanza, 4, 29.
Meneghini, 7, 48.
Ponzi, 8, 45.
Cora Chiozza, 9.

Searabelli, 13, 25.
Gorini, 16.
Malacarne, 19.
Lombardini, 22.
Cesaroni, 22.

Palmieri, Scacchi, 26.

Tornabene, 20.
Fergola, 34.
Aug. Sismonda, 44.

Anno 1854.

Lavi, 48.
Meneghini, 48.
Martius, 50.
Gastaldi, 50.
Bergmaschi, 52.
Catullo, 62.

[Paleontology |—

Massalongo, 3, 15, 23.
Oron. Costa, 28, 56.

Notices of papers and books on Mineralogy, Geology, and Pale-

ontology, by

[Mineralogy |—
Tassinari, 64.
Selmi, 65.
Sismonda, 67.
Cornalia, 87.
Sgarzi, 90.
Melloni, 113.
Ghisi, 124.
Guiscardi, 132.

[ Geology |—
Ponzi, 63.
Meneghini, 64.
Pizzolari, 77.
Pelligrini, 77.
Catullo, 82, 86, 112.

Caillaux, 84.
Pianciani, 89.
Corsini, 90.
Purgold, 91.
Melloni, 95.

Fergola, 96.

Cornaggia, 97.

Pilla, 105.

Zanon, 112.

Belli, 114.

Curioni, 119.

De Zigno, 120,123,126.
Giorgini, 121.
Fabroni, 122.
Ghirelli, 128.

Guidoni, 130.
Bianconi, 133.
Caleara, 136, 137.
Lancia, 137.

[ Paleontology |—

Meneghini, 88.
Bellardi, 98.
Massalongo, 109.
Or. Costa, 111.

De Zigno, 120, 123.
Catullo, 125.
Reyneval, 127.
Vandenheche, 127.
Ponzi, 63, 127.

276 DONATIONS.

Royal College of Surgeons, Index to the Catalogue of the Whe.
Royal Society, Proceedings. Vol. vii. No. 16.

———. No. 17.
Lord Wrottesley.—Presidential address, 560.
Obituary notice of Sir H. De la Beche and

others, 582.

Vol. si Ne. 18.
GB. Airy.—Account of pendulum experiments undertaken in

the Harton Colliery for the purpose of determining the mean
density of the earth, 13.

Vol. viii. No. 19.

Ee James.—Amount of the local attraction at Arthur’s Seat,
Edinburgh, 45.

Silesia. Zwei- und dreissigster Jahres-Bericht der Schlesischen Ge-
sellschaft fiir vaterlandische Kultur. Enthalt: Arbeiten und
Veranderungen der Gesellschaft im Jahre 1854.

Sadebeck.—Ueber die Seehohe der Thonlagers von Canth, 18.

Goppert.—Ueber die Seefelder in der Grafschaft Glatz und die
Torfbildung auf denselben, 19.

K. v. Nidda.—Ueber das Vorkommen von Graptolithenschiefer
in der schles. Grauwacke, 26.

Ueber das oberschlesische Steinkohlen- Becken, 28.

Scharenberg.— Ueber fossile Knochen aus den Galmei-gruben bei
Scharlei in Oberschlesien, 34.

Goppert.— Ueber das Kalklager zu Paschwitz bei Canth, 35.

Ueber G. C. Berendt’s in Bernstein befindliche orga-

nische Reste der Vorwelt, 57.

Statistical Society of London, Journal. Vol. xix. Part 1.
March 1856.

Vienna. Kaiserl. Akademie der Wissenschaften, Sitzungsberichte,
Math.-Nat. Classe. Vol. xvi. Part 2. May 1855.

K. Peters.—Die Nerineen des oberen Jura in Oesterreich, 336
(4 plates).

V. R. v. Zepharovich.—Jaulingit, em neues fossiles Harz aus der
J ae nachst St. Veit a. d. Triesting in Nieder-Oesterreich,
3

D. Stur.—Ueber die Ablagerungen des Neogen (Miocen und
Pliocen), Diluvium und Alluvium im Gebiete der Nordést-
lichen Alpen und ihrer Umgebung, 477.

. Vol. xvii. Part 1. June 1855.

Wohler. —Ein Meteorstein-fall bei Bremervorde, 56.

J. Heckel—Neue Beitrage zur Kenntniss der fossilen Fische
Oesterreichs, 166.

Vol. xvii. Part 2. July 1855.

W. Haidinger.—Vereinfachte Methode der graphischen Winkel-
messungen kleiner Krystalle, 187.

; Die Formen des Kalichloreadmiates, 189.

A. Boué.— Ueber die Quellen- und Brunnen-wasser zu Vosslau
und Gainfahrn, 274 (plate).

F. Wohler.~Analysis der Meteorsteine von Mezo-Madaras in
Siebenbiirgen, 284.

—

'

DONATIONS. SA i §

Vienna. Kaiserl. Akademie der Wissenschaften, Sitzungsberichte.
Vol. xvi. (continued).
L. Zeuschner.— Ueber die Verbreitung des Loss in den Karpathen
zwischen Krakau und Rima-Szombat, 288.

—_——————— ,

. Vol. xvii. Part 3. October 1855.

E. F. Glocker.—Neue Beobachtungen tiber das Vorkommen des
Stilpnomelans, 401.

F. Filipuzzi.—Della Paraffina, 425.

— Analisi del Carbone fossile di Cludinico in Carnia,

440.

F. Osnaghi.—Analyse des Mineralwassers zu Galdhof bei Selowitz
in Mahren, 443.

A. W. Scherfel.—Analyse des Schmokser Mineralwassers, 449.

W. Haidinger.—Vergleichung von Augit und Amphibol nach den
Hauptziigen ihrer krystallographischen und optischen Eigen-
schaften, 456.

L. Zeuschner.—Geologische Notizen, 475.

v. Russegger.— Bericht tiber das am 30. September 1855 Abends
gegen 9 Uhr stattgefundene Erdheben, 479.

K. F. v. Schauroth.—Ueber der geognostischen Verhaltnisse der
Gegend von Recoaro im Vicentinischen, 481 (map & 3 plates).

M. Hornes.— Ueber eimige neue Gastropoden aus den 6stlichen
Alpen, 612.

. K.K. Geologische Reichsanstalt, Abhandlungen. Vol. ii.

1855.
J. v. Pettko.— Geologische Karte der Gegend von Schemnitz
(map).
C. v. Ettinghausen.— Die tertiare Flora der Umgebungen von Wien
(5 plates).
Die tertidare Flora von Harmg m Tirol (31
plates).

Die Steinkohlen Flora von Radnitz in Boh-
men (29 plates).

K. J. Andrae.—Beitrage zur Kenntniss der fossilen Flora Siebiir-
gens und des Banates (12 plates).

. ———. Jahrbuch 1855. VI. Jahrgang. No. 1.
Janner, Februar, Marz.
W. Haidinger.—Das schwefelhaltige Bleierz von Neu-Sinka in
Siebenbirgen, 1.
Ferdinand Hochstetter.—Geognostische Studien ausdem Bohmer-
walde, 10.
J.v. Ferst].— Analyse emer neuen Mineralquelle bei Rohitsch, 39.
Karl Ritter v. Hauer.—Ueber das Bindemittel der Wiener Sand-
steine, 42.
Eduard Kleszezynski.—Die Mineralspecies und die Pseudomor-
phosen von Pribram nach ihrem Vorkommen, 46.
Karl Ritter von Hauer.—Ueber einen von dem Mechaniker Sieg-
fried Markus construirten Apparat zur Erzielung gleichfor-
miger Temperaturen mittelst emer Gaslampe, 64.
Franz Foetterle.— Ueber ein neues Vorkommen von Magnesit in
Steiermark, 68.
Karl Koristka.—Bericht iiber einige 1m mittleren Mihren ausge-
fuhrte Hohenmessungen, 72.

278 DONATIONS.

Vienna. K.K.Geologische Reichsanstalt. Jahrbuch 1855. No. 1!
(continued).

E. R. v. Warnsdorff.—Bemerkungen tiber geognostiche Verhalt-
nisse Karlsbads, 88.

E. F. Glocker.—Mnineralogische Beobachtungen aus Mahren, 95.

B, Cotta.—Die Erzlagerstatten der siidlichen Bukowina, 103.

Karl eae v. Hauer.—Ueber krystallisirte essigsaure Magnesia,
13

Mahren, 139.

M. V. Lipold.—Hohenbestimmungen im nordéstlichen Karnthen,
142.

K. Ritter v. Hauer.—Arbeiten in dem chemischen Laboratorium
der k. k. geologischen Reichsanstalt, 154.

Report and Proceedings of the Imp. Geol. Institute, 161.

Mineral price-list, 216.

. No. 2. April, Mai, June.

J ohann Kudernatsch.—Beitrage zur geologischen Kenntniss des
Banater Gebirgszuges, 219.

Eduard Kleszezynski.—Geognostische Skizze der Umgebung von
Pribram, 254.

A. Schefezik.—Ueber die Bewegung schwimmender Krystalle
einiger organischen Sauren, 263.

Karl Justus Andrae.—Bericht tiber die Ergebnisse geognostischer
Forschungen im Gebiete der 14, 18 und 19 Section der
General-Quartiermeisterstabs-Karte von Steiermark und II-
lyrien wahrend des Sommers 1854, 265.

Ludwig Hohenegger.— Neuere Erfahrungen aus den Nordkar-
pathen, 304.

Emanuel Urban.—Ueber Basalt in Schlesien, 312.

A. Hauch.—Darlegung der Resultate physicalisch-chemischer .
Untersuchungen der Mineral-Heilquellen von Szliacs in nord-
lichen Ungarn, 314.

Karl Peters.—Ein Vortrag tiber den irischen Riesenhirsch, Cervus
megaceros, Hart., 318.

Heinrich Prinzinger.—Geologische Notizen aus der Umgebung
des Salzbergwerkes zu Hall in Tirol, 328.

Fried. Rolle.-—Ueber einige neue Vorkommen von Foraminiferen,
Bryozoen und Ostrakoden in den tertiaren Ablagerungen
Steiermarks, 351.

Johann Jokély.—Geognostische Verhaltnisse in einem Theile des
mittleren Bohmen, 355.

Reports and Proceedings of the Imp. Geol. Institute, 405.

Mineral price-list, 431.

Yorkshire (West Riding) Geological and Polytechnic Society, Reports

of the Proceedings, 1849.
H. Denny.—The fossil flora of the Carboniferous epoch, with
special reference to the Yorkshire Coal-field, 1.
J. Haywood.—The formation and destruction of Limestone, 61.

Zoological Society of London, Reports of the Council and Auditors,
1852, 1853 and 1854.

. Proceedings. Nos. 227-237*, 1851; Part XX. 1852;
Part XXI. 1853; Part XXII. 1854; Nos. 284-298, 1855.

Ueber einige Stemkohlen von Rossitz in

DONATIONS. 279

II. GEOLOGICAL CONTENTS OF PERIODICALS
PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 2nd Ser. Vol. xvii. No. 97.
January 1856.

W. King.—On Anthracosia, a fossil genus of the family Unionide,
51 (plate).

L. de Koninck and Le Hon’s Recherches sur les Crinoides,
noticed, 58.

Rupert Jones’s Geological History of Newbury, noticed, 60.

J. Cocks.—Local dearth of littoral Algz, 76.

Valenciennes.—Rocks perforated by Echini, 76.

No. 98. Feb. 1856.
T. Rupert Jones.—On some species of Leperditia (plates), 81.
W. King.—On Pleurodictyum problematicum (plate), 131.
J. G. Baker’s Flowering Plants, &c., and their geognostic rela-
tions, noticed, 199.

. No. 99. March 1856.
Ww. King.—On Permian Palliobranchiata, 258.

Dunker and Von Meyer’s Paleeontographica. Vol. iv. Part 4.
Ph. Wessel und O. Weber.—Neuer Beitrag zur Tertidrflora der
niederrheimischen Braunkohlenformation (plates), 111.

Edinburgh New Philosophical Journal. New Series. No. 5. Vol. iii.
No. 1. Jan. 1856.
Anon.—Plurality of worlds, &c., part 2, 39.

D. Forbes.—Chemical composition of some Norwegian minerals, |
59.

Prof. Allman.—Introductory Lecture, 66.

D. Forbes.—Silurian and metamorphic rocks of South Norway
(geological map and plates), 79.

H. C. Sorby.—Physical geography of the Old Red Sandstone
sea of central Scotland, 112.

J. Flemimg.—Relations of the different branches of natural history,
125.

W.J. Henwood.—Metalliferous deposits of Kumaon and Gurhwal,
N.W. India, 135.

G. Langrebe’s Naturgeschichte der Vulcane, noticed, 141.

A. A. Hayes.— Native iron in Liberia, 167.

M. F. Heddle.—Meteoric lead in meteoric iron from Tarapaca,
Chili, 169.

W.S. Symonds. —Upper Ludlow bone-bed near Malvern, 172.

Hugh Miller.—Fossil floras of Scotland, 173.

Prof. Boedekir.—Vanadium and titanium in Spherosiderite from
Bonn, 185.

[Omitted—Vol. u. No. 2 :—
W. S. Symonds.—-Ceratiocaris, 404 (plate). j

Leonhard und Bronn’s Neues Jahrbuch f. Min. Geog. u. s. w.
Jahrgang 1855. Sechtes Heft.

Fr. Weiss.— Ueber die Grundgesetze der mechanischen Geologie,
641 (plate).

280 DONATIONS.

Leonhard und Bronn’s Neues Jahrbuch f. Min. Geog. u. s. w.
Jahrgang 1855. Sechtes Heft (continued).
Quenstedt.— Ueber Eugeniacrites caryophyllatus, 669.
H. Vogel, jun.—Analyse eimiger Mineralien (Arsenik- und Wasser-
Kies), 674.
Letters; Notices of Books, Mineralogy, Geology, and Fossils.

; Sieb. Heft.

Fr. Weiss.— Ueber die Griindgesetze der mechanischen Geologie,
769 (plate).

J.C. Deicke.—Eigenthiimliches Vorkommen von Petrefakten in
Meeres-molasse, 795 (woodcuts).

G. Jeusch.—Amygdalophyr, ein Felsit-gestein mit Weissigit, iil.
Nachtrag, 798.

Letters; Notices of Books, Mineralogy, Geology, and Fossils.

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.

Barrande, J. Note sur le remplissage organique du Siphon dans
certains Céphalopodes Paléozoiques.

Paralléle entre les Dépots Siluriens de Bohéme et de
Scandinavie.

Dana, J. D. Address before the American Association for the Ad-
vancement of Science, August 1855.

Dickson, S. The “ Destructive Art of Healing.”

Fairbairn, W. Useful Information for Engineers.

Further Papers relative to the Discovery of Gold in Australia. From
Sir P. G. Egerton, Bart., M.P., F.GS.

Gaudin, C. Th. et Ph. de la Harpe. Flore fossile des environs de
Lausanne.

Gilliss, G. M. The U.S. Naval Astronomical Expedition to the
Southern Hemisphere during 1849-52. 2 vols.

Hauer, F. de, et F. Foetterle. Coup d’ceil Géologique sur les Mines
de la Monarchie Autrichienne. Avec une Introduction par
Guillaume Haidinger. Traduit sur Poriginal Allemand par le
Comte Auguste Marschall.

Hauer, F. R.von. Ueber die Cephalopoden aus dem Lias der nord-
dstlichen Alpen.

Jones, T. Rupert. Notes on Paleozoic Entomostraca: No. 3. On
some species of Leperditia.

King, W. On Anthracosia, a fossil genus of the family of Unionide.

DONATIONS. 281

King, W. On Pleurodictyum problematicum.

Kjerulf, Th. Das Christiania-Silurbecken, chemisch-geognostisch
untersucht.

Logan, Sir W. KE. et T. S. Hunt. Esquisse géologique du Canada,
pour servir 4 lintelligence de la Carte Géologique et de la Collec-
tion des Minéraux Economiques envoyées 4!’ Exposition Univer-
selle de Paris, 1895.

Macgillivray, W. The Natural History of Deeside and Braemar.
Edited by E. Lankester. From H.R.H. Prince Albert.

Mortillet, G. de. Histoire de la Savoie avant l’ Homme.
———, SP rias du Chablais.

Roemer, Ferd. Paleoteuthis, eine Gattung nackter Cephalopoden
aus Devonischen Schichten der Eifel.

Ryckholt, Baron P. de. Mélanges Paléontologiques, 2™° partie.

Sedgwick, A. A Synopsis of the Classification of the British Paleeo-
zoic Rocks. With a Systematic Description of the British
Paleeozoic Fossils, by Fred. M‘Coy. 3rd Fasciculus.

Tchihatchef, P. de. Lettre sur les Antiquités de Asie Mineure,
adressée 4 M. Mohl.

The Correspondence relating to the Lancet Sanitary Commission.
From Messrs. Tegg and Co.

3 Webster, T. The case of Josiah Marshall Heath, the inventor and
introducer of the manufacture of welding Cast Steel from British
Tron.

Yates, James. Narrative of the Origin and Formation of the Inter-
national Association for obtaining a uniform Decimal System of
Measures, Weights, and Coins.

Zepharovich, V. R. von. Der Jaulingit, ein neues Fossiles Harz aus
der Jauling nachst St. Veit a. d. Triesting in Nieder-Osterreich.

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THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

ApRIL 9, 1856.
T. H. Huxley, Esq., F.R.S., was elected a Fellow.

The following communications were read. :—

1. Notes on the Groxtocy of the Neighbourhood of SypDNEY,
NewcastLe, and Brispane, AusTRALIA. By Mr. Jamess S.
* Witson, Geologist to the North Australian Expedition.

[Communicated by Sir R. I. Murchison, F.G.S. ]
(Abstract.)

THE country about Sydney is composed nearly altogether of sand-
stones belonging to the Carboniferous era, and similar in appearance
to those of the same age in the north of England. Although in the
vicinity of Sydney no coal has been found, with the exception of a
few very thin seams, seldom exceeding a quarter of an inch in thick-
ness, yet a thin seam of coal-shale of small extent occasionally occurs.
The sandstone-rocks about Sydney are generally white, consisting
of a clear quartz-sand united by a white earthy cement; there are,
however, two principal exceptions, viz. the top bed, which is a red
conglomerate, principally pebbles of trap, cemented with oxide of
iron,—and one of the lower beds, containing iron ; but in whichever
matrix the sand is found, it appears, when examined with a microscope,
to consist of minute crystals of quartz, partially rounded by abrasion.
VOL. XII.—PART I. x

284 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

The coal-shales of the Hunter River district are full of fossil
leaves, and some of them consist of a mixture of coal and clay, and
contain such an amount of bituminous matter that Mr. Beaumont
(Mineralogist to the Australian Agricultural Company) has expressed
an opinion that gas might be manufactured from them. Two seams
of coal only are being worked in this district ; a third is known to
exist, but is supposed to be too thin to pay for working at present.
It is two feet thick where seen, and is situated considerably below
the sea-level. The other two seams are from four to six feet thick,
but contain seams of carbonaceous shale which deteriorate the quality
of the coal.

At the entrance of Newcastle Harbour is a perpendicular rock
(called Nobby’s Island), once separated from the main land, but
now united by a breakwater that has been thrown across for the
protection of the harbour. The island exhibits a good section of
the rocks of the coal-field. The accompanying section shows the
arrangement of the strata.

Section of Nobby’s Island, Newcastle Harbour.

1. Mould. 6. Chert.

2. Trap-conglomerate. 7. Imperfect sandstones and shales.
3. Shales with plant-remains. 8. Coal.

4. Coal. 9. Trap-dyke.

5. Earthy sandstones and shales.

The island is intersected by a trap-dyke, 9 feet thick, running in
a direction nearly S.E. and N.W., and completely decomposed from
the top down to the sea-level, presenting only a greenish-white
greasy clay ; but beneath the water the dyke is perfectly sound and
hard; about low-water-level it crops up through the beach, and may
be seen at some little distance running out into the sea. A bed of
coal (the second in the series), that formerly extended far beyond the
present limits of the island, and through which the dyke passes, has
been washed away by the waves, with the exception of a few feet on
each side of the dyke, looking like a great half-consumed log; this

1856. | WILSON—AUSTRALIA. 285

portion is so hard that it resists the action of the water with greater
firmness than the trap-dyke itself to which it seems united.

The upper seam of coal, where it comes in contact with the dyke,
has been altered in the same manner; but the alteration extends
only a few feet on each side. A similar dyke passes through Beacon
Hill, where I saw a number of prisoners working a seam only a few
feet from the dyke, to obtain coal for the Beacon-fire.

At the top of the island, on the south side, the rocks have parted
from the dyke to the extent of about one inch, and the space has
been filled with clay and gravel, washed in from the shale and con-
glomerate above, as far down as the first coal-seam. This mixture
is highly impregnated with the oxide of some metal (supposed by
Mr. Stutchbury to be nickel), and is of a yellowish-green colour.
Nobby’s Island is about 100 feet high; but the top, as far down as
the first coal-seam, is being cut down to form a level base for the
erection of a light-house.

At a promontory called Red Head, six miles southward from
Newcastle, Mr. Beaumont showed me the remains of a fossil forest
on a broad bed of shale that was generally covered at high-water.
Roots of trees, evidently in the situation where they had grown, now
consist of rich ironstone. Some of the trees, broken off by the roots,
and lying in the place where they first fell, are similarly fossilized.
Some of the trunks are about 2 feet in diameter.

At a place three miles nearer to Newcastle, several tree-trunks, of
more than one kind, are exposed to view, all of which consist of iron-
stone. Near the same place, in the face of the cliff, but in several
beds higher in the series, a part of the trunk of a fossil tree, about
4 feet in length and 1 in diameter, stands erect in a bed of decom-
posed shale ; but this tree has nothing of the ferruginous character
of the trees of the lower bed.

In crossing the range of hills between Maitland and Singleton, I
met first with a porphyritic dyke, contaming fragments of quartz
and crystals of felspar; next was a shelly limestone, corresponding
to the mountain-limestone; and afterwards a hard conglomerate,
at a cutting west of the point where the Black Creek crosses the
road. It is of a bluish colour, and contains marine shells and water-
worn pebbles of the crystalline rocks.

From six to eight miles N.W. from Singleton are large quantities
of angular ironstone-gravel, without any appearance of having been
waterworn; and soon afterwards I found the source from which it
had descended,—namely, the remains of a fossil forest, similar to
that on the coast at Redhead. One large stem, that lay extended
from a wide-spreading root from which it had fallen, measured
12 feet in length. It appeared to me, that the rock in which these
trees are imbedded is the same in age as that containing similar
fossils at the water’s edge near Newcastle.

About five miles from Muswell Brook I saw an edge of old slate-
xe,

286 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

rocks standing vertically through the carboniferous rocks. A great
portion of the country between Muswell Brook and Mooroorundi is
comparatively level, and is generally excellent land. At the latter
place conical hills, of a trappean character, rise abruptly from the
plain-like valleys. One range, however (Wailand’s Range), crosses
within a few miles of Mooroorundi, and is rendered remarkable by
the constant burning of a coal-seam in one of the hills, called Mount
Wingen.

Mooroorundi is beautifully situated on the River Page, at the foot
of the Liverpool Range, having in view several tall peaks of basaltic
or trappean character, which may be seen ranging along the flank
of the hills, and rising above the rocks in which they had once
been enclosed.

From Mooroorundi I began to ascend the Liverpool Range, and to
pass over crystallme rocks. Soon after crossing the Page River I
found a fragment of granite that had been brought down by that
stream; a little higher slate-rocks began to appear; and about four
miles from the Page, in a deep cutting made for the road, trap is
overlaid by slate at an angle of 15°.

For a distance of thirty miles from this place, in a north and
westerly direction, I had been crossing a country of slate-rocks, but
they were so broken and deranged that I could not determine satis-
factorily any general angle of inclination ; but here I found a trap-
dyke between the slates inclined at an angle of 60°, and dipping to
the westward. A portion of the dyke seemed disposed to part into
polygonal blocks, similar to columnar basalt. Five miles further on,
quartz began to appear, and the slate-rocks presented a decided
strike and dip; the former N. by W. and S. by E. (magnetic); the
dip 60° to west. .

Having reached the Hanging Rock, at Hookanville, I went through
the diggings there, and examined the rocks of the locality. I found
a quartz-vein near the top of the rock, from which the drift-gold in
the neighbouring creeks and gullies has, without doubt, been derived.
The strike of the quartz-vei corresponds with that of the slate—
north and south. Following down the Peel River to the Peel River
Company’s Works, a distance of six or seven miles, the hills and
cliffs on each side of its course show very distinctly the position of
the rocks. They all stand vertically, and the strike is the same as
at the Hanging Rock. Dykes of porphyry and green-stone fre-
quently occur rising between the strata; and serpentine occurs im
considerable variety.

I was shown the works on the Peel River Company’s property by
the captain of the mines, who kindly endeavoured to give me all the
information that I required. There has not been much done yet,
nor are the indications very promising. Several small quartz-veins
have been opened; they all run east and west; but range in a line
north and south of each other, and may probably be connected.
They are not perfect quartz-veins, but mere incrustations of crystals.
They lean over a few degrees to the north, and the gold is found on

1856. | WILSON—AUSTRALIA. 287

that side ; sometimes in the quartz, but more commonly in a coating
of clay between the quartz and the imbedding rock. I learned also
that the veins were richest near the surface ; and were found to be
poorer in sinking.

Mr. King, at Goonoogoonoo Creek, showed me some specimens of
minerals of his own collecting, amongst which were sapphires, rubies,
and gold in quartz*, also some fossil plants. Conducted by Mr.
Moss (residing at Mr. King’s), who volunteered to be my guide, I
went to the rock from which the fossils were taken, and found it to
be a shale belonging to the carboniferous series, and containing fine
specimens of Lepidodendron; but the rock was too brittle to allow
specimens of large size being taken from it.

According to Mr. Odernheimert, ‘‘The dioritic and syenitic
rocks with their breccias, are in the gold-fields of the Peel the ex-
clusive bearers of the gold-quartz-veins, and are to be regarded as
the main source of the gold. They occupy the greatest area of that
district east and west of the Peel, from the Hanging Rock to the
north.”’......‘‘ The dioritic rocks prove to be the constant source of

old, even at a distance north and west of the metamorphosed area
of the gold-fields.”’

I would not here oppose my observations (made during one week)
of the district to those of Mr. Odernheimer, extending through
fifteen months, had not my former experience of the geology of
gold districts led me to differ in opinion from the statements made
in the report above quoted from. In the first place I would remark,
that, as above stated, in this district there are imperfect quartz-
veins only ; and that the little gold that occurs (excepting the drift-
gold) is all found in these imperfect veins.

If dioritic rocks be the source of gold, there is a much greater
abundance of such rocks nearer the Dividing Range; but no gold
has been found in them; and as to the extent of such rocks, I can
only say, that I have travelled down the bed of the river on foot,
and forded it twelve times between the Hanging Rock and the Peel
River Company’s Works, a distance of about seven miles, crossing
the strata angularly, and I very much doubt that the igneous rocks
passed over in that space would amount to a fourth part of a mile.

On our passage from Sydney to Moreton Bay we could see from
the ship that the rocks of the carboniferous formation were con-
tinuous along the coast ; and we several times saw what appeared to
be lines of coal in the sea-cliffs.

The town of Brisbane is built on crystalline rocks. These extend
uncovered a few miles to the eastward; and in the western direction
include Sir H. Taylor’s Range. On the central part of this range,

* See also Quarterly Journ. Geol. Soc. vol. x. p. 303 ; and vol. xi. p. 402.—Ep.

+ Report on the Minerals and Geology of the Peel River District; Catalogue
of the Natural and Industrial Products of New South Wales, &c. (Australian
Museum and Paris Exhibition.) [See also Quart. Journ. Geol. Soc. vol. xi.
p- 399. |

288 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

at a place called the Pass, I found a hill of felspar-granite, containing
crystals of quartz and felspar. From the vast quantities of quartz
in thin veins imbedded in the slate-rocks, I suspected that common
granite with a quartz-base might be found somewhere in the range,
and therefore went a second time to search for it, and found it at
the southern extremity of the hills, where it had apparently been
forced up in the solid state, and afforded a section of the rocks as
they appeared in their order above it. This granite seemed to pass
by imperceptible degrees into the felspathic granite, and then into
gneiss. From where the granite appears upward to the top of the
range, a height of about 1500 feet, the gneiss and other rocks of
which the range is formed, have no appearance of having been
disturbed. They dip at an angle of 15° to E.S.E., while outside the
rent, from the range, the strata have an inclination of 45°, which
increases, until at Brisbane they dip to the eastward at an angle of
60°, with a north and south strike.

I observed that the disturbed portion of the strata had mnumerable
small quartz-veins, while that portion of the range that had not been
disturbed had apparently no quartz-veins, though quartz enters largely
into the composition of some of the rocks.

The rocks in their ascending order are granite with a quartz-base,
granite with a felspar-base, gneiss, massive felspar, mica-slate, chlo-
rite-slate, and clay-slate.

Traversing the town of Brisbane, there is a large dyke of flesh-
coloured porphyry, containing crystals of quartz and felspar and
many fragments of the slate-rock through which it has been erupted.
These fragments show no indication of having been fused or altered.
The dyke is 200 feet thick; it rises up between the slates, and is
parallel to them in direction and dip.

The country between Brisbane and Sir H. Taylor’s Range is such
as at first sight I should suppose to be auriferous, but on closer
examination the quartz-veins are too small and too numerous. I
found one quartz-vein at the eastern end of South Brisbane, in
which I suspected that traces of gold might be founds and, seeing
symptoms of its having been searched for, I made inquiries, and was
credibly informed that a small quantity of gold had been found
there.

2. On the Lowest Strata of the Cuirrs at Hastines.
By 8S. H. Becxtes, Esq., F.G.S.

Tue strata of which this communication is intended to be a very
brief notice form the base of that range of cliff* which extends from
Hastings to Cliff End.

* Accumulations of recent mud and drift always more or less obscure some
details of this coast-section. The accumulations of mud are sometimes many feet
thick, and are often the result of only two or three tides: but in some places they
remain so permanently, that I have not yet at those spots had an opportunity of
seeing the Wealden rocks. After a long calm the appearance of some of these
deposits is so questionably recent, that casual visitors have mistaken them for
ancient strata.

1855. | BECKLES—-HASTINGS CLIFFS. 289

The group that I am about to describe consists of sandstone and
clays, remarkable for their great diversity of hue, and are subordinate
to those beds of conglomeratic shale and ironstone which Mr. Web-
ster has described as the lowest strata visible in the series. They
are supplemental, therefore, to the strata comprised, or intended to
be comprised, in that author’s notice*. At the date, however, of
his Memoir they were partially disclosed, although perhaps not at
those detached points where he traced his lowest strata.

Mr. Webster, in speaking of the strata to the east of Hastings,
remarks, that “‘the lowest strata visible in this series consist of a
dark-coloured shale (m, m), which is seen at the Govers and at
Cliff End, and contain small roundish masses of sandstone, toge-
ther with several layers (two of them from two to three inches thick)
of rich argillaceous iron-ore.” On the west of Eaglesbourne this last
bed rises, in an arch, to the height of about twelve feet and then de-
scends to the east. At Cliff End it reappears, and may be traced
at low-water, forming a ledge.

In Mr. Webster’s paper the “shale with its courses of argillaceous
iron-ore,”’ described as the lowest beds, are noticed to the west of
the Govers and at Cliff End; and the occupation of the inter-
mediate space (about four miles in extent) is ascribed to superior
strata. In the stratigraphical section+ annexed to that commu-
nication, the exposure of these, as well as of the substrata about
midway between the Govers and Cliff End, is clearly indicated by
an arched line from Lee Ness to Hook’s Pomt; but in the Expla-
natory Memoir the succession here is mistaken, and the lower strata
are identified by the author (who at this point did not recognize his
lowest bed) with strata lettered by him /, /7,—supposed to be much
higher in the same series.

The shale, with its associated ironstone (m, m, in the annexed
sketch-section), first emerges from the beach immediately on the
east of Hastings, gradually rising into the cliff; it reaches the height
of about 20 feet, and describes a curve, which, continumg on the
eastern side of the picturesque valley of Haglesbourne, descends to
the beach at about 440 yards to the east of Eaglesbourne After
passing under the present beach at the Govers, it reappears at the
foot of that place, and so continues until it reaches Lee Ness Point,
when it rises again into the cliff, forming another and more extended
arch from Lee Ness to Hook’s Point, when it returns a second time
to the beach, and continues to Cliff End, where it forms the ledge
described by Mr. Webster t.

The most elevated points of all these beds have long been con-
spicuous in the vertical face of the cliff; while in the intervening
depressions they have either sunk below the sea-level, or have been
obscured by the ruins of the superior strata.

Although the stratum lettered m, m, is continuous through the
section, yet it does not retain its mixed character of shale and iron-

* Trans. Geol. Soc. 2nd Series, vol. ii. p. 31 e¢ seg. tT Loe. cit. pl. 5.
t When Mr. Webster wrote, these beds were about 12 feet above the beach
at this place; they are now nearer 20 feet.

290

Length about 5 miles.

Clif-section from Hastings to Clif’ End, Sussex.

Hook’s Point.-------- WN +:

PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

Fault, -------

Fairlee Cliff..-------

Eaglesbourne. :--------- “|

WwW.

Lee Ness, ------ n\\Waed

East Cliff.

Hastings.

mn. Upper member of the lowest beds.

mm. Mr. Webster’s ‘* Shale and Ironstone.’

stone throughout; in some places the

ironstone dies out and leaves the shale as
the sole representative of the stratum ;

in others the shale passes into iron, the

band becoming ferruginous in its entire

thickness.

The strata (x, 7, of the sectional sketch)
underlying the shale and ironstone are
conformable to them, and occur in the
same irregular undulating lines: they
are also continuous, and at present more
or less visible, through the entire section,
with the exception of the neighbourhvod
of Lee Ness. They may be studied also
with advantage on the beach under Kast
Cliff, particularly on the east of Eagles-
bourne, where they occur in the follewang
descending order :—

Ist. A band of sandstone; about
4 feet thick.

2nd. Slate-coloured compact clay ;
7 feet thick.

3rd. Light-coloured clay; 4 feet
thick.

4th. Dark clay ; thickness unknown.

At Cliff End these beds have been so
far removed from their original position
(and, as it were, are so thrown over on
their sides), that the present surface of
the shore is formed of their edges, or by
a section transverse to the plane of stra-
tification.

At a distance of nearly 2000 yards to
the east of the Lovers’ Seat, several hun-
dred square yards of the upper surface
of the sandstone or superior member of
this subgroup are exposed, and form the
promontory or projection known as Lee
Ness Point, the preservation of which
may be attributed to the greater hardness
and durability, as well as the peculiar po-
sition, of the upper members of this sub-
group. On the east of Lee Ness these
strata increase considerably in thickness ;
the clays below the sandstone (which is
here about 9 feet thick) being intersected
by arenaceous deposits, and the band of
sandstone separated from the shale and
ironstone above by layers of clay, which
gradually diminish in thickness to the

1856. | BECKLES— HASTINGS CLIFFS. 291

east and west, and thin away at the extremities of the arch, where
the ironstone and sandstone may be seen in contact. At that point,
between Lee Ness and Hook’s Point,*where the elevation of these
‘strata is greatest, the height from the beach to the top of the
sandstone is more than 30 feet, and to the top of the ironstone more
than 50 feet. It may be further remarked, that these strata are the
only members of the series that seem to extend uninterruptedly
through the entire section from Hastings to Cliff End, |

Organic Remains.—The organic contents of the strata above-
described all indicate their deposition in fresh water ; but many of
them differ specifically from the Wealden fossils hitherto known.
It may be well to observe, with reference to the distribution of
Unionide in the Wealden strata, that, although interesting as
affording additional evidence of the fluviatile or lacustrine origin of
the formation, yet the species, and even the individuals hitherto
discovered, were few in number and scarcely available as stratigra-
phical indices. I have now found these fossils, however, in consi-
derable numbers in the Hastings rocks, where they afford good cha-
racteristics for certain strata. While those fossils of the Wealden
which are of terrestrial origin are distributed promiscuously through
the strata, the Unionide, like other Testacea which are indigenous
to the element in which they were included (and which do not, lke
Fish, enjoy a great power of locomotion), occur for the most part in
groups, each species being confined almost universally to one stratum
or set of strata.

The superior members of the group, or the conglomeratic shale
and ironstone (m, m, of the section, p. 290), contain Cyrene, Unionide,
Insects*, and bones of Saurians. The ironstone abounds with vege-
table remains}, for the most part in a fragmentary condition: from
some parts of the deposit, however, I have taken very fine specimens,
and others that are rare and valuable.

From the sandstone below (x of the Section, and No. 1 of the
list at p. 290), I have taken small varieties of Unio; but, like the
majority of fossils enclosed in the arenaceous deposits of the Wealden,
they are badly preserved, and in only one or two instances have I
secured instructive specimens. The most interesting traces of organic
existence are the casts of Foot-prints, which occur in relief on its
under surface, and which have formed the subject of my former com-
munication in the tenth volume of the Society’s Journal (p. 456).

The stratum, however, that I have found most interesting with
reference to its organic remains is perhaps the next below (No. 2 of
the list at p. 290). The Zamia occurs here in finer condition than
I have seen it-from any other part of the Wealden of England. In
the same bed at least two other plants are deposited ; together with
a large Anodon (?) and a small Paludina (?) ; as well as small copro-
litic bodies of only occasional occurrence. The Univalve occurs so

* See Notice of the Insectiferous Strata at Hastings by Messrs. Binfield, Quart.
Journ. Geol. Soc. vol. x. p. 171. |
+ I have also detected fossil gum in a carbonaceous deposit much higher in the

series.

292 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

sparingly, that I have not found more than one or.two specimens ;
but of the 4dnodon (?) I have taken not fewer than fifty specimens,
varying from less than three-quarters of an inch, to six inches in length;
and, although some of the specimens exhibit a slight difference of
form, yet a general uniformity of character and contour seems to
refer them all to one species*.

The last and lowest deposit (No. 4, p. 290) does not appear to be
rich in fossils ; but this apparent destitution may result rather from
an imperfect examination than from inherent barrenness. This bed
consists principally of mottled clays, such as are usually supposed to
be unfossiliferous. By the discovery of the dorsal rays of Hybodus
in these clays}, however, I have satisfactorily proved that this opi-
nion is erroneous; although the almost total exemption of these red-
stained clays from organic remains which are distributed through the
strata both above and below them, seems to support this general
impression.

3. On the PALZONTOLOGICAL and STRATIGRAPHICAL RELATIONS
of the so-called “ Sanvs of the INrerior OouiTe.” By
Tuomas Wriecut, M.D., F.R.S.E.

[Communicated by Prof. Ramsay, F.G.S. |

ConTENTS.
Introduction.
Section and fossils at Leckhampton Hill, Gloucestershire.
Ps fh} at Crickley Hill, Gloucestershire.
a4 “A at Beacon Hill, Gloucestershire.
ut rs at Frocester Hill, Gloucestershire.
a * at Wotton-under-Edge, Gloucestershire.
. A at Bradford-Abbas, Dorsetshire.
a 5 near Bridport, Dorsetshire.
Oolitic character of the Cephalopoda-bed.
Occurrence and place of the Cephalopoda-bed on the Continent,
Table of the Fossils of the Cephalopoda-bed.
New Species of Molluscs from the Cephalopoda-bed.

Introduction.—The calcareous sands which lie between the limestone-
beds of the Inferior Oolite, above, and the clays of the Upper Lias,
below, have from the time of Dr. William Smith until now been re-
ferred to the Oolitic group, and described in books as “ the sands of
the Inferior Oolite.”’ These sands exhibit a very uniform litholo-
gical character throughout their entire range in England, although
they differ much in thickness in different localities, thinning out or
even altogether absent in some places, but attaining a considerable
development in others ; in this respect they do not differ from the
great oolitic limestone-beds themselves, forming so important a
feature in the geology of Gloucestershire; as those bold mural
escarpments of freestone which impart such a picturesque effect to

* This Anodon (?) is one of at least twenty species of Unionide in my collection

from the Hastings rocks, of which the majority are new.
t+ At Bulverhithe.

1856. | WRIGHT— UPPER LIAS SANDS. 293

Leckhampton, Birdlip, and Paimswick Hills thin out and almost dis-
appear in a run of less than twenty miles from these typical sec-
tions. If we trace the so-called “Sands of the Inferior Oolite”
from Cheltenham southwards, we find them gradually thickening as
‘we proceed by Crickley, Cooper’s, and Painswick Hills, to Beacon,
Frocester, and Wotton-under-Edge, where fine sections are exposed.
The oolitic limestones, including the pea-grit, upper and lower free- _
stones, and the intervening oolite marl, which are about 190 feet
thick at Leckhampton, gradually diminish in thickness near Stroud,
and in the neighbourhood of Bath are represented by about 60 feet
of freestone, the pea-grit and oolite-marl having entirely thinned
out.

The upper ragstones, including the Gryphza-bed and the Tri-
gonia-bed, have a more constant and uniform development through-
out the tract of the Inferior Oolite, and present a similar suite of
fossils wherever they are exposed ; being always well characterized
by Ammonites Parkinsoni, Sow., A. Martinsu, d’Orb., Trigonia
costata, Sow., Perna rugosa, Goldf., Clypeus sinuatus, Leske, Col-
lyrites ringens, Desml., Holectypus hemisphericus, Desor, H. de-
pressus, Klem, Terebratula globata, Sow., T. spheroidalis, Sow.,
Rhynchonella plicatella, Sow., and R. spinosa, Sow.

The Fuller’s Earth is represented by a thin band of clay near Chel-
tenham ; it is 70 feet thick near Stroud, 128 feet near Wotton-under-
Edge, and forms a conspicuous bed, 150 feet thick, near Bath.

In Somersetshire and Dorsetshire the Sands attain a great thick-
ness, and form an important feature in the physical geography of the
oolitic districts of these counties. Wherever they are well exposed, as
in the sections about to be described, they are overlaid by a bed
of coarse, brown, marly limestone, full of small, dark, ferruginous
grains of hydrate of iron, imparting an iron-shot aspect to this rock,
which in general contains an immense quantity of individuals of seve-
ral species of Ammonites, Nautili, and Belemnites, with a few shells
of other Mollusca. Beneath this fossiliferous band, or ‘‘ Cephalo-
poda-bed,” are the so-called “‘Sands of the Inferior Oolite,”’ con-
sisting of very fine, brown and yellow, calcareous sands, often mica-
ceous, and well adapted for foundry-purposes, as they receive sharp
impressions of bodies pressed upon them. They contain in their
upper part inconstant layers of siliceo-calcareous sandstone, and
sometimes in their lower part large inconstant concretionary masses
of coarse sandstone, the lowest beds becoming blue and marly, and
passing insensibly into the clays of the Upper Lias. The line of
junction is easily detected by the springs of water which burst out
immediately above the clays. The sands themselves are not fossili-
ferous, but the nodules sometimes lying near their base often con-
tain organic remains.

As it is the object of this memoir to show, that the Cephalopoda-
bed contains a number of well-known Upper Liassic Ammonites,
Nautili, and Belemnites, and that the weight of palzeontological evi-
dence is in favour of the supposition, that it belongs to the Lias,
rather than to the Oolite-formation, | purpose to describe five sec-

294 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

tions in Gloucestershire and two in Dorsetshire to prove the stra-
tigraphical relations of the Cephalopoda-bed and Sands to the lime-
stones of the Inferior Oolite above and the clays of the Upper Lias
below.
_, My friend the Rev. P. B. Brodie, in his valuable paper “‘ On the
~Basement-beds of the Inferior Oolite*,’’ has already shown how
distinct the Cephalopoda-bed (called by him ‘the Ammonite and
Belemnite bed’) is in two of the sections hereafter to be described ;
but, in common with all local geologists, myself then among the
number, he considered these beds as the lowest of the Oolitic series,
and “the greater number of the Belemnites and Ammonites from
this division of the Cotswolds as unnamed +.’ About two years ago
I had the pleasure of submitting my collection of Ammonites from
the Cephalopoda-bed, now placed before the Society, to the inspec-
tion of M. Seemann, the well-known paleontologist of Paris, who
pronounced them to be the species to which they are referred in this
paper ; and I afterwards made an excursion to Frocester Hill with
M. Seemann, who was anxious to see a section that had yielded so
many Upper Lias Ammonites, which at that time were not known
to have been found in England.

During last summer I accompanied Dr. Oppel, of Stuttgart, to
Frocester Hill for the purpose of examining the Cephalopoda-bed
in situ. This gentleman, who is well acquainted with the Oolitic
formations of France and Germany, was clearly of opinion that it
belonged to the Upper Lias, and that it was a good representative
of a rock of the same age, “‘die harten Stemmergel voll Ammonites
Jurensis, insignis, radians, Germanii (hircinus),” which he had de-
scribed in his memoir f.

In September last I visited Scarborough and Whitby, and was
fortunate to find in the museums of those towns, and in the collection
of my friend Mr. Leckenby, several Ammonites from the Upper Lias
of Whitby identical with those collected from the bed at Frocester,
as Ammonites opalinus, Rein., A. variabilis, dOrb., and A. stria-
tulus, Sow. These facts removed all further doubts from my mind,
and convinced me that the Cephalopoda-bed and its underlying sands
belong to the uppermost part of the Superior Lias, and not to the
Inferior Oolite as formerly supposed.

Section at Leckhampton Hill.—As the magnificent section of the
Inferior Oolite at Leckhampton Hill, near Cheltenham, has been
already described in detail in the pages of the Geological Society’s
Journal §, it will be unnecessary now to do more than to enumerate
the upper beds of that section, and briefly to mention the lower strata
which are in more immediate relation with the Upper Liassic sands.
The following section has been kindly drawn by my friend Mr. E.
Hull, F.G.S., and exhibits very accurately the different beds here so
admirably exposed.

* Quart. Journ. Geol. Soc. vol. vi. p. 208. + Op. cit. p. 210.
t Der mittlere Lias Schwabens, p. 3. § vol. vi. p. 239.

1856. | WRIGHT—UPPER LIAS SANDS. 295

Section I.—Leckhampton Hill, near Cheltenham.

Nos. 1 and 2 form the upper ragstones, consisting of the ‘ Tri-
gonia-grit ’’ (No. 1), and the “ Gryphza-grit”’ (No. 2).

No. 1. The Trigonia-bed is a coarse brown ragstone, containing
many impressions of Trigonia costata, Sow., T. decorata, Lyc.,
Lima cardiiformis, Sow., Rhynchonella concinna, Sow., Ammonites

Fig. 1.—Section through Leckhampton Hill, near Cheltenham.

Leckhampton Hill.

_1. Trigonia-bed. A,B,C. Pea-grit and ferruginous oolite.
2. Gryphea-bed. Dp. Cephalopoda-bed.
3. Brown rubbly oolite. E, F, G- Upper Lias sand and Upper Lias clay.
4. Flagey freestone. H. Marlstone.
5. Fimbria-bed or oolite-marl. 1. Lower Lias clay.
6. Freestone.

Parkinsoni, Sow., Echinobrissus clunicularis, Lhywdd, Holectypus
depressus, Leske, and Clypeus sinuatus, Leske; in thickness it is
about 7 feet.

No. 2. The Gryphea-bed is an ancient oyster-bank, and is com-
posed in great part of Gryphea Buckman, Lyc., with many other
shells, as Myacites dilatata, Buck., Terebratula impressa, v. Buch,
Tancredia donaciformis, Lyc., Gervillia tortuosa, Phil., Lutraria
ovalis ?, Phil., Cypricardia cordiformis, Desh., Ammonites Mur-
chisone, Sow., and many other shells ; but the dominant shell is the
Gryphea : this bed is about 8 feet in thickness.

No. 3. A coarse, brown, shelly, rubbly oolite, well exposed to the
east of Leckhampton Hill, where it forms a mural cliff ; and between
the inclined planes at the Leckhampton quarries it contains many
fossils ; but, as the bed is not in general quarried, they cannot be
extracted: it is about 24 feet thick.

No. 4. Upper flaggy bastard-freestone, well seen above the oolite-
marl: 26 feet thick.

No. 5. The Oolite-marl or Fimbria-bed, is a cream-coloured mud-
stone, not unlike chalk-marl; the dominant shell is Terebratula fim-
bria, Sow. ; but it contains likewise Lucina lyrata, Phil., Lima

296 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

cardiiformis, Sow., L. leviuscula’, Sow., Natica Leckhamptonensis, ‘
Lyc., Natica adducta, Phil., Mytilus pectinatus, Sow., Astarte ele-
gans, Sow., Nerina, sp., Chemnitzia, sp., and masses of Coral,
chiefly Thamnastrea Mettensis, Edw. This bed was deposited
under different conditions to that of the freestone on which it rests,
as its lower portion is slightly brecciated; and the surface of the
freestone on which that breccia was deposited had been for some
time exposed to aqueous action and made smooth thereby. The
marl measures about 7 feet in thickness, and passes upwards into a
marly limestone, becoming oolitic in the uppermost layers. This
division of the bed is about 10 feet thick. The Fimbria-bed is a
constant feature in the Inferior Oolite of the Cheltenham district.

No. 6. The Freestone is a compact light-coloured oolitic limestone ;
the uppermost beds are the best for building-purposes ; the middle
beds are of an inferior quality, and are stained in part with the
peroxide of iron; the lower beds contain large oolite-grains, and are
called “‘roestone’’: the freestone in all is about 110 feet in thick-
ness.

The Pea-grit (Inferior Oolite). Ft.

A. A brown, coarse, rubbly oolite, full of flattened concretions
cemented together by a calcareous matrix. When the
blocks weather, the concretions, which resemble flattened
peas, form a very uneven surface. It contains many
fossils in: good preservation’ .... S.\.; sv ...oh > +s eee 12. 0

s. A hard, cream-coloured, pisolitic rock, made up of flat-
tened concretions, with a thickness about similar to
THOSE Gs SA ypaarls Alan fe laa nh 0-4 0s s © asses 0 10 0

c. A coarse, brown, ferruginous rock, composed of large ooli-
tic grains; it 1s readily disintegrated by the frost, and
is of little economical value. About...¢........ 5088 20 0

in.

The Cephalopoda-bed (Upper Iias),

p. A brown marly rock, full of small dark oolitic grains of

the hydrate of iron, which are strewed in profusion in a_

calcareous paste. /Alowts.. oases oe Uses ee 20
pb’. A thin.seami, of yellowish sand). j5)- 4-10-\<c sp-auss aes 0 13
E. A dark-grey crystalline limestone, extremely hard, and re-

sembling some beds of the carboniferous limestone ; it

is bored in different places by Fistulana?, the shells of

which remain in the exéayations).. . . neces ps5. Gir Oi nz
F. A brown, argillaceous, sandy bed, full of micaceous parti-

cles; passing downwards into fine brown and yellow

sands. Thickness unknown.
G. Upper Lias Clay, of a dark blue colour. Thickness pro-

DADIEE ise </</e > -ijaee ame ee EGE MER ewe Oslo dic ae 160 0

Fossils of the Pea-grit (Inferior Oolite)—a, 8, Cc.

As this bed is very much the same, lithologically and palzeonto-
logically, as the Pea-grit of Cleeve, Crickley, and Birdlip Hills, I
shall give a list of its most abundant fossils in my next section of
Crickley Hill. |

1856. | WRIGHT—UPPER LIAS SANDS. 297

Fossils of the Cephalopoda-bed—», &, F.

The lower part of bed p contains many fossils, which are not well
preserved ; they are sufficiently characteristic, however, to prove the
identity of this rock with ‘‘ the Cephalopoda-bed”’ in other parts of
the Cotteswold Range.

Cephalopoda.

Ammonites opalinus, Reinecke (primordialis, Schlotheim), d’Orbigny, Terr.

_ Jurass. pl. 62.

A. hireinus, Schlotheim, Zieten, Wiirttemberg, pl. 15. fig. 3.

Nautilus inornatus, d’ Orbigny, Terr. Jurass. pl. 14. fig. 1.

Belemnites compressus, Blainv., Voltz, Observations sur les Bélemnites,
pl. 5. figs. 1, 2.

B. breviformis, Voléz, ibid. pl. 2. figs. 2-4.

Gasteropoda.

Pleurotomaria

Techo } interior moulds only.

Conchifera.

Myacites abductus?, Phil.

Pholadomya fidicula, Sow., small var., very distinct from the large type-
form of this shell.

Gervillia Hartmanni, Miinst., Goldfuss, Petr. Germ. tab. 115. fig. 7.

Fistulana?, sp.

Trigonia Ramsayu, Wright, nov. sp. (Paleontological notes appended to
this memoir.)

Trichites ; species indeterminable, as the specimens are all fragmentary.

Cucullza, nov. sp.

Brachiopoda.

Rhynchonella cynocephala, Richard, Davidson, Monogr. Oolitic Brach.
pl. 14. fig. 10.
Anthozoa.

Montlivaltia; species indeterminable.

Section I].—Crickley Hill near Cheltenham.

The Pea-grit (Inferior Oolite).
Ft. in.
A. A coarse oolitic limestone, with large grains and numerous
concretionary bodies; exceedingly hard and crystalline
PEATE Otc a, <4) 16)c 20.5 -. # « sin ver eye eresie ee «3s about 25 0
. A coarse pisolitic limestone, composed of flattened con-
cretionary bodies which are round, oval, or flattened like

lve]

GEUMIC CIS acre ce fs ov wna ea ee Sel inn dts 25:2 about 19 8
c. A coarse brown rock, very ferrugimous and full of large

COGNATE EMIS ye eae cc's ss 2 Nekeeeaie ect + 6 ee +e about 10 0

The Cephalopoda-bed (Upper Lias).

p. A brownish marly matrix very full of large oolitic grains

of hydrate of iron, which impart a speckled appearance

£0 (Glisten ees ole icf e wo vs Soe olsray eine 206
gE. A dark-greyish limestone, very hard and crystalline .... 1 6

298 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,
F. Brownish sands, micaceous in parts, and passing down-

wards into brown marls and ferrugimous clay. Thickness

not ascertained. f
G. Upper Lias Clay, darkish blue.

Fossils of the Pea-grit and other Limestone-beds of the Inferior
Oolite—a, B, C.

The beds a and B contain many fossils, which in general are not
well preserved. The Echinodermata are sometimes found tolerably
perfect with the test in a good state of preservation. The Mollusca
are usually denuded of the shell; but when they happen to be pre-
served in clayey or sandy seams of the Pea-grit, the sculpture of the
shell is sharp and perfect. The following list contains only the most
prevailing species :—

j Cephalopoda.

Ammonites corrugatus, Sow. Juvenile state of A. Murchisone, Sow. Min.

Conch. pl. 451. fig. 3.
Nautilus truncatus, Sow.

Belemnites giganteus, Schloth.

Gasteropoda.

Pleurotomaria ornata, Defrance.
Patella rugosa, Sow.

inornata, Lycett.

Nerita costata, Sow.

Natica adducta, Phil.

Cirrus nodosus, Sow.
Trochotoma carinata, Lyc.
Chemnitzia, nov. sp.
Rimula tricarinata, Sow.
Nerinza, nov. sp.

Conchifera.

Lima duplicata, Sow.

—— notata, Goldf.
semicircularis, Goldf.
— leviuscula, Goldf. (non Sow.).
— sulcata, Minster.

lyrata, Minster.

ovalis, Sow.

Lima, nov. sp., allied to L. punctata.
Pecten, nov. sp. (non vimineus).
Pecten lens, Sow.

demissus ?, Phil.
clathratus, Remer.
Goniomya angulifera, Sow.
Hinnites abjectus, Phil.

— tuberculosus, Goldf.

, NOV. sp.

Plicatula, sp.

Placuna Jurensis, Remer.
Mytilus bipartita, Sow.
pectinatus, Sow.

— pulcher, Sow.

striatulus, Miinst.
cuneatus, Sow.

Modiola plicata, Sow.

Pinna cuneata, Sow.

Pinna fissa ?, Goldf.
Myoconcha crassa, Sow.
Ostrea costata, Sow.
Avicula? complicata, Buck.
Cypricardia cordiformis, Desh.
Lucina despecta, Phil.
Psammobia izvigata, Phil.
Ceromya plicata, Agass.
Bajociana, d’ Orbig.
Macrodon Hirsonensis, d’ Archiac.
Myacites punctata, Buck.
— dilatata, Buck.
oblonga, Buck.
Trichites, sp.

Cardium striatulum, Phil.
levigatum, Lycett.
Trigonia costatula, Lycett.
exigua, Lycett.
v-costata, Lycett.
decorata*, Lycett.
clavo-costata*, Lycett.
costata, Sow.

striata, Sow.
duplicata*, Sow.
Avicula echinata, Sow.

* Those marked with an asterisk occur in the upper ragstones only.

1856. | WRIGHT—UPPER LIAS SANDS. 299

Brachiopoda.

Terebratula simplex, Buck. (trigo-

nalis, Lhwyd.).

plicata, Buck.

submaxillata, Davidson.
Rhynchonella Wrightii, Davidson.

Rhynchonella decorata, Davidson.
— tetrahedra, Sow.

angulata, Sow.

concinna ?, Sow.

— oolitica, Davidson.

Annelida.

Serpula grandis, Goldf.
convoluta, Goldf.
—— plicatilis, Minst.
—— quadrilatera, Goldf.

Serpula socialis, Goldf.
suleata, Sow.

—— filaria, Goldf.

flaccida, Goldf.

Echinodermata.

Cidaris Fowleri, Wright, Monogr. Oolitic Echinoderms, pl. 1. fig. 4.

Bouchardii, Wright, ib. pl. 1. fig. 2.
Wrightii, Desor., ib. pl. 1. fig. 3

Rabdocidaris Wrightii, Desor., 2b. pl. 1. fig. 5.
Acrosalenia Lycetti, Wright, ib. pl. 15. fig. 1.

spinosa, Agassiz, ib. pl. 17

Diadema depressum, Agass., Wright, 2b. pl. 6. fig. 2.
Echinus germinans, Phil. 1b. pl. 12.

bigranularis, Lamarck, 2b. pl. 12.

Polycyphus Deslongchampsi, Wright, 2b. pl. 13.
Hemipedina Bakeri, Wright, ib. pl. 10. fig. 1.

tetragramma, Wright, 2b. pl. 10. fig. 4.
perforata, Wright, 1b. pl. 10. fig. 2.
Bonei, Wright, 2b. pl. 10. fig. 5.

Pygaster semisulcatus, Phil. M. G. S. decade 5.

conoideus, Wright, M. G. S. decade 5.

Hyboclypus agariciformis, Forbes, M. G. S. decade 5.

caudatus, Wright, Ann. Nat. Hist. vol. ix. pl. 3.

Goniaster ; a portion of a ray only.

Extracrinus, nov. spec.

Anthozoa.

Montlivaltia Delabechu, Edw. &
Haime.

Waterhouseil, Edw. & Haime.

cupuliformis, Edw. & Haime.

Axosmilia Wrightu, Edw. & Haime.

Latomeandra Flemingu, Edw. &
Hae.

—— Davidsoni, Edw. & Haime.

Thecosmilia gregaria, Edw. & Haime.

Thamnastrea Defranciana, Edw. &
Haime.

Terquemi, Edw. & Haime.

Isastreea tenuistriata, Edw. & Haime.

Thamnastrea Mettensis, Edw. &
Haime.

— fungiformis, Edw. & Haime.

Bryozoa.

Stromatopora dichotomoides, d’Orbig.

Fossils from the Cephalopoda-bed—p, E, F.

This bed is not so well exposed at Crickley Hill as in many other
localities, no new surface having been laid bare for upwards of twenty

VOL. XII.—PART I.

Yi

300 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

years; the fossils are for the most part fragmentary and not well
preserved.
The bed p contains—
Cephalopoda.

Ammonites opalinus, Rezn. Nautilus mornatus, d’ Orbig.
insignis, Schibler. Belemnites breviformis, Voltz.

Gasteropoda.
Turbo capitaneus, Miinst.

Conchifera.

Myacites abductus, Phil. ? Gervillia Hartmanni, Miinst.

Brachiopoda.
Rhynchonella cynocephala, Rich.

F contains many fossils in a fragmentary state, with a profusion of
small teeth of fishes. The limestone is bored by Fistulane (?).
Belemnites abound in the bed. Belemnites breviformis, Voltz, and
Belemnites compressus, Voltz, are the prevailing forms.

E contains shells in a fragmentary state; but the specimens are
indeterminable ; many fragments of the spines of Echmoderms are
likewise strewed throughout this bed.

G. The Upper Lias Clay is indicated by the outburst of springs
along the line of its junction with the sands: although this bed was
lately exposed in consequence of the falling away of a mass of debris,
still very few fossils were found; I collected Ammonites bifrons,
Brug. (Walcotiu, Sow.), small specimens, Ammonites serpentinus,
Schloth., Ammonites communis, Sow., Ammonites annulatus, Sow.

Section IJI.—Beacon Hill near the Haresfield Station on the
Bristol and Birmingham Railway.

Inferior Oolite.

A. A close-grained freestone ; resembling the same bed at
Leckhampton, but becoming rather flaggy in the upper
PANE seals os sao ae hs sore: 078 le Men een ee 15 0
A'. A close-grained yellow oolitic limestone, quarried for road-
mending ; much speckled with dendritical patches of
the peroxide of iron, and containing few fossils ; it mea-
Sites About «. «<< 2s). ce emesis ONC ris is, << cS 12
B. A yellowish sandy rock, separating into large blocks which
contain fossiliferous nodules ; the fossils are in general
well preserved in this bed; it is not used for any eco-
nomic purpose, and heaps of blocks lie close to the brown
Pauiaceous sands* soi. 26 y Pees eee oo 5 das ae

* In consequence of the position of these blocks, many supposed that they
came out of the so-called “‘ Sands of the Inferior Oolite;” and, as they contain
numerous fossils, it was said that such species had been collected from the sands.
The true position of these sandy stumbling-blocks is that now given in the
section.

1856. | WRIGHT—UPPER LIAS SANDS. 301

c. A brown sandy oolite, passing into a coarse ferruginous
oolite; containmg many fossils not well preserved ;
oolitic grains of the hydrate of iron are scattered through
the brown calcareous matrix: it measures from 8 to 10 0

Cephalopoda-bed.—Upper Inas.

D. A coarse brown ferruginous bed, extremely hard where it
is weathered, and containmg an abundance of small
oolitic grains of the hydrate of iron; many fossils are
collected from this rock, but they are not in general
well preserved ; a thin seam of clay divides the bed into
two portions; in the clay-seam nearly all the Brachio-
poda are found: the entire bed measures from 2 feet to 2 6
. Fine yellow micaceous sands, passmg downwards into
brownish sands mixed with marly bands; this bed is
non-fossiliferous ; its thickness is not accurately ascer-
tamed; it may, befrom 60'to 100 feet 2.3. ee 802 0
. The blue clays of the Upper Lias are not exposed near
the section ; but their position is shown by the outburst
of springs on the glacis of the hill.

ic]

‘x

Fossils from the Inferior Oolite beds—a, B, C.

. The freestone-beds are flaggy and not fossiliferous.
. The fossiliferous nodules contain—

wm P

Cephalopoda.

Ammonites, nov. sp., resembling A. Garantianus, d’Orbig., Terr. Jurass.
ple 125%

Conchifera.
Pholadomya fidicula, Sow. Ceromya Bajociana, d’Orbig.
Modhola plicata, Sow. Lima bellula, Lyc..
Pinna fissa, Goldf. Pecten, nov. sp., allied to P. demis-
Myacites dilatatus, Buck. sus, Phil.

Fossils from the Cephalopoda-bed—p, f, F.
Cephalopoda.

Ammonites opalinus, Rein.; very Nautilus mornatus, d’Orbig.
fine specimens. Belemnites breviformis, Voltz.

insignis, Schiibl. compressus, Voliz.

variabilis, d’Orbig. wregularis, Schloth.

. Gasteropoda.
Turbo capitaneus, Minst. Pleurotomaria, sp.
Conchifera.
Cucullza, nov. sp. Modiola plicata, Sow.
Myacites abductus?, Phil. Astarte lurida, Sow.
Brachiopoda.

Rhynchonella cynocephala, Richard. Terebratula subpunctata, Davidson.
— furcillata, Theod.
Y 2

302 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

M. Richard * thus describes the locality and bed of his Rhyncho-
nella cynocephala :—‘“ Un caleaire marno-ferrugineux, placé au-des-
sus des marnes supérieures du Lias, et au-dessous d’un calcaire ap-
partenant a4 l’oolite inférieure, qui lui-méme est recouvert non loin
de la (Bourmont, Haute-Marne) par le calcaire 4 entroques. Les
couches qui la contiennent doivent sans doute étre rapportées a l’00-
lite ferrugineuse inférieure, car on a tenté a plusieurs reprises d’en
extraire du minerai de fer pour le haut-fourneau de Vrécourt ; mais
ce mineral ne s’est point trouvé assez riche, ni peut-étre assez abon-
dant.”

Mr. Davidson, after having examined a series of Terebratula sub-
punctata, David., from the Cephalopoda-bed at Beacon Hill and
Frocester Hill, informs me that it is “ a well-known form and occurs
abundantly in the Liassic beds, and in the beds just above the
Upper Lias (the equivalent of the Cephalopoda-bed) in France,”
where he collected it with Rhynchonella cynocephala ; and that it may
probably be a variety of Terebratula punctata, Sow., which is a well-
marked species belonging to the Marlstone ; many shells from the
Marlstone near Ilminster closely resembling those from the Frocester
Cephalopoda-bed.

At the Horspools near Painswick the Cephalopoda-bed and Brown
Sands are finely exposed in a lane near the hotel, where their rela-
tion to the other Lias beds may be satisfactorily made out ; I col-
lected here Ammonites variabilis, d@Orb., fragments of Ammonites
opalinus, Rei., Rhynchonella cynocephala, Rich., Terebratula sub-
punctata, Davidson, and many other Lias shells in a fragmentary
state.

Section 1V.—4¢t Frocester Hill, near Stonehouse, Gloucester-
shire. Fig. 2.

This fine section and the one near Wotton-under- Edge are the most
typical of the beds now under consideration. The paleontological
and stratigraphical relations of ‘‘ the Cephalopoda-bed,” in particular,
to the Oolitic limestones above, and to the Upper Liassic sands
below, are admirably shown in both. [I had lately the pleasure of —
making an excursion to Frocester Hill with my friends Professor
Ramsay, Local Director of the Geological Survey, and Mr. Edward
Hull, F.G.S., who has surveyed a considerable part of the oolitic
district of Gloucestershire. At my request Mr. Hull has prepared
the accompanying diagram from a sketch made on that occasion,
which exhibits very clearly and faithfully the relation of the beds so
well exposed in this locality. The thickness of the strata indicated
in the section is only approximatively true, as it would be a tedious
process to level them all accurately.

* Bulletin Soc. Géol. de France, vol. xi. p. 263, 1840.

1856. | WRIGHT—UPPER LIAS SANDS. 303

Fig. 2.—Section of Frocester Hill, near Stonehouse.

Ss
Sy SS :
FHI 1D ig LL *

a,b,c. Inferior Oolite; 70 feet.
D, E. Calcareo-ferruginous sandstone (Cephalopoda-bed) ; 6 feet

¥. Yellow and brown sands, with inconstant and concretionary }‘‘ Upper Lias Sands.’’
bands of calcareous sandstone ; 150 feet ?

G. Upper Lias shale; 80 feet.

H. Marlstone ; hard calcareous sandstone, resting on brown and grey sands, with bands
and nodules of ferruginous sandstone ; 150 feet.

1. Lower Lias shale.

Inferior Oolite.
Ht. vine
a. A fine-grained oolitic limestone, similar to the freestone of
Birdlip, Painswick, and Leckhampton Hills; the upper
beds exhibit a most remarkable example of oblique bed-
ding, the flaggy layers of which rest horizontally on in-
clined beds of freestone: thickness about............ 50 0
b. A coarse, light-cream-coloured, gritty, crystalline oolite,
traversed at intervals by shelly layers extremely crystal-
line; a great part of the rock appears to be composed
of the fragments and plates of Crinoidea, the plates and
spines of Echinide, and comminuted fragments of the
shells of Mollusca. This white rock has a most remark-
able lithological character, and glistens brilliantly when
lit up by the sun’s rays. The shelly and pisolitic seams
which traverse this bed resemble those in the Pea-grit.
The surface of weathered slabs discloses numerous mi-
croscopic objects; the rock is in fact almost entirely
composed of organic debris. It measures about...... 10 0
c. A hard, fine-gramed, oolitic, sandy limestone, of a light-
brown colour, lithologically different from 6. It contains
many fossil shells, which are extracted with difficulty ;
and passes into a hard yellow oolite with few fossils:
thickness from 8 to 10 0
[The lithological character of this rock is very different
to that of d, on which it rests. |

The Cephalopoda-bed— Upper Inas.

d. A coarse, dark-brown, calcareo-siliceous rock, full of small,
dark, flattened grams of hydrate of iron. It contains
an immense quantity of fossils, but Ammonites and Be-

304 PROCEEDINGS OF THE GEOLOGICAL society. {April 9,

Ft. in.
lemnites are the dominant forms; some of the bivalve
shells are well preserved, but the matrix adheres to the
surface with such tenacity that they can seldom be
cleaned without injury. The Ammonites and Nautili,
for the most part, want the shell. Rhynchonella cyno-
cephala lies in the upper part of the bed, and the Am-
monites, Belemnites, Nautili, and other Mollusca in the
middle part ; the lower part is not so fossiliferous: this
bed, measures»: «:jcpreincdeaene e Gas he ee 4 6
e. A hard, coarse, brown mudstone, with hard irregular no-

dules of a caleareo-siliceous sandstone, highly micaceous

and ferruginous, and passing downwards into the sands U 9
Ff. Fine, brown and yellowish, micaceous sands, passing into

dust-coloured, grey and slate-coloured, micaceous sands,

with inconstant and concretionary bands of highly calea-

reous sandstone ; nodules of various size occur in these

bands, which are sometimes fossiliferous, containimg

chiefly Ammonites and Belemnites............+2+-+ 150?
g. Blue clay and shale, marked by the outburst of springs

and by pools of water on the terrace formed by the

Upper Lias Clay, which is about .................- 80 0
h. Marlstone; a hard calcareous sandstone, resting on brown

and grey sands, with bands and nodules of ferruginous

sandstone: “about svi. bdo ot ees ee - 2 150 0
7. The shales of the Middle and Lower Lias, sloping down

ito the valley.

Fossils of the Inferior Oolite.

A. Very few fossils in the Freestone ; those which are observed
are mostly fragmentary.

B. The fossils are so fragmentary in this bed that I have not
been able to determine them. Stems and column-plates
of Extracrinus, portions of the tests of Pygaster and
Acrosalenia, plates of Cidaris, and quantities of spines
in fragments are seen on the slabs.

c. The following shells were observed, but could not be ex-
tracted from the upper part of the bed :—

Pholadomya fidicula, Sow. Trichites, sp.; large fragments only. *
Modiola plicata, Sow. Serpula socialis, Goldf.

The frond of a Fern was found in this bed by the Rev. P. B.
Brodie. The lower part of the rock resting on the Cephalopoda-bed
is sparingly fossiliferous.

In very few localities, where the sands are exposed along the escarp-
~ments of the Cotteswolds or in the beautiful valleys intersecting
these hills, are they found to contain fossils ; at present I only know
two localities, Frocester Hill and Nailsworth: the former I have
already noticed ; the latter I must now briefly describe, as I shall in-
clude the Palzeontology of both localities in my list of species from
the Frocester district.

The fossiliferous vein at Nailsworth is found at the base of the
sands 4 or 5 feet above the Upper Lias clay. The bed consists of a

1856. | WRIGHT—UPPER LIAS SANDS. 305

fine soft ferruginous marly sandstone, of a deep brown colour, con-
taining much peroxide of iron, and many shells, mostly of the same
species as those found in the Cephalopoda-bed at Frocester. The
difference between these two beds is important, and deserves to be
noticed, as the Cephalopoda-bed at Frocester overlies the sands,
whilst the fossiliferous vein at Nailsworth is found at their base,
clearly proving that the sands and Cephalopoda-bed form only one
Stage.

Fossils of the Sands and Cephalopoda-bed (dD, ©, F) of the Frocester
district *.
Reptilia.

Vertebre of Ichthyosaurus. F.

Pisces.
Teeth of Hybodus. F.

Cephalopoda.

Ammonites opalinus, Reinecke (pri- Ammonites Mooreii, Lycett, MS.
mordialis, Sehloth.). F. nov.sp. F.
bifrons, Brug. (Walcotii, Sow.). —— discoides, Zieten. F.
1 he —— Raquinianus, d’Orb. F.N.
— insignis, Schiibler. F. and -—— Levesquei, d’Orb. F.
Newmarket and Ozleworth. concavus, Sow. F.
— hircinus, Schloth. F. — Leckenbyi, Lyc.MS.,nu.sp. F.
—— Jurensis, Zieten. F.N. variabilis, @ Orb. F.N.
striatulus, Sow. ae Nautilus inornatus, d’Orb. F.
Schloth.). F. Belemnites compressus, Voltz. F.N.
— Thouarsensis, d’Orb. F. tripartitus, Schloth. F. N.
radians, @’Orb. F. irregularis, Schloth. F.N.
Dewalquianus. F. Nodotianus, d’Orb. F.

Gasteropoda.
Pleurotomaria. Trochus ; allied to T. duplicatus,
Chemnitzia lineata?, Sow. N. Sow. N.
*Turbo capitaneus, Mist. F.N.
Conchifera.
*Lima bellula, Lycett. F.N. *Gresslya adducta, Phil. F.N.

*Pholadomya fidicula, Sow. F.N. * conformis, Agass. F.N.
*Gervillia Hartmanni, Miinst. F.N. *Myacites tenuistriatus, Agass. F.N.

*Modiola plicata, Sow. F.N. *Goniomya angulifera, Sow. F.
*Trigonia striata, Sow. F.N. *Astarte excavata, Sow. F.N.
*Perna rugosa, Goldf. N. *Myoconcha crassa, Sow. N.
*Hinnites abjectus, Phil. F. N. *Astarte modiolaris. N.
*Pecten articulatus, Goldf. F. *Cypricardia cordiformis. F.

* This list has been prepared from specimens collected by Mr. Lycett and
myself during many years, and I beg to thank my friend for the valuable aid he
has given me in making my list of Conchifera as complete as it now is; the
specimens have all been determined with much care, and I believe every confi-
dence may be placed in the accuracy of our conclusions. The letters F. N. indi-
cate that the species has been found at Frocester or Nailsworth.

306 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

*Pecten comatus, Goldf. N. Pecten textorius?, Goldf. F.
Opis carinata, Wright, nov. sp. (see Pholadomya; allied to P. media, Ag.
Appendix). F. ¥

Cypricardia brevis, Wright, nov. sp. » OY, SPs, ds Ne

(see Appendix). F. N. Astarte complanata, Remer. N.
Cardium Hullii, Wright(Buckmani, Lima ornata, Lyc. MS.,nov.sp. N.

Lycett). F.N. Astarte lurida, Sow. N.

Oppelii, Wright. N. Gervillia fornicata, Lyc. MS., nov.

Cucullza; allied to C. inzequivalvis, sp. N,

Goldf. N. Astarte rugulosa, Lyc. MS., nov.sp.
Lima electra, d’Orb. F.N. N. ;
Unicardium, nov. sp. N. Arca ; allied to A. oliveformis, Lye.

Tancredia, nov. sp. N. :
Trigonia Ramsayi, Wright, nov. Nucula ovalis?, Ziet. N.
sp. (see Appendix). F. Pholadomya ovulum?, Agass. N.

Brachiopoda.
Terebratula subpunctata, David. Rhynchonella cynocephala, Richard.
F. N. : F.

—,nov. sp. N.

The species marked with an asterisk im the above list are found
likewise in the Inferior Oolite ; but the specimens from the Sands
are nearly all dwarfed forms of the species, and lead one to the con-
clusion that they lived under conditions unfavourable to their deve-
lopment. The stinted growth of the stationary Conchifera forms
a striking contrast with the size and number of the Cephalopoda
interred with them in the same bed; in fact the dawning existence
of these Conchifera appears to have been a struggle for life, whilst
the conditions of the closing scene of the Belemnites, Nautili, and
falciferous Ammonites, were favourable to their continuance in time,
but abruptly brought to a termination by some great physical change
which took place about the commencement of the deposition of the
oolitic formations.

Section V.—At Wotton-under-Edge, near Bradley Turnptke,
Gloucestershire*. Fig. 3.

The lower beds in this section are almost a repetition of those at
Frocester Hill; but the relations of the Cephalopoda-bed to the In-
ferior Oolite, Fuller’s Earth, and Great Oolite are so admirably ex-
hibited in this locality, that I cannot omit a brief description of them.
I am indebted to my friend Professor Ramsay for the accompany-
ing diagram, which shows the succession of the strata between Sy-
monds-Hall Hill and Wotton-under-Edge. The hill is capped by
the Great Oolite; beneath this is the Fuller’s Earth, here attaining
a considerable thickness, and overlying the

* For this and the Frocester Hill district, see Map of the Geological Survey of
Great Britain, Sheet No. 35.

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WRIGHT—UPPER LIAS SANDS.

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308 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

The Marlstone—The Middle Lias.
Ft. in.
Hu. The upper bed of the Marlstone is a hard, brown, calca-
reous sandstone, which forms the capping of the Marl-
BEOMECEETACE * 1.5 vise sie nipdip totale Ae © ote aie ve 12 0
H’. The Marlstone is well developed, and consists of fox-
coloured sandstone, more or less ferrugimous, with grey
impure sandy limestone containing oolitic grains : thick-
TESS eh: eee | Ss en ks» 2 ate ticles cet oe eer 186 0
1. The Lower Lias Shales and Limestone : thickness unknown.

Fossils of the Inferior Oolite—a, B, C.

A. The Freestone-beds are not fossiliferous: the upper rag-
stones contain the common species found therem; but
they are not abundant.

B. Is not sufficiently exposed to be worked for fossils.

c. Contains—

Ammonites corrugatus,Sow.(=Am- Ostrzea costata, Sow.
monites Murchisone, Sow.). Serpula socialis, Goldf.

Fossils of the Cephalopoda-bed—p, &
D contains—

Ammonites insignis, Schiibler. . Belemnites breviformis, Voltz.
variabilis, d’Orb. compressus, Voliz.

opalinus, Rein. irregularis, Schl.

Jurensis, Zieten; only frag- Nautilus mornatus, d’Orb.; frag-
ments with the rounded back were — ments of this species.

obtained.

E. The upper beds contain nearly all the fossils: I saw few in this
layer of rock.

F. The nodules are not so well exposed as in Frocester Hill: some
fragments of Ammonites and Belemnites only were observed.

G. The characteristic Upper Lias Ammonites are here found :—

Ammonites communis, Sow. Ammonites bifrons, Brug. (Walcotii,
serpentinus, Schloth. Sow.).

H contains many well-known Marlstone forms, such as—

Ammonites margaritatus, Montfort. Pecten equivalvis, Sow.
spinatus, Brug. Gryphea gigantea, Sow.

1. The Lower Lias beds were not examined with reference to their
paleontological characters.

It has been stated by my late lamented friend Mr. H. E. Strick-
land+ that the bed herein described as the Cephalopoda-bed “is the
precise equivalent of the well-known Oolite of Dundry, near Bristol,
which may be recognized as far off as Bridport on the Dorset coast,”

* See Hull on the Marlstone Platforms of the Cotteswolds, Quart. Journ. Geol.
Soc. vol. xi. p. 485.
t+ Quart. Journ. Geol. Soc. vol. vi. p. 250.

1856. | WRIGHT—UPPER LIAS SANDS. 309

—an opinion in which I cannot concur. It is true that lithologically
the beds resemble each other, but paleeontologically they are en-
tirely distinct; ‘the Dundry Ammonite-bed”’ appertains to the
Inferior Oolite, and represents a higher zone than the Cephalopoda-
bed of Frocester, Beacon, and Wotton. The prevailing Ammonites
at Dundry are

Ammonites Humphriesianus, Sow. Ammonites Sowerbyu, Miller.
Brongniarti, Sow. —— Blagdeni, Sow.

— Gervillu, Sow. dimorphus, d’ Oro.
Brocchi, Sow. Browni, Sow.

I have already shown that not one of this list is found in “the
Cephalopoda-bed,’’ and I am assured by my friend Mr. Ethe-
ridge, of the Bristol Institution, who is well acquainted with all the
fossils that have been and are collected at Dundry, that (with the
exception of 4. variabilis and A. concavus, which lie at the base of
the bed, and a small 4. bzfrons from the Upper Lias Marl) not one
of the species of Ammonites found in the Cephalopoda-beds of Fro-
cester and Wotton have ever been collected at Dundry.

The Dundry Ammonite-bed, however, does occur in Somersetshire
and Dorsetshire with the same species of Ammonites, Pleurotomaria,
and other characteristic Dundry shells; but in these places it occu-
pies a higher stratigraphical position than the Frocester Cephalo-
poda-bed.

Between Yeovil and Sherborne the Cephalopoda-bed is well deve-
veloped, and extensively exposed; and at the Halfway House its
relations to the Sands below, and the Limestone of the Inferior Oolite
above, may be satisfactorily made out. Here it contains a great
many large Ammonites, Nautili, and Belemnites,—as

Ammonites Dorsetensis, Wright, Nautilus mornatus, d’Orb.
n. sp. Belemnites breviformis, Voltz.
— Jurensis, Zieten. compressus, Voliz.

Section VI.—At¢ Bradford Abbas, near Yeovil, Dorsetshire.

Inferior Oolite.

Ft. in.

A. Coarse, hard, brown ragstone, slightly oolitic, very irre-
gularly bedded, and containing few fossils: about .... 2 0

Bandc. Absent.

Cephalopoda-bed.

p. A coarse, brown, oolitic ragstone, composed in part of hard,
calcareous, sandy layers, grey and brown, and having
softer marly sandy seams running through the rock ; it
breaks with an uncertain fracture, and sometimes has a
flinty hardness: the ragstones are speckled with dark
brown flattened oolitic grains of hydrate of iron, and
Conta Many tessis BOONE Ole ye Cake ee me oe eS

310 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

Ft. in.

gE. A hard, greyish, crystalline limestone, raised and broken

up for road-mending ; it resembles carboniferous lime-

stone, and contains shells in a fragmentary state : it is

BONE on 0 ar pte SURE E dss noes pe ee an nea 0.9
F. Fine brown and yellowish sands, very micaceous in parts,

and contaiming hard, sandy, lenticular concretions :

thickness considerable.

Fossils of the Inferior Oolite—a.

A. Contains Pholadomya fidicula, Modiola plicata, and other
Inferior Oolite shells (undetermined) ; the same bed near
the Half-way House is overlaid by ragstones containing
Ammonites Parkinsont, Sow.; so that the upper and
lower ragstones are here in conjunction, the intermediate
freestone being exceedingly thin, or perhaps wanting.
Fine large specimens of Ammonites Truelli, d’Orbigny,
were likewise collected here.

Fossils of the Cephalopoda-bed—D, ®, F.

Cephalopoda.
Ammonites Jurensis, Zieten. Ammonites striatulus, Sow.
concavus, Sow. —— insignis, Schiubl.
—— Dorsetensis, Wright, un. sp. Nautilus inornatus, d’ Orb.
variabilis, d’Orb. Belemnites compressus, Voliz.
Gasteropoda.
Turbo capitaneus, Miinst. Turbo spinulosus, Miinst.

Sections in Dorsetshire.—The Cephalopoda-bed, with its under-
lying sands, is admirably developed in Dorsetshire. In several
places near Bridport these beds are well exposed. Watton Hill, on
the west side of Bridport Harbour, is capped with fossiliferous beds
of Forest Marble, which form the extreme south-western extension
of this formation on the English Coast. This rock consists here and
at Bothenhampton of thick limestone-beds, composed of shelly frag-
ments and interstratified with layers of a coarse oolitic sandy slate.
It contains

Lima carduformis, Sow. Apiocrinus rotundus, Miller.
Pecten lens, Sow. Echinobrissus clunicularis, Lhwydd.
Avicula echinata, Sow. Holectypus depressus, Leske.
Ostrea. Acrosalenia hemicidaroides, Wright.

Terebratula obovata, Sow. spinosa, Agass.

intermedia, Sow.

Economically it is used as a building-stone and is burnt for lime.
The Forest Marble is underlaid by a thick bed of grey marl, the
Fuller’s Earth, which attains a thickness here of about 150 feet, and
contains
Pholadomya carinata, Miinst. Ceromya concentrica, Sow.
Terebratula ornithocephala, Sow. Ostrea acuminata, Sow.

Myacites.

1856. | WRIGHT—UPPER LIAS SANDS. Sel

The Fuller's Earth rests upon the sands. I found no Ammonites
belonging to the Cephalopoda-bed at Watton Hill; but its western
escarpment exhibits an interesting coast-section of the three beds
in situ; the united thickness of the Sands, Fuller’s Earth, and Forest
Marble is here about 400 feet.

To the east of Bridport Harbour, there is a magnificent coast-
section of the Liassic Sands, which there attain a thickness of pro-
bably 200 feet: and between Bridport Harbour and Burton Brad-
stock there are several good quarry-sections which exhibit the upper
ragstones of the Inferior Oolite resting on the Cephalopoda-bed.
These two rocks lithologically resemble each other very much ; and,
but for their palzeontological characters, it would be almost impossible
to separate them; fortunately the Inferior Oolite ragstones contain
many Ammonites and other well-known Inferior Oolite Shells, Echi-
noderms, and Corals, and by them the line of separation can alone
be traced.

The Inferior Oolite beds contain—

Cephalopoda.

Ammonites Parkinsoni, Sow. Ammonites Gervilli, Sow.
dimorphus, d’ Ord. —— Humphriesianus, Sow.
— Martinsu?, d’Orb. Brongniarti, Sow.
subradiatus, Sow. Brocehu, Sow.

Gasteropoda.
Pleurotomaria Proteus, Des/ong. Pleurotomaria punctata, Sow.
elongata, Sow. ornata, Defrance.
Conchifera.
Lima notata, Mist. Trigonia costata, Sow.
semicircularis, Goldf. striata, Sow.
Astarte modiolaris, Lamk. Opis trigonalis, Sow.
- Brachiopoda.
Terebratula spheroidalis, Sow. Rhynchonella plicatella, Sow.
— Philhpsu, Morris. senticosa, Von Buch.
Echinodermata. ;
Collyrites ringens, Agass. Holectypus hemisphericus, Desor.
bicordatus, Desor. Echiuus bigranularis, Lamk.
Clypeus altus, M‘Coy. Cidaris Bouchardu, Wright.
Anthozoa.

Montlivaltia trochoides, Edw. & Haime.
The Cephalopoda-bed contains

Ammonites Dorsetensis, Wright. Belemnites breviformis, Voltz.
variabilis, d’Orb. Nautilus inornatus, d’Orb.
Echinodermata.

Ophioderma Egertoni, Broderip.
At Chideock Hill, three miles west of Bridport, the Inferior Oolite,

312 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

which caps the hill, consists of a light-brown oolitic limestone,
speckled with an abundance of dark, flattened, glistening grains of
hydrate of iron; in some beds the oolitic grains are very large, and
almost pass into a pisolite. A few years ago, when this rock was
worked, a great many fossils were obtained from it. My kind friend
Dr. Symes, of Bridport, who at that time collected the fossils obtained
from Chideock, gave me fine specimens of the following species :-—

Cephalopoda.
Ammonites Martins, d’Orb. Ammonites subradiatus, Sow.
Gasteropoda.
Pleurotomaria Proteus, Deslong. Pleurotomaria punctata, Sow.
elongata, Sow. —— ornata, Sow.
Conchifera.
Trigonia costata, Sow. Astarte trigonalis, Sow., sp.
Astarte modiolaris, Desh. Myoconcha crassa, Sow,
Brachopoda.
Terebratula spheroidalis, Sow. Rhynchonella plicatella, Sow.
perovalis, Sow. senticosa, Von Buch.
Echinodermata.
Clypeus Agassizi, Wright. Collyrites bicordatus, Desor.
altus, M‘Coy. Hemicidaris Bouchardu, Wright.
Collyrites ringens, Agass. Echinus bigranularis, Lamk.
Anthozoa.

Montlivaltia trochoides, Edw. 8 Hae.

Beneath the Inferior Oolite, there is a bed composed almost
entirely of the fragments of Pentacrinites, and underlying this is the
Cephalopoda-bed, with Ammonites Dorsetensis, Wright, Ammonites
hircinus, Schloth., Gervillia Hartmanni, Minst., Cucullea, Modiola,
and large Lime. As the Inferior Oolite beds were those chiefly
worked, it was from that rock the fossils for the most part were ob-
tained. The Cephalopoda-bed consists of a fine yellow micaceous
sand, indurated in parts, and passing downwards into the loose sands
of the Upper Lias. The same bed is exposed in two or three road-
side quarries between Bridport and Chilcombe Hill, from which I
collected many good specimens of Ammonites Dorsetensis, Wright,
and where I saw many large Nautili and Belemnites in situ. The
rock consisted of a coarse, brown, rubbly oolite, traversed by sandy
seams, and was worked for road-mending.

Oolitic character of the Cephalopoda-bed.—From the facts above
recorded, it is clear that the Cephalopoda-bed forms an important
and well-marked feature in the lower division of the Oolitic group :
although it contains sparingly a few species of Conchifera, such as—

Pholadomya fidicula, Sow. Modiola plicata, Sow.
Gervillia Hartmanni, Miinst. Astarte excavata, Sow.
Myacites abductus, Phil. Hinnites abjectus, Phil.

Pecten demissus, Phil. Perna rugosa, Goldf.

1856. | WRIGHT—UPPER LIAS SANDS. 313

with other species enumerated in the list of Conchifera from the
Frocester district, and which are found in the limestones and sands
of the Inferior Oolite, still it contains a suite of Cephalopoda which
are only found in the Upper Lias, and characterize that formation in
Germany, France, Belgium, and England: these are—

Ammonites opalinus, Rez. Ammonites hircinus, Schloth.
insignis, Schibler. Jurensis, Zieten.
variabilis, d’ Orb. Nautilus inornatus, Sow.
discoides, Zieten. Belemnites breviformis, Voltz.
striatulus, Sow. compressus, Voliz.
radians, Schlotheim. — Nodotianus, d’Orb.
Raquinianus, d’ Ord. —— iregularis, Schloth.

With these facts before us, I submit that the amount of paleeon-
tological evidence is in favour of our grouping the Cephalopoda-bed
and its underlying sands with the Upper Lias, rather than with the
Inferior Oolite, to which latter it has been considered to belong, and
as the basement-bed of which it has been described.

In estimating the value of paleeontological evidence, we ought to
look at its weight as well as its amount. It is well known, for example,
that many species of Conchifera and Gasteropoda have a much more
extensive stratigraphical range than other Mollusca; thus, certain
forms of these classes have lived in the seas that deposited the Infe-
rior Oolite, as well as in those of the Oxford Clay and Coralline Oolite :
of which, Trigonia costata, Pecten lens, Myacites abductus, Ostrea
Marshi, Myacites Jurassi, and Phasianella striata are examples.
But when we inquire what species of Ammonites, Brachiopoda, or
Echinodermata are common to the Inferior Oolite and Coral-rag, the
answer is none. ‘These three classes are therefore of more value to
the paleontologist than the Conchifera and Gasteropoda, seeing that
their species have a more limited distribution in time.

Ammonites are in fact probably the best indicators of geological
horizons; and this is the more remarkable, seeing that their Cepha-
lopodous occupants lived in these fragile shells in the high seas, at a
considerable distance from the shore. We know that the Lower,
Middle, and Upper Jias contain species which characterize these
divisions of that formation in the most satisfactory manner ; and that
even the different beds of these three divisions contain species pecu-
liar toeach. ‘The species of Ammonites found in the lower ragstones
of the Inferior Oolite are distinct from those of its upper beds.
The same reasoning holds true when applied to the Ammonites of
the middle and upper divisions of the Oolitic rocks, as well as those
found in the different stages of the Cretaceous group.

Brachiopoda are likewise good stratigraphical indicators, as has
been most clearly shown by Mr. Davidson in his magnificent ‘ Mo-
nograph on the British Brachiopoda.’

Echinodermata, although lower in the animal series in a alent
point of view, afford the paleeontologist the largest amount of data
on which to reason. The Silurian, Devonian, and Carboniferous
rocks are all characterized by distinct forms of Crinoidea, most of

314 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

which are limited to the different stages of these great groups. The
Liassic Crinoidea and Echinide are all distinct from those of the
Inferior Oolite, and its upper stages Great Oolite, Forest Marble, and
Cornbrash. The Echinide of the lower division of the Oolitic group
are all distinct from those of the middle; and the latter in like
manner are distinct from all other Oolitic forms. If this be true of
the stratigraphical distribution of the Echinodermata, it follows that
the Pea-grit (of the prevailing species of which I have given a list
in the description of Crickley Hill, p. 298) must be a very distinct
formation from the Cephalopoda-bed, on which it rests, seeing that
not one of the twenty species of Echinoidea and Crinoidea found in
that rock alone have been discovered in the Cephalopoda-bed a few
feet below it ; nor, on the other hand, has one of the twenty species
of Ammonites, Nautili, and Belemnites found in the Cephalopoda-
bed been discovered in any of the stages of the Inferior Oolite; so
that both our positive and negative evidence lead us to the conclu-
sion that the Cephalopoda-bed marked the close of the Liassic, and
not the commencement of the Oolitic formation.

Place of the Cephalopoda-bed on the Continent.—The Cephalo-
poda-bed * forms a very persistent fossiliferous band, occupying the
same geological horizon, in France, Belgium, and Germany. My
friend Charles Pierson, Esq., of this town, has shown me a small series
of fossils which he collected at Croisilles, near Thury Harcourt, Cal-
vados, from an Ammonitiferous bed which rests on the brownish
marls of the Upper Lias ; the series consists of Ammonites variabilis,
Am. Raquinianus, Am. striatulus, dm. radians, and one or two
species of Belemnites. This bed is overlaid by the Inferior Oolite,
containing Ammonites dimorphus, dm. Parkinson, Trigonia costata,
Astarte modiolaris, Desh., Pleurotomaria ornata, Def., Pleuroto-
maria conoidea, Desh., and Terebratula spheroidalis ; and is under-
laid by the shaly marls, the Upper Lias, containmg dm. communis,
Am. bifrons, Belemnites elongatus, Mill., and many other shells
which he has not preserved.

M. Terquem?+ has described the same bed as it occurs in the
“département de la Moselle’ under the name “ Grés supraliassique
ou marly sandstone.” This sandstone, he observes, might litholo-
gically be confounded with the “‘ grés medioliassique,”’ which appears
to be equivalent to our Marlstone, if paleeontology had not indicated
the distinction to be made between them. This bed is found near
the summit of Saint-Quentin, above Tignomont, in the environs of
Thionville, at the summit of the hill of Guénetrange, Saint-Michel, in
the environs of Longwy, at Mont-Saint-Martin, at Long-la-Ville, &c.

* M. Eugene Deslongchamps, in his “ Notes pour servir a la Géologie du Cal-
vados”’ (Bull. Soc. Linn. Normandie, 1856, p. 1), has described this bed as No. 9
of his section at Evrecy: it is there formed of a slightly coherent, argillaceous
limestone, penetrated often with small, ferruginous, oolitic grains slightly adhering
together. It contains many fossils, which are not well preserved, as Ammonites
opalinus, Modiola plicata, Gervillia contorta, and the characteristic Rhynchonella
cynocephala.

+ Extrait de la Statistique de la Moselle, page 22.

(1856. | WRIGHT—UPPER LIAS SANDS. 315

Fossils of the Marly or Supraliassic Sandstone.

*Belemnites tripartitus, Schl. Ceromya rotundata, Ag.
compressus, Sow. *Cardium truncatum, Phil.
abbreviatus?, Miller. Hettangia dionvillensis, Tqm.

* Nodotianus, d’ Ord. compressa, Tqm.

*Ammonites insignis, Schiib. Psammobia.
radians, Schl. *TIsocardia (Ceromya) concentrica,

* —_ opalinus, Rein. Sow.

Normanianus, d’ Orb. Trigonia navis, Lamk.
Pholadomya lyrata, Sow. litterata, Phil.
Zietent, Ag. pulchella, Ag.
decorata, Ziet. Arca Munsteri, Goldf.
obtusa, Ag. elegans, Goldf.
reticulata, Ag. Nucula Hammeri, Defrance.
Corbula Voltzii, Tqm. pectinata, Zieten.

*Pleuromya unionides, Ag. *Pinna fissa, Goldf.

angusta, Ag. Mytilus gregarius, Goldf.
—— equistriata, Ag. cephus, d’Oré.

arenacea, Tqm. *Gervillia Hartmanni, Goldf.
Ceromya (Gresslya) anglica, Ag. Tnoceramus.

major, Ag. Pecten paradoxus, Miinst.

striata, Ag. . Gryphea Cymbium, Lamk.
—— pinguis, Ag. Orbicula.

—— donaciformis, Ag.

M. Terquem distinguishes from the marly supraliassic sandstone a
bed which nearly resembles it in the forms of its organic remains.
He describes it under the name of Hydroxide oolitique ou fer supra-
hasique; it contains a great quantity of littoral shells and Belem-
mites, and at Longwy an attempt was made to work the bed for its
mineral contents. In some localities, as at Moyeuvre, Ammonites and
Nautili of large size are found in this ferruginous rock. A small
mine opened below Longwy was very fossiliferous, and the specimens
were in a state of perfect preservation. The following list represents
the contents of this bed :-—

Fossils of the Hydroxide Oolite.

*Ichthyosaurus communis, Conyb.; Pholadomya decorata, Ziet.
vertebree, ribs, and teeth. obtusa, Desh.

*Belemnites abbreviatus 2, Mill. Pleuromya angusta, Ag.

compressus, Sow. Ceromya (Gresslya) anglica, Ag.

— exilis, d’Orb. striata, Ag. :

acuarius, Schl. pinguis, Ag.

* Nodotianus, d’Orb. major, Ag.
incurvatus, "Quenst. . * concentrica, Sow.

*Nautilus mornatus, d’Orb. *Cardium truncatum, Phil.

*Ammonites opalinus, Rein. Hettangia dionvillensis, Tgm.
Aalensis, Ziet. compressa, Tym.

“ radians, Schl. Cytherea.

* variabilis, d’ Orb. * Astarte lurida, Sow.

c concavus, Sow. Trigonia navis, Lamk.

x insignis, Schl. tuberculata, Ag.

z Jurensis, Ziet. - undulata, Ag.

*

Pholadomya fidicula, Sow. — costellata, Ag.
VOL. XII.—PART I. Z

316 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

Mytilus gregarius, Goldf. Pecten paradoxus, Mist.
*Gervillia Hartmanni, Mist. * comatus, Miinst.
tortuosa, Phil. Hinnites, sp.
lata, Phil. Gryphea gigantea, Sow.

sandalina, Mist.

*Pecten demissus, Phil.
- cingulatus, Goldf.

I have marked with an asterisk all the species of the marly sand-
stone and the hydroxide oolite which have been found by me in the
Cephalopoda-bed.

The equivalent of this bed occurs in.the Province of Luxembourg,
and is well described by Drs. Chapuis and Dewalque * as Laas supé-
rieur, 6me étage,—Schiste et Marne de Grand Cour; and is re-
garded by M. Dumont as forming the superior part of the Lias.
The schist is worked for the extraction of bitumen at Aubange,
where numerous fossils have been found.

This bed is la terre a foulon of Boblaye,—la marne supérieure of
Sauvage and Buvignier. It corresponds to the Lias ¢ and to the
Brown Jura a of Quenstedt ; to the Posidonien-schiefer of Roemer ;
and to the Upper Lias Shale of Phillips. I regard it as consti-
tuting the upper stage of the “superior Lias.”” The authors found
the following Ammonites and Belemnites in this bed :—

* Ammonites communis, Sow. *A mmonites variabilis, d’ Orb.

* concavus, Sow. Belemnites acuarius, Schl.
heterophyllus, Sow. compressus, Voltz.

3 radians, Rein. tripartitus, Schl. (elongatus,
*

Raquinianus, d’ Ord. Miller).
serpentinus, Schl.

Our Cephalopoda-bed and sands are equivalent to Professor Quen-
stedt’s graue Kalkstein-Bank mit Ammonites Jurensis, formimg the
bed % the uppermost of his schwarzer Jura + (Lias), together with
the schwarze Thon mit Ammonites opalinus ¢, forming bed @ of his
brauner Jura.

Through the kindness of Dr. Fraas, of Stuttgart, I have before
mea series of authentic specimens of Ammonites from these German
beds, which I have compared with the Ammonites from the bed at
Frocester Hill; and there cannot be a doubt as to the identity of
the species : the specimens before me are—

Ammonites Jurensis, Ziet. Lias ¢, Balingen, Boll.

insignis, Sch/. Lias ¢, Balingen.

radians, Schl. Lias ¢, Aalen.

torulosus, Ziet. Brown Jura a, Laufen.

opalinus, Quenst., Rei. Brown Jura a,. Laufen and Gmiind.

The Frocester Ammonite-bed is therefore undoubtedly the equi-

* Description des Fossiles des Terrains Secondaires de la Province de Luxem-
bourg.

+ See Fraas on the Jura Formation, Quart. Journ. Geol. Soc. vol. vii. Part 2.
Miscell. p. 54 ef seq.

+ “Sehr machtig im untersten Gliede findet sich Ammonites torulosus.”—
Handbuch der Petrefacten-Kunde, p. 11.

1856. | WRIGHT—UPPER LIAS SANDS. 317

valent of the Jurensis-marl of Dr. Fraas, so well developed in Suabia,
and described in his admirable memoir “ On the comparison of the
German Jura-formation with those of France and England*.”’ This
bed was hitherto supposed both by English and continental geologists
to be wanting in England, but I have shown that it is probably as
well developed in our island as on the continent.

A Table showing the Stratigraphical Distribution of the Fossils contained

in the foregoing lists.

England France. | Belgium.|Germany.
= 2s
Names of Species. 2) S| eS ° a| O |-2 1/0 | 42] 0
: elelales| Sleporieis Pas
BiB BlBS|. € |e) S| ais | Bl &
S/P|Pip pee oR ESS Pie Set Eee Sate) pega
Ammonites opalinus, Rein. ............Jeee|eoe]ee. Halles Saw shee *
insignis, Schubl. ..... App Tae elias x1 | x * re *
VIEL ADINS BOT: vosaseciainvicreesesaccl'es's xl x| x i * *
—— discoides, Ziet........c.ccceeeees Sora litalicetal ness * sheesh * *
—— Thouarsensis, d’Orb. .........- SA lemalwaalsie! Se saat hI * *
radians, Rein. ...... Saeiioiiseonats oanstdltovee SINS a a i u's och aIh oe Mh harcia el sk PIG Me
Raquinianus, d@7Orb. ...02.sc00s000./e0s a Ae a ea = ae
—— hircinus, Schloth.........seecccsees[eeeleeele w.| slater afeok Ae |S PB «
Jurensis, Ziet. ....... sasigew’scuahiswdl sacle x] xk ee ie *
Dorsetensis, Wright ......... dealt oe ane
COMCAVUS) SOW sic seas ncncacs sce By ale a SEF) * * *
SEEIAUPIS IO OW, | cecverinsessseceesdlacse * |x| x an ce een PRE
— heterophyllus, DOIN eo eccdenacaeed| eee Ea ee Mae 2 Sue eed Wrage ele
serpentinus, Schloth. pee Ae eS Zee | c2 | x]. Em ar [>
—— bifrons, Brug.=Walcottii, Sow.]...| * | * * Pr epee oe
CUMMETUUNIS, SOW \ oe. <decaaecnceaec| eee ees ee se hod | *
—— margaritatus, Mft. Lica.
; Gime eelsckie katate cetageehane medline eo Tiss moyen:
spinatus, Brug..........006 b elarwniciae seslecslonalizemett (inde Lias moyen,
meme PEMEI, O OD. cc ccccccscseccocceces|ecslecefecs| ove * *
corrugatus=Murchisone, Sema Utes * *
—— Humphriesianus, Sow. | .........|...|.+.|... * * *
Broneuiarti, Sow. ......-.-- ba vataatlese|sca|ias * Ee peasy *
— Gervillii, Sow. ...........66 Pieaecsleralseavesel eee tao. |” asic, |oeen fio well ek
Brocehity Ob 0ws.cs.5.s6ece ss. Sesandlavslevsleneiae * x Hae (Re le:
— Sowerbyu, Miller....... Basins cial sigall stereos] | ereian ee * se *
= ACU CN s SOW aeatceaarssecgense~a0e|vos|cee[ceel sas | ao * *
ee CUIMOT ONS Oat amma cc css o6s|oesje<c] <= se * *
Parkinson, S0Ws-s--e¢-see<. a ete oe soalhee * a ee *
Martinsil, d’Orb. .......... ete Sod es Pe ee * *
——- subradiatus, Sow.......scccccsesceslecslecclees * *

* Quart. Journ. Geol. Soc. vol. vii. Part 2, Miscell. p. 42, &c.
Vip

318 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

TABLE (continued).

England.

France. ‘Belgium. Germany.

lai
S\gle | g F 3 3
Sh ora Faces «|| lee cede
~-| 2) 2) ”2% fo) n ro) n iw) n oO
, Sf; S'2o1 6 1.8) 6 aac ae
Names of Species. giAlA ais 4 | 2 een
2/5/5153) -B gi) oc | Be egy se
g\S/22°] € |B) 2\2/8/ Ele
Nautilus inornatus, d’Orb. ......-.+.2.|0 Bi Tite alee
EXLUNCALUS, SOW, | Sebdeeecaenpeeact Te ae, (Sees Vee
Belemnites breviformis, Voltz ......... coe’! | Roe ener
— compressus, Blainville............ re eee ee

— Nodotianus, d’O7rb. .......cccceees
—— giganteus, Schloth. .....cecccsseee
wregularis, Schloth....cce...+0+++

GASTEROPODA.

Turbo capitaneus, Miinst.......cesseeree
Pleurotomaria ornata, Defrance ......
Patella mugasas, SOW .ncesscscsreecess enn
MOAT, GHC. cutene cage smnseeinete
Nerita eostata, SOW. .6 cacceccssodock coer
Natica addueta, Phil. teccs..ec0 saceasoe
Cirrus NoOdOSus; SOW. ceccyscnssnsicnscen
Trochotoma carinata, Lyc. .........0+
Rimula tricarinata, Sow. .......ccceeeee|s
CHemmit712, MOV. SPrescn-+csa2-r ence sas

x * % * * X KK

CoNCHIFERA.

Lames duplicata A0tc aces) siconcawcovoeen cl
Lhinnia motatas Golds. c isccsedectiocernans
semicircularis, Goldf. ..........4.
—— suleata, Miinst.....cccccccecccescees
——='lyrata, Wiis.’ [o.owsccdeccastvoes ais
mH ovalts, SOW SF .16 eenesedacescccsetasloodlene
————= hellwla,: yein.vatceceacoe tenoceece sacle

eleetrandtOrbs sich cies icc eee
a OMMAGA MEI Cx; sandanaasscncetsuseacte
Opis carinata, Wright, nov. sp...
Trigonia costatula, Lyc. ............006|+
SoCEC CAE! UGH Seana irr ARE a8 SA
—— V-costata, Lye. .scccesesesssncecs
——— decorata,, LC. .........ccceescanese
clavo-costata, Lyc. ......
COSMEARMOOW.. | Sacss5 vance sensncwers
SEVIAUAM DOM ratte svvesccccnccacsted
GUpPER PAR IOW. ma csas.vaneopdcnarens
Hamsayt VV PiQe7 . ...sesjeondeaens
Pecten articulatus, Goldf..........+000.
—=~ lens, Sow. roaettieteseresbonsiencs
—— demissus, Phil.......ccccccccsessees

x * Ke % KK
x Xe *

Middle.

Lower.
Lower.

Upper.
Middle.

eeevececece

* eee * eee eee

1856. | WRIGHT—UPPER LIAS SANDS. 319
TABLE (continued).

England. France. | Belgium.| Germany.

my ag
a
a} §|e ° : : -
fool Dies o o o o
O/®los = SS oS 2
n| 2/2 SO a oe n we) n we)
: é].s|.S1 a9 3 Ser Ouec
Names of Species. g/S/4las S S| 5 Sa ae | =
Pia! Blas (=) mH o) I i) =] o)
4/2) sie, °F @} °F ol fet Ge gs
=i/a}] a Qs Oo 2, o Qa o a o
a] a} &)o— = oF = a = a a
e)P}P ip SS GS eed ee ee
ecten) textormus 2, Gold, cic..c...ccess[oss|o4o| |. | ~~ wea-s-fowel afaad | #

cee a COMIAGNS 25 IVINS vate: 4s cco<cucese|se-|ea|esz) *
Hinnites abjectus, Phil. ...........0c0.[sce[eo+] | *
saa CHBEFCULOSUS, GOIGf..... ..2.ccn0s0|s+<| «>| sea] 2+-
BESET PLT a astnaceieniccdacsaenalers|seeleos| 00
pean Pee ereeisina sc raaevacesscescseesesiess|+>|-+6leao| «0s
PRE HIES SES Pl cles ce sscccessenacecs 4-;necesalie-|++0]ece| «=»
Placuna Jurensis, Roemer ...........|+++|.e-[eo| «+
Modiola plieata, SOw- \...scs.cccescsceoe|---[--2| | *
Mytilus bipartita, Sow., sp. .....csecce.feceecefere] eee
PCC MNALUS OOW Es Voecceeecdsccdsceloes|sas|ees] v0.
UCM TOlLOfvcneracesaesiedsicececs|s0-[<+-|o60] «0»
SERIE UIUS LIS ie edeeecccdeascdes.\o++|s.loos| ses
CHUEAEUSMOOW ice ccescttcccdeced ooclesclese|ess) sss
_ESTLSTEDS TG 2/7 Re A en I
BINS MUL OL Of cone soiapsciess Sedesiadesalses|sssleee|’
Myoconcha crassa, Sow. .....ssccescese|ooe|e-[eee! one
Strat COSEAIA, SOD.) <2-ccccssscccoseoveae|se[ecsleoe] »s-
Avicula ? complicata, Buck. ........s...[ece[eeefeee| one
Inzequivalvis 2, SOW.....cecssescsceleee|eeefece|
CEMMALAs, OOM iovcncaccaccadssesdcen|enstcvs|eos| ca
Licina lyrata, Phil. ..0.0..ccccoeosssnece|eee|ooe|esel csc
Quenstedtia levigata, Phil. .....0c0...|+-sJees{ere| os.
Ceromya plicata, Agass. ...csccecssecs.lereleosfere] oon
Bajociana, @ Orb. ...0.000ss00000|<+s|eee/eee| se
Cuculleea, Nov. sp.s.c.siseorcss.ocessceene|eee| ees] F} oF
Macrodon Hirsonensis, d’Archiac ...|++|.+.)e++| ss.
Arca inzequivalvis?, Goldf. ....ssssees[eee|+e
Myacites punctatus, Buck. ....scsecsslore{ecs|ore| woe
—— oblongus, Buck. ...cccccscssecscsleeslece[ere] one
—— dilatatus, Buck. ...cccoccssseccvesiecs|ooe|ees
tenuiistriatus, AGdSS. .....ccceceecesees[oee|ers
Cardium Hull, Wright ......ccsssseeeleee|eee}ere
—— Oppellti, Wright .........ceescseeelece|one| ees
Pholadomya fidicula, Sow. .....se.e00.| ++[.--| *
Gervillia Hartmanni, Miinst, .........]..-|...Je+
—— fornicata, LYC. ......sc..secceccscs[erelece| ¥
Perna rugosa, Mist. esecccco.22.0205..|++-| 2.) ¥
Gresslya abducta, Phill. ..........cs00e[eee/eoe] *

*

*

o¢
Ro:
* *

%*
oe ok ee

x *

ese eee een

Xx KKH KKK KH HHH K KE HHH HK KH HH KH
*

*
5
*
- %

eee ese *

eK

COnformis; AgasSraredaceeecein scien.) sel 02
Goniomya angulifera, Sow. ............Je+/eee
Astarte excavata, Sow. ..cccccccccscesece|esefooe| *
—— modiolaris ?, Lamk.......ccccccceelees|ecclers
—— complanata, Roem. .....sccseseseferelecefoes

xe ee KK
*
a SS Sh es

xx *¥ HK KKH KK
%
*

——,

320 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

TABLE (continued).

England. . | Belgium.|Germany.

2/3 (3
AIalS | $ 3 $
Sim ieee Sie13
Names of Species. g Aa 5 ae © ° 3 °
z\sle|se| = glels
Astarte luridat SOW. iassceeshacexectess elems|eos} FO A Wee neal] eS
Se TUPTNOSA, PYG yu neistactiene see heccna| eel alee ee
Cypricardia cordiformis, Desh..........]... coeleoe| * coe |
PECWISS PTI ssp niesetime ante ts a.al nie 5 * | x
BRACHIOPODA.
Terebratuila simplex, (Buchk.”..0.-.cacses|ycc|nonlmael oe *
PHGdta, Bach Yeates. sts acece donee demiimestoataliass *
submaxillata, David. .........00+|... wosaadl aad *
subpunctata, David............ secrete mal EHS Se
Rhynchonella Wrightii, David. ......|...|...[-+ x *
—— decorata, David. ...ccccscceccccusclacsleoa|see| aos *
ANGULALA 75 SOW. soneckecsensaciececien: coslerel ace |
COWEINNA, SOW. verse ccoscovenoddecvalvaslesclewelices *
Oolitica, Sow. .ccccccee ene Bisa es, | ia A (OP Bade *
cynocephala, Rich. ............ Breet ere ial | pte Se |e Eee
— furcillata, Thiod. .........ccecesseelece| * | *| re vol ie
Thecidea triangularis............+.0+ beelis “5 | me 2
ANNELIDA.
Serpula grandis, Goldf.......... esis ge eincaliooi Risse aad : * ans] sexta
convoluta, Goldf....... sins ester creel leeeterctfeiee| ie * see [eee]
a= DiCatIS,, MAMNSE, 2 ceistassion's caeatiacl enol va) e=e gestae Be a ie:
= (AGT eLA gO Of x cogsa-creee seed becleentace * BS eral:
SOGIAIS, (GOA) .5 ce ssestecsans vouch el ha.|menteorlie. * [ec] *
sulcata ?; Goldfe, Weenssaccws ase snalqoialean| eel era a eee
flaria, Golds. capmr'ssaseensasase tl con eemleel eee eee sant geen
pooee Haccida, Goldfescesreseeanearears pistol ea) mae inal eset on gE mee
ECHINODERMATA.
Cidaris Bowleri,, Wright. .0c..«ssicecssalerelaeelseelieea a
Bouchardii, Wright ..........+. aie fiawalemel site *
Wirielita, Desop ..cc.sssense ce sival op leanterel mae] 1 Ste
Rabdocidaris Wrightii, Desor..........|.. Witalealisca|’ ak
Acrosalenia Lycetti, Wright............ Baa 85S he *
spinosa, Agassiz ...... sian eeeaee abelen : x
Diadema depressum, Agassiz ......+..|... OS an
Echinus germinans, Phil.......c.ceeeess|eoe <= 555 DAE N=
=" Pigtail aris erepe weweasn00sbeeenpas|n ‘; *
Polyeyphus Deslongchampsil, Wright|...|...|... *k
Hemipedina Bakeri, Wright .......+....|...]...| « *
—— tetragramma, Wright sscccrcscoselecalacslers| coe |

1856. | WRIGHT—UPPER LIAS SANDS. 321

TABLE (continued).

| France. | Belgium.|Germany.

Names of Species.

| Upper Lias Clay.
| Upper Lias Sands.
lopoda-bed.
Inferior Oolite.
Inferior Oolite.
| Inferior Oolite.

| Marlstone.
| Upper Lias.
| Upper Lias.
| Upper Lias.

5
|

>| Upper Lias Cepha-

Hemipedina perforata, Wright Saas eee
Waterhousei, Wright .....0ssscJece|sssfose| oes
—— Bone, Wright ........cccecseesaseeece|ecelore| one
Pygaster semisulcatus, Phil. .......+.[e0-]--e/eee] 2.
conoideus, Wright ... ...sceeese-|eceleceleoe| eee
agariciformis, Forbes ...+++...see|seefoeelere] vee
Caudatus, Wight .....0...sc00s0000|-0-)ere)eoe| oes
Clypeus Agassizil, Wright ......++se0e)-e0]--e[e0.] -08
bits, VEC Oi c.- ccc cacceesancesao]ece]sala+-) a+
Extracrinus, NOV. SP....cereeeeeeeeseeeree|eeele ees |
Ophioderma Egertoni, Broderip ......|...|... x

-««/Sarthe

* *¥ Xe He KH HK KH XK
e

ANTHOZOA.

Montlivaltia Delabechei, Edw. & H.|...|...|...] ...
Waterhousei, Edw. & Havme ...|...|...|...| «+
cupuliformis, Edw. & Haime ...|...|...|...| +++
Wrightu, Edw. & Haime.........|.+.|...|.+.] «+
Axosmilia Wrightii, Edw. & Haime ..|...|...|...| «+
Latromeandra Flemingii, Edw & H. ||...|...]...| «.-
Vavidsoni, Edw. & Haime ......)...|...Je+.| «+
Thecosmilia gregaria, Edw. 6 Haime)|...|...}...| ...
Thamnastrea Defranciana, Edw.& H.|...|...|...] «+.
—— Terquemi, Edw. & Haime......|...|...}...| «0
— Mettensis, Edw. & Haime ......|...|...|...] oe
fungiformis, Edw. & Haime ...|...|...}...] «.
Isastrea tenuistriata, Edw. & Haime .|...|...|...| «.-

eH KH HK KE HH KH KH

BRYOZOA.
Stomatopora dichotomoides, d’Orb...}...]...|...] 2-6] * |e..|

Notes on some New Species of Mollusca collected from the Cepha-
lopoda-bed, and included in the Lists of Fossils in the preceding
Memoir.

Ammonites DorseteEnsis, Wright, nov. sp.

Shell discoidal, compressed, not carinated. Each whirl in middle
age ornamented with from forty to forty-five ribs, which commence
at the umbilical margin, where they are most prominent, become
flattened and almost disappear on the sides, and reappear bifid near
the dorsal margin, each primary rib having apparently become bifur-

| Inferior Oolite.

322 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

cated at the upper third of the whirl; the ribs and their bifurca-
tions are all bent gently forwards, and each whirl exhibits three or
four contractions at nearly regular intervals of growth. Spire
formed of seven or ten whirls, according to age, which are all well
exposed ; their greatest diameter is near the umbilical border ; from
this point the sides slope gently towards the dorsal border. Back,
in middle age, narrow, rounded, and smooth both in the shell and
mould. Mouth oblong, compressed on the sides, and becoming nar-
row on the dorsal third ; when entire, it terminates in two shaped
processes. Umbilicus large, with stair-like sides; the whirls em-
bracing the half-smooth part of the shell, and exposing the inner
ribbed portions thereof.

The septa are symmetrical on the dorsal and lateral parts of the
whirls, and consist of a dorsal lobe and five lateral lobes; the
dorsal lobe is much larger than, but not so long as, the superior lateral
lobe ; it is divided by the median line into two parts for about oue-
third of its length, and is formed of six symmetrical, nearly equal-
sized lobules, which are provided with three or four unequal digitate
margins; the superior lateral lobe is smaller, but much longer than
the dorsal ; it is formed of eight unsymmetrical unequal-sized lobules ;
those on the upper side are more developed than those on the under
side, and the terminal leaf is much the largest, with large lateral
bifid ramifications ; the inferior lateral lobe is small, and directed
obliquely backwards ; it is composed of two lateral lobules, and one
terminal lobule, which are unequal ia size and either trifid or quad-
rifid on the margins; the three ventral lobes decrease in size from
above downwards; they are all directed obliquely upwards; the upper-
most lobe is tridigite, the second is bidigite, and the third consists
of a single lobule with jagged margins.

Up to the diameter of 6 or 8 inches the shell retains its ribbed
character, as described ; but when it grows beyond that size, it loses
all its ribs, the whirls become more thick, the back more rounded,
the shell smooth, and only marked with lines of growth and slight
periodical constrictions.

Dimensions. —Usual size from 8 to 9 inches in diameter; the
largest specimen known is in the British Museum, and measures
16 inches.

Affinities and differences.—This species, up to the diameter of
6 inches, resembles Ammonites Parkinsoni, and is frequently named
as such in public collections: this may have arisen in part from the
remark made by Sowerby in his description of Ammonites Parkin-
soni, that “it is the Ammonite so frequently split, polished, and
sold at Bath;”’ and again, ‘‘I suspect it may also be found in the
lower beds of the Iron-shot Oolite, as the specimen figured is from
near Yeovil.” Now the fact is, that Ammonites Parkinsoni so well
figured by Sowerby (Min. Conch. tab. 307. fig. 1) rarely exceeds
6 or 7 inches in diameter, and is not often either split or polished ;
whereas the specimens of Ammonites Dorsetensis selected by “‘ the
gothic hands of the mason,” almost always exceed these dimensions.
All the largest and finest specimens of Ammonites Parkinsoni which

1856. ] WRIGHT—UPPER LIAS SANDS. 323

I have collected retain their ribs in mature age, whilst Ammonites
Dorsetensis as constantly loses them, the whirls in old specimens
of this species being always smooth. The ribs in 4. Parkinsoni are
always more sharp and prominent than those of 4. Dorsetensis, and
the latter wants the small terminal tubercles which adorn the dorsal
ribs in A. Parkinson. In the wnould of 4. Parkinsoni the middle
of the back is slightly excavated, whereasin 4. Dorsecensis it is
rounded.

Locality and stratigraphical position.—This species characterizes
the “ Cephalopoda-bed ”’ in Somersetshire and Dorsetshire ; it is col-
lected in abundance at the Half-way House between Yeovil and
Sherborne, where the largest shells are obtained; I have found it
near Bridport, and at Burton-Bradstock. In its stratigraphical po-
sition, therefore, it differs from 4. Parkinsoni, which is always found
in the upper ragstones of the Inferior Oolite associated with Echi-
nodermata, Brachiopoda, and other fossils found only in that Oolitic
zone.

Triconia Ramsayit, Wright, nov. sp.

_ Syn. Trigonia signata, Lycett, Annals and Magazine of Nat. Hist.
ser. 2. vol. xii. p. 239.

Shell very inequilateral, flat, and elongated, the height being small
in proportion to the length; umbones near. the anterior side, small,
nether prominent nor recurved ; area well developed, lengthened,
flattened, marked with transverse lines of growth; carinz nearly
obsolete, represented bv smooth elevations.

Surface of the valves ornamented with twenty nearly equal-sized
tuberculated costz ; the anterior and posterior series form concen-
tric ridges, and the middle series are undulated ; the tubercles of the
costee are nearly of a uniform size, and placed close together on
thickened ridges of the shell.

Length 233 inches. Breadth 132 inch. Thickness 1,3, inch.

Affinities and differences.—This shell resembles Trigonia angu-
lata, Sow., in the flatness of the area, and in the absence of pro-
minent carinz in that region; but differs from it in being more
straight and elongated, and in its height being less in proportion to
its length: the umbones are likewise smaller, less prominent, and
nearer the border.
~ It differs from Trigonia signaia, Agass., with which it was iden-
tified in the absence of tuberculated carinze from the area, in being
more compressed, more elongated, and not so high ; the tuberculated
costee are more numerous, and their arrangement less regularly con-
centric. It is sufficiently distinct from all the other clavellated
species of Trigonia.

Locality and stratigraphical position.—Collected hitherto only
rarely in the Cephalopoda-bed of Frocester. The species is dedi-
cated to my friend Professor Ramsay, Local Director of the Geolo-
gical Survey.

324 PROCEEDINGS OF THE GEOLOGICAL society. [April 9,

CyYPRICARDIA BREVIS, Wright, nov. sp.

Shell triangular, equilateral, ventricose, and cordate; posterior
side short and sharply angular ; anterior side bluntly rounded ; um-
bones large, prominent, nearly central and much recurved, with an
acute carina descending from them to the posterior side; surface
nearly smooth, slightly marked with lines of growth ; margin of the
valves straight.

A. Frocester specimen.—Breadth 1,5, inch. Length 1,85 inch.
Thickness 1,2, inch.

B. Sherborne specimen.—Breadth 2,4, inches. Length 2,5, inches.
Thickness 1,2, inch.

Affinities ‘and differences. —'This shell resembles Cypricardia
Bathonica, dOrbigny, but it is a much shorter and straighter form ;
the carine on the posterior side are more prominent and acute; but
it wants the graceful twisted slope which characterizes C. Bathonica.

Locality and stratigraphical position.—I have collected this
species out of the fossiliferous nodules at the base of the Sands at
Nailsworth, and in the Upper Lias Sands at Frocester Hill, dmmo-
nites bifrons being associated with it in the same nodule; much
larger specimens are found in the Upper Lias near Sherborne. It
appears to be a very rare shell.

Opis CARINATUS, Wright, nov. sp.

Shell trigonal, its breadth nearly equalling its length ; umbones
large and incurved, bounded on their posterior borders by acute
prominent carinze which descend along the margin of the valves and
bound the posterior side; anterior side rounded; surface of the
valves ornamented with regular concentric ridges; posterior side
concave, the surface marked with sharp oblique close-set lines ;
lunule small, nearly circular.

Length 1,2, inch. Breadth 1,4, mch. Thickness +4ths of an
inch. ;

Affinities and differences.—This shell resembles Opis (Astarte)
trigonalis, Sow., in its proportionate length ; but it is distinguished
from it by the regular concentric ridges on the surface of the valves,
those on O. trigonalis being waved, by its acute prominent carinze,
and by the general sharpness in the outline of the different parts of the
shell. It differs from Opis lunulatus, Sow., in being a much longer
and more compressed form, in having more prominent carinze and a
small shallow and nearly circular lunule, that of Opis lunulatus
being large, deep, and cordate, with acute margins.

Locality and stratigraphical position.—Collected only from the
Cephalopoda-bed of Frocester Hill; it is not an abundant shell, and
is seldom well preserved.

Carpium Hutu, Wright, nov. sp.

Shell smooth, subtrigonal, inequilateral ; breadth nearly equalling
its length ; the anterior side convex and rounded ; the posterior side

1856. | BOUE—DOVER STRAITS. 32d

sloping obliquely from the umbo to the posterior border; the mar-
ginal fold of this side is slightly flattened, on which a series of con-
centric ridges are seen crossing the lines of growth at different angles ;
the umbones are small and placed near the centre; the surface is
only marked with delicate lines of growth.

Length 21 inches. Breadth 142 inch. Thickness 1,5, inch.

Affinities and differences.—This shell resembles C. levigatum,
Lyc., in the smoothness of its surface, but is distinguished from it by
the shortness of its posterior side, and the band of concentric ridges
which extends from the umbones to the posterior border.

Local and stratigraphical position. — Collected only from the
Cephalopoda-bed of Frocester Hill. The species is dedicated to my
friend Edward Hull, Esq., F.G.S., of the Geological Survey.

Carpium Opreii, Wright, nov. sp.

Shell smooth, convex, slightly inequilateral; umbones large, pro-
minent, incurved, nearly central ; anterior side rounded ; posterior
side slightly produced and gently truncated; on this more or less
angular band numerous concentric ridges are seen.

Length 2 inches. Breadth 18, imch. Thickness 1,4, inch.

Affinities and differences.—This shell resembles C. levigatum,

Lyc., but itis a more elongated and compressed form: the posterior
side is flattened and ornamented with concentric ridges which are
absent in all the specimens of C. levigatum which I have examined.
It may prove to be only a variety of that Inferior Oolite shell when
a larger number of specimens permit a more rigorous determination
to be made.
_ Locality and stratigraphical position.—Collected from the base
of the Sands at Nailsworth, where it is not common. ‘The species is
dedicated to my friend Dr. Oppel, of Stuttgart, well known for his
extensive acquaintance with continental Oolitic Geology, and author
of * Die Juraformation Englands, Frankreichs, und des siidwestlichen
Deutschlands.”’

4. On the Probable Origin of the ENcxisn CHANNEL by means of —
a Fissure. By M. Ami Bove, For. Mem. G.S.

[ Abstract. ]

Tuer author, having met with a published proposal to construct a
submarine tunnel across the Straits of Dover, pomted out that it was
highly probable that the English Channel had not been excavated
solely by water-action, but owed its origin to one of the lines of dis-
turbance which have fissured this portion of the earth’s crust ; and
that, taking this view of the case, the fissure probably still exists,
being merely filled with comparatively loose material, and would
prove a serious obstacle to any attempt to drive a submarine tunnel
which would have to traverse it.

OO

t- a

326 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

Apri 23, 1856.
Lester Lester, Esq., was elected a Fellow.

The President read a Letter from the Directors of the New River
Company, in answer to a Memorial, signed by many Members of the
Society, relative to the Artesian boring at Kentish Town :—the
Directors expressed their regret that they did not feel it to be their
duty to the Proprietors of the Company to proceed further at pre-
sent with the boring.

The following communication was read :—

On the Formation of Craters, and the Nature of the Liqutp-
iry of Lavas. By G. Poutrerr Scrops, Esq., M.P., F.R.S.,
F.G.S.

CoNTENTS.
Introduction.
I. Formation of Cones and Craters.
Hypotheses of crater-formation by ‘ Elevation,” ‘‘ Denudation,” and
“ Engulfment.”
Circular form of Craters.
History of Vesuvius.
II. Nature of the Liquidity of Lavas.
Plutonic rocks.
Lamination, cleavage, and foldings of rocks.

Introduction.—It is now some thirty years since I published two
works* upon the Phznomena of Volcanos, Active and Extinct. I
described in them, as accurately as I could, by pen and pencil, what
I had observed during a residence of some duration among the vol-
canic districts of France and Italy; and explained, in considerable
detail, the laws which, from those observations, I believed to regulate
the remarkable developments of subterranean energies usually called
volcanic, which have played so important a part in the construction
of the superficial crust of our planet.

The general principle on which I proceeded in the theoretical
portion of these works was the same which had been previously em-
ployed by Hutton and Playfair, and was subsequently adopted, with
signal success, by Sir Charles Lyell,—namely, to refer, so far as is
possible, appearances the origin of which has not been witnessed, to
such causes as are seen or known to produce analogous appearances
in the present day,—instead of resorting for the purpose to imaginary
hypotheses.

In the earlier volume of the two (the Considerations on Volcanos),
however, I certainly overstepped this wholesome rule, by entering
towards the conclusion of the work upon some rather crude specula-
tions on a general theory of the globe; and this, together with
defects of style and arrangement, and likewise of illustration, of
which I became sensible only when it was too late to amend them,

* “ Considerations on Volcanos,” &c., 1825-6. ‘ On the Geology of Central
France,” &c., 1826-7.

1856. | SCROPE—CRATERS AND LAVAS. 27,

sufficiently accounts for the different reception these two works met
with from geologists at the time. Neither, however, I presume to
hope, were wholly without some beneficial result. At the period of
their publication, the Wernerian theory of the precipitation from
some aqueous menstruum, not merely of granite, and what were then
called the primitive formations, but even of all the trap-rocks, still
prevailed, and had the support of a large school of geologists in this
country. I venture to think that the facts reported in my two
volumes (especially those represented to the eye in the atlas illustra-
tive of the volcanic remains of Central France) had some share in
the final extinction of that German romance, —which some geologists
as old as myself may remember to have been regarded almost in the
light of a gospel-truth, and defended with all the acrimony of pole-
mical controversy.

Some of the opinions, however, expressed in these works with
respect to the laws that govern volcanic action, were severely criticised
at the time. Others have been since opposed by rival theories. And,
as these disputed questions have an important bearing on some of
the most interesting problems of geology, I trust it may not be un-
profitable to call the attention of our Society to the more prominent
among them. 7

I will advert on this occasion to two subjects especially, viz.

I. The origin, or mode of formation, of volcanic cones and craters.
II. The nature of the liquidity of lava at the time of its protrusion
from a volcanic aperture.

I. Formation of Cones and Craters.—In both of the works to
which I have alluded, I referred the formation of those remarkable
circular hollows, usually called craters, which are of such frequent
occurrence in volcanic districts, to explosive aériform eruptions,
breaking their way through the superficial rocks; and that of the
external more or less conical hill or mountain which generally, but
not always, environs a crater,—and which, indeed, often occurs with-
out a crater, but always characterized by the qua-qua-versal dip of
its constituent beds of lava and conglomerates,—to the accumulation,
round and above an eruptive vent, of its fragmentary ejections and
the lava-streams poured out from it.

I considered this law to be without exception; attributing the
differences in figure and structure apparent among volcanic cones to
the greater or less number and violence of the eruptions to which
they were owing,—some being the product of a single eruption,
others of a vast number, often repeated through a series of ages,—
to differences in the position of the orifices of discharge, whether
from the summit of the cone, or its base, or any intermediate points,
—and whether from under water, or in the air,—to the varying
mineral character of the products,—and to the influences of subse-
quent degradation.

At the same time I remarked that the earthquakes which always
more or less accompany volcanic eruptions render probable a certain

328 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

amount of elevation in mass of the pre-existing superficial rocks ;
and moreover that the rents they cause in the solid substance of the
cone of a volcano in repeated eruption, into many of which rents
liquid lava will be injected from the column rising in the central
chimney, and cool down afterwards into more or less vertical dykes
of solid rock, must have added considerably to the bulk and elevation
of such a mountain, by a sort of inward distension.

This was no closet-theory,—because, as respects the cone and
crater of Vesuvius at least, I had the advantage, in the years 1818,
1819, and 1820, of watching with my own eyes the outward growth
of that cone, through a series of almost continual eruptions of a
comparatively tranquil character, which during those years added
considerably to its height and bulk by external accretions of ejected
scoriz and lava-currents. These last, the lava-streams, issued from
small cones and craters formed upon the solid platform which then
composed the summit of the great cone, and dribbled slowly down
its slopes, consolidating so rapidly there as in few instances to reach
the base of the cone at all; although night after night they were to
be seen flowing from the summit in streams of considerable breadth
and bulk, and glowing with a bright light on its steep sides.

Afterwards, in the latter part of the year 1822, I had seen the
upper portion of this solid cone blown into the air (by which it lost
a full third of its height), and a crater of vast dimensions drilled
through its axis by continuous eruptive explosions of twenty days’
duration.

I had previously made a close examination of the cones and craters
of Etna, the Phlegrzean Fields, the Lipari Isles, Central France, and
the Rhine district; and their appearances accorded so completely
with the supposition of an analogous mode of formation im their
instances, that, upon the principle of explaining the unknown by the
known, it seemed impossible, or at least unnecessary, to imagine any
other origin for them.

“< Elevation,” ‘‘ Denudation,’ and “ Engulfment’’ Theories of
Crater-formation.—It was, therefore, with no small surprise that I
have since found this simple and natural mode of production denied
to all cones and craters—including those of Vesuvius itself; and an
hypothesis substituted of their originating in some sudden elevation
of previously horizontal beds around a centre,—not (it would seem)
of eruption, but of maximum elevation. I allude, of course, to the
“ Hlevation-crater theory”? of MM. Von Buch and Elie de Beau-
mont.

Sir Charles Lyell, M. Constant Prevost, and others, have amply
refuted this unphilosophical theory ; which, however, still appears
to hold its ground to some extent on the Continent, through the
prestige of the great names attached to it. It may, therefore, not
be wholly useless to adduce some additional proofs of its unwarrant-
able character. But I must first be permitted to remark, that even
Sir Charles Lyell, while supporting the view indicated above, of the
generally eruptive origin of volcanic cones, has had recourse, in the
case of some craters, to another agency, the influence of which I am

1856. | SCROPE—CRATERS AND LAVAS. 329

induced to think he over-rates;—I mean the excavating power of the
sea in forming what he calls “craters of denudation.” This phrase,
I think, he first employed in a paper on the subject read before this
Society in December 1849. It is not repeated in the latest edition
of his ‘ Principles,’ and I imagine, therefore, that he is no longer
desirous of maintaining its propriety.

I by no means doubt, that in the case of craters formed beneath
the sea, or in such close vicinity to it as to allow its waves and cur-
rents to enter and sweep round their interiors, these circumstances
must have considerably modified the result. In the former case,
that of subaqueous eruption, the resistance of the water above the
vent would probably tend to throw off the ejected materials over a
wider area. And thus, perhaps, we may account for the vast hori-
zontal dimensions of the great crateriform basins of Italy,—Bolsena,
Bracciano, Albano, and others, evidently of submarine origin. In
the latter case, that of subaérial craters to which the sea has had
access through some lateral opening, no doubt great degradation of
their internal slopes and cliffs, as well as of the outside, will have
often taken place. Many, indeed, will have had their enclosure re-
duced to a mere skeleton, like Santorin. Some, like Graham’s Isle,
have been entirely swept away. But the question being as to the
origin of these crateriform hollows, not as to the cause of any sub-
sequent alteration of figure, this, I believe, may in every instance,
without exception, be most reasonably referred to volcanic explosive
eruptions. And, therefore, the employment of such a phrase as
“craters of denudation,’ im contradistinction to ‘craters of erup-
tion,” can only lead to a wrong conception of the originating forces.

Where, indeed, is to be found a crater, the formation of which
cannot be accounted for (making allowance for the subsequent modi-
fications already referred to) by eruptive phenomena of the same
character as those which have before the eyes of trustworthy ob-
servers repeatedly drilled enormous craters through the axis of the
cone of Vesuvius ?

Is it the vast size of some craters which should render such an
origin incredible in their instances? For example,—of the Val di Bué
on the flank of Etna, the Caldera of Teneriffe, that of Palma, San-
torini, or the external crater of Barren Island ; which measure some
three, five, or even six miles in diameter? But the crater of Vesu-
vius, formed in 1822, before my eyes, by explosions lasting twenty
days, measured a mile in diameter, and was more than a thousand
feet deep. The old crater of Somma, which half encircles the cone
of Vesuvius, is about three times as wide as the crater of 1822. Are
we, then, on that account alone, to believe that it could not have
been produced by an eruption of proportionately greater violence,—
when, too, such an eruption is known to have occurred about the
time this crater must haye been formed, namely in the year 79, and
to have overwhelmed three cities at the base of the mountain be-
neath its enormous fragmentary ejections? Is it not, on the con-
trary, much more in accordance with sound philosophy to ascribe
the excavation of the old concentric crater of Somma to the same

330 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

cause which but the other day was seen to excavate the new crater
of Vesuvius, through the heart of the same mountain, than to invent
for the former a different and fanciful process? But if Somma be
admitted, notwithstanding its extent, to be a true crater of eruption,
the same origin cannot be denied to that of Palma, Santorini, or
others, on the ground of their size, which scarcely, if at all, exceeds
that of Somma.

Sir Charles Lyell seems to doubt the Val di Bué being a true
crater of eruption upon two grounds. First, because the beds com-
posing the surrounding cliffs do not show the usual qua-qua-versal
dip, but generally slope towards the sea. This, however, is merely
the result of the eruption having broken out on one side of the
central axis of the mountain,—a circumstance of frequent occurrence ;
and naturally so, because the old central vent is apt to be sealed up
by the consolidated products of former eruptions, and the point of
least resistance to the subterranean eruptive force will often, there-
fore, be a little on one side,—probably on a fresh point of a fissure
broken through the flank of the mountain.

In fact, there must be a contest between the resisting powers of
the sides of the mountain and of its upper part; and the weakest
part, whichever it is, will give way, and be blown up.

Sir Charles’s second reason is, that a sufficient amount of conglo-
merates is not to be seen on the mountain-slopes around the Val di
Bué, to account for the vacuity. But, besides that he himself speaks
of ‘‘ enormous masses of scorize on the flanks of Etna,”’ it should be
remembered that the aériform explosions, when long continued, tri-
turate the ejected matters, owing to their repeated fall into and
rejection from the crater, to such a degree as to reduce the greater
part at length to an impalpable powder, which is carried by the
winds to a distance, sometimes of hundreds of miles, and spread in
a thin layer over an enormous area of sea or land. And, moreover,
the larger the dimensions of any crater, the more powerful and en-
during will have been, in all probability, the explosions, and the
more thoroughly triturated, during the process of its gradual enlarge-
ment, would be the fragments thrown up by them.

I remember being exceedingly surprised, after the termination of
the Vesuvian eruption of 1822, forming a continual fountain of stones
and ashes some miles in height, lasting through twenty days, and in
the end completely gutting the mountain, to find that the prodigious
amount of fragmentary matter thrown out from the crater had coated
the outer slopes of the mountain only to an average thickness of a
foot or two at most. But then the ashes which day by day were
reduced to a finer and at length to an impalpable powder, so fine as
to penetrate the closest rooms in the houses of Naples, were borne
to vast distances by the winds. Much, too, was carried down into
the plain, or the sea below the mountain, by the torrents of rain
(producing lave di fango, or mud-lavas), such as overwhelmed Her-
culaneum, and which accompanied, as usual, the paroxysmal erup-
tion of 1822.

Indeed, if we consider the statements adduced on good authority,

1856. | SCROPE—CRATERS AND LAVAS. 301

of the prodigious distances to which ashes, and even large fragments
of lapillo and of pumice, have been occasionally borne away from
some of the volcanoes of South America and the Pacific (as, for ex-
ample, in the eruption of Coseguina in 1835, and of Galongoon in
1822),—distances of more than a thousand miles (a large segment
of the circumference of the globe), the whole of which intermediate
space must have been strewn with them (and, in the first of these
instances, it is said, to the depth of ten feet at the distance of twenty-
four miles from the volcano), we may well conceive that eruptioris
productive of such an enormous amount of ejected matters may (nay,
must) have blown into the air entire mountains of a magnitude far
exceeding that of Vesuvius and Somma itself, or the bulk of matter
wanting in the Val di Bué, and left in their place craters of corre-
sponding dimensions.

Sir Charles Lyell suggests (as others have done before him), in
regard to some of the largest known craters, another possible origin,
which he calls Hngulfment—-that is, the subsidence of the upper
part, or a large area, of a volcanic mountain into some abyss suddenly
opened beneath. With respect to this supposition, without attempt-
ing to dispute its possibility, I must say that I am not aware of any
such process having been ever witnessed by any credible observer so
placed as to be able to distinguish between engulfment and ejection ;
and consequently that it were well to be cautious in admitting the
occurrence of such a phzenomenon, if the ordinary mode of action
be sufficient to explain the facts really observed. We possess revorts,
it is true, of eruptions and earthquakes in Java, Sumatra, the Andes,
and elsewhere, having caused the disappearance of the entire summit
of a mountain, leaving a vast cavity in its place. But this is pre-
cisely the result that was observable after the eruption of Vesuvius
in 1822. And in that mstance we know there was no subsidence.
The leading example usually adduced of such immense (supposed )
engulfments is the truncation of the lofty cone of Papandayang, in
Java, by an eruption in the year 1772. ‘There, it is always said, a
great area of the volcano “fell in and disappeared,” swallowed up in
the bowels of the earth, together with forty villages and their inha-
bitants. Such are the phrases usually made use of on these occasions,
and very naturally so, by alarmed and unscientific observers. But
recent explorers, especially Professor Junghuhn, have stated that
these towns and villages of Papandayang were not swallowed up at
all, but buried, like Pompeii, under the ejectamenta of the volcano ;
and Dr. Junghuhn, therefore, very properly refers the truncation ‘of
the mountain to eruptive explosions, rather than to subsidence.

It is, no doubt, quite conceivable, that within a volcanic mountain
some internal reservoir, or subterranean lake of liquified lava, coated
over by a crust of hardened rock or the accumulation of fragmentary
matter, may be tapped, as it were, by an earthquake, and empty
itself out of an aperture in the side of the mountain at a low level,
leaving a cavity, which another earthquake, or the explosion of vapour
and gases accumulated within it and increasing in temperature, may .
cause to burst, like a vast bubble,—the overlying crust of rocks

VOL. XII.—PART I. 2A

332 PROCEEDINGS OF THE GEOLOGICAL society. [April 23;

falling inwards. But such a supposition is, in the present state of
our knowledge, purely conjectural, and unwarranted, if, as I have
endeavoured to show, the ordinary phenomena of eruption suffice to
account for the formation of the largest known craters. If it is to
be resorted to in any case, it would be, perhaps, in that of the very
small pit-craters, occasionally met with in volcanic districts, such as
the Gour de Tazana, and the lakes Pavin, Du Bouchet, and Serviéres
in Central France. But even these show marks of explosive eruption
in the scoriz sprinkled around their banks. And the occurrence of
even a single scoria is certain proof of some explosions having taken
~ place from a body of liquid lava beneath; though, as I have said,
this may have been accompanied or followed by engulfment. Per-
haps the singular character of the crater of Kilauea, in Owyhee, may
be thought to claim for it an origin in subsidence rather than erup-
tion. It is described as a vast sudden depression in what would
otherwise be almost a level plain, on the side of the gently sloping
volcanic mountain of Mauna Roa. It has an irregularly oval form,
from three to five miles in diameter, and is usually encircled by ver-
tical cliffs some hundred feet high. Its bottom consists of a lake
of lava, on some points (which occasionally change their situation)
in continual ebullition, and at a white heat ; but coated over for the
most part by an indurated crust upon which it is often possible to
walk. Sometimes, however, the incrusted portion is in the centre
of the lake, forming a rough platform, surrounded by a circle of
incandescent and seemingly fused lava,—sometimes the outer circle
forms a solid shelf, within which an imner basin of lava boils at a
greater or less depth below its edge. It is evident, from the inter-
esting story of this crater given by Professor Dana, in the ‘American
Journal of Science,’ as gathered from the relations of various observers
during nearly a century past, that the surface of a vast boiling lake
of subterranean lava existing here, rises and sinks at irregular inter-
vals of several years in duration; sometimes filling the entire cavity,
and even pourimg over its outer margin sheets of a very liquid lava,
—sometimes sinking to a depth of a thousand feet or more,—espe-
cially when some outburst from a lower vent, or chain of vents, has
tapped the internal reservoir. But, however interesting the charac-
teristic features of this crater, both from the facilities it affords for
observation, and the great scale on which they are developed, they do
not seem to me to prove the origin of the cavity other than that of
ordinary craters. The phzenomena of Kilauea are not so exceptional
as; at first view, might be supposed. Visitors who looked down
into the great Vesuvian crater for a few years after its formation in
1822, saw pools of liquid and incandescent lava at its bottom, and
small cones of scorie thrown up by an almost constant ebullition.
The difference in the violence of the explosions, and in the amount of
ejected scorize, arises, no doubt, as Professor Dana very justly ob-
serves, from the difference in the relative liquidity of the lavas,—those
of Kilauea being very liquid, those of Vesuvius much more viscid
and unyielding*. So also during the Vesuvian eruption of 1753,
* Dana, ‘ American Journal,’ 1850, vol. ix. p. 383.

1856. | SCROPE—CRATERS AND LAVAS. 333

persons who ventured to the summit of the cone observed jets of
liquid lava thrown up from the surface of a mass which occupied
the bottom of the crater, and conducted itself exactly in the manner
of a liquid in ebullition. Spallanzani remarked a similar appear-
ance within the great crater of Etna in 1788. In the volcano of
the Isle of Bourbon, Bory de St. Vincent describes a source of very
liquid and glassy lava ceaselessly and somewhat tranquilly boiling
over in concentric waves from the summit of a dome-shaped hillock
composed of its overflowings.

Circular form of Craters.—A consideration which has not, per-
haps, been sufficiently adverted to by geologists speculating on the
origin of volcanic craters, is the cause of their invariably circular or
nearly circular figure. If I am right in attributing their formation
exclusively to aériform explosions, it follows that each is in fact
simply the external orifice of a more or less cylindrical bore drilled
through the pre-existent rocks by repeated discharges of highly ex-
pansive aériform fluids (probably for the most part steam) forcing
their way upwards at some weak point; and that it is to the equal
pressure in all directions of the expanding fluid that the circular
form of the section of this orifice is due,—the same cause, in fact,
which gives a spherical form to a bubble of air or gas rising through
water. Indeed the eruptive explosions must be considered as occa-
sioned by the rise of a succession of enormous bubbles from a great
depth in the fluid lava below. Each single explosion attests the
bursting of such a bubble from the surface of the liquid mass of lava
in the vent. In moderately tranquil eruptions these succeed each
other at. considerable intervals. In the case of Stromboli, I noted
that about five minutes usually occurred between every two explo-
sions. When the eruption assumes a violent character, as in the
Vesuvian one of 1822, the eructations, for such they are, succeed
each other so rapidly as to produce an almost continuous roar, like the
blowing-off of a thousand steam-boilers. And each explosion gives
birth to one of those great globular volumes of white vapour, which,
rolling over and over each other as they rise in the air in a vast
column, occasion one of the most remarkable and magnificent appear-
ances of a paroxysmal volcanic eruption. In the midst of these
clouds of snowy vapour, a black column of stones, scorize, and ashes -
may be seen to shoot up to a vast height, generally attended with
copious discharges of electricity generated by the friction of the
ejected fragments, and forming a singular contrast to the jet of aéri-
form matters.

In some rare cases it is possible to witness the actual rise and
bursting of these great bubbles of vapour. Spallanzani on his visit
to Stromboli in 1780 saw the liquid surface of lava at a white heat
within the orifice of the volcano surge alternately upwards, and after
bursting like a great bubble, fall back again out of sight. In 1819 I
was myself able to witness the same interesting pheenomenon probably
from the same position, a high point of the external crater-rim which
overlooks the vent. At each belch, a shower of tattered fragments
of lava, torn from the surface of the bubble as it broke, rose into the

2a2

— 334 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

air with a cloud of vapour and a fierce roar; while steam seemed to
be at intervals blowing off from another neighbouring vent. Hoffman,
who visited the same volcano a few years later, describes in minute
detail precisely the same pheenomena.

The vast size of some craters, already noticed, may afford a notion
of the enormous volumes of gasiform matter that must have been
discharged through them at the time of their formation by continu-
ous explosions lasting for weeks and even months; since each indi-
vidual bubble of vapour must have been of a magnitude to fill the
entire horizontal section of the crater; and even for some time to aid
in enlarging the area of this aperture by violent pressure against its
rocky sides. The prodigious force with which they ascend, and
therefore the great depth at which they are generated, may be judged
from the vast vertical height, measured in miles, to which they have
been seen to shoot up a continuous columnar fountain of ejections,
consisting not merely of scoriee and ashes, but often of rocky frag-
ments of great size.

These, by their mutual friction, as they alternately fall back and
are thrown up again, become, as already has been said, greatly com-
minuted ; and the source of the explosive vapours having sooner or
later exhausted its energies, the accumulation of these ashes in the
vent at length appears to stifle their further development, and quies-
cence for a time ensues. [I am speaking here, of course, of the case
of such a paroxysmal eruption as I had the advantage of witnessing
in 1822. ]

I have said that every crater is more or less circular in figure ;
but, since the orifice of discharge will almost necessarily be opened on
the least resisting point of some fissure broken through the solid pre-
existing rocks, we might expect its section to be often lengthened in
the direction of this fissure, and consequently to be rather oval
than strictly circular. And this expectation is justified by obser-
vation. Sometimes two orifices have been opened upon the same
fissure so near together that their craters or cones intersect each
other. In the range of Puys of Auvergne and the Velay such
examples are frequent. And in the eruption of 1850 of Vesuvius
two craters were formed on the summit of the cone divided oniy by
a narrow ridge ; their common horizontal axis coinciding with the
line of the great fissure, which in the preceding year had been visibly
broken through the side of the cone towards the north-east. Some-
times aériform explosions take place from openings upon lateral fis-
sures, and produce those minor, or (as they are often called) parasitic
cones, of which several examples occur on the flanks both of Vesuvius
and Etna. At other times, the explosions are confined to the central
vent of the volcano, the lava alone welling out, perhaps, at some
lateral orifice. This, indeed, is the normal character of these phzeno-
mena. And it is this habitual predilection (as it may be called) of
volcanic eruptions for the same identical vent, that occasions in so
many instances the heaping up of some vast mountain mass above
and around it, subject to the occasional blowing up of the central
portion, to be re-formed again and again by subsequent eruptions.

1856. | SCROPE—CRATERS AND LAVAS. 335

The result of the irregular alternation of these paroxysmal explosions
and subsequent gradual expulsions of new matter is the appearance,
so common in volcanic mountains, of a minor and central cone with
its crater, rising within the circumference of some larger crater of
earlier date, or in its immediate vicinity. The walls of the latter
crater are of course often broken down on one or more sides (gene-
rally on the line of the original fissure) ;—perhaps reduced to a mere
segment of its original circuit, by the combined operation of volcanic
convulsions and aqueous erosions. Whoever will take the trouble
to examine carefully an accurate map, on a sufficiently large scale, of

‘almost any volcanic district (such, for example, as Vesuvius and the
Phlegrzean Fields, Etna and the Lipari Isles, the Roman Territory,
the Grecian Archipelago, Madeira, Teneriffe, the Azores, Bourbon,
St. Helena, Barren Island, the Leeward Isles, &c.), will see numerous
unquestionable examples of this law by which crater is formed within
crater, and new cones upon the ruins of old ones.

History of Vesuvius.—At the risk of repetition, I must be per-
mitted to illustrate this law by the trite, but instructive, example of
Vesuvius,—which only comes so often before us because from its
proximity to Naples it has been open to more constant and accurate
observations than any other known volcanic mountain. What, in
brief, is the history of this voleano during the last century? Pre-
cisely one hundred years ago, in the year 1756, Vesuvius possessed
no less than three cones and craters, one within the other, like a
nest of boxes, besides the great encircling crater and cone of Somma
(fig. 1). Sir W. Hamilton gives us a drawing of its appearance in
this state.

Fig. 1.—Outline-sketch of Vesuvius as it existed in 1756.
(After Sir W. Hamilton. )

a Ay w
a Wp ae WY Hit
e { With ne ji! lu
Weg? if

WW py

‘My lv

a. Somma.

By the beginning of the year 1767, the continuance of moderate
eruptions had obliterated the inmost cone and increased the inter-
mediate one, until it very nearly filled the principal crater (fig. 2, a, B).
An eruption in October of that year, 1767, completed the process,
and re-formed the single cone into one continuous slope all round

336 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

from the apex downwards (fig. 2,c). The dotted lines in fig. 2
(after Hamilton) represent the shape of the outer and inner cones
before this eruption, and the space between them and the firm out-
line represents the amount by which the cone was in the intervening

Fig. 2.—Outline-sketch of Vesuvius as it appeared in October 1767;
with dotted outlines of its form in July and in May of the same
year.

ten years augmented in bulk and height by the ejectamenta of that
eruption. An interval of comparative tranquillity followed, until, in
1794, the paroxysmal eruption occurred, described by Breislak, which
completely gutted this cone, then solid, lowered its height, and left
a crater of great size bored through its axis. Later eruptions, espe-
cially that of 1813, not merely filled up this vast cavity with their
products, but once more raised the height of the cone by some hun-
dred feet. When I first saw it in 1819 the top formed a rudely
convex platform, rismg towards the south, where was its highest
point. Several small cones and craters of eruption were in quiet
activity upon this plain, and streams of lava trickled from them
down the outer slopes of the cone. So things went on until October
1822, when the entire heart of the cone was again thrown out by the
formidable explosions I have so often referred to, and a vast crater
was opened through it; while the cone itself was found to have lost
several hundred feet from its top. In fact, nothing but an outer
shell of it was left (fig. 3). Eruptions, however, soon recommenced.
In 1826-7 asmall cone was formed at the bottom of the crater, and,
continuing in activity, had reached a height which rendered it visible
from Naples in 1829, when of course it must have nearly filled up
the crater. In 1830 it was 200 feet higher than the crater’s rim ;
and in 1831 this cavity was completely filled, and the lava-streams
began to flow over it down the outer cone. In the winter of that
year a violent eruption once more emptied the bowels of the moun-
tain, and left a new crater, which soon began to fill again from ejec-
tions upon its floor; and by the month of August 1834 this crater
had been in its turn obliterated, and lava overflowed its edge towards
Ottaiano. In 1839 the cone was again cleared out, and a new crater

1856. | SCROPE—CRATERS AND LAVAS. 337

appeared in the shape of a vast funnel, accessible to its bottom,
which for a few years then remained in a tranquil state. In 1841,
however, a small cone began to form within it, and increased so
rapidly, that in 1845 it was visible from Naples above the brim of

Fig. 3.—Crater of Vesuvius after the Eruption of October 1822.

the crater, which soon after was completely filled. And the cone
from that time went on increasing in bulk and height from the effect
of minor eruptions, until in 1850 one of a violently explosive cha-
racter opened the two deep craters on its summit, of which I have
already spoken. The more recent eruption of May last, being con-
fined chiefly to a prodigious efflux of lava from the outer side of the
cone, unaccompanied by any extraordinary explosive bursts from the
summit, has not altered materially the form impressed upon it in
1850.

It is thus seen that within the last 100 years the cone of Vesuvius
has been five several times gutted by explosive eruptions of a par-
oxysmal character, viz. in 1794, 1822, 1831, 1839, and 1850; and
its central craters formed in this manner as often gradually refilled
with matter, to be again in due time blown into the air. Meanwhile
the old external crater of Somma is itself becoming choked up by
the accumulation of all the lava-streams and fragmentary matter
that are expelled towards the northern and outer side of the cone.
It would be, therefore, in exact accordance with the habit of this
volcano (as of volcanic mountains in general), if, after some further
period either of quiescence or of moderate activity, the entire cone
of Vesuvius should be blown up by a more than ordinarily violent
paroxysm, and the crater of Somma itself reformed.

With this well-authenticated history of the mountain within our
knowledge, would it not be wholly unphilosophical to deny (except
upon such grounds of impossibility as have never been adduced)
that the larger containing crater in the case of Vesuvius (and the
argument applies to other similar volcanic mountains) had the same
origin as the smaller contained ones ; and that the external cones were

338 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

produced in the same manner as the internal, and similarly consti-
tuted ones? And therefore those who refuse to believe the former to
be of eruptive origin must be prepared to extend their incredulity to
the latter. Indeed the elevation-crater theorists usually do not
shrmk from this consequence. With them the cone of Vesuvius,
and that of Monte Nuovo itself, were not the products of eruption,
but of elevatory expansion by a single shock. Obviously, it ought
to follow, that no volcanic mountain was ever in eruption at all, that
the whole is an ocular illusion; at least, that the lava-streams we see
pouring for weeks and months from the summit of a cone and hard-
ening there, and the enormous showers of fragmentary matter which,
during equally long periods, we see thrown up from the crater and
falling on the surface of the cone, do not, even in the lapse of ages,
add to its bulk or tend by their frequent repetition to compose the
substance of a volcanic mountain, but, by some unaccountable pro-
cess, disappear without leaving a trace behind. I own that, to my
mind, such an hypothesis is wholly unintelligible. I see in the
ordinary phenomena of a volcanic mountain, such as I have described
them in the brief regord of the principal eruptions of Vesuvius
during the last century, a simple and natural process by which such
a mountain is gradually built up; and, having observed this mode of
formation going on in some instances before my eyes, I think it
reasonable to apply it to explain the mode of formation of other
mountains of the same class, with their cones and craters, old and
new, central and lateral, or parasitic; and making allowance, as I
said at first, for a certain amount of internal accretion and elevation,
by means of intrusive dykes and earthquake shocks, 1 know nothing
in the appearance, figure, or structure of any volcanic mountain yet
discovered, which such an ordinary and observed mode of formation
will not account for.

Il. The nature of the liquidity of lavas——So much for that
branch of my subject,—the formation of cones and craters. I wish
now to ask attention to some circumstances respecting the mode of
emission and nature of the lavas that proceed from them. I have
already spoken of the comparatively tranquil manner in which some
lava-streams are seen to well out from the flank of a volcano, or its
summit, and the probability that differences in the liquidity or vis-
cosity of the heated matter at the time of its efflux may occasion
corresponding differences in the character of the phenomena. Ob-
servation confirms this expectation ; and it has been remarked, that
the very liquid and vitrified lavas, such as those of Kilauea and
Bourbon, are poured out more or less tranquilly without any very
violent explosions, their imprisoned vapours evidently escaping with
comparative ease, while the more viscous and ultimately stony lavas,
possessing a minor degree of liquidity, and consequently not allowing
so easy a passage to the vapours that rise through, and struggle to
escape from them, are protruded with fiercer explosive bursts, and
the ejection of far greater quantities of scorize and other fragmentary
matters.

This observation, coupled with other reasons to which I shall pre-

1856. | SCROPE—CRATERS AND LAVAS. 339

_ sently advert, led me to an opinion expressed in the works above
referred to, that the ordinary crystalline or granular lavas (making
exception of the vitreous varieties), although at a white heat at the
moment of their emission from a volcanic vent, are not in a state of
complete fusion; that a large proportion, at least, if not all, of the
crystalline or granular particles of which, when cooled and consoli-
dated, they appear composed, are already formed and solid, their
mobility bemg aided by the intimate dissemination through the
mass of a minute but appreciable quantity of some fluid,—in all pro-
bability water,—which is prevented from expanding wholly into
vapour by the pressure to which it is subjected while within the
volcanic vent, or in the interior of the current, until that pressure is
sufficiently reduced to allow of its expansion in bubbles, or its escape
through pores or cracks, by which it passes into the open air from
the surface of the intumescent lava.

I was strengthened in this opinion by several concurrent censi-
derations :—

1. If all lavas are (as they are usually supposed to be) im a state
of complete fusion when they issue from a voicano, how is it that
they do not all present the same glassy texture which is seen in
some, the obsidians, pitchstones, and pumiceous lavas especially, and
in the ropy, cavernous, filamentous basalts of Kilauea, Iceland, and
Bourbon, and which these very crystalline and stony lavas them-
selves put on when melted under the blowpipe or in a furnace? The
usual answer is, that the granular and crystalline texture is acquired
subsequently to emission by slow cooling ; and the experiments of
Gregory Watt and Sir James Hall are cited in support of this
assertion. In the present day, probably the process by which
Messrs. Chance and Co., of Birmingham, devitrify a mass of fused
basalt (from the Rowley rag, near Dudley) by causing it to cool
slowly in an ‘‘annealing furnace,’’ would be considered as a strong
confirmatory fact.

But there is no fact more certain than this, that the superficial
portions, at least, of a lava-current flowing in the open air, do not
cool slowly. On the contrary, they are rapidly, | might say instan-
taneously, upon their exposure, consolidated and cooled down to a
temperature which permits them to be handled and even walked
upon without damage. How is it that this scoriform crust, or the
solid cakes and slabs which so instantly form upon every exposed
surface of lava, nay, even the scorie which are tossed up im a liquid
state by the eruptive jets, and harden while yet in the air before
they fall, exhibit on fracture no glassy texture, but much the same
earthy or stony grain, and occasionally crystals of considerable size
in the solid matter separating their cellular cavities, as is found in
the interior of the current which is known to have cooled very
slowly? How is it that some lava currents are stony throughout,
others vitreous throughout, as, for example, some of the large
pumice-streams of Lipari, Iceland, and the Andes ?

I have recently visited the manufactory of the Messrs. Chance, at
Oldbury, near Birmingham, for the purpose of examining the mode

340 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

in which the basalt used there (and which is the same upon which
Mr. Gregory Watt experimented) conducts itself in their furnaces,
and I found, that when the liquid and fused contents of a furnace at
a white heat is poured out upon a brick or other floor into the open
air, so as to represent a stream of lava flowing out of a volcanic
vent, it consolidates throughout, whatever its bulk, into a homo-
geneous and purely vitreous black obsidian, in fact, an absolute glass,
with a conchoidal fracture and sharp cutting edges. It is only when
made to consolidate very slowly in an oven kept at a high tempera-
ture for some days, that it assumes the deadened and semi-crystalline
texture of the manufactured article.

If this process be interrupted, it is found to have commenced by
the formation, at numerous points within the vitreous mass, of
globular concretions about the size of a small pea, of a lighter colour
than the base, and having a pearly lustre and radiated structure.
The multiplication and confusion of these crystallites or sphzerulites
ultimately destroy the glassy character of the substance altogether,
and give to it a pearly semi-crystalline texture, without, however,
restormg the far more crystallme aspect of the basaltic rock. A
similar change may be often observed to have taken place in nature
among the vitreous lavas, which pass into pearlstone and pitchstone
by the formation of the same kind of sphzerulitic concretions, and of
course there is no question as to the complete state of fusion in which
such lavas have been produced. But there is no trace of such a
process in any of the ordinary earthy, and stony or crystalline and
porphyritic lavas. Iam not aware of a single current from either
Etna or Vesuvius having ever exhibited, even on its most rapidly
cooled surfaces, any passage into true obsidian, or sphzerulitic pearl-
stone, or any portion of such vitrifactions. A pellicle, or glaze, of a
semi-vitreous appearance coats the surface in some parts, or lines
the cellular cavities; but it seems evident that the bulk of the matter
could not have been at the time of its emission in that thoroughly
fused condition which it assumes when melted in a furnace or under
the blowpipe.

2. It struck me that temperature does not alone determine the
fusion or liquefaction of substances ; and that compression may pre-
vent the liquefaction of a solid at a high temperature, just as it pre-
vents the vaporization of a liquid, in the common experiment of
boiling water at a lower temperature in a rarefied atmosphere. If
so, the intense pressure to which heated lava must be subjected be-
fore it rises from the bowels of the earth to discharge itself on the
surface, intensified by the reaction of its own expansive force from
the confining surfaces, might perhaps prevent its complete fusion,
however high the temperature.

3. I had long been impressed by the vast volumes of aqueous and
other elastic vapours evidently discharged from every volcano in
eruption, and to all appearance the chief agents in the expulsion of
lavas from the bowels of the earth. That this vapour is liable to be
developed in every part of the mass of lava is shown by the forma-
tion of vesicles throughout its substance wherever the pressure is so

1856. | SCROPE—CRATERS AND LAVAS. 34]

reduced as to permit their expansion; for instance, in the super-
ficial portions of a current; and in some lava-currents throughout
the entire mass.

The experiments of Mr. Knox, related in a paper read before the
Royal Society in 1824 *, had taught me that water in an appreciable
quantity is mechanically combined with the elementary particles of
all the crystalline rocks of igneous origin. The question, therefore,
arose,— Might not the water thus intimately disseminated through a
mass of crystalline lava, although at an intense temperature, remain
unvaporized, owing to the still greater intensity of the pressure by
which it is confined while yet within the bowels of the earth? and
would it not under these circumstances exert an intense expansive
force upon all the confining molecular or crystalline surfaces between
which it lies, and thus occasion a tendency to separation among these
solid particles whenever the compressing forces were relaxed, or the
temperature increased sufficiently, so as to give a certain degree of
mobility to these particles inter se, and an imperfect liquidity to the
mass composed of them? And, supposing the intumescence thus
occasioned to raise any portion of this semi-liquid matter into the
open air, would not the instantaneous absorption of caloric from the
contiguous particles, that must accompany the vaporization of this
water, and its escape in bubbles or pores and through cracks, owing
to the nearly absolute cessation of pressure, account for the sudden
cooling down and setting, or consolidation, of the exposed surfaces,
without having undergone complete fusion (except in the case of
mere superficial films), notwithstanding their previous intense tem-
perature, amounting even to a white heat ?

This supposition seemed to me to account satisfactorily, not only
for the absence of a vitreous texture even in superficial portions of
many lava-streams, and their imstantaneous consolidation on expo-
sure, in cellular or porous slabs and cakes, but also for several other
characteristics of igneous rocks, not easily to be reconciled with the
idea of their having always issued from the earth in a state of abso-
lute fusion; such, for example, as the cracked and vitrified aspect of
the felspar-crystals of many trachytes, the broken and dislocated
appearance of the leucites, felspars, and other crystals in many
basalts; the frequent arrangement of their longest axes in the direc-
tion of the bed of the rock, that is, of the movement of the lava
when liquefied ; the finer grain often exhibited towards the tail or
extremity of a current than at its source, the brecciated lavas which
appear to have enveloped fragments in great number of the same
material without any fusion even of their finest angles. So also
might be explained the more or less spongy, porous, and loosely
crystalline texture of many trachytes, and their disposition in thick
beds or dome-shaped bosses, attesting their protrusion in a very im-
perfect state of liquidity, more resembling the intumescence of some
kinds of dough in an oven than the fusion of metal in a furnace.

And here let me remark, that Dr. Daubeny, and some other
writers on volcanic phenomena, have spoken of the vesicles or air-

* Phil. Trans. 1825.

)

42 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

bladders in lavas, as being proofs of their having been in a state of
complete fusion. But have the loaves baked in our ovens been in
fusion? The comparison of a cellular scoria with a loaf or a French
roll will show that vesicles of precisely similar appearance to those of
lavas are producible in substances of a pasty consistence, which owe
their liquidity to an aqueous vehicle, the heat applied being only
sufficient to develope the contained gases. Other kinds of baked
cakes are porous rather than cellular, and aptly represent the texture
of the earthy and porous trachytic lavas.

Plutonic rocks.—This theory as to the nature of the liquidity of
many lavas appeared to me so reasonable, that I proceeded to ex-
amine its applicability to the still more generally crystalline plutonic
rocks, from the alteration of which by heat lavas are usually sup-
posed to derive. I asked myself, what would probably be the effect
on a mass of granite, for example, containing water intimately com-
bined with its molecular particles, and confined beneath overlying
rocks and seas, under circumstances of intense compression, and at
the same time high and increasing temperature? Surely a tendency
to intumescence, which, wherever, and in proportion to the extent to
which, it takes place, must elevate and fracture the overlying rocks,
and likewise disintegrate more or less the crystalline particles of the
swelling mass, through the irregularities of their internal movements
and mutual friction. Many of the crevices broken through the
neighbouring rocks would be injected by the intumescent matter.
Some may be sufficiently enlarged to allow of its forcing its way into
the open air as a lava, perhaps accompanied by eructations of the
gases and vapours developed in the lower parts of the mass, or,
should the liquefaction not be sufficient to admit-of the rise of aéri-
form bubbles, as matter of a porous, pasty, or glutinous consistency,
perhaps even semisolid in texture and bulky in form.

It might happen that, circumstances occasioning in turn the pre-
ponderance of the compressing over the expansive forces (by reason,
for example, of a diminution of temperature), portions of the sub-
terranean crystalline mass will, after a partial intumescence of the
kind supposed, return to a state of solidity. The result may bea
more fine-grained rock, owing to the partial disintegration of the
crystals; or, if the disintegration had proceeded sufficiently far, new
mineral combinations might take place. Indeed, Watt long since
proved that the particles of even apparently solid rocks are capable,
through changes in temperature, of internal motion sufficient to
admit their rearrangement according to polarity, that is, of crystal-
lization. Still more likely is this result to occur on the condensation
or escape of any fluid which had previously kept them from contact
with each other, since the crystalline polarity can only exert itself
within minute distances. And thus might be accounted for the fre-
quently observed passages of granite and gneiss into syenite, green-
stone,- trap, or trachyte, and the varieties of mineral composition
which these rocks at times exemplify. So also the transitions from
the larger crystalline grain to the finer, and the dykes and veins
which these rocks so often contain themselves, or intrude into their

1856. | SCROPE—CRATERS AND LAVAS. 343

neighbours. So too the finer grain of the sides, or selvages, of such
dykes might be owing to the greater disintegration of the crystals by
friction along these sides as the matter was driven through them.

Another problematical fact which this theory of an aqueous vehicle
in heated granite would account for, is the usual appearance of the
quartz in this rock, not in crystals, but as a paste or base, seeming
to be moulded upon the crystals of felspar. Had the rock crystal-
lized from a state of fusion, the felspar, bemg far more fusible than
quartz, might have been expected to be the last, not the first, to
crystallize. But if the water disseminated through the rock were
supposed to have taken the quartz into solution by aid of the alkalies
present in the felspar, the fluid vehicle would in fact become a liquid
or gelatinous silicate ; and upon consolidation would naturally mould
itself on the felspar crystals, or appear asa paste to them. I adduced
the hot siliceous springs of Iceland and other volcanic districts as
proofs that heated water under such circumstances could dissolve silex.

Those who will take the trouble to refer to the 2nd, 4th, 5th, and
6th chapters of my ‘ Considerations on Volcanos,’ will see that the
above is a brief summary of the arguments there put forth, perhaps
at too great length, and in a form which may have hindered their
obtaining at the time of their publication the attention which I
believe they merited.

Certain it is, that they were at that time, now thirty years back,
neglected, or generally discredited. I was told that my views were
“‘unchemical.”” I was represented as asserting incandescent lava to
be “cold or thereabouts” *. The igneous and the aqueous origin of
certain rocks had been so hotly contested, and fire and water were
usually considered so antagonistic, that it seemed at first view an
absurdity to imagine that both could be combined in a substance
seemingly in fusion. Probably also the idea was scouted at first
through the notion that water could not be present within an incan-
descent mass of lava without causing it to explode like a mine; which
might of course be the result of any considerable body of water being
localized at one point. But the view I entertained, as has been ex-
plained, was that the water (and to some extent, perhaps, liquefied
gases), to which I attributed much of the liquidity of some lavas, was
disseminated throughout its mass, occupying minute interstices, and
in intimate, though probably mechanical, combination with every
molecule,—indeed intercalated between the plates even of its solid cry-
stals; and moreover that the pressure to which the rock was subjected
while beneath the earth was so enormous as to prevent the vapori-
zation of these minute portions of liquid anywhere except at points
where the intensity of temperature and consequently of expansive
force overcame the resisting forces, and thereby caused either the
formation and rise of great bubbles of vapour from the lower depths
of the subterranean lava-mass, or the inflation of minor bubbles and
pores throughout it, or at least in the superficial portions which by
intumescence were forced into the open air.

Of late, however, views precisely in accordance with the theory

* Westminster Review.

344 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

printed by me in 1824 have been put forward, and have attained
extensive adhesion among continental geologists.

M. Delesse has proved by experiment the solubility of the silex of
rocks in heated water containing either of the mineral alkalies. And,
indeed, the manufacture of artificial stone is now carried on in this
country (Messrs. Ransom’s process) by saturating loose sand with
an artificial hydrate of silica. Huge blocks of flmt, I understand,
are thrown into the hot alkaline water, and melt down like so much
sugar.

seh the experiments of Boutigny have shown that water at a
white heat remains unvaporized, in the form of spheroidal globules,
in which form it is obvious how readily it would communicate
mobility to the solid particles among which it was entangled; and
how (according to these experiments) it might flash into bubbles of
vapour on the reduction of its temperature by exposure to the air.

M. Deville, in his recent observations on the vapours disengaged
from Vesuvius since the eruption of May in last year (for the perusal
of which I am indebted to the kindness of my friend Dr. Daubeny),
arrived at the conclusion, to use his own words, that ‘‘ water in the
proportion occasionally of 999 per mille must have formed an integral
part of the Vesuvian lava at the moment of its emission; and con-
sequently, that in the interior of the incandescent lava there is such
an arrangement of molecules, as to permit the gaseous and volatile
matters to remain there imprisoned, until in the progress of cooling
and consolidation, they evolve themselves.”

Above all, M. Scheerer, of Christiania, the eminent Norwegian
geologist, who is better acquainted perhaps than any other with the
granites of that country, published in 1847 a theory, which, he says,
his observations had suggested to him in 1833, on the production of
granite, entirely identical with that which I had ventured to suggest
in 1824-25. I take the following account of it from the paper read
before the Geological Society of France in 1847, and published in
the fourth volume of the Bulletin de la Soc. Géol., p. 468.

M. Scheerer attributes what he calls the “plasticity’’ of granite
when protruded on or towards the surface of the earth (a condition
evidenced by the veins it throws into the fissures of neighbouring
rocks) to the combined action of water and heat. He describes the
water as “intercalated between the solid atoms of the crystalline and
other constituent minerals, endeavouring to escape by its tendency to
vaporization, and consequent elasticity, but unable to do so owing to
the pressure to which the enclosing mass is subject.” He considers
the water so contained in granite to be “primitive,” that is, one of
the origimal bases of the rock, and not the result of infiltration. He
attributes to it the solution of the quartz, aided by the alkali, and the
consequent moulding of this mineral on the felspar-crystals. He
even goes the length of styling the condition of granite before its
protrusion by the term “une bouillie aqueuse,”’ a granitic broth.

These theoretical opinions of M. Scheerer appear to have received
the assent of M. Elie de Beaumont and other French geologists*.

* See Bulletin de la Soc. Géol. France, new series, vol. iv. p. 1312.

1856. | SCROPE—CRATERS AND LAVAS. 345

Their exact comformity with those which were first developed in my
treatise on Volcanos, published 1824-25, and repeated in the Preface
to my volume on Central France in 1826-27, will be evident to any
one who will take the trouble to refer to those works.

It is not, however, for the vain purpose of claiming a priority in
these views, that I now ask the attention of the Society to them, but
because the subject has not, I think, yet attained the consideration
it deserves from the geologists of this country ; and especially because
of its leading, if followed out, to further inferences of considerable
importance, which were likewise suggested by me in 1825, but have
been hitherto only partially pursued to their legitimate consequences.

Laminated.or schistose rocks, slaty cleavage, and folded rocks.—
I refer to the mechanical changes in the texture and structure
of the plutonic rocks which could not fail to have resulted from the
mutual friction of the component crystalline particles attendant on
their internal movements, whether caused by mere dilatation and
re-compression in place, or by a shifting of the entire mass in any
direction, under intense and opposite, but irregular pressures.

I was led to reflect on this by observation of the ribboned pitch-
stones of Ponza and Ischia, in which, while in a state of vitreous
fusion, crystallites had formed (just like those of the Oldbury ob-
sidian), and subsequently been broken up by the movement of the
semi-liquid mass, and drawn out into long stripes, giving a ribboned
appearance to the rock.

Further examination proved to me that the ribboned trachytes of
Ponza and Ischia, and some ribboned clinkstones, owed that character
to a similar elongation of the felspar crystals and felspathic particles
which they previously contained, in the direction in which the semi-
liquid mass flowed, or rather was forced to move, and in which the
pores or cells, when there are any, are equally elongated. These
observations suggested to my mind the reflection that the solid
particles of any crystallme rock which is put in motion while in a
state of imperfect solidity, and under the influence, of opposing
pressures, must be subject to a great amount of mutual friction or
disturbance, by which their final arrangement when wholly consolli-
dated will be determined.

Thus suppose a mass of granite, of which A B (fig. 4) represents

Fig. 5.

ia
=

l
\»

the section, consisting of crystals of felspar and mica irregularly dis-
posed in a basis of more or less liquefied or gelatinous silex, exposed

346 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

to movement in the direction A B, while under vast pressure both
from above and below, that is in the opposite directions C and D.
Whether the surface, C, or D, or both, remained fixed, or merely
moved, owing to resistances, at a slower rate than the other parts,
the crystals in the latter would be turned round by internal friction,
and rearranged and drawn out in stripes or planes in the direction of
the motion, while the proportionate dimensions of the mass would be
equally varied so as to produce a section something like E, F, G, H
(fig. 5), m fact, a rock which, if no further change occurred in it
except consolidation in place, would have all the characteristics of
gneiss. The same movement, if still further continued, might, it
appeared to me, be expected to disintegrate the angular crystals of
felspar altogether, so as to cause them to disappear, perhaps to force
their elementary molecules to melt into the intensely heated silicate,
to which they would impart their alkalies. And the resulting rock,
supposing the laminz of the mica-crystals to slide readily past each
other, when lubricated by the silicate, and not therefore to be so far
disintegrated as those of felspar (as from their peculiar form might
be expected), would put on a lamellar structure, and very much
resemble mica-schist,—especially since the great flexibility of the mica
would render its laminee extremely liable to yield to the irregularities
of pressure pervading the mass, in a variety of directions, and conse-
quently to take such wavings and contortions as are often exemplified
inthat rock. Whoever will examine the tortuous way in which the
plates of mica envelope and bend round nodules of half-melted quartz
or crystals of garnet in mica-schist, will be convinced, I think, that
the whole mass has been subjected to great internal movement and
consequent friction in the direction of the layers of mica, while under
intense pressure, and in a comparatively softened state, the mica
being lubricated, as it were, by a vehicle of liquid or gelatinous quartz.
Whatever fissures or cracks were formed during this movement m
the semi-solid rock, or subsequently, so long as the silicate remained
unconsolidated, would be necessarily filled by it, and ultimately appear
in the shape of the quartz-veins so frequent in this class of rocks.

Under this supposition gneiss and mica-schist would bear the same
relation to granite as the ribboned trachytes and schistose lavas (clink-
stone) to ordinary crystallized or granular trachyte ; and the quartz-
rocks associated with granite, represent the quartzose trachytes of
Hungary, Ponza, and the Andes.

These views, developed by me in 1825, I cannot but think, deserve
the attention of geologists engaged in investigating the origin of the
so-called ‘‘ plutonic’? and ‘‘metamorphic”’ rocks. It seems to me
more probable that some process of this kind may have metamor-
phosed granite into the laminated rocks of plutonic origin, gneiss,
and mica-schist, than that these rocks should have been formed by
the mere fusion and reconsolidation or crystallization in place of sedi-
mentary strata already laminated, according to the usual ‘ meta-
morphic’? doctrine. I can understand the clay-slates and other
fine-grained schists to have been formed through the mechanical dis-
integration of mica-schist, but not mica-schist by the baking or

1856. | SCROPE—CRATERS AND LAVAS. 347

meltmg and cooling of the clay-slates in place, in the manner sug-
gested by Sir C. Lyell.

In the formation of the clay-slates, perhaps, the action of heat was
not concerned (except as engendering the pressure to which they
have evidently been subjected), but that of water or an aqueous
silicate only. Still in their case also internal movements and mutual
friction of the component particles under extreme and irregular
opposing pressures have, I am convinced, had a primary influence in
occasioning that parallel arrangement of the scaly and flaky mica-
ceous particles to which their slaty cleavage is due. This, at least,
was the conviction forced upon my mind by a close examination of
the fissile clinkstone of the Mont Dor and Mezen, which is used for
roofing-slate, and is in its lamination and cleavage undistinguishable
from many clay-slates. And that opinion I recorded at the time in
my ‘ Considerations on Volcanos *.’

I have since found this view of the origin of slaty cleavage sup-
ported by Mr. Darwin in his work on ‘ Volcanic Islands,’ and by
Mr. Sorby in his paper on slaty cleavage in the Edinburgh Philoso-
phical Journal for 1853. I need not say that such support affords
strong confirmation of its correctness.

Of course we are led to connect the movements under extreme

pressure, to which this peculiar texture of the laminated rocks is here
attributed, with the action of those same forces by which their beds
have been so generally bent and contorted into a series of folds or
wrinkles, more or less at right angles to the general strike.
_ If we seek to discover under what circumstances these flexures
were brought about, we can hardly be wrong in ascribing them to
the same violent process by which they have been elevated, usually
on the flanks of some protruded ridge or enormous dyke of crystal-
line rock, which is seen to form the axis of the mountain-range to
which they belong.

Now what may we suppose to have been the character of this ele-
vatory process ?

The phenomena of active volcanos, and the protrusion of intumes-
cent crystalline matter on so many points of the earth’s surface, and
at all periods of its history, may be admitted to prove the continued
existence beneath a very large area of that surface—if not the whole
—of a mass of intensely heated crystalline matter, having dissemi-
nated throughout its substance (in the manner already dwelt upon)
some fluid or fluids, such as water, affording an imperfect liquidity
to the mass, and, by its intense elastic force, communicating to it a
powerful tendency to expansion. Now suppose any considerable di-
minution to occur locally in the amount of pressure confining this
expansible mass beneath the crust of the globe,—such as might be
brought about by any extraordinary concurrence of the ordinary
barometric, tidal, oceanic, or excavating causes (not to suggest
others),—or, on the other hand, any considerable increase of its ex-
pansive tendency, owing to a local increase of temperature, from some

* See pp. 103, 144, and 202.
VOL. XII.—PART I. 2B

348 PROCEEDINGS OF THE GEOLOGICAL society. [April 23,

unknown, but easily imagined, cause,—we should anticipate, as the
necessary result, the violent fracture and elevation of the overlying
crust of rocks, and the extrusion through some principal fissure, or
line of fracture, of a ridge of the subterranean intumescent crystalline
matter.

It seems very probable that under such circumstances the central
axis of the protruded ridge may retain its irregularly crystalline
grain and structure, but that the portions of crystalline matter that
from either side would rush or be thrust up by pressure from behind
(consisting partly of the weight of the overlying rocks en the semi-
liquid matter below them) towards the opening should be subjected
to so much internal friction of their crystalline particles, and so much
pressure at right angles, or nearly so, to the direction of the move-
ment, as must stretch and draw them out into parallel planes,—
just as happened evidently to the striped and ribboned trachytes in
the protruded dykes of Ponza and Palmarola. ‘This friction and
pressure would be extreme, of course, along the lateral parts of the
protruded mass, that is, the selvages of the great dyke ; which, if the
original mass were granite, would thus appear composed of an axis of
granite, passing on either side into gneiss (or squeezed granite) and
further on into mica-schist. |

But every irregularity, whether on the large or the small scale,
obstructing more or less the even motion of the layers, must create a
waving or contortion in them, especially in the planes of slippery
mica-plates, such as is exemplified even in hand-specimens of the
Ponza trachytes, and also on the largest scale in the same locality.
And the extreme irregularities of motion, occasioned on the upper
layers of the intumescent mass by the pressure and resistance of the
overlying beds, may be expected to carry their wavings still further,
and at the throat of the fissure where the squeeze and jam of the
protruded matters must be at its maximum, to occasion those enor-
mous and repeated zigzag foldings of the laminated beds, so fre-
quently observed in mica- and chlorite-schists in such positions.

Meantime another influence would be similarly affecting the over-
lying stratified rocks above, or on the outer flanks of the elevated
axis, namely their own specific gravity, urging them to slide or slip
laterally when tilted up at (perhaps) a considerable angle on either
side. The more compact and indurated strata would be partly frac-
tured into cliffy masses, partly broken up into breccias and_conglo-
merates by this movement; but the softer beds, especially those
which were saturated with water (perhaps even yet under the sea), or
which contained interstratified beds of silt, shale, or clay, permeated
with water, would glide laterally away from the axis in extensive
land-slips, and be wrinkled up into vast foldmgs under the intense

" pressure compounded of their own weight, and that perhaps of por-

tions of the protruded matter thrust against them,—in a manner very
similar to the contortions produced in the more crystalline laminated
rocks by the violent squeeze which accompanied ¢heir protrusion.
It may even be difficult to draw a line between the effects of these
two replicating and fracturing forces. But, together, they seem to

1856. | SCROPE—CRATERS AND LAVAS. 349

me sufficient to account for most of the phenomena of the kind ob-
servable in mountain-chains.

These were the ideas on this subject which I endeavoured to de-
velope, though very imperfectly I am aware, in the more theoretic
portion of my work on volcanos, so often referred to, and they were
illustrated by a rude ideal section of an elevated mountain-chain in
the frontispiece to the volume. I still think they will be found a not
improbable solution of this the greatest problem in the dynamics of
geology. It appears to me, that the results would be much the
same, whether we suppose this elevatory action to have been paroxys-
mal and simultaneous, or gradual, taking place by minor and success-
ive expansive throes or shocks, or even still more slowly in the man-
ner of a creep, as Sir Charles Lyell would probably conceive it to
have operated, and to be still continuing. On these last assumptions,
the earthquake-shocks which certainly accompany at present every
effort of elevation, and appear to be propagated in waves through the
substance of the earth’s crust, in directions usually at right angles to
the principal axes of elevation, or fissures of crystalline protrusion,
may indicate the force by which the extreme replications and slaty
cleavage of the laminated beds are occasioned.

I would ask of geologists to consider whether such a mode of pro-
trusion of the laminated crystalline rocks and of the lateral replica-
tion of the more earthy schists and marine strata, as is here suggested,
does not accord with the general facts known respecting their posi-
tion? Let me take two descriptions of the general position of the
crystalline rocks from two writers of experience, judgement, and
wholly impartial character, as respects the theory here indicated.
Mr. Evan Hopkins* gives as the results of his extensive mining ex-
perience in the Andes and elsewhere, “that the great base [of all
mountain-chains| is below more or less granitic, strongly saturated
with mineral waters, and that this passes upwards by insensible gra-
dations from a crystalline homogeneous compound into a laminated
rock, such as gneiss, and still higher up into schists in vertical planes ;
the peculiar varieties of the higher rocks depending on the mineral
character of the ‘parent rock’ below; the schistose rocks forming,
in short, the external terminations of the great universal crystalline
base,”—that is to say (as I would phrase it), the squeezed out, and
therefore laminated, upper and lateral portions of the inferior cry-
stalline mass.

Mr. Ruskin, in his recently published volume, having closely ex-
amined the structure of the Alps with the eye of a geologist no less
than of a painter, but certainly without any theory to support, de-
clares that the central axes of “irregular crystallines”’ (as he calls
the granitic rocks) uniformly graduate on either side into the foliated
or “‘slaty crystallines,”’ 7. e. into gneiss and ultimately mica- and
chlorite-schists.

One point observed in the structure of the Alps and many other

-* Quart. Journ. Geol. Soc. vol. xi. p. 144.
2B2

390 PROCEEDINGS OF THE GEOLOGICAL society. [May 7,

mountain-chains I may notice before I conclude, namely the occa-
sional dip of the elevated strata towards the central axis of extruded
crystalline rock, producing a synclinal, instead of an anticlinal, ridge.
Another section copied loosely in the frontispiece to my work on
voleanos, from Von Buch’s paper on the Tyrol, may show the mode
in which I conceive this to have occurred through the injection of a
mass of crystalline matter into a wedge-shaped fissure, opening down-
wards; such as must have frequently occurred among the fractures
of the overlying strata—giving occasion in some cases to the further
rise of the heated and intumescent matter into the hollow between
the outer slopes of the synclinal valley. It would indeed accord with
the theory suggested above, if such dykes or extravasations at syn-
clinal axes were found to alternate frequently with the elevated anti-
clinal axes, for the cracks formed in indurated beds of overlying rock
would very frequently open alternately upwards and downwards*.

Time will not. allow of my dwelling now upon other points expla-
natory of geological problems, which are afforded by the theory of
an expansive subterranean crystalline mass preserved by external
pressure in a more or less solid condition beneath the crust of the
globe, but always ready to expand and perhaps to intumesce upwards
on any relaxation occurring in the overlying pressure. But I sug-
gest it now, as I did thirty years since, as the solution most recon-
cileable with the known facts of the structure and relative position of
the great elevated rock-formations of the globe, and as a theory
founded, not upon mere guess-work, but on careful and extended ob-
servation of the phzenomena of both active and extinct volcanos, and

the disposition of volcanic products of all ages.

May 7, 1856.
The following communications were read :—

1. On some Footmarks in the MitusroneE Grit of TINTWISTLE,
Cuesuire. By E. W. Binney, Esq., F.G.S.

Some years since a series of strange impressions was found in one
of the lower beds of Millstone Grit in a quarry belonging to James
Rhodes, Esq., at Rhodes Wood, near Tintwistle, m Mottram-en-
Longdendale, Cheshire. Mr. Rhodes was much struck with the
impressions, from the fact of two of them bearing some resemblance
to the mark of a human foot; and the workmen employed in the
quarry, when they first showed him the impressions, remarked,
“‘ Master, somebody has been here before us.” During several
weeks the quarry was visited by many hundreds of people from
Glossop and the surrounding neighbourhood. The common opinion
was that the impressions were the footprints of some of Noah’s

* See the diagram at p. 205 of ‘ Volcanos.’

Quart. Journ. Geol. Soc. vol. xu. to face page 350.

StncE the above paper was in print my attention has been called to
a translation, m our Journal for February 1848, of the essay of
Prof. C. F. Naumann, “On the probable eruptive origin of several
kinds of gneiss, &c.,’’ i which views very similar to those here en-
tertained are given, in relation to the laminated and fissile structure
of the crystalline plutonic rocks,—reference being there made to my
observations on the 7rachytes of Ponza and Palmarola, and the
Phonolites generally, as illustrating the mode of formation of gneiss
and mica-schist, and leading to the inference that these rocks owe
their structural parallelism rather to pressure and friction accom-
panying their eruptive protrusion, than to the effect of metamorphic
action upon sedimentary strata. I rejoice to find my early views on
the subject supported by such high authority, and trust that other
geologists of weight and influence may thereby be induced to give
them their unbiassed consideration.

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1856. | BINNEY—FOOT-TRACKS AT TINTWISTLE. 3501

family. This was founded on the supposition that the ark had
rested on the high hills above Woodhead. Other parties, who would
not so readily admit of this change of all previously received ideas
as to the resting-place of the Ark, contended that they were the
footprints of people who had lived before the flood. These opinions
are introduced for the purpose of showing how great was the re-
semblance of some of the specimens to the impressions of a human
foot, in the eyes of ordinary people.

_ The writer of this notice went over to Tintwistle, and examined
the impressions as they lay in the rock, and before they had been at
all disturbed. At that time there were five marks visible, and the
commencement and termination of the track could not be perceived,
owing to the circumstance of its commencing near some old workings,
and proceeding up into the hill-side where the rock had not been
excavated ; so there were in all probability many more impressions,
if the track could have been followed in either direction. However,
only one series was met with; and, from the effect their discovery
produced on the workmen, it appears pretty certain that none had
been met with there for some time.

As previously stated, the quarry is in the lowest part of the Mill-
stone Grit; certainly 1000 feet down in that deposit, and very near
to the Limestone Shale. The strata dipped towards 80° west of
south at an angle of 12°. Ata depth of about 25 feet in the quarry
which is situate on the hill-side opposite to that on which runs the
Manchester and Sheffield Railway, a series of five casts taken from
as many moulds was met with. ‘They all lay in a straight line, and
nearly on the rise and dip of the strata.

The mould or impression on the western side (No. 1 in the draw-
ing*) was nearly oval in shape, turned a little towards the north ;
the two next (Nos. 2 and 3) somewhat resembled in form marks
made on very wet sand by a human foot with a shoe on; and the
two on the eastern side (Nos. 4 and 5) resembled No. 1, with the
exception of being rather more circular than that one.

The long impressions did not part with their casts in the stone so
well as the oval and circular ones; consequently they are not so
clean and sharp; indeed part of the cast still remains in them, the
stone having broken. In all, the wet sand of the matrix appears to
have partly run into the mould before the cast was taken, and they
have more the appearance of having been made under water than on
an exposed sandy beach.

No two of the impressions were exactly alike in shape; but the
bulk of the wet sand which had been displaced out of the holes was
the same in each instance, whether the impressions were deep and
short, or shallow and long; and the sand removed was forced up on
the western side, and on that side only, of every impression ; it being
in the former thrown a little more to the south than in the latter ;
just as if the force acting on the soft matrix had in each instance

* This drawing, made to scale, is deposited in the Society’s library. It re-

presents three of the impressions, now in the Museum of the Manchester Society,
and one (No. 1) not preserved.

352 PROCEEDINGS OF THE GEOLOGICAL society. [May 7,

been pressed down at certainly two, if not more, distinct times; at
the first projecting the sand further towards the west than the sub-
sequent force, which did not send the sand more than one half the
way over that first discharged ; so that the surface of the stone now
shows two terraces,—just what we might expect to see, if one portion
of a semi-fluid mass had been displaced, and then another portion
poured partly over it.

The distances between the impressions, from the middle of one to
the middle of the next, measured 2 feet 104 inches in every instance.
Nos. 2 and 3, those most resembling human footmarks, were each
13 inches in length at the bottom, and 17 inches at the top; their
breadth being respectively 4 and 33 inches at the bottom, and 8 and
9 inches at the top; their depth bemg about 3 inches*. In these
two impressions, as before observed, the cast has not come clean
out of the mould, but left a little of it in; so the depth is not easy
to obtain. The bottom of the impressions was concave, so far as
they can be seen; and in two of them there were marks of something
resembling claws or nails visible.

Nos. 1, 4, and 5 (the last of which is not figured, but resembled
exactly its neighbour, No. 4) were about the same size, and measured
6 by 8 inches at the bottom, and 10 by 12 inches at the top; their
depths bemg about 5 inches each. The bottom parts of these im-
pressions are concave, and their casts have come cleaner out of the
moulds than the longer ones have done.

No portion of the sandstone-rock (which is a coarse grit contain-
ing white quartz-pebbles, sometimes nearly an inch in diameter) nor
the beds of shale, either above or below it, afford any evidence what-
ever of sun-cracks. This is the case, so far as the writer has examined,
with the whole of the great Lancashire Coal-field, comprising arena-
ceous and argillaceous beds to the thickness of 6600 feet, although
he has met with numerous instances of such markings in the sand-
stone beds of the Trias at Lymm, and at Weston Point near Runcorn,
where the tracks of the Labyrinthodon and Rhynchosaurus are found.
The English Coal-measures up to the present time have not afforded
evidence of sun-cracks ; but Sir Charles Lyell has noticed them in
the Carboniferous strata of the United States at Greensburg? ; so it
is probable they will be ultimately met with in this country as well.

How have the impressions above described been produced? At
the time of their discovery it was safely concluded that they had been
made by some force acting upon the sandstone before it was consoli-
dated, and when it had existed in a soft or semi-fluid state; and that
such force had in each case acted twice, so as to displace two portions
of wet sand at two different, but not long distant, periods. The
straight line of the track, and the regular distances between the
impressions led many persons to believe that they had been made by

* The measurements are difficult to make correctly; for the surface of the
matrix has evidently shrunk near the sides of the impressions, and some of the
wet sand gone into them.

+ Manual of Elementary Geology, 3rd edition, p. 337.

1856. ] BINNEY—FOOT-TRACKS AT TINTWISTLE. 353

an animal, but whether a biped or a quadruped no one ventured to
decide. This opinion was maintained, notwithstanding the varying
characters of the markings. One gentleman suggested that a tree
with a projecting stump, carried by short waves towards a sandy
beach, might cause such appearances by allowing the stump to touch
the wet sand each time it came into the trough of the wave. This
hypothesis would no doubt account for the regular distances of the
impressions, and the sand having all been pushed out on one side ;
but it would not account for the two distinct projections of sand:
besides, there is this objection,—waves so short as the distances be-
tween the impressions are not now very commonly met with.
By the liberality of Mr. Rhodes, the impressions Nos. 1, 2, and 3
are now in the museum of the Manchester Geological Society. On
seeing these last year, Sir Charles Lyell expressed himself much in-
terested in them, and it was at his instance and request that this
sketch was written, the writer having some years since given an ac-
count of the specimens for a local print. Lately, Mr. Waterhouse
Hawkins has examined the specimens, and he is strongly inclined to
believe that the impressions are the track of an immense Chelonian
Reptile, resembling the Chelichnus gigas, figured by Sir William
Jardine in Plate I. of his ‘Ichnology of Annandale,’ or the C. Titan
which the same author alludes to, but does not figure. This opinion
is further borne out by the varying character of the impressions, and
it accounts for the pushing out of the wet sand at two successive
times, namely first on the planting of the fore-foot of the animal, and
then of the hind foot in the same or nearly the same place, and for
the similar quantity of wet sand displaced and thrown back in each in-
stance. In tracks of Batrachian Reptiles, like those of the Labyrintho-
don of the Trias, the impressions are nearly in a straight line, and the
mark of the small fore-foot is not always seen, even when the impres-
sions have been taken in a fine stiff red clay, resting on a fine sand,
and partly hardened by the sun. In the impressions described in this
paper there is a probability that they were made on soft sand under
water, for the sides of the matrix have given way and partially run
into the moulds in a manner such as we scarcely ever see now in foot-
prints made by animals on a sandy beach. Under these conditions,
we could hardly expect to find a distinct fore-foot mark, even if the
track were that of a Labyrinthodon, which it resembles in its straight
direction more than that of a Chelichnus. But no animal of the genus
Labyrinthodon appears to have pushed out the wet sand behind, in
the same way that the Tintwistle fossils show. The Chelichnus
shows this protrusion ; therefore it is more probable that the impres-
sions under consideration were made by an animal of the last-named
genus, or one allied to it. The distance (in breadth) between the
hind and fore foot-marks, which is certainly greater than that seen
in the tracks of the Labyrinthodon, may have disappeared by the
two impressions being nearly opposite to each other, having run
together and formed one wide hole, as in specimens Nos. 1, 4, and
5; whilst in specimens Nos. 2 and 3, the hind foot came nearly in
the same place as, or only just behind, the impression of the fore foot,

354 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 7,

and thus caused the long and shallow mark. A heavy slow-walking
animal, like a Tortoise, with an irregular gait, on wet sand, it is pro-
bable may have caused the track. This creature must have been of
immense size, even larger than the Chelichnus Titan of Sir William
Jardine, and for a provisional name I would propose to call it
Chelichnus ingens.

Before concluding, I may add that Mr. Rhodes, the proprietor of
the quarry where the specimens were found, not only presented the
original slab to the museum of the Manchester Geological Society,
but he took a plaster-cast of them, which he is desirous of presenting
to some public institution.

2. On the Lignitre Deposits of Bovey Tracey, DEVONSHIRE.
By Dr. J. G. Croker.

[Communicated by the President. |
(Abstract.

Tue author first described the physical features of the basin, sur-
rounding the junction of the Teign and Bovey Rivers, in which these
beds of lignite and their associated clays (used in pottery) are found.
The lignite-beds come to the surface at Bovey Heath towards the
north-western margin of the basin; they underlie towards the south-
east about 11 inches in the fathom, and are covered by clays and
gravels ; their vertical thickness is about 100 feet. In the upper
portion of the lignitic series are several (five and more) beds of
loose lignite, covered and mixed with variously-coloured clays and
granitic detritus ; a ferruginous sandy clay, 9 feet thick, succeeds,
which is followed downwards by ten beds of “ good coal ” or lignite,
separated by bluish clay-beds, and worked for fuel.

Fir-cones, referable to the Scotch fir (Pinus sylvestris), have been
found in one of the uppermost iayers of loose lignite. Large flabel-
liform leaves also are represented by fragments 2 feet long and
20 inches wide in some of the higher beds, together with tangled
masses of vegetable remains. In the second and fourth beds of good
coal (the latter about 80 feet from the surface) the lignite abounds
with the little seeds lately described as Folliculites minutulus by
Dr. Hooker in the Society’s Quarterly Journal*. The lignite gene-
rally is composed of compressed coniferous wood, and retin-asphalte
is locally abundant.

The Bovey Basin is about 60 feet above the sea-level, and was
almost a swamp until it was drained within the last ninety years.
A peat-deposit, in which fir-timber is found, covers the lignites to-
wards the south.

The author also referred to the extensive denudation that the
district has undergone, and pointed to the Dartmoor granitic tract as
the source of the clays of the lignitic deposits. He also noticed the

* vol. xi. p. 566.

1856. | BUNBURY—DRAINED MERE. 355

several writers * who have treated of the lignites and the geology of
the neighbourhood. Lastly, Dr. Croker supplied some notes on the
local occurrence of the numerous varieties of rocks and minerals in
the vicinity of the Teign, such as ores of lead, manganese, and iron,
also labradorite, schorle, &c., all of which, as well as the lignite and
its vegetable remains, were illustrated by a large series of specimens.

3. Notice of some appearances observed on DRAINING a MERE
near WretTHAM Hari, Norroux. By Cuaruss J. F. Bun-
BuRY, Esq., F.R.S., F.G.S.

WretHam Hatt, the seat of Wyrley Birch, Esq., is situated about
six miles north of Thetford, in that extensive tract of open sandy
plains which occupies much of the south-western part of Norfolk
and of the north-western part of Suffolk; a tract which may be
called upland in comparison with the fens, but of very moderate ele-
vation above the sea-level, as is shown by the slow course of the
streams flowing from it. About Wretham there are several meres,
or small natural sheets of water, without any outlet. The one to
_which my attention was particularly called by Mr. Birch occupied
about forty-eight acres, and was situated in a slight natural depres-
sion, the ground sloping gently to it from all sides. The water has
been drawn off by machinery, for the purpose of making use, as
manure, of the black peaty mud which formed the bottom. This
black mud, which is in parts above 20 feet deep, is nothing else
than a soft, rotten, unconsolidated peat; or perhaps it should be
described as vegetable matter in a more complete state of decom-
position than ordinary peat, showing no distinct trace of vegetable
structure. At the depth of about 15 feet, in this peat, occurs a
distinct horizontal layer, from 2 to 6 inches thick in various parts,
of compressed but undecayed moss, unmixed with any other sub-
stance. The stems and leaves of the moss, though closely matted
together, are easily separable, and are in so good a state of preser-
vation as to show their distinctive characters very clearly under the
microscope. All that I have examined belong to one species,—
Hypnum fluitans ; a moss by no means uncommon in watery bogs
and fenny pools throughout the British Islands, and often growing
in dense masses in shallow water. The layer that I speak of is of
considerable extent, although apparently not extending over the
whole area of the mere, as there are parts in which the whole thick-
ness of the black mud has been penetrated without finding it.
While wet and fresh, it is of a bright rusty red colour, turning to a
yellow brown when dry. What is remarkable, I think, in this case,
is the occurrence of a distinct bed of moss, perfect and undecayed,
beneath 15 feet of mud, in which no trace of moss is to be seen.

* See Phil. Trans. vol. li. p. 534 ; Parkinson’s ‘ Organic Remains,’ vol.i. pp. 112,
126; Trans. Geol. Soc. 2 ser. vol. vi. p. 439 ; and De la Beche’s ‘ Report on the
Geology of Devon,’ &c., p. 143.

356 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 7,

Numerous horns of Red Deer have been found in the peaty mud,
generally (as I was informed) at 5 or 6 feet below the surface,
seldom deeper; many attached to the skull, others separate, and
with the appearance of having been shed naturally. What is most
remarkable, several of those which were found with the skulls at-
tached had been sawn off just above the brow antlers,—not broken,
but cut off clean and smoothly, evidently by human agency. Some
of these horns are of large size, measuring 9 inches round imme-
diately below the brow antler.

The black peaty mud (which is of the same quality beneath as

above the layer of moss) rests on a bed of light grey sandy marl,
which effervesces briskly with acids. This is the lowest stratum
that has been reached, owing to the difficulty of keeping out the
water. I could find no trace of shells, nor learn that any had. been
found, either in the peat or the marl. Wood is found in the peat,
though not in great quantity : we found some pieces, apparently of
birch, and saw a trunk of considerable size, I believe of an oak,
which had lately been dug out. The wood of this is of a dark brown
colour, and was in a very soft and almost pasty condition when fresh
and wet, but when dry becomes tolerably hard. Its tissues, at least
the woody fibre and medullary rays, appear to be in good preserva-
tion; but, as is usually the case with wood under similar circum-
stances, it has become too opake to be easily examined under the
microscope.
_ The peat shows appearances of bedding, and thin horizontal
layers or seams of white sand may be observed in it here and there,
but are seldom continuous for more than a very few feet, often only
for a few inches. Stones are also found singly imbedded in it in
various places, without any sort of order; partly irregular flints,
partly rolled and rounded pebbles of quartz, exactly as in the gravel
of the country.

Numerous posts of oak-wood, shaped and pointed by human art,
were found standing erect, entirely buried in the peat.

It would appear, from the facts I have stated, that a great part of
the thickness of peaty mud overlying the bed of moss must have
been accumulated before the time when the Red Deer became extinct
in this part of England; and consequently, that the age of the bed
of moss must be some centuries at least. Dr. Lindley, in his cele-
brated experiment* on the destructibility of different plants by im-
mersion in water, found that the very few kinds of Mosses which
were subjected to his experiment decomposed rapidly ; and he in-
ferred, that the extreme rarity of this family of plants im a fossil
state was owing to their perishable nature. The fact observed at
Wretham, however, seems to show that (as might have been sus-
pected) the aquatic Mosses are not rapidly destroyed by exposure
to moisture ; aud I think we must seek some other explanation for
the almost universal absence of the Musci from the strata deposited
in former geological periods.

* See Fossil Flora of Great Britain, vol. iii. p. 4.

1856. | DICK—CLEVELAND IRON-ORE. aay,

4, Analysis of the CLEVELAND [Ron-ORE * from Eston.
By A. Dick, Esq., Metailurgical Laboratory, School of Mines.

[Communicated by Dr. Percy, F.G.S.]
THE ore was weighed after drying at 100° C.

PiGrOxtGe Of ATOM: . 4. . ss. eee es ae 39°92
eee TOL SOU. oe ee a ks aha ae ae 3°60
Proroxide of mancanese........2-4.+. O95
AUT a er engi Bk ie irey oe tes eee 7°86
LETS, Geis UR eS ee eos Pes 7°44
LLANE Sits Aiea, eM degre a ial le le 3°82
Reis eee yet, s = aa 5s = Epa Ame bac 0°27
oP LOL Cech eee eee ereree & 22°85
Phosphoric acid . tole ea
Silica, soluble in hydrochloric acid .... 7:12
STU UES 2 2 A ener trace
Bisulphide of iron (iron-pyrites) ...... O°11
Waterim combination. . ..:........... 2°97
IRSA GE MIGHUCT Oh G6: cine ix 6 ois: ois: «Sige ay « trace

Residue, insoluble in hydrochloric acid... 1°64

100°41

Composition of the residue insoluble in hydrochloric acid :

Silica, soluble in dilute caustic potash, con-
sisting chiefly of oolitic concretions.... 0°98

Silica, insoluble in dilute caustic potash .. 0°52

Alumina with a trace of peroxide of iron.. 0°10

Titanic acid; about Pe en ie 0:03
LASTED Sea, Qi es ire NS ag A i la trace
1°63

_ The ore contains no metal precipitable by sulphuretted hydrogen
from the hydrochloric acid solution.

In the residue insoluble in hydrochloric acid, minute, bright, black
crystals were detected, which were proved to contain titanium, and
were supposed to be anatase. Prof. Miller of Cambridge has ‘been
able to measure certain of the angles, and found them to be identical
with similar angles of anatase. The discovery of this mineral in the
Cleveland ore is at least a point of considerable mineralogical in-
terest, and may possibly furnish some additional indication of the
nature of the rock from which it was derived.

The silica in the insoluble residue exists, it will have been ob-
served, in two states, about two-thirds being soluble in dilute caustic
potash, and one-third insoluble in that solvent. The rounded white

* See also the ‘ Memoirs of the Geological Survey,’ 1856, p.95. This iron-ore
is derived from the Marlstone or Middle Lias series of the Cleveland district in
the north-eastern portion of Yorkshire. See also a notice of this ironstone by
Mr. Crowder ; Edinb. New Phil. Journ. new ser. vol. iii. no. 2. April 1856, p. 286.

398 PROCEEDINGS OF THE GEOLOGICAL Society. | May 7,

particles, which, according to Bowerbank, have a truly oolitic or con-
conn concretionary structure, are entirely formed of the soluble
silica.

The silica which existed in the hydrochloric acid solution was that
which was present in a state of combination in the ore, probably
with both protoxide and peroxide of iron; and the peculiar greenish-
grey colour of the ore was doubtless due to the presence of this
silicate of the mixed oxides of iron, just as the colour of the green
particles in the so-called greensand is believed to be due to the like
cause.

The proportion of phosphoric acid in the ore is comparatively
large, and may be easily accounted for by the fossiliferous character
of the ore. The quality of the iron smelted from this ore would cer-
tainly be very sensibly affected by the proportion of phosphorus, and
probably also by the silica existing in a state of combination.

5. On the Occurrence of Coau near the City of E-u in Cuina.
By the Rev. R. H. Cossoxp.

[Forwarded from the Foreign Office by order of the Earl of Clarendon. ]

On Monday, December 17, we left the city of E-u, and, after walk-
ing a few miles, met every hundred yards with men bearing coals.
On inquiring of them where the coals were obtained, they pointed
to some hills in front of us, called the “ Coal Hills.’’ As the mines
were said to be but a short way off our road, we determined to visit
them. About a mile off the main road the work of the miners was
very evident, and rude straw huts, dotted about on the sides of the
hills, showed both where the pits were, and: the residences for the
workmen. Two of the nearest pits were visited, and I was sorry
that Ihad not seen the working of coal in England, that I might have
been able to make, in various particulars, a better comparison, and
so give a clearer account. The pits were from 300 to 500 feet deep.
The descent was made by about ten storeys (in the first we visited) ;
so that only 40 or 50 feet were descended at once ; and then a fresh
platform, with a fresh windlass reaching another 50 feet ; and so on
to the last : from each platform galleries were cut, about 6 feet wide,
following of course the vein of coal. The workmen did not descend
by the basket, as I believe is usual at home, but climbed down the
pit by means of beams let into the sides. The mouth of the pit
was about 6 feet by 4, and this seemed to be the dimensions all the
way ‘down. The descent was thus very easily and very safely
effected, the men swinging themselves from one side to the other, as
if they were going down some huge chimney. About forty men
were at work in each pit, besides those engaged in sorting and pack-
ing the coal on the surface. ‘The coal was very bright, but it was
not bituminous.

The price at the pit’s mouth varied from 200 to 500 “cash” for a
_ burden of 130 catties, which gives 1°62 to 4 dollars per ton ( English).

1856.] MOORE—SILURIAN ROCKS OF WIGTOWNSHIRE. 3959

The best seemed of a very good quality, and considerable care was
taken in its packing.

Those who open pits have to pay a certain rate to Government.

The nearest place of any importance to these pits is the city of
F-u, a place without walls, though a third-class city, in the prefecture
of King-hua, from which it is distant by water 120 leagues, or forty
English miles. After even moderate rains, there would be plenty of
water for boats of a large size; we were there after a long season
of drought, when probably no boat could have borne a freight of more
than 1000 catties, or somewhat more than an English ton. From
King-hua water-carriage is direct by Lau-ke, Yeu-chow, and Foo-
gang to Hangehow, about two days’ journey. [King-hua is situated
in lat. 29° 15’ N., long. 119° 46’ E. |

Ningpo, 14 Jan. 1856.

May 28, 1856.
The following communications were read :—

1. On the SiLur1AN Rocks of WicGTownsuHIRE.
By J. C. Moors, Ksq., F.G.S.

THE objects of the following communication are—lst, to point out a
remarkable arrangement in the rocks which form the Peninsula
between the Mull of Galloway and Corswall Point* ; and

2ndly, To show the relative positions of the Graptolitic Schists
of Wigtownshire to the coarse Conglomerate and Limestones of
Ayrshire.

I. In a paper which I had the honour to read before the Society
in 1849, the principal object of which was to give an account of the
Limestones on the Stinchar and their fossils, I stated that the rocks
from the Corswall Lighthouse for a great distance to the south have
in the main a southerly dip; but that, after passing to the south of
Port Patrick, the dip is found to be reversed, that is, to the north.
Visits since made at different periods to these coasts have enabled me
to add to my acquaintance with the arrangement of these rocks, and
I find them to obey a certain law. From the Corswall Point, which
consists of a coarse conglomerate of blocks of granite, &c., to within
six or eight miles of the Mull of Galloway the rocks are bent into a
series of anticlinal and synclinal folds, which are thrown over to the
N., the axes of the curves dipping south. The shorter side is often
quite vertical, while the longer is inclined at varying angles, often not
more than 30°, and in some cases less. The crown of the arch may
sometimes be found still subsisting, but in many more cases it has
disappeared from denuding causes; still its former existence can be
inferred thus:—for some hundred yards the rock will consist of
vertical beds, which as we proceed to the south gradually begin to

* For sketch-map and sections of this district see also Quart. Journ. Geol.
Soc. vol. v. p. 12, &e.

360

Fig. 1.—Section from Corswall Point to the Mull of Galloway. Length about 30 miles.

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PROCEEDINGS OF THE GEOLOGICAL SocIETY. [May 28,

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1856.| MOORE—SILURIAN

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362 PROCEEDINGS OF THE GEOLOGICAL society. [May 28,

have a southerly dip ; advancing further in the same direction, they
fall to a lower and lower angle, until they reach their minimum eleva-
tion; the next rock we come to is suddenly vertical, and so continues
for a space, when it again gradually subsides to a low angle which
again is succeeded by vertical beds. This arrangement prevails for at
least twenty-five miles, during all which distance, although northerly
dips do occur (and in one instance for near 200 yards), yet they are
quite insignificant in comparison with those to the south, and are
never at such low angles. See fig. 1.

Without fatiguing the Society with too many details, I will state
briefly that good examples of this structure may be seen along the
coast from Airies to Cairnbrock, and thence to Galdenoch. Between
the two last-mentioned places occur some very fine instances of flags
bent so sharply that the two planes are almost parallel, while no
fracture is to be perceived at the angle, and both limbs of the syn-
clinal dip southward. From Galdenoch by Larbrax to the Knock,
the rocks have always a southerly dip, when not vertical, and the
synclinals are sometimes seen with both legs dipping south. North
of Killantringan Bay the rocks dip north for about 200 yards, being
almost a solitary exception. They then recover their southern dip,
and continue so until near the Dunskey Glen, where they are verti-
cal. We then pass another anticlinal, and, approaching Port Patrick,
the rocks fall down to a low angle, dipping south. Immediately
south of Port Patrick, the rock is again vertical, and the beds from
which Port Patrick Harbour was built are then seen to form a magni-
ficent arch, of which the northern limb is vertical, and the southern
gradually dips away to the south, and so sometimes past the old
castle of Dunskey to the Morroch Bay, where again the rocks are
vertical. From thence by Cairngarrock to Port Float, great masses
of intrusive plutonic rock interfere, but a prevalence of south dip
may still be traced among the stratified rocks. Further south in the
parish of Kirkmaiden the same arrangement subsists, but with an
opposite direction, the axes of the folds always dipping north. About
a mile to the north of the Grennan, where slate is quarried, the
rocks begin to dip pretty persistently to the north; and from thence
to the Mull of Galloway, the rocks are either inclined to the north
or vertical.

I do not pretend to have entered in my note-book all the folds
of the rocks for a distance of thirty miles: to get the materials for
such a section would require an amount of labour which I have not
had opportunities of bestowing upon it. Sometimes the flexures are
very numerous, for in parts which I have studied in detail, as for
instance from the granite of Dunman to the Mull of Galloway, as
many as fifteen occur in five miles. Still there is no part of this coast
which I have not visited, and I feel satisfied that this view of the
structure is rigidly true. The section (fig. 2) from the Grennan to
the Mull of Galloway, a distance of six miles, is pretty accurate, no
fold of importance being omitted ; it will there be seen that the rock
dips constantly north, or is vertical, with two trifling exceptions,
where the rock dips south at an angle of about 80°; but these form

1856.| MOORE—SILURIAN ROCKS OF WIGTOWNSHIRE. 363

no exception to the rule that the axis of the curves bends to the
north.

If, now, we cross over to the east side of the Bay of Luce, we shall
find confirmations of the same structure. From Port William to the
Burrow Head, the rock is seen to dip north; then it is perpendi-
cular ; and after three magnificent undulations, of which the northern
sides are the longest, it plunges perpendicularly into the sea.

Returning to Port William, which is about the parallel of the
Grennan Rocks, where the change of dip is seen on the western
side of the bay, we find that here also as we go north the dip is
reversed ; and from thence to Glen Luce, the rock is either vertical
or dips south. From thence to the Cairn, the section, being inland,
is too much concealed to give any results; and I would remark that
all these observations are drawn solely from coast-sections; as in
those only where the base is washed by the sea can the rocks be
followed uninterruptedly for any distance. Whenever we leave the
coast, the rock, particularly when inclined at low angles, is so covered
by drift that no conclusions can be arrived at. Omitting therefore
everything until we reach the Cairn (fig. 3), we there find the slates
vertical ; about a quarter of a mile to the north they are seen dipping
south at an angle of about 30°; from thence to Glen App they are bent
into three or four sharp folds, always dippmg south; on the north
side of Glen App they are seen for the last time highly inclined, but
still with a south dip; and from thence set im a series of flaggy beds
which also dip south, or are vertical, until we reach the coarse con-
glomerate, with blocks of granite and porphyry, which is the conti-
nuation of the beds of conglomerate at Corswall Point, from which
we set out. The beds cannot be pursued much farther, since at the
Correrie Burn the rock changes its character ; and from thence to the
Stinchar consists solely of porphyry, greenstone, and amygdaloid.

The structure I have described is similar to those inversions of
rock in the north of Germany, in the Ardennes, and the Eifel, and
to that of the Appalachian chain in the United States. It has never
yet been observed in this country on so considerable a scale; and
what is very remarkable, if my view be correct, it does not obtain in
the parts of the chain to the eastward. There, according to the
published sections of Prof. Harkness, Prof. Nicol, and Sir Roderick
Murchison, the lowest rocks form an anticlinal of the normal cha-
racter, with the newer beds on their flanks dippmg away from the
older: whereas in Wigtownshire, as I shall presently show, these
Graptolitic schists in the centre of the section are older than the con-
glomerate to the north, on which they appear to repose. It is also
observable, that where the change in the dip of the axes of the curves
takes place, there is no such change of circumstances as to hint at
the cause. In the parallel cases quoted above there is always present
some great mass of granite, gneiss, or crystalline schist, which appears
by its forcible intrusion to have occasioned the inversion of the masses
on its flank. Here nothing of the kind is observable: the hills pre-
serve the same heights with little variation: there is no unusual ap-

VOL. XII.—PART I. 2C

364 PROCEEDINGS OF THE GEOLOGICAL society. [May 28,

pearance of violence or dislocation. It is true that a mass of granite
(Dunman) is intruded near that quarter, and that the bearing of that
granite towards the granite of Cairnsmuir in Kirkeudbrightshire is
nearly in the line of strike of the stratified rocks. But the granite of
Cairnsmuir is nearly thirty miles distant from that of Dunman; and
this last does not occur at the point of change of dip, but about two
miles to the south of it. Moreover there are many reasons which
show that all the principal movements which these Silurian rocks have
undergone had been impressed upon them previously to the intru-
sion of the granites, which have deranged the E.N.E. strike of the
rocks—not occasioned it. Lastly, it seems to me that the intrusion
of a small wedge of rock, not two miles thick, is wholly inadequate
to account for a displacement which is felt for a distance of more
than thirty miles.

II. I now come to the question of the relative ages of the Grapto-
litie schists of Wigtownshire and of the coarse conglomerates of the
south of Ayrshire. :

There can be no doubt that the slate and anthracitic schists of
Selkirkshire and Peebleshire* are the equivalents of similar rocks
seen along the western coast of Wigtownshire; and also that the
Wrae limestone with its associated conglomerates is the counterpart
of the limestones and conglomerates of the south of Ayrshire. And
as Prof. Nicol, in a section laid before the British Association in
1852, distinctly places the Wrae limestone above the Graptolitic
slates of Grieston, the question may appear to be determined. Still,
as the two sections appear to be contradictory, the whole country for
many miles to the south of the Stinchar appearing, as above described,
to lean on that to the north, it may be worth while to attempt to
reconcile them.

Beginning about three miles southof the Corswall Lighthouse(fig. 4),
at the point marked ‘ Burn-foot’ in the Ordnance Map, near Dally
Bay, we find thick-bedded grit overlying red shales and black shales,
which are in all respects similar to the shales of the Cairn on Loch
Ryan, and contain the same Graptolites: all these rocks dip south at
a high angle. As we proceed north, the thick-bedded grit is again
met with, traversed by a band of porphyry, and apparently forming
a sharp synclinal, with both legs dipping south. Next to them, to
the north, the red and black shales fill up all the space to the middle
of Dally Bay: they are vertical, or have a slight dip to the south.
The rock then becomes almost amorphous, with scarcely a trace of
bedding; but is of the same fine-grained material as the black
shales. This amorphous rock forms the north side of Dally Bay; still
further north the black shales, covered by red flags, and these last by
a thick-bedded grit, again appear, dipping north. It is clear that
we have passed an anticlinal, and the amorphous rock is doubtless
the dark shale, which, being in the centre, has suffered enormous

* See Papers by Prof. Nicol, Prof. Harkness, and Sir R. Murchison: Quart.

Journ. Geol. Soc., vol. iv. p. 204; vol. vii. p. 46 & p. 139; vol. viii. p. 393;
vol. xi. p. 468; and vol. xii. p. 238.

1856.] MOORE—SILURIAN ROCKS OF WIGTOWNSHIRE. 365

pressure by the folding, and so has preserved no vestiges of strati-
fication.

The beds then decline to a low angle, becoming almost horizontal,
still showimg red shales covered by thick-bedded grit, until at the
north side of Port Naughan Bay they resume their south dip at an
angle of about 15°. At the south side of Garvillan Bay the red flags
dip S.E. at an angle of 60°, and a little farther north, the rock under-
lyimg these red flags loses all traces of bedding ;—again suggesting
that we have arrived at an anticlinal folding. Accordingly a little
farther north, near the Genock Rocks, vertical red flags are seen, with
thick-bedded grit to the north of them. These continue to a point
a little south of the Ox, where the first bed of coarse conglomerate
occurs, and from thence to the Corswall Lighthouse the rocks con-
sist of repetitions of red flags, grit, and conglomerate, all vertical or
nearly so. Where the conglomerate first occurs, it is almost in-
distinguishable from the grit: it is, in fact, a grit of the same kind
of sand, but containing here and there a block of granite or felspar-
porphyry from 1 to 2 feet in diameter.

Farther north, near the Lighthouse, the rock is mainly composed
of these blocks, some of them of very large dimensions. I have
measured one of 63 feet in its greatest diameter.

If we take the section along the eastern shore of Loch Ryan, and
examine it carefully, we shall come to the same results. The coarse
conglomerate is found on the Ayrshire shore near the Finnart Point,
and from thence to the Cairn the Graptolitic schists appear to lean
against it: but I believe the following to be the true interpretation. At
the Cairn the schists are vertical ; a quarter of a mile to the north they
are seen dipping at an angle of about 30° to the south; from thence
to Glen App they are bent into three or four folds which all dip
south: at the south side of Glen App they are still seen, containing
the Graptolites and dipping south at an angle of about 45°. From
thence to the north side of the bay all rock has been washed away :
but at the north side the slates are seen again vertical, and some
highly contorted flaggy beds immediately to the north of them. I
infer therefore that Glen App is the site of an anticlinal arch, and
that the valley has been scooped out along a line where the fracturing
of the rocks has facilitated their removal by denudation. From
thence to the conglomerate at Finnart Pomt the Graptolitic schists
never re-appear ; but the rocks consist of flaggy beds similar to those
which intervene between the conglomerate and schists first described
along the Irish Sea. From both of these sections, therefore, I con-
clude that the coarse conglomerate is superior to the schists with
Graptolites.

With respect to the rocks from thence to the Mull of Galloway, I
would only state briefly that the red and buff shales near the Mull
of Galloway are lithologically very like those next to the coarse con-
glomerate at the Corswall Point; that the bluish slates of the Gren-
nan, and perhaps also the dark anthracitic shales of Morroch Bay,
containing Graptolites, are probably repetitions of the blue flags of
the Cairn; and lastly, that certain dark gritty beds, consisting of

2c2

366 PROCEEDINGS OF THE GEOLOGICAL society. [May 28,

grains of dark sand, white quartz, and fragments of slate which pre-
vail in the neighbourhood of Port Patrick, are probably the lowest
exhibited.

2. On the Action of OcEAN-CURRENTS in the Formation of the
STRATA of the Kartu. By C. Bassacs, Esq., F.R.S.

[Communicated by W. H. Fitton, M.D., F.R.S., F.G.S.]
(Abstract.)

In the year 1834 the author communicated to the Society a paper
on the Temple of Serapis, at Puzzuoli, near Naples, in the concluding
portion of which paper* he suggested an explanation of the fact that
certain portions of the earth’s surface are subject to periodical alter-
nations of elevation and depression, extending through vast periods
of time: and the extreme slowness with which certain very fine powders
of a heavy substance (emery) subside in water, suggested to the
author the vast extent to which very finely divided matter suspended
by the Gulf Stream might be spread over the bottom of the Atlantic,
—a subject alluded to by him in 1832 in the ‘ Economy of Manu-
facturest.’

Some years afterwards, looking for better explanations of the phe- )

nomena of outliers and the folding and inversion of strata than he
had hitherto met with, Mr. Babbage reverted to the consideration of
sedimentary deposition. Hence the origin of the present communi-
cation.

In the first part of this paper the author traced out the laws
which regulate the distribution of very finely divided earthy matter,
borne outwards from river-mouths and sea-cliffs into the ocean-cur-
rents, over extensive areas. The time that a particle of matter
requires to fall through a given distance im a resisting medium
depends—

Ist. On the specific gravity of the particle itself.

2nd. On its greater or less magnitude.

3rd. On its form.

Ath. On the law of the resistance of the medium through which

it falls.

These several points were treated of by the author, who then pro-
ceeded to show under what conditions certain finely triturated sub-
stances, of given size and composition, suspended in a current of a
given velocity, would be deposited in a sea of a given depth.

Supposing a river to send out, suspended in its water, particles of

triturated limestone, of different degrees of fineness, and the river at
its junction with the sea to be 100 feet deep, and the sea to have a
uniform depth of 1000 feet over a great extent, the different results
in the deposition of the several varieties of the suspended particles

* Proc. Geol. Soc. vol. ii. p. 75 ; and Quart. Journ. Geol. Soc. vol. iii. p. 206, &c.
t+ Art. 63, 4th edit.

1856. | BABBAGE—OCEAN-CURRENTS. 367
are shown in the following table, in which four varieties of sediment,
falling respectively through 10, 8, 5, and 4 feet of water per hour,
are laid down :—

Greatest di-

: Nearest di-
wo. tip, [mecatae | TGgeshot |e
Bat iamkecee: Miles. Miles. Miles.
1 10 180 20 200
| 2 8 225 25 250
ba 5 360 40 400
4 4 450 50 590

Thus four separate deposits will be found at various distances from
their common origin.

The author noticed also how the uniformity of a stratum might be
interfered with by the varying conditions both of the sediment and
of the sea-bottom. Altered relations between the specific gravity,
the shape, and the size of the particles, when duly adjusted, render
ocean-currents capable of either separating mixed substances, or of
combining together different substances. Hence endless combina-
tions arising from the variation of these conditions.

Local elevations and depressions of the sea-bed, on which sediment
brought from a distance is deposited, were pointed out as probable
causes of irregularities in stratified deposits,—giving origin, indeed,
to outliers or disconnected masses, which might be sometimes sup-
posed to have been due to subsequent denudation.

Sedimentary matter carried by ocean-currents to the profound
depths of the ocean subside into these depths beyond the reach both
of currents and of wave-action. The downward motion becomes
continually diminished, and the particles ultimately come to absolute
rest, or move through water of increasing density with excessive slow-
ness, so as to cover the ocean-bottom with an incoherent pulpy mass
of fluid mud, of great thickness, and less dense for the most part in
the upper than in the lower part,—or to form a similar mass of sedi-
ment suspended in mid-water.

It was also pointed out that in the immense peviod) of time during
which this sediment is subsiding into the profound ocean-depths and
massing itself into a mud-bed, various hydrographical changes might
take place and cause new currents to bring different sediments over
the same area, which newer deposits might descend into and be
mingled with the older precipitates.

The author proceeded to treat of the effects of an alteration of
isothermal surfaces, caused by the interference of this more or less
suspended mud-cloud with the conduction of heat from the earth’s
surface. Consolidation of the lower strata would be caused by the
isothermal surfaces below the ocean rising upwards. Currents of
heated water, similarly caused, might variously disturb the sediment
and give it flexuous stratification. Heated water might be retained

368 PROCEEDINGS OF THE GEOLOGICAL society. [May 28,

in portions of the sedimentary masses, and alter by its solvent power
the constituent materials; or the heated water might be converted
into steam, or generate permanent gases, which might derange or
alter the suspended material in various ways. If the sediment had
not reached the bottom, but formed a freely suspended mud-cloud
in mid-ocean, the effect of the interposed bed of fluid mud impeding
the upward progress of heat from the lower region would be neces-
sarily to increase the heat of the water below the mud, and thus
place the sediment between the upward pressure of the heated water
and the downward pressure of the overlying water. The ocean above
would cease to derive its usual supply of heat from below, and be-
come climatally altered. The now consolidated mud-bed would of
its own weight either sink bodily down, and take different positions
according to its consistency and the form of the ocean-bottom, or it
would be contorted and broken through from the effect of the aceu-
mulated heat below. In tracing the results of this upward pressure
and bursting, the author observed that on the enormously thick and
partially consolidated stratified mass one or more weak points would
admit of the formation of elevated domes, and that from the burst-
ing of one of these domes, in a sea of much greater length than
breadth, a vast wave would be propagated through the plastic matter,
which would advance and be followed by others less perhaps in de-
gree. As the original wave advanced, the diminishing depth of the
ocean would cause the head of the wave to advance with greater
speed than its base, impeded by friction on the ocean-floor, and give
it its advancing form and a steeper declivity in front than on its hind
side ; this might be carried so far that the foremost wave might even
double itself over, and yet, owing to the plasticity of the mass, there
might be no breach of continuity. To the transmission of such im-
pulses through semi-consolidated strata, the author refers for an ex-
planation of the overlapping and inversion of strata seen in the Ap-
palachian and other mountain-ranges.

The paper concluded with remarks on the indications of the age,
and causes influencing the structure of deposits, such as cleavage,
&c., m connexion with the foregoing observations on sedimentary
formations, and as illustrating, with them, some of the consequences
of several physical causes which act through vast intervals of time
upon the strata forming the crust of the earth.

1856. | PLANT—UPPER KEUPER SANDSTONE. 369

JUNE 4, 1856.

Ernest P. Wilkins, Esq., was elected a Fellow.
The following communications were read :-—

1. On the Upper* Kevurrer Sanpstone (included in the New
Rep Marts) and its Fosstus at Leicester. By James
Puant, Esq.

[Communicated by J. W. Salter, Esq., F.G.S.]

Bens of Keuper sandstone were first ascertained to exist in this lo-
cality by my brother, Mr. John Plant, in 1849; they were then found
in the cuttings of a short branch line made to connect the Leicester
and Swanington Railway with the Midland Railway.

At the time that several short hills on the line were excavated, an
opportunity occurred for selecting specimens of the superficial casts
and markings, together with the cololitic remains of Annelida, from
the thin shaly beds of grey marls and sandstones which were abun-
dantly exposed to view ; thus a large collection was got together, and
specimens were distributed to the museums of the metropolis and to
others in the country. A notice of their occurrence was also read at
the Meeting of the British Association in that year at Birmingham.

The finishing of the railway debarred a satisfactory examination in
that direction ; but as the strike and dip of the beds had been ex-
posed in the cuttings, it was not difficult to follow them along a low
and narrow ridge for about two miles in a north-east direction, and
one and a half mile to the west, until lost under a part of the town.

It is from the excavations in the immediate vicinity, and under
the town itself, that additional knowledge of the beds forming the
Keuper has been gained ; while many interesting discoveries of their
organic contents, such as Crustaceans, Teeth, Bones, Plants, and a
Foot-mark, have been made in the strata traversed by well-shafts,
which have been recently sunk to a depth of 75 feet.

The development of the Keuper sandstone on the north and west
sides of the town varies from one mile to a mile and a quarter in
width at the surface; the strata cropping out at intervals,—at the
Castle Mount, Danett’s Hall, Dane Hill, and at several knolls on
both sides of the Braunstone Turnpike Road; generally they are
hidden under clays and marls of the alluvium and drift. The dip of
the beds is to the east, at an average angle of 3°, and they soon dis-

* T have reasons for concluding, from lithological characters and from the
position of the strata, that there are two distinct beds of Sandstone, an Upper and
Lower, included in the New Red Marls, and separated from each other by a con-
siderable thickness of red clay; the lower bed lying at about the same distance
horizontally and vertically from the ‘‘ water-stones,” as the upper does from the
base of the Lias. I may probably have a further notice upon this point when my
examination is more matured. It is the upper sandstone alone that the present
notice describes.—July, 1856. J.P.

370 | PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4,

appear under the deep beds of gypsiferous clays and marls of the
Spinney and Knighton Hills.

The sandstone agrees very closely with the same formation in
Gloucestershire and Warwickshire, as described by Murchison and
Strickland in their memoir*,—even to the “pink tinge and small
fragments of decomposed felspar,’’ as mentioned at pages 334, 335
of that memoir. The Keuper sandstone is described by them as
consisting, in detail, of the following members :—

a. Finely laminated, flag-like, marly sandstone, of delicees
greenish and light-drab colours, alternating with marls,
20 to 30 feet.

6. Thick-bedded, finely laminated, soft, siliceous sandstone, of
various colours, the prevailing one being a white or pinkish-
white, with occasional tints of green, purple, &c., 15 to
30 feet.”

ce. Finely laminated, flag-like sandstone, similar to a.

At the boring in the vicinity of the Old Roman Wall these flag-
like marly sandstones were penetrated, and it was difficult to decide
whether it was the upper or lower member, until during the progress
of the boring the Red Clay was reached, which at once decided it to
belong to the latter ; the boring was carefully measured and gave
the following results :—

Feet.

Drift and gravels .... Pht Oe eS
Thin, flag-lke, marly sandstone........ 35
Wotalideptho.' 122s Sok Paes

These marly sandstones rarely exceed 4 inches in thickness, vary-
ing from that to half an inch ; generally they are 1 inch laminations,
and are separated by way-boards of green marl of unequal thickness
(in this respect resembling the same beds at Inkberrow, Shrewley -
Common, and other localities in Gloucestershire and Worcestershire).
Their surfaces are so entirely covered with impressions and markings
as to be quite irregular and rough. The commonest markings are
broad unequal ripple-marks,—and small nodules and granular casts in
relief, which usually are considered as rain-markings ; together with
most abundant remains of Annelid-markings; there also occurred a
single well-formed footstep, 4 ches in diameter, in form similar to
the well-known Labyrinthodont footmarks of Storeton in Cheshire.
The surfaces of these shales are crossed in all directions by cracks,
which had subsequently been filled in with a fine white sand.

At the railway-cutting (at a distance of about two miles in a straight:
line from the well), in excavating for ballast, for which the thick
beds (the middle member) are admirably suited, they have recently
penetrated these thin flag-like sandstones to a depth of about 2 feet ;
the following section (fig. 1) will illustrate this :—

* Transact. Geol. Soc. 2nd series, vol. v. p..331.

1856. | PLANT +-UPPER KEUPER SANDSTONE. 371

Fig. 1.—Section of the Keuper Sandstone on the North-east side of
the Railway-cutting at Shoulder of Mutton Hill, near Leicester.

Ky
oe

3. Drift, with boulders of Syenite, &c.: § to 10 feet thick.

2. Soft white sandstone, ‘‘ Middle beds: ’’ 14 to 16 feet.

*, Black carbonaceous band, with supposed Alye.

1. Thin marly sandstones, ‘‘ Bottom beds :’’ exposed to the depth of about 2 feet.
Average dip about 5° to the South.

This shows the middle member from 14 to 16 feet thick. It con-
tains numerous fragments of pure coal, no doubt from the Ashby
field. On the top are alluvial deposits, containmg remains of Deer
and Ox, with nuts, leaves, and vegetable debris; and Drift-clay with
granitic boulders and detached and worn fossils from the Qolitic,
Liassic, and Carboniferous formations. Where the upper surface of
the thick soft beds is exposed by the removal of the drift, it is found
to be very irregular and grooved, and is much harder than the mass
of the beds (which can be rubbed into sand with the fingers), and
seems to contain lime, which has agglutinated the particles of silex
strongly together,—forming, in fact, a kind of hard skin, thus pre-
serving the soft sandstone below. The upper member I consider to
have been here entirely denuded ; and its debris has assisted in form-
ing the numerous sand-beds found so abundantly along the river-
valley. The accompanying section (fig. 2, p. 372) from the Red Clay,
on the west, to the Lias, on the east, will serve to illustrate this.

In support of this view, I may mention that I have taken many
specimens of the thin sandy shales containing the Annelid-markings
in the sand- and gravel-pits, at a depth of 15 feet from the surface.
They are slightly rounded and worn, and mingled with rolled Oolitic
and Liassic fossils. It is obvious that these worn specimens could
not have been derived from the lower member of the Keuper Sand-
stone; as that would require the whole of the middle member—the
thick beds—to have been swept away. ‘They can only be considered
as the remnants of the upper thin sandy shales; the whole of which
appears to have been denuded in this locality ; and, from the scored
and worn character of its upper surface where exposed, a great por-
tion of the middle member (possibly to the extent of one-half of its
original thickness) was probably at the same time removed : in that
case, it would bring up the thickness of the middle portion to the
standard of the similar member in the Keuper Sandstone of Glou-
cestershire and Worcestershire.

372 PROCEEDINGS OF THE GEOLOGICAL society. [June 4,

Fig. 2.—Section across the River-valley at Leicester.
Length about 5 miles.

Se Se
oo: Ss.
- mS ;
Le 2 iden me
re i me gus le
eS © EPS aig =
me r= at On wigs)
as 3 ae =a "DO
ae BS SS ere
6
ey ANN 5
AAU
ASS LA 4

——— —— ea aE mh

—

(Ze

- Gravels and clays, with bones, boulders, &c.
Lias.

| Wpperimarls yc)... seem ce alee

. Upper sandstone- shales SH OONDOODS |
- Middle sandstone (‘‘ soft beds ’’)..

. Lower sandstone-shales..........
a(Peedielayerd s.ciccieoeys tiie aeiee et Ginete

-Upper Keuper.

mw Do ON

[ Note. In this section the Marls No. 5 are not represented suffi-
ciently thick, whilst Nos. 4 & 6 are proportionally too thick. |

Combining the data afforded by sections south and north of the
river-valley, the followimg table will show the position and extent of
the Upper Keuper beds, from the base of the Lias to the Red Clay
in descending order :—

Lias.

a. Upper Keuper marls, containing beds of gypsum and
- [ several thin bands of green marly sandstone, on which
5, are found numerous pseudomorphic salt-crystals ;
5 thickness from 80 to 120 feet.
= 6. Thin sandy shales, with way-boards of green marl;
2 25 to 30 feet.
©, | ce. Thick soft beds of white sandstone, 20 to 30 feet.
- | d. Thin sandy shales, similar to 6; 35 feet.

Total about 200 feet.

Red clay.

It is considered that on the north and north-west side of the river-
valley, the whole of the beds a & 6 (5 & 4 of the Section, fig. 2),
and part of c, have been denuded, and a large accumulation of drift-
clay, gravel, and alluvium deposited on the thick soft beds (and pro-
bably, where that is entirely denuded, on the lower shales, d) to the
thickness in some places of from 60 to 80 feet.

Most of the fossils contained in the following list were collected
from the well-boring in the town, excepting one very fine detached
tooth, which was found in the thick beds at the railway-cutting.

1856. | PLANT—UPPER KEUPER SANDSTONE. | 373

Plante.

Casts of Echinostachys oblongus and Equisete, and remains of
Voltzia.

I am inclined to think, from the impressions left on the overlying
bed of sandstone, that the jet-black deposit intercalated in the thick
beds (middle member) contains the remains of d/ge.

Annelida.
Cololitic remains of Amnelids, and casts of their tubes.

Crustacea.

Listheria minuta* ; found both in the green marls and the thin
sandy shales.

Pisces.

Teeth of Placoid Fishes +; widely scattered through the strata ;
the surfaces are marked with three grooves aud the anterior edges
finely serrated.

Ichthyodorulites ¢, of a curved and slender form; these are but
rarely found perfect ; their existence is often to be traced in an inta-
glio impression, stained with a dark red oxide of iron, or by a cavity
from which the organic form has perished, leaving only the mould
and external markings impressed on the sandstone. The longest
spine measures 10 inches, decreasing from a diameter of three-quarters
of an inch to one-eighth.

One of the best specimens is deposited in the Museum in Jermyn
Street, another in the Town Museum at Leicester (the ribbed surface
is very sharp and distinct upon this specimen) : these both show the
fibrous structure of the interior and the socket-like hollows which
run through their entire length.

On the surface of some of the shales nodules are frequently found,
which from their appearance are most probably the casts and re-
mains of Fish-coprolites.

Fragments of bone have also been found m one of the beds of
marly sandstone, about 2 inches thick; the largest fragment is
5 inches in length, and nearly an inch in diameter ; it is coloured
by a light red oxide of iron ; the centre of this specimen is filled up
with a fine sand, but the hollow may prove to be the effect of crush-
ing forces having brought the edges of the bone together, as it seems
greatly distorted and broken. Another fragment of bone is firmly
cemented to an Ichthyodorulite.

* This is the little Triassic shell that has been termed Postdonomya and Posi-
donia minuta. In Morris’s ‘ Catalogue of British Fossils,’ 2nd edit. 1854, it is
included in the Crustacea (as Estheria minuta); but (apparently from inadvert-
ence) it has not been expunged from the list of Molluscs in that work. Mr.
Rupert Jones having informed me that, from a microscopical examination of this
little fossil, he had been enabled to determine its real Crustacean character, I
have on his authority entered it here as a Crustacean.—July, 1856. J. P.

+ According to Sir P. Egerton, to whom I sent a selection of the teeth, they
resemble those of the genus Strophodus ; but may possibly be of a new gerus.

~ Probably belonging to the same species as the teeth.

374 PROCEEDINGS OF THE GEOLOGICAL society. [June 4,

2. On the Upper Kevurrer SANDSTONE (included in the New Rep
Mart) of WarwicksHire. By the Rev. P. B. Broniz,
M.A., PiG.8. : .

Havre lately obtained some slabs with Posidonia (Hstheria) mi-
nuta * from the Keuper Sandstone near Warwick, and these being
finer specimens than are usually procured, I thought a few of them
might be acceptable to the Society.

The Keuper formation of Warwickshire has been already so ably
described by Sir R. I. Murchison and Mr. H. E. Strickland +, that
I have but little to add respecting it. The slabs with Posidonia
occur plentifully along the banks of the canal near Shrewley, in
green marls and sandstone, a few feet above the inferior red marl ;
but the specimens are best preserved in the sandstone. The old
quarries on Shrewley Common, now enclosed, are entirely stopped
up ; but a partial excavation near the canal last summer afforded
numerous Ichthyodorulites of various sizes, and probably belonging
to an undescribed species of fish, the small palatal teeth of which
are the same as those which had been previously noticed by my
friend Mr. Symonds and myself at Pendock, in Worcestershire, and
which Sir P. Egerton considered to be referable probably to a new
genus {. Portions of long, thin, slender bones were also discovered,
and one of some size, but too imperfect to be determined. I have
also in my cabinet a cranial bone of a Labyrinthodon from Shrewley.
A few small teeth and scales of fish occur in the soft gritty bed in
No. 2 of the Section given below.

Most of the blocks of sandstone are strongly ripple-marked, a
prevailing character with this portion of the Keuper in Warwickshire,
Worcestershire, and Gloucestershire. On some slabs I found the
footsteps of a small Batrachian ; and, though I carefully instructed
the workmen to preserve all markings on the stone, few were
brought me which could be traced to any organic origin. The
Ichthyodorulites are met with both in the sandstones Nos. 2 and 6,
chiefly in the former, and in the gritty sandstone intercalated with
it. The palatal teeth of Acrodus, with small teeth and scales, ap-

pear to be confined to the gritty sandstone.

The following is a section of these strata on the banks of the

‘Canal at Shrewley, in descending order :—

eooreen: Marl oo ie see ee eee eee 0 3or4
2. Beds of grey and light-coloured fine-grained

sandstone, divided by marl; with Poszdonia

minuta, and ripple-marks. In the middle

occurs a coarse gritty sandstone with white

: specks (less coarse than at Pendock in

Worcestershire),which contains bones, teeth,
ald ‘Spimem Oo. Aerodis ee ee

* See Appendix, p. 376. t+ Trans. Geol. Soc. 2nd Ser. vol. v. p. 331.
+ See Quart. Journ. Geol. Soc. vol. xi. p. 451. Sir P. Egerton thinks that it
is possibly the same as that figured in Trans. Geol. Soc. 2nd ser. vol. v. pl. 28. fig. 3.

Or

1856. | BRODIE—UPPER KEUPER SANDSTONE. 37

Ete) im
pemee ON Earl et 2 oe a0 RE Ue Smet eee Je 0 24
4. More finely grained sandstone, more or less
ripple-marked ; with footsteps of Ladbyrin-
thodon ER er os eee a
MRC ar ly os. tists sa ae ae tess grote O82

Oo or

. Hard workable sandstone (‘bottom bed’’),
the only good building-stone of the locality;
with imperfect casts of Posidonia........ 3. 6
. Thin beds of sandstone, divided by green
marls; with remains of plants (Volézia,
Calamites?, and Fucoides’). This is best
Seen at Nowlns Ons FIs8 A LOS:0
8. Red Marl.
Beds horizontal.

“SI

The last 10 or 15 feet of sandstone and marl reposing immediately
on the red marl are not quarried here; but at Rowington, on the
Canal-bank, about a mile and a half to the west, these are better
seen; and from them I have procured a small series of imperfect
remains of Plants, some of which appear to belong to Voltzia and
Calamites?, and some small Fruits not easily determimed. Fucoids
(or markings such as are usually referred to Fucoids) occur in more
or less abundance throughout, especially in the marls.

The Warwickshire Keuper agrees both lithologically and zoologi-
cally with that of Worcestershire. In Mr. Symonds’s paper * on
that formation at Pendock, it will be seen that the green marls are
thicker and more indurated, and the gritty sandstone, which he calls
““osseous conglomerate,” is a much finer band at Shrewley, and with
fewer traces of bones and teeth, and no particles of carbonaceous
matter (which often struck me when examining the quarry at Pen-
dock), although identical with it im every other respect. The plant-
beds at the bottom also seem to be similar to those at Rowington.

The New Red Sandstone group in England is on the whole, as is
well known, by no means rich in organic remains ; if the beds for-
merly classed as “ Bunter’’ are correctly assigned to the Permian,
we have only the Keuper to afford us any insight into the paleeonto-
logical history of that period, and the fossils are neither numerous
nor well preserved. It is singular too, that the little Posidonia
should be the only shell + at present known in strata of such extent
and thickness as the Trias,—and the more so, as there seems no
reason why the sea should not have been tenanted by other contem-
porary forms of Mollusks equally suitable to the same conditions
of marine life. The prevalence of peroxide of iron in the overlying
and underlying red marls may account for the absence or extreme

* Quart. Journ. Geol. Soc. vol. xi. p. 450.

+ Since the above was in type, Mr. Symonds has shown me a little shell
which he had detected in the Keuper at Pendock, quite distinct from the Posi-
donia; and I have an imperfect cast of what appears to be another genus, fror
the Shrewley sandstone. [October 1856.—P. B. B.]

376 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 4,

rarity of marine animals ; but the intervening Keuper is an exception
to this rule.

APPENDIX.

Note on EstHERIA MINUTA. By T. Rupert Jones, Esq.,
Assist. Sec. G.S.

Nort long since the Rev. W. Symonds favoured me with some well-
preserved specimens of this little Triassic fossil; and, with Prof. J.
Quekett’s kind assistance, I was enabled to see most distinctly the
true Crustacean character of the tissue of its valves. This confirmed
an opinion I had long held that this fossil is not a Molluse, but
closely allied to the Limnadia, Limnetis, and Estheria *, bivalved
phyllopodous Crustaceans (Entomostraca) of the present day; and
indeed, as far as the carapace-valves are concerned, it well represents
the Lstheria of Ruppell and Baird + (Isaura, Joly).

In the Quart. Journ. Geol. Soc. (1847) vol. ii. p. 274, Sir C. Lyell
figured a similar fossil from the coal-shales of Eastern Virginia, and
remarked that, with Mr. Morris, he doubted whether the so-called
“* Posidonomya’’ may not be a Crustacean rather than a Mollusc f.
Similar fossils, of different species, occur in the Devonian rocks
(Caithness and Orkney), Carboniferous (Northumberland), Liassic
(Skye and Gloucestershire ), Oolitic (Scarborough), Purbeck (Dorset),
and Wealden (Sussex). Others are met with in the Jurassic Coal-fields
of North Carolina and Virginia §, and along their north-eastern ex-
tension, forming the so-called ‘‘ New Red Sandstone” of Virginia
and Pennsylvania ||; in the plant-bearmg sandstones of Central
India {| (Nagpur and Mangali) ; and in the Triassic deposits of
Europe.

Although occurring so constantly in the different geological pe-
riods, from the Devonian to the Wealden**, and again in the recent
marine and fresh waters, yet it is in the Triassic deposits of England
and the Continent, im the sandstones and shales of Virginia and
Pennsylvania, and in the plant-bearing beds of Virginia and Central
India, that this little bivalved Entomostracan appears to be pre-
eminently abundant; so as to serve probably as a faithful index
of a peculiar geological horizon+f.

In like manner, among the still lower forms of life, the Nummu-
lite is represented in the Silurian {t, Carboniferous, Liassic, and

* See also above, p. 373, nofe. t+ Proc. Zool. Soc. part 17. p. 86.

t See also Lyell’s ‘ Manual of Geology,’ 5th edit. p. 332.

§ Lyell, loc. cit.; and W. B. Rogers, Boston Nat. Hist. Soc. Proc. v. p. 15.

|| Continuous with the Sandstones of New Jersey, and most probably with
those of Connecticut also: Rogers, loc. cit.

q Quart. Journ. Geol. Soc. vol. xi. p. 370.

** T have no satisfactory evidence of the presence of the genus in question in
the Cretaceous and Tertiary deposits.

tt Prof. W. B. Rogers has already pointed out (/oc. cit.) the probable value of
this little fossil in the comparison of the Mesozoic rocks of North Carolina and
Virginia, and of these with the so-called Triassic beds of the United States.

tt Annals and Mag. Nat. Hist. ser. 2. vol. xv. p, 58.

1856. | JONES—ESTHERIA MINUTA. BY

Oolitic rocks, and exists also at the present day ; but it particularly
distinguished one epoch (the Tertiary) by a surprising fecundity
and a temporary profusion of individuals.

The occurrence of a fossil Estheria in the Upper Sandstone and
Shale of the Scarborough district (H. concentrica, Bean*, sp.) is of
interest, as being indicative of the association of this Crustacean with
the Oolitic flora in England, as it is in India and America.

In India a Triassic Labyrinthodont Reptile (Brachiops laticeps*)
is found in the same strata as yield the Hstheria at Mangali and the
plants at Nagpur; and in Pennsylvania reptilian remains ¢ occur
with the so-called “ Posidonia”’: in America indeed the evidence
seems to point to a contemporaneity of the Virginian plant-beds,
the shales and sandstones of Pennsylvania and New Jersey, the foot-
marked sandstones of Connecticut, and the upper red sandstone of
Nova Scotia and Prince Edward’s Island, which is also reptilife-
rous § ; and it is evident that in the Virginian and Pennsylvanian
shales the minute Crustaceans under notice are important fossils.
The plants of Nagpur and Virginia having a Jurassic facies, like
those of Scarborough, it will be interesting, as further evidences
turn up, to see how far we are to regard the Triassic or the Jurassic
element as preponderating, or whether a passage-group of deposits
are indicated by the evidence,—or, lastly, whether these Plant-beds
with Reptiles and Crustaceans indicate the terrestrial and lacustrine
conditions only of the early secondary period.

The Jurassic flora of Australia || and that of Southern Africa have
been hitherto collected without affording any clear traces of the
Estheria. The latter country, however, has its probably Triassic
Reptile, the Dicynodon, imbedded with this flora 4] ;—so that the
peculiar association above-indicated for India and North America
obtains there also.

In pointing out these facts of the geological and geographical dis-
tribution of the fossil Hstheria, I merely touch upon the salient
points of an interesting subject of research,—for the elucidation of
which careful inquiry at home and abroad is still requisite.

In conclusion, although the recent H’stherta is a marine Crustacean,
yet, since very closely allied forms are of freshwater habits, and since
among bivalved Entomostracans different species of a genus and even
the individuals of a species occasionally live either in marine or
in fresh water, there is no certain evidence afforded by the fossil in
question whether the so-called Triassic deposits in which it is found
were formed in rivers, lakes, or seas.

* Mag. Nat. Hist. ix. p. 376.
+ Quart. Journ. Geol. Soc. vol. ix. p. 37 & 371.
t+ Lea on Clepsysaurus Pennsylvanicus, Journ. Acad. N. Sc. Philad. n.s. vol. ii.
p. 185; and on Centemodon sulcatus, Proc. Ac. N.Sc. Philad. vol. viii. p. 77.
§ Leidy on Bathygnathus borealis, Journ. Acad. N. Sc. Philad. n. s. vol. ii.
woes. .
|| See M‘Coy’s paper, Annals and Mag. Nat. Hist. vol. xx. p. 145, &c.
q Trans. Geol. Soc. 2nd series, vol. vii. part 4. p. 227, note.

378 PROCEEDINGS OF THE GEOLOGICAL society. [June 4,

3. On an ORTHOCERAS from CHINA.
By S. P. Woopwarp, Esq., F.G.S.

(Piate VI.)

THE specimen in question is one of several that were obtained by
Mr.’ Lockhart of Shanghae, from some place 200 miles distant, and
transmitted by him in 1854 to Daniel Hanbury, Jun., Esq., of Plough
Court. They are longitudinal sections in thin plates of limestone,
and seem to have been used as screens, for they were mounted in
carved-wood frames with stands. The same gentleman at an earlier
period communicated some Devonian Brachiopoda, identical with
French and Belgian species, described by Mr. Davidson in the Geo-
logical Journal, 1853, p. 353.

The largest specimen measures in length 29 inches, and 4 in its
greatest diameter ; it wants the last chamber and about 5 inches of
the spire. The angle of the spire is only 6°, and the intervals be-
tween the septa vary from } to less than + the diameter of the cells.
The siphuncle is central and quite simple.

The most instructive specimen is smaller, measuring 18 inches in
length and 4 in diameter ; it only wants the last chamber (see PI.VI.
fig. 1). The angle of the spire is 12 degrees, and the depth of the
chamber is from 4 to less than 4 their diameter.

The siphuncle is filled with dark reddish-brown limestone ; the air-
cells are lined with white spar and filled with converging crystals of
the same, or with greenish-grey stone. The shell has been entirely
replaced by grey stone, recording its outline and thickness, except in
some of the thinner septa which are only indicated by curved lines.

The siphuncle is simple, central, and incomplete ; the shelly part
of the tube (s) extending only one-third of the way from the con-
vexity of each septum towards the concavity of its predecessor. In
the last seven chambers, only two of which (a, a) are represented in
the figure, the siphuncle appears to have been completed by a mem-
branous tube (¢), which has disappeared from those of the spire.

In the last of these chambers, with an incomplete siphuncle (4),
the lining membrane appears to have separated a small space from
the wall, equally all round ; this space being filled with spar, whilst
the general cavity of the chamber is occupied by red stone, like the
siphuncle.

In the next chamber the separation and contraction of the lining
membrane has proceeded to a greater extent ; and so on in each suc-
cessive chamber, until the fifth, after which the siphuncle seems re-
placed by it, and gives off on each side a process directed towards the
anterior angle of the cell. The originally membranous nature of
this tube (formed by the contracted lining of the air-cells) is shown
by its want of symmetry. Towards the apex of the fossil it is black,
as if carbonized. The space (c,c) between the true shell and its
lining membrane is lined with spar, and sometimes filled with it, as
before mentioned ; but in some instances the limestone has pene-
trated, after the dissolution of the shell.

The changes which this specimen has undergone appear to be

1856. | WOODWARD—ORTHOCERAS. 379

these :—1. When buried in the sea-bed, mud entered the siphuncle
and filled the remains of those chambers in which the siphuncle was
incomplete. 2. Water containing carbonate of lime in solution
penetrated the air-chambers and other closed spaces, and coated all
the surfaces with tufa. 3. The shell was dissolved and removed,
before the consolidation of the surrounding mud, which thus obtained
access to all those cavities whose calcareous lining was incomplete.
4. The cavities which the mud could not enter were filled, or nearly
filled, with crystalline carbonate of lime.

The same structure is exhibited, with great regularity, in the
small specimen represented by fig. 2 (the locality of which is un-
known) ; in this the more highly curved lines alternating with the
septa represent the collapsed lining of the air-cells.

I have before noticed similar appearances in many polished sections
of Actinoceras, especially those from the black limestones of New
York, one of which is represented in Pl. VI. fig. 3. In these “it is
evident that the mud has gained access to the air-chambers along
the course of the blood-vessels ; but the chambers are not entirely
filled, because their lmmg membrane has contracted, leaving a space
between itself and certain portions of the walls, which correspond in
each chamber *.

The collection of Prof. Tennant contains the apex of a small Or-
thoceras from the Carboniferous Limestone of Ireland, one side of
which is fractured, showing what appears to be an enormous siphun-
cle, slightly moniliform, and nearly filling the shell (fig. 4a). On
making a section of this specimen, however, the true siphuncle
(fig. 4 6, s) proved to be small, central, and cylindrical, and contracted
at each septum. The lining membrane of the air-cells has separated
from the outer shell-wall only (c, ce), producing the appearance
noticed on the outside.

A specimen of the same species of Orthoceras, in the British
Museum, measures a yard in length and 6 inches in diameter at the
larger end, although the body-chamber is nearly all wanting. Part
of the apex has been slit, and shows the same structure as Mr. Ten-
nant’s specimen, but is less regular, and the septa are closer.

Something of this kind was noticed by Mr. Charles Stokes in a
Russian Orthoceras (Geol. Trans. 2nd series, vol. v. p. 712. pl. 60.
f. 4), and was attributed to a separation of the laminze of the septa.
The figure is very obscure, and the specimen probably lost f.

It will probably be found that these appearances are of constant
occurrence in the shells of this genus; and that they arise from
changes which took place in the lifetime of the animal, commencing
at the apex and progressing onwards, and resulting to a greater or
less extent in the death of the shell.

* Manual of the Mollusca, 1851, p. 82.

+ At the sale of Mr. Stokes’ collection all the most important specimens of
Orthocerata were purchased for the British Museum ; but unfortunately many of
those figured in the ‘Geol. Trans.’ by Dr. Bigsby (2nd series, vol. i.), including
the type of Bronn’s genus Conoceras, and others figured by Mr. Stokes himself,
could not be found.

VOL. XII.—PART I. aia 2D

380 PROCEEDINGS OF THE GEOLOGICAL society. [June 4,

I was formerly of opinion that some progressive changes could be
observed in the siphuncle of the Orthocerata; but of this I have
not yet obtained entirely satisfactory evidence.

In the work before referred to I stated that the Orthocerata did
not appear to have become decollated in their old age, and that ‘the
preservation of the shell was provided for by the increased size and
strength of the siphuncle, and its increased vascularity. In Hndo-
ceras we find the siphuncle thickened by internal deposits, until (in
some of the very cylindrical species) it forms an almost solid axis.”

This last statement was founded on Prof. Hall’s figures *, there
being no specimens of Endoceras in Europe. The diagram I gave
was ideal, and most likely incorrect ; for the internal tubes are pro-
oe invaginated siphonal joints (if anything) as suggested by Mr.

alter.

In the Chinese Orthoceras, now described, and in all the typical
species of the genus, the siphuncle is a simple tube, as in the recent
Nautilus, where it is nevertheless vascular and connected witha thin
membrane lining the air-chambers. But in those species which
have been separated under the generic name Actinoceras (including
Hormoceras and Huronia), the siphuncle possesses a complicated
internal structure, the appearance of which is liable to be modified
extremely by fossilization. In all these the structure is essentially
like that of the specimen figured and described by Mr. Stokes as
Hormoceras Bayfieldi (l. c. pl.60. f. 1), the vascular siphuncle being
divided into segments, which are radiately plaited and calcified.
The vessels which supplied the lining membrane of the air-chambers
(Pl. VI. fig. 3, s) passed through intervals or foramina between the
beads of the siphunele ; in Actinoceras Bigsbyi, and other Silurian
species, these foramina radiate equally from all sides of the siphuncle,
but in 4. giganteum, and others from the Carboniferous Limestone,
the foramina occur in only the ventral side of the beads.

The reduplicatiou of the vascular siphuncle is most remarkable in
“ Orthoceras”’ trigonale (Pl. VI. fig. 5) from the Devonian of Ge-
rolstein.

The figure given by MM. d’Archiac and Verneuil + is taken from
a large specimen, and does not represent any peculiarity of structure ;
and those in the splendid work of the brothers Sandberger on the
Devonian fossils of the Rhinet are not so definite as the example
now figured, which was obtained by Sir R. Murchison, and given
by him to Mr. Stokes. This specimen seems to have escaped more
attention from having passed as a fragment of ““Cyrtoceras” Hifeliense
(J. e. pl. 29. f. 1a), which has a similar siphuncle ; and probably
belongs to the same genus, although O. triangulare has a straight
shell. Aim
With regard to the position of the siphuncle in the eccentric Or-
thocerata, it seems probable that such species would occupy, nor-
mally, an inclined position near the bottom of the sea, with the

* Paleontology of New York, vol. i. pl. 18.

+ Geol. Trans. 2nd series, vol. vi. pl. 27. f. 1. i
+ Verst. des Rheinischen Schichtensystems in Nassau, p. 155. pl. Xvi.

SP Woodward del. Geo West bith

Quart.Journ.Geal Soc VolLXITPLV1.

W West Srp.

Orthoceras and Actinoceras

1856. | SALTER— DIPLOCERAS. 381

dorsal side upwards, like the recent Nautilus. In this case the
siphuncular side would be ventral.

EXPLANATION OF PLATE VI.

Fig. 1. Section of an Orthoceras from China; representing the apical portion
[divided on the plate], and two out of the seven last air-chambers in
which no alteration had taken place.

a, a, air-chambers; 6, 6, the same contracted; ¢, c, intra-mural spaces ;
s, siphuncle; ¢, membranous tube.
in the British Museum.

Fig. 2. Apex of a small Orthoceras (O. conicum, His. ?) in red limestone ; showing
the septa alternating with more strongly curved lines of the collapsed
lining membrane. Locality unknown.

In the British Museum.

Fig. 3. Section of Aectinoceras Lyonii, Stokes, from the Black-river Limestone
of New York ; the membranous siphuncle and the tubes leading from it
to the contracted air-cells are filled with black marble; the empty
spaces with white spar.

In the British Museum.

Fig. 4a. Fragment from near the apex of an Orthoceras (0. striatum, Sby.?),
from the Carboniferous Limestone of Ireland; the surface is broken
away, showing what appears to be a large internal siphuncle.

Fig. 44. Section of the same specimen, showing the small central siphuncle and
the line of separation of the internal membranes from the shell-wall.

In the Cabinet of Prof. Tennant.

Fig. 5. Siphuncle of Orthoceras trigonale, d’Arch. and Vern. ; magnified 23 dia-

meters ; from the Devonian of Gerolstein.
In the British Museum.

4. On a New Genvs of CepuHatopopa, Diretoceras (Orthoceras
bisiphonatum of Sowerby) ; and on the occurrence of ASCOCERAS
in Britain. By J. W. Satter, Esq., F.G.S.

(Abstract.)
[The publication of this paper is deferred. ]

In this communication the author pointed out the apparent relations
of this peculiar form, which has been figured in the ‘Silurian
System’ and in ‘Siluria.’? It possessed ordinary septa, pierced by
an excentric beaded siphuncle, and also had a deep lateral cavity
(supposed hitherto to be a second siphuncle) passing down side by
side with the siphuncle, and affecting at least seven, if not more of
the uppermost septa. :

Mr. Salter remarked that the structural peculiarities of Ortho-
ceras paradoxicum and of Gonioceras might offer some analogy with
the shell in question; but he thought that the real affinities were
with Ascoceras and Cameroceras.

Mr. Salter also described a new species of Ascoceras (A. Bar-
randi), found not long since in the Upper Ludlow rock, at Ludlow,
-and at Stansbatch in Herefordshire. The genus is new to Britain.

Ip 2

382 PROCEEDINGS OF THE GEOLOGICAL society. [June 4,

5. On TRap-pyKEs intersecting SYENITE in the MALVERN HItts,
WoRrCESTERSHIRE. By the Rev. W. 8. Symonps, F.G.S.

Among the varied phenomena described and registered respecting

the Malvern Hills in Prof. Phillips’s admirable work in the ‘ Memoirs

of the Geological Survey of Great Britain’ (vol. ii. part 1), I am not

aware of any notice of the effect of injected and intersecting trap

upon the syenite of which the great mass of the Malverns is com-
osed.

I had for some time been aware that greenstone and trap-dykes
traversed syenite in a quarry worked between the Winds-point and
the Obelisk, and to which last autumn I directed the attention of
Mr. C. J. Fox Bunbury. Having been requested by Sir W. Jar-
dine to examine the site of the great Malvern bonfire of January
last, in order to discover whether any signs of the vitrification of the
rocks were visible, I did so, and was immediately struck with the
appearance of the roasted syenite which formed the platform, and
the similarity presented by the baked mineral to syenite in contact
with dykes of trap and greenstone at the quarry at the back of News
Wood, half-way between Winds-point and the Obelisk.

I was accompanied during this investigation by a Swiss geologist,
Dr. De la Harpe, well accustomed to metamorphic phenomena; he
was much struck with this most interesting quarry.

I may here mention that a high wind prevented the flames of the
Beacon fire ascending to any height, and I was informed by those
present that an intense glow was concentrated upon the syenitic
platform.

At the quarry in question several dykes traverse and alter the
syenite, and the metamorphism presented by the rock in contact
with the greenstone is nearly identical with the effect produced by
the Malvern fire.

One of the dykes runs nearly north and south, and is about 10 ft.
thick, another from east to west ; while a third, of a different kind
of trap, traverses from north-east to south-west.

The syenite is altered for several feet from its contact with the
dykes, and then gradually assumes its crystalline form.

I have traced the dyke running from north to south to a consider-
able distance, and at the Gullet Pass it traverses the Holly Bush
sandstone, metamorphosing that rock into a steatitic gneiss.

At the valley of the White-leaved Oak, trap is again seen in contact
with Holly Bush sandstone, and there also changes it into a gneissose
schist. Iam inclined to attribute this effect to a prolongation of
the same dyke in a southward extension, and I think that the infil-
tration of the trap took place before the upheaval of the syenite,
but after that rock was consolidated.

1856. | SAWKINS—SOUTH SEA ISLANDS. 383

6. On the MoveMENT or LAND in the Soutu Sra IsLANDs.
By James Gay Sawxins, Esq., F.G-S.

TONGATABOO, one of the Friendly Islands, was visited a few months
previous to my sojourn there in 1854 by an earthquake, when the
north-east portion of it was tilted down to an inclination sufficient to
produce an encroachment of the sea for nearly two miles inland,
gradually diminishing to the south-eastern shore as far as Nuku-
alofa, where it now washes the roots of a tree that grew within a
garden adjoining a house that has been entirely destroyed. The
western coast has visibly risen some feet, and a spring of water has
sunk below the surface.

The island is formed of coral; there is no appearance of volcanic
intrusion through it ; but there have been disturbances that have
elevated some parts as high as 116 feet, with a good depth of vegetable
soil on them, which in the low land assumes the form of peat, emit-
ting under the rays of the sun strong humic acid.

The overflow of the sea on the northern and eastern sides of the
island, and the elevation on the south and west, are interesting in
connection with the report of another island having appeared about
this time to the westward. This fact was asserted by many, and
among them by a whaling captain who had cruised often over the
same track, and who landed in an open boat with his crew on the
western coast, having stranded his vessel on the said island, which he
described as being only a_few inches above the ocean (at a distance
of thirty miles), and covered with black sand exactly like that on
the shores of other volcanic islands in this and the Haabai group ; he
said that “tons of this sand were being levelled down by the wash of
every wave.’ I made particular inquiry of the natives of Tongataboo
if they had ever before seen any appearance of land in that direction,
to which they replied, No,—but that it was their belief that it rose
on the night of the earthquake (Christmas-eve, 1853), when the sea
came over the land at Hihifo (the North Point).

Since this occurrence an eruption took place at Niuafoou, an
island to the north, which destroyed nearly one half of its inha-
bitants ; it occurred about midnight, and so sudden was the over-
flow of lava from several apertures in the vicinity of a village, that
the people who ran for the shore were overtaken by it and destroyed.
This eruption was not felt at Tongataboo.

From these and other circumstances I am very doubtful if there
exists so great an amount of subsidence as of upheaval of land at
present in the Pacific ; also the fact of my never having been able
to find a well-rounded pebble or much-waterworn stone among the
alluvial deposits in the interior of any of these islands, convinces me
there has been no drift as in Europe, and forcibly leads me to the
opinion that a continent is forming and not disappearing, as some
have been led to suppose by a similar oscillation, perhaps, as I have
endeavoured to describe.

When examining the Island of Tahiti, one of the Society Islands,
ascending some of its higher mountains I found several strata of

384 PROCEEDINGS OF THE GEOLOGICAL society. [June 18,

coral and volcanic matter alternately overlying each other; and at
the borg of an artesian well near the town of Pepita five alternate
strata of coral and volcanic ashes were bored through in the space
of 25 feet, showing not only that several eruptions had occurred,
but that sufficient time must have intervened for the zoophytes to
have formed the coral between each, long before the island was ele-
vated to the height it now is. The same thing occurs at Oahu (near
Honolulu), one of the Sandwich Islands, at the foot of an extinct
crater called “the Punch bowl*.’’ In conclusion I must say I re-
turned from the Pacific Islands with a conviction there is a greater
extension of land going on by volcanic and coral formations, than
diminution by abrasion or subsidence.

7. On the Possible Origin of Veins or Goup 1n Quartz and
other Rocks. By L. L. B. Isserson, Esq., F.R.S., F.G.S.

[Abstract.]

Havine mixed a solution of gold in nitromuriatic acid with five
times its weight of water, and placed it in a Berlin evaporating-dish
on a thick sheet of copper over a gas-lamp, the author observed a
crack in the basin, which was increasing. On transferring the solu-
tion to another basin, he found that the crack presented a vein of
gold; the pure goid forming small nodular masses along the fissure,
both inside and out, and resembling veins of gold im auriferous
quartz-rocks. Under the circumstances of the low temperature at
which the solution was being evaporated, the diluted state of the
solution still left unevaporated, and the difference of the appearance
of the nodular form of the gold-vem from the usual appearance of
the metallic gold obtained by evaporation from such a solution, the
author thought it worth while to describe and exhibit the specimen
to the Meeting.

JUNE 18, 1856.

SPECIAL GENERAL MEETING.
Sir C. Lyell, V.P.G.S., in the Chair.

1. It was announced from the Chair that, in consequence of the
lamented decease of Daniel Sharpe, Esq., the late President, the
Society was now called upon to elect a President and a Member of
Council.

* This was filled with fresh water until 1837, when it disappeared during an
earthquake.

1856.] | CHARTERS—CLEAVAGE AT MONT LACHA. 385

2. Scrutineers were appointed, who, after the Ballot, reported
that Col. Portlock, R.E., F.R.S., was unanimously elected Presi-
dent; and that Hugh Falconer, M.D., F.R.S., was unanimously
elected a Member of Council.

ORDINARY MEETING.
Col. Portlock, President, in the Chair.
The following communications were read :—

1. On a SECTION near Mont BuaAnc.
By Major S. Cuarters, F.G.S.

[In a letter to Dr. Fitton, F.G.S.]

On looking over an old note-book I found a Section which satisfies
me that Mr. D. Sharpe is correct in the view he has taken of the
cleavage. I send you a copy of it, which, if you have an oppor-
tunity, you may show him,—not that the observations of so unscien-
tific a geologist as Iam can have any weight, but it may be satisfac-
tory to him, now that his paper has been attacked, to see that the
difference between cleavage and stratification, as exhibited at Mont
Lacha, attracted the attention of such a mere dilettante as myself,
now five years ago,—and that I scouted the idea of strata plunging
under the igneous rock that had upheaved them ; and that, until I
had made out the cleavage of Mont Lacha, I had attributed the
anomaly to reversal.

M. Blane.
a _
3 As
tal
i oS
< ‘2 a
om =
S.E cS & = ‘s N.W.
So =] st S
os 3 3
o o al =>
a E q
= i) = S
wn e eS es

River Arve.

Crystalline schist. Anthraciferous schist. Crystalline schist.

The dotted lines represent the lines of cleavage perpendicular to those of stratification,

which dip to the north-west at an angle of 75°.

Ascending the torrent of La Gria, which nearly marks the sepa-
ration of the calcareous rocks of Mont Lacha from the crystalline
rocks of the Aiguille de Gouté, we find a dark-coloured compact
limestone, the strata of which dip at an angle of 75° to N.W. Pro-

ceeding further up the ravine, the calcareous rock becomes more ~

schistose, and frequently talcose. Belemnites and Ammonites, in

386 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18

bad preservation, are not rare in the calcareous schists, but I found
no impressions of plants. At first sight, the cleavage may easily be
mistaken for stratification ; but by attentive observation, the strata
are evident, and their dip is normal, supposing Mont Blanc to be the
centre of upheaval. The Forclaz is a continuation of Lacha, but
towards the N.W. end, where it is separated by the River Arve from
the Aiguilles Rouges, the rocks are crystalline and the strata nearly
vertical.

The above section is a true copy of one taken by myself on the
spot in 1851.

Mont Lacha throws anal light on the apparently abnormal posi-
tion of the strata in some points named by Prof. Forbes, as Mont
Fretty, Cote de Piget, at the foot of Mont Bochard, &c.,—in short
the whole ‘‘Superposition Monstrueuse”’ of De Saussure disappears,
and I am fully convinced (as far as the Section here described is
concerned) of the accuracy of Mr. Sharpe’s observations.

Until I studied the stratification and cleavage of Mont Lacha, I
was under the delusion that the strata of Mont Fretty, &c. dipped
towards the crystalline rocks ; but as they were mere fractions, com-
pared to the immense masses of Mont Cramout, Mont Carmot, &c.
on the south of Mont Blanc, all in their normal position, I attributed
them to reversal.

Bath, April 25, 1856.

2. Further Notice* of the Recent Eruption from the VoLcano
of Mauna Loa in Hawart (OwHYHEE). By W. Miter, Esq.,
H.M. Consul-General for the Sandwich Islands.

[Forwarded from the Foreign Office by order of Lord Clarendon. }
(Abstract.)

TuHE stream of lava burst forth in August, 1855, from the side of
Mauna Loa, which rises to a height of 14,000 feet above the sea, at
a short distance below the summit, and about sixty miles in a direct
line from the harbour of the town of Hilo in Byron’s Bay. At the
date of Mr. Miller’s letter it had not ceased to flow, and had then
continued for a period of twenty-three weeks, and the stream had
a length of about fifty miles in all its windings. For the first
three weeks it had flowed uninterruptedly about thirty-eight miles,
when it met with a dense forest of trees and jungle which arrested
its rapid progress. It had forced its way through ten or twelve
miles of the forest, at the rate of about halfa mile in a week. There
still remained about three miles of the forest to the open ground
which extends to the town of Hilo, the lava being about five or
six miles distant from the town.

* Dated March 1, 1856. For the first notice, see this volume of the Journal,
p. 171. Mr. Miller’s communication was accompanied with a sketch-plan of the

position of the Lava-stream, and with a box of specimens of lava, &c. collected
by Mr. John Ritson.

1856. | SPRATT—BULGARIA. 387

Mr. Bishop, who examined the stream near the place it had then
reached, thus describes * what he saw :—On ascending a low hillock
between two nearly dry cascades he saw before him the blazing
woods and jungle and the flowing lava in a narrow dull sluggish
stream filling a side channel of the brook. It appeared to be about
100 yards in advance of a larger body, about 300 yards wide, which,
unobstructed in the smooth channel, rolled on about 100 feet in an
hour ; its front a glaring red, cooling as it flowed. A bright tongue
of the stream dashed forward, and rolled with dull plash over the
precipice. It formed a brilliant cascade of 25 feet, first in a broken
and at last in a continuous torrent, striking on a ledge, and sliding
off into the deep pool below. It gradually heaped up a mound of
half-solidified lava. It is stated that the higher regions of the
mountain were flooded with vast tracts of smoking lava, while the
streams which flowed down the side spread over a surface of several
miles in breadth ; and that the main stream now runs all the way in
a covered duct, so that it can be seen only at its vents which let off
the gas. A vessel at sea saw the light caused by the eruption at a
distance of fifty miles.

3. On the Groxoey of Varna and its Vicinity, and of other parts
of Butearia. By Capt. Spratt, R.N., F.R.S., F.G.S.

[ Abstract. ]
(The publication of this paper is postponed.)

Cart. Spratt first noticed a series of whitish calcareous sandstones
and marls, seen on the Bulgarian coasts ; these are nearly 1000 feet
thick, and are overlaid by reddish sands and marls. The former are
of marine origin and of Eocene tertiary date ; the latter are chiefly
of freshwater origin. Near Varna the freshwater beds have been
much denuded, and are not anywhere more than 200 feet thick. At
Cape Aspro, fifteen miles south of Varna, both of the series—the
grey and the red deposits—are seen disturbed and dipping to the
south, but unconformably, one series (the lower) having an angle of
30°, whilst the upper dips at 20°. At Cape Emineh, south of Cape
Aspro, and forming the termination of the Balkan, these beds are
still more disturbed and dip to the north. Capt. Spratt then de-
scribed the geological appearances along the coast southward. At
the Gulf of Bourgas and in the vicinity are igneous rocks, and de-
posits formed from their waste. Granite occurs on the southern
point of the bay.

Returning to Varna, Capt. Spratt pointed out the localities of the
fossils collected in the neighbourhood. The calcareous sandstones
abound in casts of shells and in Oysters and Pectens immediately
around Varna; and contain Nwmmulites in profusion at the upper
part of the Lake near Allahdyn. In this last-named neighbourhood

* In ‘ The Friend,’ Honolulu, March 1, 1856.

388 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18,

the uppermost strata, left by the denuding agencies that have affected
the district, are more durable than the underlying marls, &c., and
have a thickness of about 20 or 30 feet. They consist of a stony
mass of Nummulites, Operculine, and Orbitoides, with Pectines,
Terebratule, and Ostree. This harder portion of the superficial
rock has become apparently weather-worn into vertical pillars, either
isolated or still connected above by an horizontal layer of hard rock
which has resisted the destructive action of the weather. Capt. Spratt
observed that in some places in the vicinity the surface-rock was
split by vertical cracks, so as to resemble an open pavement. These
fissures, operated upon by atmospheric agencies, illustrate, in the
author’s opinion, the method in which the columnar fragments above
alluded to, and other masses more or less spherical, remaining on the
land, must have originated. The Nummulites contained in the dis-
integrating rock have not been destroyed, but remain intact, lying
about in heaps around the remaining nodules of limestone.

Capt. Spratt referred to the possibility of this columnar state of
the hard rock of the upper marine series having been brought about,
during the period which intervened between the deposition of the —
marine strata and that of the freshwater beds overlying the marme
series in the neighbourhood, by means of water-action: as it is
possible that the columnar surface of the degraded eocene beds may
have been covered up by the later deposits, and subsequently re-
excavated. This opinion seems to be supported by the fact of
columns occurring in a part of the Bay of Varna, at about 5 fathoms
depth. But Capt. Spratt leans to the opinion that the columnar
degradation is atmospheric, modern, and in actual progress.

Capt. Spratt then described the geology of the coast north of
Varna. The Kocene deposits (yellowish limestone and sandy marls)
occur as far nearly as Mangalia. The reddish freshwater sands and
marls then come in, overlying, and form generally the steppes of the
Dobrudcha. Land-shells occur in some of the upper beds of this
district. The author then dwelt on the points of correspondence
between the rocks composing the termination of the Balkan with
those of the Crimea, and of the steppes of the Dobrudcha with the
northern part of the Crimea.

Capt. Spratt proceded next to consider the age of the overlying
red marls and sands; and pointed out their resemblance to the fresh-
water deposits on the northern shore of the Sea of Marmora, on the
Macedonian coast, the northern end of Euboea, and the Locrian
shore. In fact, almost all the Thracian peninsula is composed of
freshwater deposits of brown and grey marls and sandstones, nearly
horizontal and attaining about 500 feet of thickness, which appear
to be contemporaneous with the upper pliocene freshwater deposits
on the western side of the Archipelago, in Eubcea and Macedonia,
and in Rhodes, &e. on the south.

The author concluded with a notice of a post-tertiary or recent
marine deposit on the coast of the Dardanelles at a height of about
15 or 20 feet above the present sea-level.

1856. | BOWEN—TRINIDAD. 389

4. On the Geology of Trin1pav. By H.G. Bowen, Ksq., F.G.S.
[ Abstract. ]

THE northern district of the Island of Trinidad, with the islands
between it and the mainland, is composed of flagstones, slates, and
schists, with quartz-veins and some dark-coloured intercalated lime-
stone. These rocks are all apparently unfossiliferous ; the slates
often abound with iron-pyrites and magnetic iron-ore, and some of
the ochreous quartz-veins (gossans) are slightly auriferous. Stalac-
titic caves occur in the limestone of the Island of Gaspar Grande,
and at Las Cuevas and Arouca. Alluvial beds of clay and gravel
are extensive in this district, and are sometimes 60 feet thick. At
Lateen Bay, im Chicachicare Island, a patch of aluminous clay-slate
occurs, with seams of crystalline limestone. The soil of this northern
district is fertile on the limestone, and barren on the slates. The
slate-rocks appear to be the same as those of Venezuela, which over-
lie the quartz-rock that crops out at Upata ; and rounded boulders of
quartz-rock occur in the flagstones.

In the south of the Island of Trinidad, red sandstone abounds,
often ferruginous, and associated with clays which are often either
bituminous or pyritous, and contain lignite and impressions of dico-
tyledonous leaves. In the Erin district the clay-beds have been
sometimes indurated and jasperized by heat. They afford also small
aluminous, chalybeate, and sulphuretted hydrogen springs, and in
the blue-clay formation are found hillocks throwing up mud and
water, and ponds covered by a film of mineral tar. The mud-vol-
canos throw up saline water and greyish mud, in a cold state, with
iron-pyrites and water-worn pebbles of blue limestone like that of
the northern part of the island, and sometimes of sandstone. They
do not appear to be connected with the sea ; and are most active at
the close of the rainy season. At Moruga small hills of granular
limestone occur. The succession of deposits in this southern part of
Trinidad appears to be—beginning from below—1. Sandstones, varie-
gated sands, lignitiferous clays (sometimes jasperized), and the Mo-
ruga limestone; 2. Blue and brown clays, with bitumen ; comprising
the pitch-lakes, salt and alum springs, &c. ; 3. Modern marine sand
formation, from 50 to 100 feet thick; and alluvial deposits, seldom
more than 30 feet thick. 7

The eastern coast of Trinidad appears to consist of the red sand-
stones and bituminous clays as far north as Matura, beyond which
the clay-slates set in. 3

The western coast of the island, south of Port of Spain, which is
built of the slate-rocks and limestone, exhibits only modern alluvial
deposits, sometimes calcareous, frequently ferrugmous, and appa-

rently resting towards the south on the red sandstone of the southern

district.

390 PROCEEDINGS OF THE GEOLOGICAL SociETY. [June 18,

5. On the Fossils found in the CHALK-FLINTS and GREENSAND of
ABERDEENSHIRE. By J. W. Satter, Esq., F.G.S.

[ Abstract. ]
(The publication of this paper is postponed.)

A norice of the occurrence of chalk-flints and greensand in Aber-
deenshire* has been published by W. Ferguson, Esq., F.G.S., in the
Proceed. Glasgow Phil. Soc. vol. in. p. 33, and the Phil. Mag. 1850,
p- 430, and some of the facts had been previously noticed ; but no
lists of the fossils had been given.

This communication showed the presence of characteristic Upper
Greensand fossils in the low ground at Moreseat : Thetis minor, Arca
earinata, Pinna tetragona, and Galerites castanea; with other
species, some of them new.

Among the Chalk fossils, Lima elegans of Nilsson is a new fossil
to Britain, and is found with the ordinary Inocerami and Echinites
of the Chalk in the rolled flints which form terraces round the hills
in Aberdeenshire. The probable continuity, therefore, of these beds
with those of the south of Sweden, where the same order of suc-
cession prevails, is inferred ; the extension of the Upper Greensand
so far north is a point of much interest.

6. On the CorRELATION of the MippLE Eocene TERTIARIES
of ENGLAND, FRANCE, and BELGIUM.
By J. Prestwicu, Esq., F.R.S., Treas. G.S.

[ Abstract. |
(The publication of this paper is postponed.)

In a former paper the author had shown the correlation of the
strata beneath the Bracklesham series in England, the Caleaire
grossier and Lits Coquilliers m France, and the Upper Ypresian
system in Belgium, and had proposed to designate that lower series
the “‘ London Tertiary Group,” from the circumstance of these strata
attaining the largest and most distinct development in the English
area. In the present paper Mr. Prestwich entered into an account of
the structures of the deposits next above. In France this is the Ca/-
caire grossier, which the French geologists have divided into four
stages:—1. a series of white and light-green marls, apparently of
freshwater origin; 2. an upper divison, of calcareous rock, harder
and more flaggy than the next below, and rich in Miliolites and Ceri-
thium, mixed with a few freshwater shells and the remains of plants
and land-animals ; 3. a middle one, of a calcareous freestone abound-
ing in marine organic remains (Grignon, Courtagnon, and other cele-
brated localities being in beds of this zone) ; and 4. a lower one of green
sands, with few fossils. Each division attains at places a thickness of
30 to 40 feet, but the lower ones are thickest in the centre and west

* It appears not very satisfactorily proved that the chalk and greensand exist
in sttu in this locality ; Proc. Glasgow Phil. Soc. vol. iii. p. 44 e¢ seg.— Eb.

1856.| PRESTWICH—BRITISH AND FOREIGN TERTIARIES. 391

of the Paris basin ; whilst the upper, on the contrary, are thickest to
the eastward. The total thickness of the deposit, therefore, rarely at
any one place exceeds 100 feet, whilst the Upper Bracklesham series,
with which it corresponds, is more than 500 feet thick. This dif-
ference the author attributed to a more rapid subsidence of the
English area than of the French at that geological period. This, he
showed, was accompanied by more marine conditions prevailing all
through the English deposit, and by the continuance throughout of
the same green sands which in France were confined to the lower
division. ‘That the whole series was, however, synchronous with the
Calcaire grossier he considered proved by the circumstance, that,
although the freshwater beds which existed in France did not extend
to this country, yet the organic remains of some of the beds of the
Bracklesham series gave evidence of an upper division higher than
the beds with the Venericardia planicosta and Cerithium giganteum of
Bracklesham, for at the latter place the proportion of shells ranging
up into the overlying Barton series was 30 per cent., whereas in some
beds recently discovered by Mr. F. Edwards at Bramshaw, and ap-
parently at the top of the Bracklesham series, the proportion is
46 per cent. The middle beds of the upper Bracklesham series show
the closest affinity with the Middle Calcaire grossier, although there
are only 140 species in common. The lowest division of this series
is more fossiliferous in England than in France, showing a closer re-
lation (43 per cent.) with the underlying beds than does the mass of
the Calcaire grossier, in which the proportion is as 28 per cent.
The total number of Molluscs in the Calcaire grossier of the Oise
is 651, and in the Bracklesham series of Hampshire 368. |
Above this zone is the series of the Sables moyens in France and
Barton clays in England. Owing to the number of Calcaire gros-
sier fossils which had been found at Barton, these beds had been
considered synchronous with the Calcaire grossier, a view which
the author himself had formerly adopted with reserve. Seeing,
however, that the Bracklesham series probably represents all the
divisions of the Calcaire grossier, and that the distinction between
the Bracklesham and Barton series was of equal value to that be-
tween the Calcaire grossier and the Sables moyens, the author now
correlated the Barton clays with the Sables moyens, as suggested by
M. Graves, M. Dumont, Sir Charles Lyell, and M. Hébert. He,
however, alluded to the difficulty of dog this upon the evidence of
any small number of organic remains, or even of a few species con-.
sidered characteristic in one area; and he showed that in the Barton
clay itself, although there were many Sables moyens species (63), still
there were a greater number of Calcaire grossier species (69). In
the same way in the Laeckenian system of Belgium, which overlies
the Bruxellian system (the equivalent of the Calcaire grossier),
there are forty-five Calcaire grossier and Bracklesham sand species,
and only forty-four Barton and Sables moyens species. But Mr.
Prestwich showed that, taking the per-centage of species which
range from the lower to the higher series, each area offered nearly
an equal amount of distinction ; as out of 100 species of the lower

392 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 18.

series there are in England 30, in France 35, and in Belgium 32,
which range upwards.

Mr. Prestwich mentioned that M. Graves had recognized several
well-known Barton species, such as the Voluta depauperata, V.athleta,
Oliva Branderi, Conus scabriusculus, &c., in the Sables moyens of
the Oise. The total known number of the Sables moyens species is
377, and of the Barton clay species 252.

These series the author proposed to term the ‘Paris Tertiary
Group ’”’ (its lower part), as the several members of it were more
complete in France than in England, and contained a richer and better-
preserved fauna. This Paris group forms the great Nummulitic
zone. Hitherto none of these Yoraminifera (Nummulina) have been
found in the London group.

The author concluded with some general observations on the extent
of the ancient seas and the position of the dry land, and took occasion
to observe on the fact, that, although the several deposits in each
country were so rich in organic remains, yet so small a proportion of
them should have hitherto been identified as common to the several
areas. Nevertheless the same genera prevailed, and the relative
number of species of each genus was generally tolerably well main-
tained. He hoped, therefore, that Paleontologists would, in cases
where there was now good reason to believe the strata to be synchro-
nous, inquire further into the extent of variation which the same
species might undergo in areas where the sea had presented such dif-
ferent conditions of depth, mineral composition of sea-bottom, &e.
A certain number of peculiar species must necessarily result from
such different conditions, but the author considered it probable that
the same causes would lead to the existence of such marked varieties
as might, viewing each area separately and independently, cause
some varieties to assume the permanence and importance of specific
differences. Until the exact synchronism of any deposit is esta-
blished, the Paleeontologist cannot always fully take these causes
into consideration, and many admirable monographs on Tertiary fos-
sils have necessarily been founded, in great measure, upon the dif-
ferences actually apparent and persistent in the several areas. 7

Mr. Prestwich stated that it was his intention to continue this
inquiry at a future period, and to examine into the correlation of the
interesting freshwater and fluviatile series overlying the Barton clay
on the Hampshire coast and in the Isle of Wight.

393

DONATIONS
TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY,

From April 1st, 1856, fo June 31st, 1856.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

AMERICAN Journal of Science and Arts. 2nd Ser. Vol. xxi. No. 62.
March 1856. From Prof. Silliman, For. Mem. G.S.

A. A. Hayes.—Specimen of Native Iron from Liberia, Africa, 153.

H. Rose.—Preparation of Aluminium, 164. :

J. D. Dana.—Supplement to Dana’s Mineralogy, No. 2, 193.

C. N. Sheppard.—Meteoric Iron, Orange River County, South
Africa, and Mexico, 213.

T. Coan.—Recent eruption of Mauna Loa, 237.

J. D. Dana.—Voleanie action at Mauna Loa, 241.

Aluminium and Silicium, 258.

W. P. Blake, T. A. Conrad, and L. Agassiz.—Fossils from Cali-
fornia, 268.

Sir R. +7 Murchison.—Rocks and Fossils of the North Highlands,
276.

J. A. Hugard.—Mineralogical Cabinet of the Garden of Plants at
Paris, 280.

Bailey.—Deep-sea Soundings, 284.

Notices of Books, 302.

No. 63. May 1856.

A. K. Isbister.—Geology of North America, 313.

W. B. Rogers.—Protocarbonate of Iron in Coal-Measures, 339.

A. Sedgwick.— Paleozoic Strata of Great Britain, 343.

J. W. Bailey.—Fossil Diatomacez, 356.

G. B. Airy.—Pendulum Experiments, 359.

W. P. Blake.—Tulare Lakes, California, 365.

R. I. Murchison.—Fossil Wood and Rocks of the Arctic Archi-
pelago, 377.

A. A. Hayes.—Serpentine, 382.

J. M. Gilliss —Earthquake of April 2, 1851, in Chile, 388.

Aluminium and Silicium, 404.

Artesian Well in the Bois de Boulogne, 404.

Se

394 DONATIONS.

American Journal of Science and Arts. 2nd ser. Vol. xxi. No. 63.
May 1856 (continued).
Mitscherlich.—Crystalline form of Selenium, Iodine, and Phos-
phorus, 411.
Riche.—Tungsten, 416,
Mohr.—Copper, 417.
Peligot.—Uranium, 418.
Wohler.—Crystallized Silicon and Carbon, 418.
J. Leidy.—Stenacanthus nitidus and Cylindracanthus ornatus, 421.
Hipparion occidentale and Hyopotamus americanus, 422.
Geological Survey of the State of New Jersey (Waste and Subsi-
dence of Coast, &c.), 423.

Geological Survey of Missouri, 427.

W. J. Taylor.—Pseudomorph of Smithsonite, 427.

W. B. Carpenter.—Foraminifera, 429.

J. G. Jeffreys.—British Foraminifera, 432.

W. Gregory.—Diatomacez, Phytolitharia, and Sponge-spicules
in Soils supporting Vegetation, 434.

J. W. Dawson.—Submerged Forest at Fort Lawrence, Nova
Scotia, 440.

Hochstetter.— Bohemian Forests and Peat-bogs, 442.

J. Wyman.—Fossil Footprints, 444.

W. P. Blake.—Earthquakes in California, 449.

Notices of Books, 450.

Atheneum Journal for April, May, June 1856. From C. W. Dilke,
Esq., F.GS.
Notices of Meetings.

Bengal Asiatic Society, Journal. New Series, No. 77. 1855, No. 7.
Silt of the Hooghly, 704.
Kunkur from Kedgeree, 704.
Artificial bricks, 704.
Burdwan and Chunar Stone, 704.
Darjeling Copper, 706.
Cuttack Iron-ores, 708.
Coal from Thayet Myo, Pegu, 709.
Clays, &c. from Debrugher, Upper Assam, 726.

Bent’s Monthly Literary Advertiser. Nos. 625, 626.

Berlin. Zeitschrift der Deutschen geologischen Gesellschaft. Vol.
vi. Part 4. August—October 1855.

Proceedings and Letters, 547.

A. Huyssen.—Die Zoolquellen des Westfalischen Kreidegebirges,
ihr Vorkommen und muthmaaslicher Ursprung, 567.

Von Strombeck.—Ueber das Vorkommen von Steinsalz im
Norden vom Harze, 655.

Fr. L. Sonnenschein.—Ueber eine in einem Hochofen entstan-
dene Legirung von Blei und Eisen, 664.

Canadian Institute. Canadian Journal. August 1852.
Distribution of Gold, 17.
Volcanic Eruptions in the Sandwich Islands, 18.
Ironstone of Cleveland, Yorkshire, 18.

September 1852.

Chatin on Rain-waters, 43.

October 1852.

DONATIONS. 395

Canadian Institute. Canadian Journal. November 1852 (continued).
E. Forbes on the Natural History of the British Seas, 109.
E. W. Logan.—Geological Survey of Canada, 112.
The Iron-trade, 119.

November 1855.
J. D. Dana.—Geology in America, 385.

December 1855.
Mastodon giganteus in Canada, 405.
Yield of the Copper-mines for 1855, 413.

————.. New Series. No.1. January 1856.
H. Croft.—New Salts of Cadmium, and Iodides of Barium and
Strontium, 13.
J. W. Dawson’s Acadian Geology, noticed, 39.
Geological Notes, 74.
Steel, 74.
Mineralogical Notes, 79.
——. No.2. March 1856.
E. Billings’s Canadian Naturalist and Geologist, noticed, 164.
Preservation of Organic remains, 186.
Purple Copper-pyrites, 187.
Aluminium, 192.
Cadmium-salts, 193.

Charleston (South Carolina), Elliott Society of Natural History,
Proceedings. November 1, 1853—July 24, 1855.
L. Agassiz.—Tertiary and Recent Sharks, 4
F. S. Holmes.—New fossil Balani (plate), 21.
Chemical Society, Quarterly Journal. Vol. ix. No. 1. April 1856.
D. Campbell on the Source of the Water of the deep wells in the
Chalk under London, 28.

Cincinnati, Young Men’s Mercantile Literary Association of, Twenty-
first Annual Report of the Board of Directors for the year
1855-56.

Civil Engineer and Architect’s Journal. No. 265. Vol. xix. April 1856.

B. de St. Hilaire.—The Nile and its Sediment, 138.
No. 266. May 1856.
W. Truran.—The Iron-manufacture of Great Britain, 149.

a No, 267. - dune T1856.
A. S. Hewitt.—Production of Iron, 194.
J. Wilson.—<Action of Rivers on their beds, 196.

Critic. No. 364. June 2, 1856.
Notices of Meetings.
=>, No. sno. June 16, 1856:

Warren’s Description of Skeleton of Mastodon giganteus, noticed,

Nowe of Meetings.
Dijon, P Académie Impeériale des Sciences, Arts, et Belles-Lettres,
Mémoires, 2 ser. Vol. iv. Année 1855.
Partie des Sciences :—
A. Perrey.—Bibliographie seismique, |.
VOL. XII.—PART I. 41)

396

DONATIONS.

Dublin Geological Society Journal. Vol. vii. Part I. 1855-56.

J. Kelly.—Localities of Fossils of the Carboniferous Limestone
of Ireland, 1.

————. Part 2. 1855-56.

France.

J. B. Jukes and J. W. Salter.—Classification of the Devonian
and Carboniferous Rocks of the South of Ireland, 63.

W. King.—Permian Magnesian Limestone at Tullyconnel, near
Artrea, i in the County of Tyrone, 67.

Lord Talbot de Malahide.—Anniversary Address, 82.

Société pcre see Bulletin. Deux. Sér. Vol. xii. Feuill.

52-60. 1855.

Jules Marcou. bo ceiae explicatif (une carte géologique des
Etats Unis et des provinces anglaises de l’Amérique du Nord
(Pl. XX. et XXI.) (fin.), 817.

E. Bayle.—Notice sur le systéme dentaire de |’ Anthracotherium —
magnum, Cuvier (Pl. XXII.), 936.

Deshayes.—Quelques observations au sujet de la famille des
Rudistes de Lamarck, 947.

. Vol. xin. Feuill. 3-7, 1855.

Ville.—Notice sur les gites d’émeraudes de la haute vallée de
PHarrach (Algérie) (fin.), 33.

F. Cailliaud.—Sur les terrains tertiaires inférieurs des communes
de Campbon, Arton, Chéméré et Machecoul (Loire-Infé-
rieure), 36.

Ch. Lory.—Note sur les Oursins perforant le granite sur les
cotes de Bretagne, 43.

Deshayes.—Observations sur les communications ci-dessus de
MM. Cailliaud et Lory, 46.

Th. Ebray.—Accidents géologiques survenus pendant la forma-
tion de la craie tuffeau du Poitou et de la Touraine, 51.

De Keyserling. —Explications relatives a une note sur la succes-
sion des Ctres organisés dans les couches sédimentaires
(Bulletin, 2 série, t. x. p. 355), 60.

A. Boué.—Renseignements sur les mines de Maidan Pek, en
Servie, 63.

A. Sismonda.—Lettre 4 M. Elie de Beaumont sur une course
exécutée par lui avec M. Fournet autour du Mont-Blanc en
septembre 1855, 64.

A. Damour.—Note sur un sable magnésien des environs de Pont-
Sainte-Maxence (Oise), 67.

EK. Bayle. Ri sur le Spherulites foliaceus, Lam.
(Pe) ea7.

Ed. Piette. suNbaes sur les coquilles ailées de la grande oolithe
de |’Aisne, des Ardennes et de la Moselle (Pl. II a V.), 85.

KE. Bayle.—Observations sur le Radiolites Jouanneti, Des Moul.
(sp.) (Pl. VI.), 102.

Franklin Institute, Journal. 3rd Series. Vol. xxxi. No.4. April
1856.

Geneva.

Downing.—Drainage of Haarlem Lake, 227.
Mémoires de la Société de Physique et d’ Histoire Naturelle

de Genéve. Vol. xiv. Part 1. 1855

C. Marignac.—Sur les formes cristallines de quelques composés
chiniques, 201 (3 plates).

DONATIONS. 397

Geological Survey of Great Britain and Museum of Practical Geo-
logy, Memoirs 1856.

W. W. Smyth, A. Dick, and J. Spiller.—The Iron-ores of Great

Britain. Part 1. The Iron-ores of the North and North-

midland counties of England. With preface by Dr. Percy.

of the United Kingdom, Memoirs. Figures and descrip-

tions illustrative of British Organic Remains. Decade v.
[Echinodermata.] 1856.

Institute of Actuaries, Assurance Magazine. Vol. vi. Parts 3 and 4.
April—July 1856.

Journal of the Indian Archipelago and Eastern Asia. Vol. viii.
No. 13 (Supplementary No. for 1854).

Ist Supplement for 1854. Ethnology of the Indo-Pacific
Islands: Language, Part 2. 1855-56.

. vol. ix. Nos. 4-6 (in one). April—June 1855.
——. vol. ix. Nos. 7-9 (in one). July—Sept. 1855.

Liége, Société Royale des Sciences, Mémoires, 1855. Vol. x.
L. de Koninck.— Une nouvelle espéce de Davidsonia, 281 (plate).
I. Kupfferschlaeger.—Procédé pour analyser par voie séche les
minerais de zine, 289.

Linnean Society, Journal of the Proceedings. Vol.i. No.2. June
1856.

Literarium. No. 40. May 14, 1856.

No. 43. June 4, 1856.
R. Owen.—On Ruminants and the Aboriginal Cattle of England,
684.

No. 44. June 11, 1856.

Literary Gazette for April, May, June, 1856. From L. Reeve, Esq.,
F.G.S. 3 és
Notices of Meetings. i
Warren’s Description of Mastodon giganteus, noticed, p. 341.
Notice of D. Sharpe, Esq., p. 351.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xi. No. 73. May 1856. From R. Taylor, Esq., F.G.S.

Dennis.— Fossils from the Lias Bone-Bed, 393.

Laurent.— Valenciennes Coal-basin, 394.

R. Harkness.—Red Sandstones of South Scotland, 395.

J. S. Wilson.—Notes on Australia, 396.

H. 8. Beckles.—Hastings Cliffs, 396.

T. Wright.—Inferior Oolitic Sands, 396.

A. Boué.— Straits of Dover, 397.

W. Hopkins.— External temperature of the Earth and other
planets, 398.

C. Rammelsberg.— Volknerite, or Hydrotalkite, and Steatite of
Snarum, 405.

. ——. No. 74. June 1856.
A. Dick.—Metallurgy of Copper, 409.

398 DONATIONS.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xi. No. 74. June 1856 (continued). .
G. P. Scrope.—Voleanic Craters and Lavas, 477.
G. W. Binney.—Foot-track in the Millstone-grit, 479.
J. G. Croker.—Bovey Lignite, 480.
C. J. F. Bunbury.—A Mere in Norfolk, 480.
A. Dick.—Cleveland Iron-ore, 481.
R. H. Cobbold.—Coal in China, 482.
A. Reuss.—Coprolitic deposit in Bohemia, 486.

London, University College, Proceedings at the Annual General
Meeting, Feb. 27, 1856: Report of Council, 1856.

Munich. Abhandlungen der math.-phys. Classe der k. bayerisch.
Akad. der Wissensch. Vol. vu. Part 3. 1855.

K. bayerisch. Akad. Almanach fiir 1855.

Paris. L’Ecole des Mines. Annales des Mines. 5 sér. Vol. vil.
live: de E855.

Bibliographie, premier semestre de 1855.

E. de Rivero.—Sur les mines de charbon de terre du Pérou, 459.

E. Roger.—Sur les mines d’anthracite du bassin du Drac (Isére),
525 (plates).

Herbert.—Sur l’importation et exportation du fer, ainsi que du
charbon minéral, dans le Royaume-Uni pendant les années
1853 et 1854, 587.

D. De Saint-André.—Sur l’existence de terrains auriféres dans la
province de Fernambouc (Brésil), 604.

Arnoux.—Notes minéralogiques sur les environs de Quang-ngai,
Moyenne-Cochinchine, 605.

J. Wilson.—Sur l’industrie du fer aux Etats-Unis, 616.

Cazotte.—Sur l’industrie minérale dans les provinces d’Atacama
et a Concepcion (Chili), 625.

Breuil.—Sur les recherches de mines au Brésil, 628.

Ch. De Sénevier.—Sur les conditions économiques de l’industrie
de l’acide borique, 629.

Sur la legislation des mines dans l’Etat de Vénézuéla, 637.

Pennsylvania. Franklin Institute Journal. 3rd Ser. Vol. xxxi. No. 4.
Downmg.—Draining Haarlem Lake, 227.
Fusion of rocks for purposes of art, 278.

——-. No. 5.

Photographic Society, Journal. Nos. 40, 41, 42, 43.

Ray Society. Report of the Council, 1855.

Royal Asiatic Society of Great Britain and Ireland. Vol. xvi. Pt. 2.

Royal Astronomical Society, Memoirs. Vol. xxiv. 1856.
Monthly Notices. Vol. xv. 1855.

Royal College of Surgeons of England. Index to the Catalogue of
the Library, 1853; and Additions to the Index, 1855.

.. Descriptive Catalogue of the Fossil Organic Remains in
the Museum of the Royal College of Surgeons. Plants.

————. ——__——.- Reptilia and Pisces.

DONATIONS. 399

Royal College of Surgeons of England. Descriptive Catalogue of
the Fossil Organic Remains in the Museum of the Royal Col-
lege of Surgeons. Invertebrata.

From the Royal College of Surgeons.

Royal Geographical Society of London, Journal. Vol. xxv.
W. Bollaert.—Coal in Chile, 172.

———. Proceedings. No.1. Nov. and Dec. 1855, and Jan.
1856.

No. 2. April 1856.

—. No.3. April and May 1856.
Callen: —Gold in the Isthmus of Darien, 78.

Royal Society of London, Proceedings. No. 76.
Society of Arts, Journal. Vol. iv. -No. 17 gi:
a Vol. iv. No. 178.

“Vor. Noy t79.
Teoretrade of France, 393.

Vol. iv. No. 180.
Vol. av: > No? 187.
———_——, Vol.iv. No. 182.
Clark. —Water Supply, 429.

————-. Vol.iv. No. 183.
Simon and Campbell.— Water Supply, 470.
Vol. iv. No. 184.
ae Voleive- Nox 185.

Calvert and others. —Water Supply, 505, 507.
———. Vol.iv. No. 186.
—_—_——. ——. Vol.iv. No. 187.
—__——. ———.. Vol.iv. No. 188.
—_——. —-—. Vol.iv. No. 189.
Vol. iv. No. 190.
ieee of Marble or Stone, 592.

Somerset Notes and Queries, and Journal of the Taunton School of
Art. Edited by W. A. Woodley. 1856.
J. D. Pring.—Notices of the Geology and Fossils of Taunton
and the Quantock Hills, 14, 16.

Statistical Society of London, Journal. Vol. xix. Part 2.
June 1856.

Turin. Memorie della Reale Accademia deile Scienze di Torino.
Serie Seconda. Vol. xv. 1855. .
Richelmy e A. Sismonda.— Un apparechio destinato alla lavatura
dei minerali, e particolarmente dei minerale auriferi, xii.
A. Sismondi e Cantu’.—La Carbonizzazione del legno, della torba,
della lignite, &c., Ixxiv, xe, xcix.

400 DONATIONS.

Turin. Memorie della Reale Accademia delle Scienze di Torino.
Serie Seconda. Vol. xv. 1855 (continued).
Plana.—Depressione della Superficie del mar Caspio sotto quella
del mar Nero, xeix.
Provano di Collegno.—Osservazioni geologiche fatte negli statti
della ferrovia che mette a Susa, ex.
K. Sismonda e Moris.—Flora dei terreni terziarii di Novale, nel
Vicentino, exi.
A. e H. Schlagintweit.—Sur la hauteur du Mont-Rose, 63.
L. “te di.—Catalogo ragionato dei Fossili Nummulitici d’ Egitto,
i 171

Van Diemen’s Land Royal Society, Papers and Proceedings. Vol. ii.

Part 3. Jan. 1854.
T. Moore.—Geological Specimens collected in Tasmania, 424.

. ———. Tasmanian Contributions to the Universal
Exhibition at Paris.
Victoria Philosophical Society, Transactions. Vol.i. 1855.
R. B. Smyth.— Building-materials of Melbourne, 24.
W. Blandowski.—Geology, &c. of the central parts of Victoria, 50.
R. B. Smyth.—Influence of the Physical Character of a Country
on the Climate, 203 (plates of sections).
W. Blandowski.—Fossils from the Upper Yarra District, 221
(plate).
SEN Geological Notes on Melbourne, &c., 229 (plates).
D. E. Wilkie.—Water Supply of Melbourne, 234.
C. Hodgkinson.—Rocks and Soils of Victoria, 260.
Proceedings of the Society.
R. Scott.— Physical Character of the County of Heytesbury, xix.

Warwickshire Natural History and Archeological Society, Twentieth
Annual Report.

II. GEOLOGICAL CONTENTS OF PERIODICALS
PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 2nd Ser. Vol. xvi. No. 100.
April 1856.
W. King.—On Permian Palliobranchiata, 333.

No. 101. May 1856.

S. P. Woodward.—On the Occurrence of Conoteuthis in England,
402.

R. Owen.—On the Gastornis parisiensis, 440.

On Fossil Mammalia from the Red Crag of Suffolk,

a a

441.

a, No. 102. June 1856.
H. Falconer.—On Cuvier’s Laws of Correlation, 476.
W. B. Carpenter.—Structure of Brachiopod Shells, 502.
Stur.— Influence of Soil on the Distribution of Plants, 520.

DONATIONS. 401

Dunker and Von Meyer’s Paleeontographica. Vol. iv. Part 5. 1855.
P. Wessel and O. Weber.—Neuer Beitrag zur Tertiarflora der
miederrheinischen Braunkohlenformation (continuation, with

plates).

. Edinburgh New Philosophical Journal. New Series. Vol.iu. No. 2.
April 1856.
J. D. Forbes.—On the Geological Relations of the Secondary
and Primary Rocks of the Chain of Mont Blane (plate), 189.
A. A. Hayes.—Native Iron from Liberia, Africa, 204.
Plurality of Worlds, 218.
A. Thomson.—On Prof. B. Powell’s Views, and the Human
Skeleton found near Mickleton Tunnel, 247.
R. Edmonds.—Earthquake of May 1855, and Disturbance of the
Sea on June 6, 1855, at Penzance, 280.
W. Crowder.— On the Cleveland Ironstone Beds, 286.
Lyell’s Manual of Geology, noticed, 305.
W. Gregory.—On the Diatomaceous Sand of Glenshira, 346.
M. F. Heddle.—On Galactite and Natrolites, 349.
On Mesolite, Faroelite, and Antrimolite, 351.
D. Page.—On new Crustaceans from the Forfar Flagstones
(Kampecaris Forfarensis, STESnUnUs Powriensis, and Sli-
mona), 351,
Meteorites in Hanover and Norway, 367.

Leonhard und Bronn’s Neues Jahrbuch ftir Min. Geog. Geol. u.
~ Petref., 1856. Erstes Heft.
Ue Posselt. —Die Kupfer-distrikte des Obersee’s( Lake Superior), 1.
D. F. Wiser.—Bericht tber Schweitzerische Mineralien seiner
Sammlung, 11.
J. J. Kaup.—Ueber einen vollstandigen Halitherium-Gaumen
mit Zahnen, 19 (plate).
Gergens.—In Chalcedon von Oberstein eingewachsene krystal-
lizirte Mineralien, 22.
Letters: Notices of Books, Mineralogy, Geology, and Fossils.

———.. Zweites Heft.

J.C. Deicke. —Geognostische Skizze des Untern Thurgau’s und
der Umgebung von Oeningen, 129.

Gergens.— Ueber emige Pseudomorphosen aus der Bleigrube von
Kautenbach bei Berncastel an der Mosel, 135.

Castendyck.—Die Gegend um Wildungen im Firstenthum
Waldeck, 140 (plate).

C. F. Naumann.—Ueber die Krystallreihe des Quarzes nach
Descloizeaux, 146.

Letters: Notices of Books, Mineralogy, Geology, and Fossils. -

402 DONATIONS.

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.

Alder, J., and A. Hancock. A Monograph of the British Nudi-
branchiate Mollusca. Part 7. From the Ray Society.

Babbage, C. Observations addressed, at the last Anniversary, to
the Royal Society, after the delivery of the Medals.

Beaumont, E. de, Dufrenoy, et E. de Verneuil. Rapport sur un
Mémoire de M. Jules Marcou, relatif 4 la Classification des
Chaines de Montagnes d’une partie de l Amérique du Nord.
From M. Jules Marcou.

Bengal Government, Selections from the Records of the. No. VI.
Report on the Tin and other mineral productions of the Tenas-
serim Provinces, by Capt. G. B. Tremenheere, and Remarks on
the Report, &c. by T. Oldham.

——_—_—_——. ——. No. VIII. Report of the Examinations
of the districts in the Damoodah Valley and Beerbhoom pro-
witli: Iron-ore, by T. Oldham.

No. XIII. Notes on the Manufacture of
Salt in the Tumlook Agency. Report on the Coal-mines of
Lakadong in the Jynteah Hills. Memorandum of the results
of an Examination of Gold-dust and Gold from Shuy-gween.

From T. Oldham, Esq., F.G.S.

Blofeld, J. H. Algeria, past and present.

Bryce, James. A Cyclopedia of Geography, descriptive and physical.

Carpenter, W. B. Researches on the Foraminifera [Orbitolites].

Dana, J. D. On Volcanic Action at Mauna Loa.

Science and the Bible: a Review of ‘The Six Days of
Creation’ of Prof. T. Lewis.

Second Supplement to Dana’s ‘ Mineralogy.’

Deslongchamps, E. Description d’un Nouveau Genre de Coquilles
Bivalves fossiles, Elymus, provenant de la Grande Oolithe du
Département du Calvados.

Erdmann, A. Ut6 Jernmalmsfalt i Stockholms Lan.
Faraday, M. Experimental Researches in Electricity, 30th Series.

and P. Riess. On the Action of non-conducting bodies
in Electric Induction.

Favre, A. Recherches sur les Minéraux Artificiels.

Ferguson, W. America by River and Rail.

Gaudin, C. Th., et Phil. De la Harpe. Fiore fossile des Environs
de Lausanne.

DONATIONS. 403

Harkness, R. On the Geology of the Dingle Promontory.

and John Blyth. On the Cleavage of the Devonians of
the South-west of Ireland.

Haughton, S. The Solar and Lunar diurnal Tides on the Coasts of
Treland.

Hennessy, H. Notes on Meteorology.

Hermann, F. B. W. von. Ueber die Gliederung der Bevolkerung
des Konigsreichs Bayern.

Hopkins, W. On the External Temperature of the Earth and the
other Planets of the Solar System.

King, W. On the Occurrence of Permian Magnesian Limestone at
Tullyconnel, near Artrea, in the County of Tyrone.

Lamont. Denkrede auf die Akademiker Dr. T. Siber und Dr. G. S.
Ohm.

‘Loftus, W. K. On the Geology of Portions of the Turko-Persian
Frontier.

Lyell, Sir C. On the successive Changes of the Temple of Serapis.

Magnetical and Meteorological Observations made at the Observatory,
Bombay, 1852 and 1853. From the Hon. E. I. Company.

Marcou, Jules. Esquisse d’une Classification des Chaines de Mon-
tagnes d’une partie de l Amérique du Nord.

Le Terrain Carbonifére dans ? Amérique du Nord.

Notice sur la formation Keupérienne dans le Jura
Salinois.
Recherches Géologiques sur le Jura Salinois. Part 1.

A

Réponse 4 une Lettre de MM. Foster et Whitney sur
le lac Supérieur.

Résumé explicatif d’une Carte Géologique des Etats-
Unis et des Provinces Anglaises de ? Amérique du Nord.

Ueber die Geologie der Vereinigten Staaten und der
Britischen Provinzen von Nord-Amerika.
Parliamentary Report. Further Papers relative to the Discovery of
Gold in Australia. From Sir P. G. Egerton, Bt., M.P., F.G.S.

Payot, V. Catalogue de la Série des Roches de la Chaine du Mont
Blane, &e.

Perry, A. Note sur les Tremblements de Terre ressentis en 1854.

Prado, C. de. Mémoire sur la Géologie d’ Almaden, d’une partie de
la Sierra Morena; suivi d’une description des Fossiles qui s’y
reucontrent, par MM. de Verneuil et Barrande. From M. E.
de Verneuil.

Quenstedt, F'. A. Beitrage zur rechnenden Krystallographie.

—. Ueber Pterodactylus Suevicus im lithographischen

Schiefer Wiirttembergs.
VOL. <1)-—-FARD i 2F

404 DONATIONS.

Renevier, E. Dates de la publication des Espéces contenues dans
les Planches de la Conchyliologie Minéralogique de la Grande-
Bretagne, par J. Sowerby et J. de C. Sowerby.

Résumé des Travaux de M. D. Sharpe sur le Clivage et la Foliation
des Roches.

Roemer, F. Ueber den Bau von Melonites multipora, ein Echinid
des Amerikanischen Kohlenkalks.

Suess, EH. Ueber die Brachiopoden der Hallstatter Schichten.

—. Ueber Meganteris, eine neue Gattung von Terebratu-
liden.

Tasmanian Contributions to the Universal Exhibition of Industry at
Paris, 1855. From Sir C. Lyell, V.P.G.S.

The Genesis of the Earth and of Man, edited by R. 8. Poole. From
the Author.

The Great Arctic Mystery, by ®IAOI ZYMBOYAEYOMENOI.
From the Authors.

Third Report of the Commissioners for the Exhibition of 1851.

Wallace, A. R. On the Law that has regulated the Introduction of
New Species.

Williams, D. H. A Geological Report on the Damoodah Valley.
From T. Oldham, Esq., F.G.S.

—. A Geological Report on the Kymore Mountains, the
Ramghur Coal-fields, and on the Manufacture of Iron, &e.
From T. Oldham, Esq., F.G.S.

Wiiiiams, S. A Reminiscence of G. A. Mantell, Esq., LL.D. ; with
an Obituary, by Prof. Silliman.

THE

QUARTERLY JOURNAL

GEOLOGICAL SOCIETY OF LONDON.

EDITED BY

THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.

VOLUME THE TWELFTH.

1856.

PART II. MISCELLANEOUS.

LAVATORY 1

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4 ‘4 - 1 i Vie ey
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CONTENTS OF PART IL.

Alphabetically arranged—the names of the Authors in capital letters.

Page
Alpine Trias, HoOERNES on some Gasteropoda from the............ 24
Alumina, Haver on a method of procuring ................000- 15
Argentiferous Galena of Pribram, Bohemia, Kiteszczynsky on the
Extraction of the Silver and Lead from the.................. 17
Banat, KuDERNATSCH on the Geology of ................00000- 23
BaRRANDE. On Silurian Fossils from Wossek, Bohemia.......... 15
PANale SCH, PMETIMICNE Olly ae elalle aca’ ess oe ca viicieessa cass 19
Benscu. - Onan Experiment on Basalt .. 2.0.0.0... cee eee eens 19
Bohemia (Central), JokELY on the Gneiss and Granite of ........ 5)
BrEITHAUPT. Ona Mineral Vein near Guadalajara in Spain...... 4
Carinthia, LipoLp on the Geology of the North-Eastern part of.... 1
Carlsbad, HocHsTETTER on the Thermal Springs of ............ 18
. on the Geology of the Environs of ............eeeeee 12

CaTULLO. On the Upper Sedimentary Deposits of the Venetian Terri-
tory, and on the Fossil Bryozoa, Anthozoa, and Sponges contained

TA CNN UE ee aN oS 05a, 2nci 0, che 0,045; 08wi oe 05 3¥% Soak ake 26
Cephalopoda (Jurassic), from Wurtemberg, OpPEL on some ...... 22
Cividale, HAUER on a Quicksilver-deposit near ..........-+..008- 8
Earthquake in Switzerland, NoEGGERATH on the..............4.. 9
Erzgebirge, VALLACH on a remarkable derangement of a Metalliferous

Berrien tno ere estore ats ascorirne ain 6 sins: oc al'e' 6) Sballoteys a’ sanshetsis: eral 0:0 18
Ferriferous Deposits of Hiittenberg in Carimthia, MUNICHDORFER

and Lipoutp onthe ..... SE eee Sheet. cee ie ae Sais hoe 2
Mossi ob Alistria,) LEBCK ET, OW, SHE- 5 ..0,050 vieseca ccs oe eee 6,6 we aye ie
Gasteropoda from the Alpe Trias, HoERNES on some............ 24
Geology of the Environs of Carlsbad, HocHsTETTER on the ...... 12

of the North-Eastern part of Carmthia, Lipoup on the ...... 1
Gneiss and Granite of Central Bohemia, JoKkELY on the .......... 5
Greece, on post-tertiary Shells from the coast of..........0022000 28
Guadalajara, Mineral Vem near, BREITHAUPT ON @.........0000. 4
Haver. Ona method of procurmg Alumina........ Pepe oe acne 15
——. Ona Quicksilver-deposit near Cividale.............s0008. Ree

oa OPAL Het ye PaeecE EOS Oba LAELITED sata: osinigs ai»: <'0' 0/0) 0/e) #6; bye oak thaliohaiaye 11
Hausruck, Upper Austria, HincGERAU on the Lignites of the ...... 16
HecKmen, On the Cosstlehistrot Anistria. i... 2.2.5 ou: «evom! a oy oragelal ote 12
Hincerav. On the Lignites of the Hausruck, Upper Austria .... 16
HocustettTerR. On the Geology of the Environs of Carlsbad...... ee

——. Qn the Thermal Springs of Carlsbad ..................+. 18

iv

Horrnes. On post-tertiary Shells from the coast of Greece ......
—. On some Gasteropoda from the Alpine Trias ..............
Hiittenberg in Carinthia, Minicuporrer and Lipo p on the Fer-
riferous Depasits Ofse.. gx «otmtgoyeiinsins ¢< st iks <ey Se
Johnstonite; trom Transylvania .42:...... 0.0. cae 0 4os se
JoxkéLy. On the Gneiss and Granite of Central Bohemia ........
Junkerite, KENNGOTT OM ..4.0 04 oc bees s sues de sehen
Jurassic Cephalopoda from Wurtemberg, OPPEL on some ........
Kainach, Styria, RoE on the Lignite of
KENNGort:: On Fumleerit@ 0... ier iieintes A) «oasis vay oO
. On’ Piauzite from: Stymie. sc i.c:. «on 0's, 5.0 socks ool

. On remarkable Crystals of Quartz and Fluor-Spar..........
Kueszczynsky. On the Extraction of the Silver and Lead from the
Argentiferous Galena of Pribram, Bohemia..................
KupDERNATSCH. On the Geology of Banat

Lignite of Kainach, Styria, ROLEE on the ...... 20.20.6002 eneees
Lignites of the Hausruck, Upper Austria, HINGERAU on the ......
Lipoup. On the Geology of the North-Eastern part of Carinthia .
Lithia, Haver on the, prepatiationid£ ©.) sic. so ciea.uihle ts alee ee
Lower Greensand and Blackdown Fossils of England, RENEVIER on
TG onn:aiis 5's aeiabpspplepabs safe mcats PIE spetaiele Goltuenes es -ayietaned et ual a

Metalliferous Veins of Pribram, Bohemia, Reuss on the ..........
Mineral Vein near Guadalajara in Spain, BREITHAUPT ona.......
MiunicHporFrer and Lipoutp. On the Ferriferous Deposits of Hiit-

tenberg, im, Camnthiay! o5.500% ae%h sitet devs We ald.
NoEGGERATH. On the late Earthquake in Switzerland...........
OprEeL. On some Jurassic Cephalopoda from Wurtemberg........
PaTERA. On the Extraction of Silver, Cobalt, and Nickel from the

Juachimstial’ Sifver-Ores' oo. 3c. <<... ep sem rieet oe ee
Piauzite from Styria, SOENNGOTT OM... es ee ee a oe ones
Post-tertiary Shells from the coast of Greece, HOERNES on........
Pribram, Bohemia, Reuss on the Metalliferous Veins of ..........
, KEESZOZYNSKY on the Silver-ores Of ...0........ 2. aus

Quartz and Fluor-Spar, KENNGorT on remarkable Crystals of ....
Quicksilver-deposit near Cividale, HAUER On &..........0.-0000:
RENEVIER. On the Lower Greensand and Blackdown Fossils of

Pima siete 57s 5 = Paw aia so ole a selesel bo bon ores owe As 6 eee er
Reuss. On the Metalliferous Veins of Pribram, Bohemia..........
Rout.’ On the Lignite of Kaindcht, Styrid... 3. cece soe ss ee

Silurian Fossils from Wossek, Bohemia, BARRANDE on ..........
Silver-ores, PaTERA on the Extraction of Silver, Cobalt, and Nickel

front the Jaatimmsihal Sos. das oe ie ets 0 ons 2 +
Styria, Kuneormom Pruzite (Om 0 ae cp os => +s es
Switzerland, NoEGGERATH on the Earthquake in...............

Tertiaries, CATULLO on the Venetian, noticed ..............02%
Thermal Springs of Carlsbad, HocusrTerrer on the .......... ate
Transylvania, Jolnistomipe monn 0101.0 T cece se og eos ee eee
VaLuaAcH. On a remarkable derangement of a Metalliferous: Vem in

the Erzgebiree: 5 tetany = apdionecs: Atinie oie1st> slinenalt are aa
Venetian Tertiaries, CATULLO on the, noticed..........-..-eseee

Wossek, Bohemia, BARRANDE on Silurian Fossils from ..........
Wurtemberg, OpPEL on some Jurassic Cephalopoda from.........

ceecere rere ee oreo eee ere we ee

———

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the Grouoey of the NoRTH-EASTERN. PART 0f CARINTHIA,
By M. V. Livoxp.

[Proceed. Imp. Geol. Instit. Vienna, March 6, 1855.]

M. Bovz’s supposition that eocene strata exist near Guttaring,
N.E. of St. Veit; was confirmed by Von Hauer’s examination of the
organic remains found in that locality. Still more recently M. Hoernes
has determined among the Guttaring fossils fifteen species peculiar
to the lowest portion of the eocene formation, and strikingly agreeing
with those of the Val di Ronca.

This formation appears in the basin of Guttaring, and forms the
ridge separating this basin from the Goerschitz valley, and another
ridge separating it from the vicinity of Althofen, without advancing
as far as Althofen or into the Goerschitz valley itself. It also appears
in some isolated patches at the Dachberg, 8.E. of Althofen, near
Kappel, and at the Piemberg, W. of Klein St. Paul.

The strata succeed each other, in ascending order, as follows :—

Clay, unfossiliferous.

Marls and limestones, with fossils and beds of coal.
Sands, white and yellow.

Nummulitic limestone and sandy strata.

The nummulitic limestone of the Piemberg contains numerous
Echinoderms.

The eocene strata on the northern slope of the Guttaring basin
rest immediately on argillaceous mica-slate; those on the south
slope, together with those at the Piemberg and Dachberg, rest on
cretaceous deposits.

Lignites are found in them near Kappel and on the Somberg,
where they are worked. The four coal-beds on the Somberg (the
largest of them being scarcely 5 feet thick) are separated from each
other by beds of marl-slate and limfestones, abounding in Bivalves.
The irregularities of the course and shape of the coal-beds denote
considerable disturbances in the includinz strata.

The eocene beds on the north slope of the Guttarmg basin dip
conformably to the south ; those on the south slope have a north-

‘VOL. XII.—PART Il. B

Z GEOLOGICAL MEMOIRS.

ward dip. Generally the eocene deposits of North-eastern Carinthia
are of no considerable extent, and their thickness does not exceed
800 feet.

The cretaceous deposits occupy a far more considerable range in
this region. M. F. von Rosthorn was the first who referred the
Rudista-beds between Althofen and the Mannsberg to the Cretaceous
formation. M. M. Lipold found confirmation of this both in the
Rudista discovered at Mount Calvary near Althofen, on the Zenns-
berg, and on the Reinberg, near St. Paul; and in the petrogra-
phical agreement of the Althofen strata with the known cretaceous
rocks of Upper Austria, Salzburg and Styria,—especially with the
cretaceous marble of the Untersberg near Salzburg.

Limestones, i beds 3 feet thick, predominate among the creta-
ceous deposits of N. E. Carinthia, marls and sandstones also occur-
ring. Near the base of the formation, breccias of calcareous or
schistose rocks are met with.

Besides the Rudista, some species of Corals and undetermined
specimens of Bivalves were found in the limestone by M. Lipold.

The range of hills separating the valleys of Goerschitz and the
Silberbach, and running from Althofen and Guttaring (on the north)
to Eberstein and Mannsberg (on the south), is wholly composed of
cretaceous rocks. Isolated portions occur at the Zennsberg, N.E.
of St. Georgen on the Langsee, S. of Silberegg, near M. Wolschert
on the right bank of the river Gurk, and on the left bank of this
river at Wieting and Unter St. Paulin the Goerschitz valley. Besides
at these localities, cretaceous rocks appear in the lower Lavant
Valley at the Reinberg, E. of St. Paul, near St. Martin, S.W. of
St. Paul (where they reach as high as the pass leading to Eis), and
between Lavamiind and Unter-Drauburg, near Rabenstein, in the
shape of rocky cliffs rismg amidst the surrounding gravels.

Cretaceous strata have been found resting both on Werfen and
Guttenstein strata (Unter St. Paul, Mannsberg, Zennsberg, St. Paul
in the Lavant valley), and immediately on grauwacke-slate and argil-
laceous mica-schist (Wieting and Althofen). M. Lipold estimates
the thickness of the cretaceous deposits as not exceeding that of the
eocene (800 feet). (Count M.]

On the Ferrirerovs Derosits of HUTTENBERG im CARINTHIA.
By MM. Frep. Minicuporrer and M. F. Lrpoup.

[Proceed. Imp. Geol. Instit. Vienna, March 13, 1855.]

Tue rocks of the district are gneiss, mica-schist, argillaceous mica-
schist, clay-slate, crystalline limestone, amphibolic gneiss and slate,
and eclogite. Mlica-schist predominates near the mountain ; and cal-
careous and amphibolic rocks appear only as subordinate layers in
it. The calcareous beds are of particular importance, the iron-
ores being exclusively confined to them. The gneiss includes one of
these beds, and there are four in the mica-schist. They are parallel

MUNICHDORFER AND LIPOLD—IRON ORES OF CARINTHIA. 3

to each other; striking S.K. and N.W., and dipping conformably
with the stratification of the surrounding crystalline slates. The
thickness of these calcareous strata is from 360 to 2400 feet; and
they are separated from each other by masses of slates 600 to 2400
feet in thickness.

The iron-ores are chiefly met with as lenticular masses, forming
regular beds in the lowest calcareous stratum (nearly 2400 feet thick),
belonging to the mica-schist. The ferriferous beds of the principal
ore mountain are distinct from those of the other mountain; the
former are again subdivided, on account of their occurring either in
the Hiittenberg or in the Lolling district. There are altogether
twenty-four of the ore-bearing deposits at present opened at twelve
distinct levels, the maximum vertical distance of which is 600 feet.
These deposits have generally a lenticular. shape, and are dispersed
through the whole of the respective limestone beds, without any
visible mutual connexion. They disappear gradually, or lose their
integrity, or even pass insensibly into sterile carbonate of lime (pure
or magnesian [Rohwand]), both in their length and their depth.
Les are sometimes also cut off by strata of the including crystalline
Slates.

The average longitudinal extent of these ferruginous deposits is
from 600 to 1200 feet; their thickness is from 24 to 30 feet. In
one instance the length is as much as 2040 feet; while in other
places it diminishes to from 120 to 180 feet, the thickness then
amounting only to 3 or 4 feet.

The continuity of the deposits of ore is occasionally interrupted by
sterile masses of crystalline limestone or of mica-schist; and derange-
ments and irregularities of direction and thickness are not uncommon.
They generally extend 8.E. and N.W., and dip to the S.W. at an
angle of 45° to 50°; in each respect conformably with the including
limestone.

Sulphate of barytes is a constant attendant to these iron-ores,
either in the shape of masses or layers, or mtimately mixed with the
ore. Sometimes also it occurs in beds 2 or 3 feet thick. The purest
ores occur associated with this mineral, which is worked for the use
of the white-lead manufactories.

The iron-ores are smelted in the blast-furnaces of Lolling, Heft,
Mosinz, Eberstein, and Treibach, and are either carbonate of iron
(“white ores”’), or fibrous and compact hydroxides of iron (“ brown
ores”), or oxide of iron (“blue ores’’), or decomposed ochrey
hydroxide of iron (“ Motte’’), or, lastly, very poor carbonate of iron
(‘“‘Rohwand”’). Generally the blue ores predominate in the highest
levels ; brown ores in the middle ; and the white ores in the deepest.
Spheroidal masses of fibrous or compact hydroxide of iron, either
having a central cavity, or enclosing a nucleus of carbonate of iron,
frequently occur on the level of the Lélling chief-gallery, and seem
to owe their origin to a process of decomposition from without
inwards.

Other minerals occurring in these iron-deposits are skorodite (arse-
niated iron), caleareous spar, stalactitic arragonite (flos ferri), man-

ae

4 GEOLOGICAL MEMOIRS.

ganese-graphite, quartz, chalcedony, several ores of manganese, the
variety of arsenical pyrites known under the name of “ Leellingite,”
and grey sulpho-antimoniate of copper.

In M. Miinichdorfer’s opinion, the ferriferous deposits of Hiitten-
berg are of contemporaneous origin with the associated crystalline
limestone, and have not resulted from injections or sublimations.

M. Lipold, who surveyed this district in the summer of 1854,
remarks that it is a mistake to suppose that all the deposits of iron-
ore occurring on the southern slope of the Carinthian Central Alps
belong to one and the same formation or ferriferous zone. Geological
investigations have shown the necessity of a separation between the
western deposits (Kremsgraben near Gmiind and Turrach) from the
eastern ones (Hiittenberg, Walch, &c.). MM. Stur and Peters have
proved that the western group belongs to the lowest portion of the
Carboniferous formation ; while the eastern group is always enclosed
in crystalline slates, such as mica-schist, gneiss, &c. Moreover, the
former is due essentially to pyrites and hydroxides of iron, and their
decomposition ; while the latter has for its constituent mineral the
carbonate of iron, partly reduced to the state of brown hydroxide.

The geodes (Kernerze), described by M. Minichdorfer, are of
great service in the illustration of the origin of the ferrugimous
deposits and of the changes they have undergone. MM.von Haidinger
and A. von Morlot have proved that the carbonate of iron is pro-
duced by a catagenic (reductive) process going on at great depths ;
in opposition to the anagenic (oxidating) origin of the hydroxide of
the same metal, caused by the influence of air and water, where they
have access to the ferriferous deposit. Observation on a larger scale
has confirmed this explanation ; the carbonate of iron occupying the
deeper parts of the ore-mountain of Hiittenberg, which are mac-
cessible to air and water; while the hydroxide is found nearer to the
surface. The presence of red oxide of iron at the highest level may
depend upon particular circumstances, deserving further investigation.

[Count M.]

MiIneERAL VEIN near GUADALAJARA 7a Spain. By A. BreiTHavupt.

[Leonhard u, Bronn’s N. Jahrb. f. Min. u. s. w. 1855, p, 705; and Hartmann’s
Berg- u. Hiitten-mann. Zeitung, 1854, 2, p. 9.]

Tue formation of the main lode in the mining district of Hiendelaen-
zina near Guadalajara, in Spain, agrees very much in its characters
with that in the Neue Hoffnung Gottes mine at Braunsdorf near Frei-
berg. Quartz is the oldest member, and partially massive. With
the silver minerals,—sulphuret of silver and antimony (schilfglaserz,
freieslebenite), crystallized, and even in compact masses, red silver
(rothgiiltigerz, pyrargyrite), compact and crystallized, and miargy-
rite, as yet found only im a compact form,—occur bournonite and
galena. In the shallow levels, which especially carry galena, ear-
bonate of lead and sulphate of lead also occur. [T. R.J.] -

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the GNeiIss and GRANITE 0f CENTRAL BOHEMIA.
By M. Joxéty.

* (Proceed. Imp. Geol. Instit. Vienna, March 13, 1855.]

Durine the summer of 1854, M. Jokély exammed the gneiss and
granite mountains around Millotitz in Central Bohemia. The gneiss
occurs only at the southern extremity of the district in question, and
forms the extreme northern termination of the gneissic group of
Southern Bohemia. It constitutes an elevated plateau of slightly
‘undulating country, only in a few localities attaining more than the
average altitude of 1500 feet. The strike of the gneiss corrésponds
with the boundary-line of this formation ; the dip is between N. and
'W., so that it plunges everywhere beneath the granite.

- The most conspicuous rock subordinate to this gneiss is granite ir m
the form of beds or veins. The granite beds, lymg conformably with
the gneiss, are connected with veins and masses of auriferous and
argentiferous quartzites, formerly the object of mining enterprise.

Granulite and amphibolic slates appear locally. Patches of ter-
tiary sand, clay, and gravel, overlying the gneiss, at altitudes of as
much as 1400 feet, occupy a larger extent of surface. These deposits
were once connected with the tertiary freshwater basin of Wittingau,
at the N.W. extremity of which they form a bay.

Alluvial deposits and kaolin, resulting from the decomposition of
granitic rocks, are the most recent formations within the district
under notice.

The granite prevails within the district; its surface is highly ae
latiag ; the average elevation.is 1800 feet some isolated cones attain
a height of 2500 feet. The chief varieties of the granite are granitic
gneiss, more or less fine-grained true granite, micaceous granite, and
porphyritic granite, which as they nearly everywhere contain par-
ticles of amphibole, may also be called amphibolic granites.

Subordinate to the granite are granites in beds or in veins with
quartzites, and amphibolites with diorites and porphyries. The
stratiform granites, lithologically identical with the fine-grained light-
coloured granites of the gneiss, are especially frequent in the eastern
portion. of the district ; their strike is between*N.E. and E., and

VOL. XII.—PART II. c

6 GEOLOGICAL MEMOIRS,

they are of some importance from their association with metalliferous
quartzites.

The amphibolites, of variable granular texture, and always con-
taining some oligoklase, occur in mass, especially around Ob- and
Unter-Huip, Milin, and Brezuitz. The diorites accompany them as
beds or veins ; and, from the conditions of their association and their
transition one into the other, the diorites and the including amphi-
bolites appear to have been contemporaneous in their origin.

The porphyries are all quartziferous and euritic ; the granitic and
biotitic varieties are the most extensive; true euritic porphyries
being only subordinate. The last, only locally mterspersed with
quartz, and frequently composed of unmixed eurite, may be regarded
as a compact, finely crystallized variety of stratiform granite.

Granitic porphyries differ from porphyroid granite only by their
fundamental mass being compact and more or less fine-grained. This
variety of porphyry, which is met with only in a few localities, is
generally associated with micaceous (biotitic) porphyry, characterized.
by containing exclusively the variety of mica named “‘ biotite.’ Ac-
cording to M. Grailich, the apparent optical angle of the biotite is
very small, varying between 0 and 3°. The biotitic porphyries are
bedded, with a strike between N.E. and E., and form distinct zones,
exclusively confined to the granitic mass, enclosed between two areas
of clay-slate, and quite wanting in the rest of the granitic district.

The metalliferous minerals of the granitic district are not of
importance, the working of gold- and silver-ores in the light-coloured
bedded granite and the biotitic porphyries having been long since
abandoned. At present workings are carried on in the silver-ores
and red oxide of iron in the amphibolites of Ober-Lichnitz and Sh-
witz, and the antimony-ores of the biotitic porphyry of Mitteschau.

[Count M.]|

On the Extraction of S1LvER, CoBALt, and NicKkEt from the
JOACHIMSTHAL SILVER-OrzEs. By M. Patera.

[Proceedings Imp. Geol. Institute, Vienna, November 6, 1855. ]

In simultaneously extracting silver, cobalt, and nickel from the
rich ores not long since discovered in the Joachimsthal Mines *, in
Bohemia, M. Patera first roasts the ore in an atmosphere of aqueous
vapour, to prevent loss by. the escape of gases and volatilization ; the
roasted ore is then placed in wooden tubs and treated with moderately
diluted sulphuric acid, mixed with some nitric acid, at a high tempe-
rature. Nearly the whole of the silver, cobalt, and nickel is dissolved ;
and the solution contains also some iron, copper, and arsenic. The
silver is then precipitated by means of a solution of sea-salt ; the chlo-
ride obtained, reduced by iron and smelted, gives a silver of great
purity. The arsenic is separated by the addition of chloride of

* See also Quart. Journ. Geol. Soc. vol. xi. part 2, Miscell. p. 37.

ROLLE—LIGNITE OF KAINACH, STYRIA. 7

iron, and by neutralizing the solution with carbonate of lime ; basic
arseniate of iron is precipitated, together with an excess of oxide of
iron, the solution remaining free of arsenic and iron. The cobalt
is precipitated from the neutral solution by a solution of subchlorate
of lime ; and afterwards the nickel, in the state of hydrated oxide,
by the addition of caustic lime. This oxyhydrate undergoes drying
and heating to redness ; it is then ground to a fine powder, brought
to a tenacious consistence by means of black meal and syrup, cut
into cubical pieces, and again submitted to a red heat. The nickel,
so reduced to a metallic state, preserves the cubical form, if the
oxide had the proper degree of purity. Some of these nickel cubes
were analysed by M. Wisoky, who found only 14 per cent. of other
metals, with a trifling proportion of cobalt.

From Karl von Hauer’s analysis * of the nickel extracted by M.
Patera from the rich silver-ores of Joachimsthal, it appears that 100
parts of this nickel contain

Nel) Sa. eee: ote 86°
1

Sulphur 62 2% 45%
EHOA, Set ores
Copper............ very slight trace.

Hence it may be regarded as equal, if not superior, in purity to
the best sorts produced in England and Saxony.
[Count M.]

On the Lignite of Karnacu, Styria. By Dr. Rowe.
[Proceed. Imp. Geol. Instit. Vienna, November 6, 1855. ]

Tue tertiary basin of the Kainach Valley in Styria, West of Gratz,
follows the course of the rivulets Gaessnitz, Lankowitz, Graden, and
Kainach, forming a deep sinuosity in the crystalline rock district of
Central Styria. It is enclosed on the south and west by mica-schist,
gneiss, and transition-limestone, on the north by Gosau-sandstone,
and it communicates on the eastward with the basins of Southern
Styria and Hungary. Its average length is 4900 fathoms (10,163
yards), and breadth 1200 fathoms (2489 yards); so that its total
area embraces about 3 of an Austrian square-mile. The whole of
this surface consists of one lignite-bed, having a depth varying from
3 or 4 fathoms (6°222—8°3 yards) to 10 or 14 fathoms (20°74— —
29:04 yards). The bed is generally horizontal, or slightly undu-
lates; sometimes it has a dip of considerable steepness im the vici-
nity of the surrounding rocks of older date. Its thickness, generally
varying from 3 to 15 fathoms (6°222 to 31°11 yards), increases
sometimes even to 20 fathoms (41°48 yards), and averages not more
than 8 or 10 fathoms (16°59 to 20°74 yards). The lgnite-bed is

* Communicated to the Imp. Geol. Institute, Nov. 15, 1855.
Cz

8 GEOLOGICAL MEMOIRS.

here and there intercalated with sandy clay and shale; four such

layers, 3 to 1 foot thick, are known near Pibersteim. Near Voits-

dorf and Oberdorf the lignite is interrupted by a clay-bed 8 feet

‘thick ; the former having a thickness of about 6 fathoms (12°444
yards) above, and about 7 fathoms (14°52 yards) beneath, the in-
tercalated clay.

The bed of lignite immediately overlies either the older rocks

or a thin stratum of grey or blue plastic clay, loose sandy conglome-
Yate, or arenaceous clay. It is overlaid by greyish-blue clay, or
occasionally by some gravel or loam.

Generally the uppermost and lowest portions of the lignite-bed are
not worth working, and remain untouched.
The lignite preserves the texture of wood, rarely exhibiting bands

.of compact and shining coal. Thirty specimens, from different loca-
lities, examined by Chev. Ch. de Hauer in the laboratory of the

Imp. Geolog. Institute, gave Ash 3°43 per cent., Water 13°68 per
cent.

In its heat-producing power, 13°48 ewt. of the lignite (123-4 pounds
avoirdup.) are equivalent to one klafter (100°401 cubic feet) of fir-
wood in logs of 30 inches length. The lignite, leaving very little
ash, and containing no sulphur, is fit for general technical use ; and is
in this respect equal to tertiary coal in general.

Supposing the average thickness of the bed to be not less than

6 fathoms (12°444 yards), it may be estimated, from the extent of

its area, to contain above 3400 millions ewt. of fuel. It has long
been worked ; the official lists of 1852 enumerate nearly fifty persons
working it. The produce in 1853 amounted to 350,990 ewt., worth
33,717 florins (about £3507 sterling); it was nearly all sold at
Gratz at the price of from 24 to 28 kreutzers* for 123-4 pounds
avoird. ; the carriage of 123°4 pounds costing from 18 to 20 kreutzers.

Recently a mining company has been formed to work an area of
884,595 square fathoms, estimated to contain above 760 millions ewt.

-of fuel. A privilege for the construction of a railroad within two
years from Gratz to Koeflach, a distance of 20,313 fathoms (above

23°57 English miles), has been lately granted to this newly esta-

-blished company. [Count M. |

On a QUICKSILVER-DEPOSIT near CIVIDALE.
By Chev. von HAvER.

[Proceed. Imp. Geolog. Instit. Vienna, November 13, 1855.]

-In the spring of 1855 some marl containing globules of native
‘quicksilver was found near Gagliano, near Cividale, in the province

of Eldine [Venetian Lombardy]. It was discovered in the cellar of

-a house which was built on a hill, a few feet high, S.S.E. of Gagli-

ano. The rock is at present dug to the depth of about 2 klafters

-(4:148 yards), and does not differ from the common variety of ma-

* The Austrian florin=60 kreutzers=£0°104 sterling.

NOEGGERATH—EARTHQUAKE IN SWITZERLAND. 9

cigno ; its strata dip S.W., at an angle of 24° to 30°. The mercury
appears to be disseminated irregularly over a space of probably very
narrow horizontal extent ; no trace of the metal being found im a
trench dug outside the house. It does not seem, however, to be
confined exclusively to one spot, as several instances of its occur-
rence around Cividale, both in ancient and modern times, have been
recorded. : :

The macigno of Cividale and the beds of solid calcareous sand-
stone (quite analogous to the “granitic marble’? of the lower
Bavarian Alps) are thought by Chev. de Hauer to belong to the
eocene nummulitic formation, notwithstanding that some few rolled
fragments of Hippurites have been here and there imbedded in the
sandstone. :

The recently discovered mercuriferous drift-deposits, such as those
of Sulbeck near Luneburg, &c., found by Prof. Hausmann,—those of
Illye, west of Deva in Transylvania, mentioned by M. Grimm,—the
deposits of Lisabon and Montpellier, known some time since, &c.,
bear some resemblance to the deposit of Gagliano, but nevertheless
differ from it in several essential particulars. - :

The deposit at Sulbeck seems to have belonged originally to a
block of sandstone washed into the drift with other fragments, and
subsequently totally disintegrated. This explanation is not appli-
cable to the mercuriferous marl of Gagliano, the constituent par-
ticles of which were evidently carried to their present site as minute
grains and not in blocks. Two other quicksilver-deposits in. Tran-
sylvania, mentioned by M. Grimm (Baron Hingenau’s ‘ Austrian
Mining Journal,’ 1854, No. 35), although not yet fully understood,
seem to bear a closer analogy with that of Gagliano. Springs issuing
from the Carpathian sandstone near Esztelek, north of Keydy Vasar-
hely, in Transylvania, and near Neumarckt, in Galicia, are said to
carry sometimes with them globules of mercury, especially after
violent thunder-storms. This fact, together with the existence of
the cinnabar-mines of Dumbrawa and Baboja, near Zalathna, is a
proof that mercury aud its salts are to be met with in the Carpathian
sandstone of other regions; although, according to M. Grimm’s
statements, the mercury and cinnabar deposits of Idria, together
with the cinnabar-ores of the Pototschnigg ravine, in Upper Carniola,
according to M. Lipold, are subordinate to the carboniferous group.
At all events the mercury of Gagliano may prove to be wortn work-
ing on scientific and economical principles. [Count M.]

On the late EARTHQUAKE in SWITZERLAND.
By Prof. NozEGGERATH.

[Proceed. Imp. Geol. Instit. Vienna, November 13, 1855.]

In September 1855, Prof. Noeggerath - visited the Visp Valley:
(Vallée de Viége), Canton de Valais, in order to study the effects. of,

10 GEOLOGICAL MEMOIRS,

the recent earthquake. The Visp Valley is one of many descending
from the crest of the Valais Alps (the Monte Rosa group) to the
Valley of the Upper Rhone. It consists entirely of crystalline, with-
out any trace of volcanic rocks.

The subterranean commotions, so frequent in these parts during
the summer of 1855, extended their destructive effects as far as Sion
(Sitten) in the Rhone Valley ; their greatest activity, however, was
concentrated about Vispbech (Viége), at the entrance of the valley,
Stalden, and St. Nicholas ; so that the centre of the earthquake-action
may be supposed to have existed between these three localities.

Nearly all stone-buildings were more or less damaged or destroyed,
and most of the churches were so much injured by fissures as to
necessitate their being pulled down. The rocks also exhibit recent
crevices from 3 to 6 inches wide. Everywhere numerous new springs
of water have made their way to the surface, whilst formerly existing
springs have disappeared.

Nearly all the devastation suffered by buildings is the effect of
a single strong commotion, which took place on July 25, 1855,
before one o’clock p.m. The subsequent movements had but sub-
ordinate effects, although they had not ceased in September, and
occurred at intervals as late as October. The line of greatest energy
extends from N.N.W. to 8.8.E., for a distance of six hours (about
14 English miles). The earthquake of July 25 was felt through the
whole of Switzerland, the Savoy Alps, Lombardy, part of France,
Baden, Wirtemberg, Bavaria, and the Hessian territories.

[Count M.]

* JoHNSTONITE from TRANSYLVANIA.
[Proceed. Imp. Geol. Instit. Vienna, November 13, 1855.]

Baron CzoERnNING lately presented to the Museum of the Imperial
Geological Institute of Vienna some specimens of a mineral, disco-
vered in M. G. Hoffmann’s lead-mines of Neu-Sinka, near Fogaras,
in Transylvania, to which the discoverer had given the name of
‘‘Sinkanite.””? This mineral is a mechanical mixture of galena, an-
glesite, and sulphur. In one of these specimens, white compact
anglesite (sulphate of lead) traverses, in the shape of veins, a dark-
grey compound of sulphur and galena, being itself intersected with
delicate fissures filled with sulphur. This specimen shows evidently
the mode in which decomposition is gradually proceeding ; the sul-
phuret of lead disappearing, and sulphate of lead with sulphur re-
maining as a residuum.

The mineral substance in question was first found at Dufton and
described by Mr. Johnston. Subsequently M. Haidinger named it
«< Johnstonite.’’ The Transylvanian variety has been described by
M. Haidinger, von Hauer, and R. Hoffmann (Jahrb. Imp. Geol.
Reichsanst. 1855). Another variety was found several years ago
in the Rhine Provinces by Professor Noeggerath, whose views con-
cerning this substance are identical with M. Haidinger’s. It occurs,

HAUER—PREPARATION OF LITHIA. oH |

associated with unaltered galena, some sulphate of lead, and a small
quantity of sulphur in a vein near Musen, in the Siegen mining-
district, and is known among the miners by the name of “ burning-
galena.”’ [Count M.]

On the PREPARATION of Lirnia. By Chev. K. von Haver.
[Proceed. Imp. Geol. Instit. Vienna, November 13, 1855.]

Tue author in this communication explained his new method of ob-
taining lithia in large quantities and at a comparatively low price.
The metallic base of the lithion-alkali was discovered in 1817 by M.
Arfvedson, in the laboratory of the celebrated Berzelius. As far as
we at present know it occurs only in mineral substances, especially
in petalite, lithion-spodumen, amblygonite, triphyline, apyrite, tour-
maline of Utoen, and lepidolite. All of these contain rather con-
siderable quantities of lithia, but occur rarely, except lepidolite,
which, although proportionally poorest in lithia, is met with in great
quantities at some localities. The Austrian Empire, possessing in
some places great stores of minerals scarce elsewhere,—such as tel-
lurium, in Transylvania, uranium, in Joachimsthal, &c.—has also a
considerable mass of lepidolite in Mount Hradisko near Rozna in
Moravia, where lithia-mica, in association with granite-veins, is im-
bedded in gneiss.

M. Foetterle, having brought with him last summer a quantity of
this mica, afforded the laboratory of the Geol. Institute an oppor-
tunity for experimenting on the production of lithia. The methods
hitherto known for extracting this substance requiring great expense
of money and time, it ranks amongst the rarest and most costly of
chemical preparations.

M. K. von Hauer tried the use of sulphate of lime, a substance
obtainable at a very low price. Lepidolite, finely pulverized, is mixed
with an equal weight of powdered gypsum, packed into hessian cru-
cibles, and submitted to a red heat for some hours. The firmly
agelutinated mass is comminuted after cooling, and thrown into hot
water, for the purpose of dissolving the sulphates of potash, lithia,
and manganese produced by the mutual action of the lepidolite and
gypsum. ‘The solution, concentrated as much as possible by evapo-
ration, deposits partly its sulphate of potash. Manganese and a
small residue of gypsum are precipitated by sulphuretted ammonia
and oxalate of ammonia. The remaining solution, having been filtered,
contains only sulphates of potash and lithia, and is treated with
soda, for the purpose of precipitating the lithia in the form of an
insoluble carbonate. The precipitate so obtained, when filtered and
washed, contains only an insignificant portion of carbonate of soda.
It may be reduced to a state of chemical purity by solution with
hydrochloric acid; and precipitation by carbonate of ammonia.

One hundred parts of Rozna lepidolite, thus treated, give three
parts of carbonate of lithia, answering to 1*1 part of the pure alkali ;

12 ; GEOLOGICAL MEMOIRS.

and, as Prof. Rammelsberg found in lepidolite 1:3 per cent. of lithia,
the loss in operating on a large scale may be considered as trifling.
The expenses of this new method exceed scarcely the cost of the fuel
consumed.

Hitherto lithia has had no technical use except in fire-works, bene
mixed with combustible matter to communicate to the flame a beau-
tiful carmine tint. But even for this purpose it could be but of rare
use, aS half an ounce cost from 8 to 10 florins set shill. to £1
sterling). [Count M.]

On the Fossit Fisn of Austria. By M. HEcKEL.
[Proceedings Imp. Acad. Sciences, November 16, 1855. ]

In continuation of his ‘ Contributions to the knowledge of the Fossil
Ichthyology of Austria,’ M. Heckel communicated a memoir contain-
ing :—1. A new arrangement of the Pycnodont family, together
with descriptions of twelve new or imperfectly known species: viz.,
two from the bituminous strata of the Karst, five from Dalmatia, two
from Monte Bolca, one from Cracovia, one from Mount Lebanon,
and one from Mont-Aimé, near Chalons-sur-Marne ; 2. Two new
species belonging to the family of Cheirocentri (still represented by
an existing species) ; one from the Karst and the other from Monte
Bolca ; 3. Three new species of the family L/opi, from the Karst ;
4. Two new species from Monte Bolea, dcanthurus Lanosse and.
Carangodes cephalus; one from Bude, Smerdis Budensis, and three
from the “ Calcaire grossier ”’ of the Leitha Mountains, near Vienna,
Lates Partschi (a Percoid), Labrus Agassizii, and L. parvulus ;
5. An extinct genus, with pectinated anterior branchial operculum,
—Ctenopoma ; represented by one species, C. Temelka.

(Count M.]}

On the GroxoGy of the ENvirons of CARLSBAD.
By Dr. HocusretrTer.

[Proceed. Imp. Geolog. Instit. Vienna, December 18, 1855. |

Since Becher made the first analysis of the Sprudel Spring (1770),
the chemical, mineralogical, and geological constitution of this water-
ing-place has attracted the attention of a great number of naturalists,
among whom Klaproth, L. von Buch, Struve, Goethe, Berzelius, von
Hoff, von Warnsdoff*, and Haidinger may be especially mentioned.

Klaproth (1790) attempted to explain the origin of the springs by
supposing coal-beds to have been in combustion, the heat having been
developed by the decomposition of pyrites. Berzelins (1823), struck
with the analogy between the environs of Carlsbad and the extinct
volcanoes of Auvergne and Vivarais, saw in these hot springs the last
and vanishing effect of primeval volcanic action. The question is

* See Quart. Journ. Geol. Soc. vol. xi. part 2, Miscell. p. 45.

HOCHSTETTER— GEOLOGY OF CARLSBAD. 13

now decided by Prof. Bischoff’s theory, and its experimental demon-
stration by Struve.

The controversy concerning the Carlsbad granites has not yet been
brought to a satisfactory conclusion. M. von Hoff (1825) con-
sidered the coarse-grained and the fine-grained varieties of Carlsbad
granite to have been contemporary in their origin; and this able ob-
server was the first who referred to the existence of a deep and broad
fissure, the result of volcanic action, and filled up with granitic brec-
cia. All the Carlsbad springs rise to day along this fissure, which
is known by the name of “ von Hoff’s line.”

M. von Warnsdorff (1846) considered the two varieties of granite
to have been produced at different periods, intimately connected with
the origin of the springs themselves, as these latter issue out exactly
on the limiting plane between the coarse-grained, or older, and the
fine-grained, or younger granite. The Schlossberg of Carlsbad is
not a granitic breccia, but a solid granite-mass, traversed with nume-
rous veins of silex deposited by the springs in the form of hornstone.
This opinion of M. von Warnsdorff’s is now pretty generally accepted,
as being confirmed by previous and later observers; but his views
relating to the different ages of the Carlsbad granites are still not
quite assented to.

Dr. Hochstetter, after a careful examination, came to the followmg
conclusion. The granitic rocks of the Tepl Valley, near Carlsbad,
form a portion of an extensive granitic mass, evidently of an eruptive.
character, stretching from Marienbad through the whole of the Carls-
bad mountains, and far into the interior of Saxony beyond the Erzge-
birg. This granite is undoubtedly younger than the crystalline
slates surrounding it, and is characterized by abundance of tin-ore.
It varies in its grain frequently throughout its range ; near Carlsbad
the fine-grained variety a prevails on the right bank of the River
Tepl, whilst the left bank is chiefly occupied by the porphyritic fine-
grained variety 6, which contains the well-known twin-crystals of
felspar of Elbogen. The bottom of the Tepl Valley, as well as the.
declivities immediately bordering it, are composed of a third variety
of granite, c, hitherto thought to be identical with @ or 6; but which
ought to be carefully kept distinct in thoroughly investigating the
geology of the Carlsbad district. The last-named variety has a por-
phyroid aspect, its chief mass being fine-grained like the variety a,
but having interspersed isolated crystals of felspar and quartz, or
larger aggregations of scaly mica. In other localities, for instance,
at Schellerhau near Altenberg, in the Erzgebirg, this variety passes
into genuine porphyry. Its component minerals are potash- and
soda-felspars, black and white micas (the last probably containing
litbia), and quartz, both crystallized and uncrystallized ; while the
variety 4 is a compound of potash-felspar, black mica, and quartz, _

The differences in the mode and. result of decomposition are still
more. striking. The varieties a and 6 easily decompose into gravel,
the large felspar-crystals of 6 remaining unaitered. In the variety e,.
the decomposition commences with these crystals, which are gradually
reduced into a yellowish-green steatitic or a reddish-brown earthy

14 GEOLOGICAL MEMOIRS.

substance; the principal mass of the rock offering considerable re-
sistance to the altering agents, as may be seen in the steep declivities
and in the columnar sharp-edged peaks around Carlsbad. The sur-
face of these rocks is full of cavities marking the places of the iso-
lated felspar-crystals now decomposed.

The varieties a and 0 are less liable to be divided by fissures,
caused by atmospheric agency, into masses with plane surfaces and
sharp edges than is the variety c. The River Tepl, as far as it runs
through the variety c, follows exactly the direction of these clefts or
fissures. When basaltic eruptions, very probably immediately con-
nected with the origin of the thermal springs, disturbed the rock-
masses of the Carlsbad territory, the deepest fissures, it is considered,
must necessarily have been formed in the variety c, on account of its
lithological constitution and the mode of its fissuring. This supposi-
tion may serve to explain why all the springs issue from the fissure
in the variety c. There is nothing to confirm the idea of a difference
of age among the granites; which is indeed rather contradicted by
the insensible transitions from one variety into another, and by the
presence of tin-ore in all the granites, even in and around Carlsbad.

Dr. Hochstetter distinguishes his three varieties of Carlsbad granite
by special names ; variety a is his ‘‘ Kreutzberg granite ;”’ var. 6 is
his “ Elbogen granite ;”’ and var. c his “‘ Carlsbad granite.” A map
of the territory of Carlsbad, by the author, on the scale of +

115209

is preparing for publication. [Count M.]

On Pianzite from Styria. By Dr. Kenneorr.
[Proceed. Imp. Geolog. Institute of Vienna, January 8, 1856.]

Tus mineral was first described by M. Haidinger m 1844*, as
a new species of fossil bitumen, to which he assigned the name of
Pianzite, indicative of the locality where it was first discovered. It
occurs at Mount Chum, near Tuffer, in Styria, under the same cir-
cumstances as at Pianze in Carniola. This new locality has been
made known by Chev. Pittoni de Dannenfeldt, of Gratz.

According to the communications of M. Wodiczka, Imp. Mining
Inspector at Cilli, the pianzite occurs, though only in small lumps
and very thin layers, in nearly all the mines by which the carboni-
ferous strata running westward from Tuffer, over Goufe and Hrast-
nigg, to Trifail and Sagor, are at present worked. Near Tuffer,
3000 Vienna pounds (3702 pounds avoirdup.) of this substance have
been brought to day.

The pianzite is a black resin, much resembling slaty and lamellar
black coal; its texture, never crystalline, varies from compact to
lamellar or scapiform ; its colour when scratched is light-brown. It
melts into a black mass, similar to pitch, at a temperature exceeding

* Poggendorft’s Annalen der Physik und Chemie, vol. Ixii. p. 275,

BARRANDE, FOSSILS FROM BOHEMIA.—HAUER, ALUMINA. 15

300° C.; and it burns with a bright and yellow flame, with a large
proportion of soot. [Count M.]

On StturR1AN Fossits from Wossex, BoHEMIA.
By M. J. Barranpe.

[Proceedings of the Imp. Geol. Institute of Vienna, January 8, 1856.]

AN interesting collection of fossils was made, chiefly during the sum-
mer of 1855, by the Austrian Geological Surveyors in the environs
of Rokitzan in the Silurian basin of Bohemia. These are of the
more interest as M. Barrande’s search for fossils in this locality had
been hitherto unsuccessful. The fossils were found at Wossek, N.E.
of Rokitzan, in M. Barrande’s “ Quartzite stage D,” and may be
regarded as belonging to the commencement of the Second Bohemian
Fauna. They are in a rather imperfect state of preservation and oc-
cur in very hard quartzose nodules, remaining on the surface of the
ground after the decomposition of the schists in which they were
originally imbedded.

M. Barrande recognized altogether 37 species among these organic
remains from Wossek, trilobites (13 species) bemg prevalent; and
only 5 of these 13 species have previously been found with stage D.
Cephalopods are very scarce ; there are only 4 species, and the spe-
cimens are generally badly preserved. ‘The Gasteropods are repre-
sented by 5 species, including the Ribeiria phodadiformis, Sharpe,
which occurs also in the Silurian rocks of Portugal. There are
3 species of deephala; one of them, Redonza, being also represented

in the Second Silurian Fauna of France.

The fossil fauna of Wossek also includes 4 species of Brachiopods
and 2 of Echinoderms. [Count M.]

ee

On a method of procuring ALUMINA. By Chev. von Haver.
[Proceedings of the Imp. Geol. Institute of Vienna, January 15, 1856.]

Pure alumina is best obtained from ammoniacal-alum, or from sul-
phate of alumina, wherever, as in Hngland, those salts are produced
on a large scale. At Vienna, however, where they are still scarce
objects of commercial transaction, chemists are obliged to operate on
potash-alum or on kaolin. The alumina extracted from the first of these
materials, even in quantities of a few pounds, requires long-continued
washing with hot water, sometimes during several weeks, to get rid
of the potash adhering to it. The kaolin requires hot concentrated
sulphuric acid for its decomposition, so that operations on a large
scale are very troublesome and difficult. The Imperial Geological
Institute received some time ago specimens of a very pure kaolin,
which forms a bed of about 6 joch (345°342 acres) between Znaim and
Brenditz, in Moravia. The quantity yearly raised is between 6000
and 8000 zentners (740,400 to 987,200 pounds avoirdup.), but may
be easily augmented, if required, to 20,000 zentners (2,468,000

16 GEOLOGICAL MEMOIRS.

pounds avoirdup.). A hundred pounds weight (123°4 pounds
avoirdup.) of this kaolin, carefully washed and refined, costs at Vienna
2 florins, 24 kreutzners (4 shill. 93 pence).

The analysis of the kaolin gave—Silica ...... 48°1 per cent.
BA a Pe Alumina... 38°6 e

ae ie Water <=... 13°3 s.

Lime and Oxide of Iron ... traces.

Chev. von Hauer attempted to decompose this kaolin by treating
it with gypsum under the influence of high temperature, this method
having proved successful with other mineral substances. The kaolin,
mixed with gypsum in a proportion adequate to the quantity of
alumina contained in it, was heated in a roasting-furnace to a moderate
red heat, so as to prevent the decomposition of the sulphate of alumina.
After this preliminary operation, the whole of the alumina could be
extracted by cold sulphuric acid very considerably diluted. The
water for elixiviation is to be mixed with no more acid than what is
strictly necessary (together with what is contained in the gypsum)
to form a trisulphate of alumina. The filtrated solution is adapted for
the production of chemical preparations containing alumina. As yet
this method has only been used in the laboratory ; but it may be ex-

pected to be profitably employed for technical purposes.
| [Count M.]

33

re

On the Lienites of the Hausrucx, Upper AvsTRIA.
By Baron HincERAv.

[Proceedings of the Imp. Geol. Institute of Vienna, January 15, 1856.]

Tue Hausruck-Wald is the eastern portion of the mountain-range
running between Mattighofen, Friedberg, Frankenburg, Voeklabruck,
Wolfregg, Haag, and Ried, along the frontier between the Hausruck
and Inn Circles.. The western part of the range bears the name of
Kobernauser Wald.

The succession of strata in the lignitic deposits of the Hausruck-
Wald (in descending order) is—

1. Gravel and conglomerates, 30 klafters (62°22 yards), and more
in places.

2. Sandy clay, 6 inches.

3. Lignite, 1 to 3 feet.

4. Argillaceous marl, known by the provincial name of “ Schhier,”’
variable in thickness, at Thomasroith 15 klafters (31-11 yards).

5. Lignite-bed, 2 klafters (4°158 yards).

6. Clay, with fragments of coal, variable in thickness.

7. Lignite-bed, 1 to 13 klafter (2°074—3°111 yards).

8. Bluish argillaceous marl, or ‘‘Schlier,”’ frequently occurring in
this part of Upper Austria, at a level of 1000 to 1800 feet above the
sea. Its fauna, judging from the fossils collected between Ottnang
and Wolfsegg, and determined by Dr. Hoernes, is analogous to that
of the Vienna “Tegel,” having a ‘“ Neogene’’ character.

KLESZCZYNSKY—SILVER AND LEAD FROM BOHEMIA. 17

The lignites above referred to are known at Vienna under the
name of ‘“'Traunthal coal,’ and are at present worked over a surface
of 6977 joch (17,240 acres). They yield from 19 to 22 per cent. of
water at a temperature of 100°C.: heated in closed ovens, they give
40 to 45 per cent. of coke; and, when burnt in the open air, they
leave 5 per cent. of ash. In a well-constructed heating-apparatus,
15-16 zentners (1851—-1974°4 pounds avoirdup.) are equivalent to
100°401 English cubic feet of fir-wood. The ashes of the lignite
have been successfully used for manuring moist meadow-land.

The total mass of this fossil fuel, as at present known from mining-
operations, may be estimated, at a moderate rate, as about 6 millions
of cubic feet, or 4 millions 800,000 zentners. [Count M.]

On the Extraction of the Sitver and Leap from the
ARGENTIFEROUS GaALENA of PrispRAM, Bouemia. By
M. Kieszczynsky.

[ Preceedings of the Imp. Geol. Institute of Vienna, January 22, 1856. ]

Tue ores of Pribram* are argentiferous galena, copiously mixed with
zinc-blende, carbonate of lime, and sulphate of barytes, together with
quartz, carbonate of iron, iron-pyrites, and grey copper in less pro-
portions. The separation of the blende from the galena is the chief
difficulty, as it cannot be brought about by a merely mechanical
means. The ores and “Schlichs” produced, during 1852, contained
an average of =4,, of silver and +4, of lead.

The operation for the extraction of the silver and lead begins with
submitting the ores to three consecutive roastings in the open air.
Recently the experiment was made of effecting the roasting in furnaces
by means of coal, and it succeeded in diminishing the expense. The
roasted ores are mixed with 5-8 per cent. of cast iron, 10-12 per
cent. of plumbiferous residuum from former smeltings, and 36—48 per
cent. of soft-iron-slags, for the purpose of facilitating the fusion and
to remove the superfluous sulphur, and are melted down in furnaces.
Each smelting requires about eighteen days, and is followed by a
‘cleansing and repairing of the furnace. The substances obtained by
the operation are argentiferous lead, cast into iron moulds (with
about 3 per cent. of silver, slags, furnace-dust, and concretions
[Gekraetz]). The lead-cakes are melted down on a flat circular
bellows-furnace, with an artificial marl-sole, on which, as a final re-
sult of the operation, is left a cake of pure silver, the oxidated lead
running out of the furnace or being imbibed into the marl-sole. The
silver, after having been completely purified from all trace of hetero-
geneous substances by undergoing fusion in crucibles, with a mixture
of wood-ashes and burnt bones, together with some borax and salt-
petre, is finally cast into the form of bars.

* See Quart. Journ. Geol. Soc. vol. xi: part 2, Miscell. p. 40.

18 GEOLOGICAL MEMOIRS.

The impure or black oxide of lead (litharge) is again melted down
to obtain argentiferous lead and slags. These slags are again melted
down for lead, and this is repeated until the slags are worthless.
The purer sort of litharge is either sent away to be sold, or is added
to the ores to be smelted with them, or submitted to a peculiar fusion,
with results analogous to those of the smelting of the black sort.

The total of the substances submitted to metallurgic operations in
the course of the year 1852 amounted to 74,637 cwt. of ores and
19,880 cwt. of argentiferous substances, together holding 35,111
marks of silver and 33,985 cwt. of lead. The loss was 64 per cent.
of silver, and 36 per cent. of lead. [Count M.]

On a REMARKABLE DERANGEMENT 0f a METALLIFEROUS VEIN in
the Erzcesirc. By M. Vauacnu.

[Proceedings of the Imp. Geol. Institute of Vienna, January 22, 1856. ]

Tue Gellnau tin-vein, in the Schlaggenwald tin-mines, about 3 inches
thick, and dipping S8.E. at an angle of 40°, and another secondary
vein, dipping S.H. at an angle of 95°, traversing the chief vein and
deranged by it, are cut through by three argilliferous fissures, 7 to 4
inch wide, dipping N.W. at an angle of 50°, and 5 inches distant
from each other. The two exterior of these fissures have included,
and, as it were, lifted up, a portion of the chief vein, about 10 inches
long; while the middle fissure went through the same vein without
causing or suffering any derangement. Above the point of disturb-
ance, the three fissures unite into one, cutting through the secondary
vein and bending it upwards. Similar derangements are not rare in
the numerous stanniferous veins running in all directions through the
crystalline rocks of the Erzgebirg. [Count M.}

On the THERMAL SPRINGS of CarRusBaAb. By Dr. Hocusrerrer.
[Proceedings of the Imp. Geol. Institute of Vienna, February 14, 1856. ]

In this communication Dr. Hochstetter stated the results of his in-
vestigations on the situation of the fissures from which the thermal
springs of Carlsbad* take their rise. Hitherto all these springs have
been regarded as coming from the same fissure, namely that known
as “ Von Hoff’s line,” running in an.average N. and S. direction.
M. von Hoff (1825) considered the Schlossberg of Carlsbad to be
a granitic breccia filling up this fissure. M. von Warnsdorff (1846)
proved the Schlossberg to be of solid granite, traversed by a great
number of veins of hornstone, and declared the fissure known as
“Von Hoff’s line,” to be identical with the plane of contact between
two granites of different age.

* See Quart. Journ. Geol. Soe. vol. xi. part 2, Miscell. p. 45; and above, p. 12. .

° rer Oo

BENSCH— EXPERIMENT ON BASALT. 19

The author had viiocly proved (Meeting of the Imp. Geol.
Institute, Dec. 18, 1855) the presence of three varieties of granite,
coequal in age, and not separated by any contaet-fissure, m the
Carlsbad territory. He had further found evidence that all the
thermal springs in question belong to one of these granites ; and that
“Von Hoff’s line” is merely a local phenomenon. Dr. Hochstetter
now proves that the Carlsbad springs occur along two parallel hnes,
—the one the Sprudel, the other the Muhlbrunn,—both running
N.W. & S.E., and each having a secondary fissure, parallel to the
principal line. The superficial valleys correspond to the direction and
extent of these two fissures, which are essentially connected with the
clefts produced by gradual decomposition in the “ Carlsbad granite.’
The principal set of fissures have a N.W. & S.E. direction, and the
secondary set from N.E. to S.W., corresponding to the run of
numerous quartziferous and siliceous veins. As to the situation of
the thermal springs, their central point is the Sprudel, corresponding
to the point of intersection of the principal Sprudel fissure with the
secondary fissure of the Tepl Valley. The Marktbrunn and the
Schlossbrunn are beyond the Tepl, along the continuation of the first
of these fissures. The next springs occur along lateral and secondary
fissures, and have their supply of water more or less directly from
the principal Sprudel fissure. As these communications partly take
place through the Schlossberg, which is interposed between the prin-
cipal Sprudel fissure and the secondary fissure of the Muhlbrunn,
the origin of the warm waters everywhere pouring out of this hill
may be easily explained, together with the other phenomena obser-
vable in the Carlsbad springs in general. An accurate knowledge of
the fissures giving rise to the springs, and a correct map illustrative
of these features, would be of great practical importance, both for
regulating the springs, and for preventing any operations that might
injure them either in quality or quantity. [Count M.]

EXPERIMENT on Basatt. By A. Benscu.

[Leonhard u. Bronn’s N. Jahrb. f. Min. u. s. w. 1855, p. 597 ; and Ann. Chem.
Pharm, 91. p. 234. ]

Some years since the author reduced to a very fine powder, in water,
by means of a porphyry slab and grindstone, some of the basalt of
the Hirschberg near Grosse-Almerode, intending to apply it to the
glazing of bricks, The wet powder remained many months in a glass
cup covered with paper, and became so hard a mass that a very
severe blow of a hammer could scarcely separate a fragment from
the mass. The fracture of this mass was similar to that of the
natural basalt. The mass presented a black nucleus, of waxy lustre,
surrounded by a somewhat less dense substance, but still very hard
and grey. Exposed for some time to the air, the surface of the
altered basalt exhibited an efflorescence of carbonate of potash, and
of this 1-8 per cent. could be removed by water.

20 ‘GEOLOGICAL MEMOIRS.

The specific gravity of the natural basalt used in the experiment
was 2°887. After lixiviation of the soluble alkaline salt with water,
and after drying in the air, until there was no further loss of weight,
the specific gravity of the altered basalt was taken; that of the nu-
cleus was 2°1588; that of the less hard external portion was 2°0423.

It is evident that i this case the formation of a hydrate had taken
place: and this behaviour of the basalt under the influence of water
and of the atmosphere must prove to be of some interest to geologists.

(T: Reda

On JUNKERITE. By A. KennoGorr.

-{Min. Notizen, xiv. p. 13; and Leonhard 4 MISS Jahrb. f. Min. &c. 1856,
p. 49

THE examination of a specimen of junkerite from Poullaouen, in
Brittany, confirmed Breithaupt’s statement that junkerite is rhom-
bohedral and belongs to siderite. It occurs as crystals on quartz,
which form a crystalline coatmg, and are also met with as single
crystals. The isolated crystals, although very small, can be recog-
nized as exhibiting a combination of an acute rhombenedeame in the
opposition mR! (taken on the primary form R of siderite), with the
basal planes. The rhombohedral planes are somewhat lustrous and
convex; the basal planes, rough and dim. ‘The convexity arises
from the presence of a scalenohedron, which sharpens the lateral
angles of the rhombohedron, the planes of which however by the
convexity of the rhombohedral planes can form no distinct angles of
combination. The crystals, completely cleavable parallel to the
planes of the primary form R (which is the case also in siderite), are
yellowish-brown and transparent.. [T. R. J.]

On remarkable Crystals of QUARTZ and FLUOR-SPAR.
_ By A. Kenneorr.

[ Min. Notizen, xiv. p. 20,22; and Leohn. i Broun’s N. Jahrb. f. Min. &c. 1856,
p- 39 ;

In the eclogite of the Sau-alps in Carinthia emanate peculiar

crystals occur, which are there known by the name of ‘‘ white topaz.”’

Close examination, however, shows that these are either imperfect or

misformed crystals of quartz.

At Schlackenwald in Bohemia the joint-surfaces of a fine-grained
granite are covered over with small quartz-crystals, and on this coat-
ing are crystals of fluor-spar of two different kinds, occurring side
by side, viz. green octahedrons and violet-blue rhombie dadeca-
hedrons. The latter, fully formed, appear at first sight as triakis-
octahedrons, on account of white stripes in the position of the longer
diagonals. On close examination, it is seen that the layers corre-
sponding to the three chief sections are colourless, whilst the rest of
the mass of the crystals is violet-blue. [T. R. J.]

TRANSLATIONS AND NOTICES
OF

GEOLOGICAL MEMOIRS.

On the LowER GREENSAND and the BLackpown Fossits of
ENGLAND. By M. E. RenevieEr.

[Bulletin Soc. Vaudoise Sc. Nat. vol. v. p. 51-52, 1856. ]

In communicating the general results of his comparison of the lower
cretaceous fossils of England (large suites of which his late visit to
England had enabled him to study) with those of France and Switzer-
land, M. Renevier offered the following observations :—

Ist. Lower Greensand.—Palzontologically the Lower Greensand
does not represent the Neocomian of Switzerland, as most geologists
have thought; but, on the contrary, exactly corresponds to the series

‘of Aptian beds which M. Renevier has recognized, at the Perte-

du-Rhone, between the upper Neocomian (Urgonian) and the Gault.
The lower strata of the Lower Greensand (Perna-beds and Crackers)
contain a fauna which is quite analogous to that of the Lower Ap-
tian (Rhodanian) of the Perte-du-Rhone, whilst the arenaceous series,
about 650 English feet thick, which occurs between the Crackers
and the Gault, evidently belongs to the Aptian proper. These two
faunas (Aptian and Rhodanian) are, however, much more closely
related in England than on the Continent ; hence the two series have
not hitherto been separated by the English geologists. Lastly, as in
Switzerland, the Aptian fauna is somewhat poor; whilst the Rhoda-
nian fauna (Perna-beds and especially the Crackers) is on the con-
trary very rich.

2nd. Blackdown.—The beautifully preserved fossils of Blackdown
have always drawn the attention of the paleontologists of England to
this locality. The fauna has been sometimes referred to the Lower,
and sometimes to the Upper Greensand (Cenomanian); some, of
late, have referred it to the Gault; and M. D’Archiac has regarded
it as representing all three of the above-cited series.

M. Renevier was enabled to add a considerable number to the
known species of Blackdown fossils; but does not offer a definite
opinion on the age of the deposit in question. Many of the species
are peculiar, but the majority belong also either to the Lower Green-
sand, the Gault, or the Upper Greensand. The Cephalopods are
few, both as specimens and species ; and though they are Gault forms,
yet the author thinks their evidence to be insufficient to decide the
question of the relative age of the deposit. Of the other classes, a
nearly equal number of the species are found also in the Upper
Greensand and the Gault ; and a somewhat less number occur in the
LowerGreensand. There is no doubt whatever of the mingling of these
species and of their occurrence in the same deposit. ([T.R. J.]

VOL, XII.— PART. II. D

99 GEOLOGICAL MEMOIRS.

On some Jurassic CePHALOPODA from WURTEMBERG.
| By Dr. AtBert OpPEL.

[Wirttembergische Naturw. Jahreshefte, 1856, pp. 104-108.]

1. Acanthoteuthis antiquus.—During his late visit to England, the

author obtained at Christian Malford* in Wiltshire, a very perfect spe-
eimen of Acanthoteuthis antiquust, with which he has since carefully

compared some conical bodies, similar to the alveoli of Belemnites,
that he has obtained from the clays with dm. Jason and Am. ornatus
from Gammelshausen, near Boll; and from the result, he feels as-
sured that the correctness of dividing Belemnites Puzosianus from
Acanthoteuthis is well established, although the inside of the phrag-
macone of the latter has an organization but little differing from that
of the alveolus of a Belemnite.

The phragmacones from Gammelshausen have a silicified inner cone,
which tapers at an angle of 25°, possesses a siphuncle and sheath, and
is covered with a thin calcareous layer. The latter appears to have a
similar structure to that of the Belemnite sheath; its cross-fracture
shows a dark crystalline mass. In the English specimens it consists

of a white friable substance. The external form, on the contrary, in

specimens from both localities is closely similar ; and is quite different
from the sheath of the Belemnites.

The author points out the importance of the presence of the si-
phuncle and the parallel sheath-walls in the specimens from Gam-
melshausen ; these not having yet been distinguished in the Christian.
Malford specimens. In England the Belemnites Puzosianus fre-
quently occurs in the same clay with the Acanthoteuthis antiquus ;
which circumstance, in the author’s opinion, has led to the associa-
tion of the parts of the two animals by some authors. In Wurtem-
berg, however, the Acanthoteuthis antiquus alone is found; and this
affords an indirect proof of the distinctness of the two forms.

2. Ammonites planorbis with Aptychus.—When in: England last
year, the author saw in Mr. C. Moore’s collection a fine suite of
Ammonites, particularly the Falcifert of the Upper Lias, enclosing
Aptycht. Dr. Oppel also observed in the same collection an “‘ undi-
vided”? Aptychust in an Am. planorbis, Sow. (Am. psilonotus,
Quenst.). On his return home he determined to examine the Pszlo-
notz of Wurtemberg, and the first specimen he split open exhibited an
“‘undivided”’ or univalve 4ptychus lying in the body-chamber of the
Ammonite, much as in the known species, but evidently not divided
by a median fissure. As the Am. planorbis is the first Ammonite
occurring above the “ bone-bed,”’ it is the oldest jurassic species.

[Ts tidal

* The grey laminated clay with Acanthoteuthis belongs to the base of the Ox-
ford Clay; and there are a considerable number of fossils common to it and the
“ Ornatus-clays”’ of the Continent.

+ Morris’s Catalogue Brit. Foss., 1854, p. 289.

t See also Mr. Strickland’s paper on a univalve 4ptychus in an Ammonite from
the lower lias, Quart. Journ. Geol. Soc. vol. i. p. 234.—Eb.

TRANSLATIONS AND NOTICES

GEOLOGICAL MEMOIRS.

On the GroLocy of Banat. By M. J. KupERNATSCH.
[Proceedings Imp. Acad. Sciences Vienna, May 8, 1856.]

In this memoir by the late M. Kudernatsch, communicated to the
Academy by Dr. Hochstetter, the central mountain-chain of Banat
was described as consisting of strata grouped around a huge granitic
nucleus which has been erupted through an enormous fissure, and
has an altitude of 3000 feet. The gneiss, resting on the granitic
mass, is overlaid by sedimentary strata folded into three great antt-
clinals or saddles (at Steierdorf and at Natra), and three chief basins.
These rocks have been traversed in a direction parallel to the long
axis of the saddles by fissures now forming valleys, on the bare sides
of which the lias, together with the brown and white jura, are seen
cropping out and immediately overlying the gneiss. The basins or
synclinals are occupied by extensive deposits of lower and upper neo-
comian limestones, raised up into elevated ranges or forming plateaux,
analogous to those of the Karst as regards their funnel-shaped de-
pressions, caverns, Xe.

The coal-deposits of Steierdorf and Domau belong to the upper
keuper or lower lias sandstone ; and wherever the saddles are fissured,
these coal-beds are seen to overlie a red sandstone of still unascer-
tained age. Five seams of excellent coal, characterized by remains
of Zamia and Pecopteris, have been found within a thickness of from
24 to 30 feet of strata. These coal-bearing deposits are overlaid by
brown and white jura and by cretaceous strata, both rich in organic
remains. Spheerosiderite forms regular beds in a liassic shale, and in
the calcareous plateaux large accumulations of pisiform iron-ore
occur.

The small basin of Szekul was the only known locality of the true
carboniferous deposits in Banat before the late M. Kudernatsch had
ascertained that they occurred extensively in the imperfectly known
south-eastern portion of the Banatian mountains beyond the Almas.
These strata, still lying untouched amid extensive primeeval forests,
may become highly important in the future progress of industrial
activity. [Count M.]

VOL. X11.— PART II. E

24 GEOLOGICAL MEMOIRS.

On the METALLIFEROUS VEINS of PRiBRAM, BOHEMIA.
By Prof. Revuss.

[Proceedings Imp. Acad. Sciences Viehna, May 23, 1856.]

In this paper the author communicated the general results of his
researches on the relative ages and the origin of the metalliferous
veins of Pribram* in Bohemia. These veins appear to form a system
of distinct vein-formations, partly of sedimentary origin. The oldest
belong to Prof. Breithaupt’s “ Zimciferous formation ;” these are
succeeded by the ‘‘ Plumbo-zinciferous” ; more recent formations,
such as the “ Argentiferous,”’ are only represented by isolated por-
tions.

The great variety of minerals constituting the Pribram veins per-
mits of no doubt of their having been formed at distinctly different
periods. By a careful investigation, no less than twenty-four of
these genetic periods were made out. Sulphuret of zinc, galena,
quartz, and carbonate of iron belong to the most remote of these
periods ; and the ascending series is closed by cale-spar and iron-
pyrites. Most of these minerals have been formed repeatedly at
different periods. Thus calc-spar reappears five times, iron-pyrites
four times, quartz three times, and galena, sulphuret of zinc (blende),
sulphate of barytes, magnesio-calc-spar (brown spar), &c., each twice.
The successive formations of the same mineral species are generally
so different in shape, mode of grouping, and colour, and sometimes
even in their chemical characters, that asomewhat practised eye may
distinguish them at first sight.

There are also highly diversified pseudomorphoses, which are very
interesting and instructive as bearing witness to the chemical changes
undergone by some minerals from the action of successive agents.
Some species are the first link of a continuous series of successive
modifications ; thus the argentiferous and antimoniferous galena have
in the course of time given origin to stemmannite, grey sulphuret and
white oxide of antimony, native silver, carbonate and phosphate of
lead, &e. Grey sulphuret of antimony is the root from which by
successive modifications the red sulphuret of antimony, native anti-
mony, and the arseniuret of antimony have been derived. Iron-py-
rites, by its decomposition, has furnished materials for ferro-chlorite
(eisen-chlorite), acicular iron-ore (nadel-eisenerz), red oxide of iron,
&c. Thesulphate of barytes, of the older formation, exhibits a series
of the most interesting decompositions. [Count M.]

On some GASTEROPODA from the ALPINE TRIAS.
By Dr. M. Horrnes.

[Proceedings Imp. Acad. Sciences Vienna, March 1856.]
In this communication Dr. M. Hoernes described and illustrated—
Ist, several fossil mollusca recently collected at Unterpetzen, near

* See also M. Kleszeznski on the Mining District of Pribram, Quart. Journ.
Geol. Soc. vol. xi. part 2, Miscell. p. 40.

HOERNES— ALPINE TRIAS. 29

Schwarzenbach,—2nd, others discovered by M. Lipold on Mount
Obir, N.W. of Eisenkappel in Lower Carinthia,—3rd, another series
from Esino in the Val Pelaggia, on the eastern border of the Lake
of Como, which were kindly submitted for the author’s examination
by M. Escher,—and lastly, some fossils from the Hallstadt strata,
lately found by Dr. Fisher, of Munich, at Sandling* and at Selt-
schen, near Aussee in Styria.

The Esino fossils were found in a dark-grey or black dolomitic
limestone in the detrital accumulations (schutt-halden), on the
northern slope of the Val Pelaggia. The limestone is intersected by
veins of white calcareous spar, and has a slight bituminous smell
when struck with a hammer. MM. Escher and Curioni found also
Crinoidal joints in this limestone.

The number of species common to the several fossil faunze here
referred to is but small, but may however be regarded-as sufficient
to indicate that the Hallstadt and the St. Cassian strata are closely
related, and that in a palzeontological pomt of view the dolomitic
limestones of Esino, Hall (Tyrol), Unterpetzen, &c., are members of
the extensive St. Cassian series.

The following table exhibits a synoptical view of the relative oc-
currence of the Triassic fossils described in Dr. Moritz Hoernes’

paper.

ey ass Sly Gets hey hee le
Sgt aaa NS SOAPS By
5 |= | 4
Ammonites Aon, Miinst. ...............-.- sas . ate * * *
Gaytaniy Kish o oo... cece yas Se 2-dee os Soe one * * *
Johannis Austrie, Klipst. ......... a sat * * *
Janbas Manche) 408 BI a. . * * *
Turbo Suesst,“AOrn) d.csccbbstecceseccss * aoe
subcoronatus, H6rn. .........<«s00- a * *
GE BTCSSUST PA OEI wees aie ctie nn ece «+ * ne
Nermea prisca, Horn. .....5..-se...s02 mae be *
Watien Tipoldi orn. 3.200. cle. s 608k. Ee *
COmMe#nNSIS HOR: 5... 658206 bsdo deed. * st : oe F
Sublineataa., MinSt. ..osiccc.vsciescas ves ais Res we * ao *
NMICTIAMI MEOW ec ccvceccneeccvcc~ shen * * ae
— lemniscata, Horn. .................- * ine
PRPENIDEA OTN S co500s2cseascdeescn =: Soa Maer * S
| Nerita Prinzingeri, H@rn.....0......000000 we * ses
Chemnitzia eximia, Hérn.......... eek (nie * * ome yee
SEMI MGUA LOTTE Meno... J onesavesinee<>- ** Me * x z
— Rosthorni, Horn..................026- a: re * *
— tumida, Horn. ...........-.....c000ee- Be *
—— Escheri, H6rn........0....ccscecceeees * ee ee said Ge i
EOTINOSA, VAG IDS) sey eee. 2850.2 05.455 tas Tee tet * ak *

[Count M.]

* See also Quart. Journ. Geol. Soc. vol. xi. part 2, Miscell. p. 23,
es

26 GEOLOGICAL MEMOIRS.

On the Uprer Sepimentary Deposits of the VENETIAN TER-
RITORY, and on the Fosstu Bryozoa, ANTHOZOA, and SPONGES
contained in them. By T. A. Catutyuo. 4to. 88 pages and
19 lithograph plates. Padua, 1856.

(Dei Terreni di Sedimento superiore delle Venezie e dei fossili Bryozoari, Antozoari,
e Spongiari ai quali danno ricetto Memoria di Tomaso Antonio Catullo, &c.]
Tats work, to which the author has devoted much time and research,
is almost entirely devoted to the description and illustration of 154
species of Bryozoans, Zoophytes, Sponges, &c. from the Tertiary
deposits of the Venetian portion of Italy. But, before entering on
the main object of the work, the author devotes a few pages to the
geology and geographical extent of these upper sedimentary forma-
tions, following the classification proposed by Sir C. Lyell, in pre-
ference to that advocated by M. D’Orbigny ; because, in his opinion,
the objection made to the per-centage of species does not invalidate

the stratigraphical distinctions laid down by Sir C. Lyell.

The upper deposits at the foot of the Venetian Alps bear a very
close similitude to those analogous formations of Hungary and
Austria, composed of strata representing the Pliocene, Miocene, and
Eocene epochs. The author obserses that Vicentine tertiaries are
also in every respect similar to those of the southern part of Russia ;
and that many years ago he discovered in fragments of nummulitic
rock brought from the neighbourhood of Cairo, Melania costellata,
Fusus intortus, Turritella imbricataria, and other shells very common
in the Vicentine beds of that period.

These Italian tertiary deposits well represent, according to the
author, Lyell’s three divisions; the most ancient (Hocene) being
composed of plastic clay, sandy glauconite, and nummulitic limestone,
accompanied by the usual marls; the Miocene is represented by
marls and molasse ; the Pliocene consists of marls and sands; which
last admit of a division into Lower and Upper Pliocene. ‘The Eocene
series is more developed and more complicated than the others. In
a few localities it forms a continuous band, and from the Heights of
Frisuli and the Bellunese, it spreads out in the Feltrino, the Vicentino,
aud other regions, not excepting the Euganean Hills, as the author
demonstrated by means of their fossils as early as 1828. The sea,
therefore, in which these deposits were formed was of considerable
extent. Signor Catullo then furnishes a detailed list of various loca-
lities where the nummulitic rock, which forms a large portion of the
Venetian state, is visible, and remarks that the same species are
everywhere found, except (as is the case in the other periods) where
some species are peculiar to one horizon or locality only. Thus the
Echinoderms are particularly abundant in the nummulitic rocks,
while the grey sandstone (molasse) is remarkably poor in those fossils,
although it contains innumerable spines, which may be perhaps
referable to some species of the genus Clypeaster? Onthe contrary,
the Eocene and the Miocene of the Vicentine are rich in Corals, of
which scarcely a trace can be found in the corresponding formations
of the Veronese, the Friulano, and the neighbourhood of Belluno.

The author dwells at some length on the basaltic eruptions of the
Vicentine, to which the brecciated beds are attributable; and he

CATULLO—VENETIAN TERTIARIES. 27

remarks that, of the corals enveloped in the breccia of Monteviale,
Sangonini, Montechio-Maggiore, and a few other localities, some few
have been referred by Michelin to the Chalk ; but that these excep-
tional specimens might have been transported by the basaltic
eruptions.

The nummulitic zone is at times very complex, being in some
localities composed of its most characteristic rocks, whilst in others
several of these are wanting. Thus at Brendola, the nummulite-
rock overlies a peperite, which in other localities alternates with it,
both rocks containing similar eocene fossils; elsewhere, however, as
at Sangronini and Ronca, the peperite affords numerous specimens
of Flabellum appendiculatum, Orbitoides Prattu*, and other species
peculiar to it and not found in the overlying limestone. The plastic
clay is not always found underlying the nummulitic rocks.

The author next enters into some details relating to the Middle
Tertiary or Miocene beds, as far as he has examined them in the
Venetian territory ; and states that the age of the hill of molasse to
the north of Belluno (Valle dell’ Ardo, Libano, Tisoi, Orzes, &c.),
is determined by its containing miocene fossils, and by the underlying
glauconite. The fossiliferous molasse, so extensive in Switzerland
and Piedmont, attains a considerable development in the valleys to -
the north of Belluno, from whence the author obtained most of his
miocene fossils. Leaving these valleys to the right, and advancing
towards the northwest, the author found at the Ponte del Gresal
that the molasse changes to a marl-rock, or a molasse of very fine
grain. He observes, that, if he has formerly given the name of
Pliocene to the middle tertiaries of some localities, they must be now
referred to the Miocene, because none of those deposits present
characters such as to entitle us to consider them as equivalents of
the upper subapennine zone, which, from the recent observations of
Prof. Doderlein, of Modena, is known to overlie miocene deposits
rich in marine remains. Signor Catullo limits himself at present to
observing that the fossils from the marl of Asolane are for the most
part miocene and not pliocene, as supposed by Sir R. Murchison in
the Philosophical Magazine for 1829, as well as in his memoir on the
Structure of the Alps, published in 1849.

The author concludes his discourse on the tertiary deposits of the
Venetian territory, by observing that the Eocene zone, from its
extent, the diversity and peculiarity of its rocks, the thickness of
the beds, and the considerable altitude it attains above the sea-level,
differs materially from the Miocene zone, which is composed some-
times of molasse, sometimes of marl and marly limestone, inter-
stratified with thm bands of sand or sandy rock, and is of small
extent and attains no considerable elevation, unless deposited on a
pre-existing eminence, as happens with the beds covering the glau-
conite of the Bellunese and vicinity of Ceneda.

The fossils described in this memoir were chiefly derived from the

* This Foraminifer is termed “ Orbitulites’”’ by Catullo, and included in his
“ Bryozoari”’: his Orbitulites nummuliformis is also an Orbitoides, and so also
probably is his Lunulites subradiata. Signor Catullo’s figure of Lunulites andro-
saces (Michelotti) closely resembles Nummulites (Assilina) granulosus, d’Arch. ;
and his L. depressa has a similar character, judging from the figures.—Ep.

28 GEOLOGICAL MEMOIRS.

Castellini collection, now forming part of the Museum of Natural
History in the University of Padua. [T. By

On Post-TERTIARY SHELLS from the Coast of GREECE.
By Dr. M. Horernges.

[Proceed. Imp. Geol. Instit. Vienna, January 29, 1856.]

Dr. HorerneEs communicated a list of 87 species of marine molluscs,
found subfossil near Kalamaki, on the Isthmus of Corinth, and
lately sent to the Imperial Museum by M. Th. de Heldreich, Director
of the Royal Botanical Garden at Athens. The specimens were
found between Kalamaki and Lutraki, at a height of from 30 to 60
feet above the present high-water-mark, imbedded in a mass of
shell-fragments, with small rolled pebbles of serpentine and reddish
quartz, altogether forming a calcareous sandstone. All the species
are still living in the neighbouring sea. |

Similar deposits are known to exist along nearly the whole coast
of the Mediterranean,—in the Morea, in Rhodes, Cyprus, Sicily,
Italy (Puzzuoli), Algeria, Spain, &c. Hence it may be concluded
that at an earlier epoch the countries surrounding the Mediter-
ranean have undergone an upheaval, which, as careful investigations
seem to prove, has affected the continents of Europe, Asia, and
Africa bodily; so that at the epoch known under the name of
“Neogene”? (Pliocene and Miocene of Lyell), the Atlantic Ocean
and the Mediterranean may have extended considerably further than
they do now. In the south and south-west of France, in the May-
ence and Upper Danube basin, in the basins of Vienna and Hungary,
in the plains of Germany, a great portion of Russia, the whole extent
of the valley of the Po, and elsewhere, there exist evidences of the
waters having covered all these areas. At the same epoch the
Caspian Sea was still in immediate connexion with the Euxine, and
Africa was an island, the bormgs undertaken by the Canal-com-
mission having shown that the Isthmus of Suez is for the most part
composed of deposits abounding in Neogene fossils. Similar fossils
have been found in Algeria and in Oran, so that the whole of North
Africa, together with the Sahara, may be reasonably supposed to
have formed part of the Neogene sea.

It also appears that the upheaval was extremely slow, all the
neogene fauna of Europe exhibiting gradual passages ‘from an extinet
fauna to one pertectly agreeing with that of the present Mediter-
ranean fauna. ‘The species of the lowest neogene strata have a sub-
tropical character; those of later date indicate a climate more and
more approaching to that existing at present ; and of the 87 species
from Kalamaki, fifty are identical with forms from the Vienna basin.

From the sinking of the relative level of the sea, as an effect of
the upheaval, and the influx of fresh water into limited basins, the
true marine species died out and gave room to a new fauna peculiar
to brackish water (the Cerithian strata); just as changes are now
taking place on the shores of the Caspian. At last even these
species could no longer exist with the gradually diminishing water-
level, and made room for the comparatively few molluscan forms at
present inhabiting our dry lands and fresh waters. [Count M.}.

— iii ie

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. ]

Aberdeenshire, Mr. Salter on the fossils
found in the chalk-flints and green-
sand of, 390.

Africa, South, Mr. Rubidge’s notes on
the geology of, 237.

Alluvia of Switzerland, marine shells in
the, 120.

Alps, Mr. Sharpe on the last elevation
of the, with notices of the heights at
which the sea has left traces of its
action on their sides, 102.

Altitudes of terraces in the Swissvalleys,
table of, 122.

Altitudes of the heads of Swiss valleys,
table of, 122.

Ammonites Dorsetensis, 321.

Analysis of the Cleveland iron-ore, 357.

Annan, red sandstones of the, 259.

Annelide-tubes in the Longmynd rocks,
249.

Anniversary Address of the President,
xxvi. See also Hamilton, W. J.

Annual General Meeting, i.

Annual Report, i.

Ansted, D. T., description of remarkable
mineral veins, 144; on the copper-
lode of Cobre, Santiago de Cuba, 144.

Aptornis otidiformis, tibia of, 210.

Arenicola didyma, 248.

Argyllshire, raised beaches in, 167.

Artois, axis of, 59.

Ascoceras Barrandii, 381.

Ascoceras, Mr. Salter on the occurrence
of, in Britain, 381.

Asia Minor, coal of, 1; fossils from, 3;
nummulitic limestone in, 4.

Austen, R. Godwin-, on the newer ter-
tiary deposits of the Sussex coast, 4;
noticed, lvii; on the possible exten-
sion of the coal-measures beneath the
south-eastern part of England, 38;
noticed, lii.

Australia, Mr. Wilson on the geology
of parts of, 283.

Award of the Donation Fund, xxv.

Wollaston Medal, xxi.

Axis of Artois, 59.

Ayrshire, red sandstones of, 262.

Babbage, C., on the action of ocean-
currents in the formation of the strata
of the earth, 366.

Balena, remains of, in the red crag,
228.

Ballochmoyle bridge, sections of the
upper permian sandstone of Dumfries
near, 139, 262.

Banks, R. W., on the tilestones, or
Downton sandstones, in the neigh-
bourhood of Kington, and their con-
tents, 93 ; noticed, 1.

Bear, remains of, in the red crag, 227.

Beckles, S. H., on the lowest strata of
the cliffs at Hastings, 288.

Bedford, E. J., on some raised beaches
in Argyllshire, 167.

Binks, fossil tracks at, 243.

Binney, E. W., on some footmarks in
fhe millstone grit of Tintwistle,
Cheshire, 350; on the permian cha-
racter of some of the red sandstones
and breccias of the south of Scotland,
-138.

Birds’ tibiz, characters of, 205.

Bone-bed, Rev. Mr. Dennis on probable
mammalian bone from the, 252.

Boring through the chalk at Kentish
Town, London, 6.

Boué, A., on the probable origin of the
English Channel by means of a fis-
sure, 325.

Bovey Tracey, Dr. Croker on the lig-
nite deposits of, 354.

Bowen, H. G., on the geology of Trini-
dad, 389.

- Bridport, section near, 310.

Brisbane, geology of, 287.

British and foreign middle eocene ter-
tiaries, the correlation of the, 390.
Brodie, Rev. P. B., on the upper Keuper

sandstone of Warwickshire, 374.

Bubalus moschatus, fossil and recent
crania of the, 127.

Bulgaria, Capt. Spratt on the geology
of parts of, 387.

Bunbury, J. F., notice of some appear-
ances observed on draining a mere
near Wretham Hall, Norfolk, 355. -

Cambrian rocks of the Longmynd and
North Wales, fossil remains from,
246.

Canis, remains of, in the red crag, 226.

Carboniferous series, mountain or car-

INDEX TO THE PROCEEDINGS.

boniferous limestone, 55; old red
sandstone, 51.

Cardium Hullii, 324.

Oppelii, 325.

Carlingford, granites of, 192.

Carnivora, remains of, in the red crag,
226.

Cephalopoda bed, characters of the,
312; continental equivalents of the,
314; in Dorsetshire, 310; in Glou-
cestershire, 292.

Ceratiocaris, Mr. Salter on the, 33.

Cervus dicranocerus, 224, 225.

Cervide, remains of, in the red crag,
Pe

Cetacea, remains of, in the red crag,
228.

' Chalk, boring through the, at Kentish

Town, 6.

Chalk-flints and greensand of Aberdeen-
shire, fossils from the, 390.

Charters, Major S., on a section near
Mont Blane, 385.

Chelichnus ingens, 354.

China, occurrence of coal in, 358; an
Orthoceras from, 378.

Chondrites from near Bangor, 246.
Church Stretton, ripple-marks on the
surfaces of the flagstones near, 251.

Circular form of craters, 333.

Clay-slates, Mr. Scrope on, 347.

Cleveland iron-ore, Mr. Dick’s analysis
of the, 357.

Cliffs at Hastings, the lowest strata of
the, 288.

Coal-basin of Valenciennes, 252.

Coal-growth, form of the terrestrial sur-
face of the, in the British area, 42;
in the Belgic area, 47; in the Bou-
lonnais, 47; in the Franco-Belgic
area, 48.

Coal in Asia Minor, Mr. Poole on the, 1.

Coal-measures near Lesmahago, sec-
tions of the, 25; Mr. Godwin-Austen
on the possible extension of, beneath
the south-eastern part of England, 38.

Coal near the city of E-u in China, the
Rey. R. H. Cobbold on the occur-
rence of, 358.

Coal-seams of Newcastle, Australia, 284.

Cobbold, Rey. R. H., on the occurrence

of coal near the city:‘of E-u in China, .

358.

Cobre, Santiago de Cuba, the copper-
lode of, 144; section across the
mineral field of, 148.

Cones, formation of volcanic, 327.

Copper-lode of Cobre, Santiago de Cuba,
Prof. Ansted on the, 144.

Corncockle Muir, sandstones of, 256.

Correlation of the middle eocene ter-

tiaries of England, France, and Bel-
gium, 390.

Craters and lavas, Mr. Scrope on, 326.

Crater-formation, theories of, 328.

Cretaceous series, extent of the, 68.

Croker, J. G., on the lignite-deposits
of Bovey Tracey, Devonshire, 354.

Crustacea from the uppermost Silurian
beds, 26.

Cuba, copper-lodes of, 144; general
section across the eastern end of the
island of, 145.

Cygnus ferus, tibia of, 211.

Cypricardia brevis, 324.

Dead Sea, Mr. Poole’s notice of a visit
to, 203.

Degousée and Laurent, MM., on the
Valenciennes coal-basin, 252.

Dennis, the Rev. Mr., on some organic
remains from the bone-bed at the
base of the lias at Lyme Regis, 252.

Dick, A., analysis of the Cleveland iron-
ore from Eston, 357.

Dicranoceros, remains of, in the red
crag, 225.

Dinornis casuarinus, tibia of, 210.

Dioplodon, remains of, from the red
crag, 228.

Diploceras, Mr. Salter on, 381.

Distribution of the fossil Estheriz, Mr.
Jones on the, 376.

Dolphin, remains of, from the red crag,
228.

Donation Fund, award of the, xxv.

Donations to the Library, 74, 154, 268,
293.

—— to the Museum, Vii, viii.

Dorsetshire, inferior oolite and upper
lias sands of, 310.

Downton sandstones of Kington, 93.

Draining a mere near Wretham Hall,
Norfolk, Mr. Bunbury’s notice of

- some appearances on, 355.

Dumfriesshire, permian rocks of, 254.

Earthquake at Tongataboo, effects of
an, 383.

Elevation of the Alps, Mr. Sharpe on
the, 102.

English Channel, M. Boué on the pro-
bable origin of the, 325.

Equus, remains of, in the red crag, 223.

Equus plicidens, 223.

Erosion on the Alps, traces of, 102.

Eskdale, Silurian rocks of, 238.

Eston, analysis of iron-ore. from, 357.

Estheria minuta, Mr. Jones on the, 376.

E-u in China, the occurrence of coal
near, 358.

Eurypteride, 26.

Eurypterus pygmeus, 99.

Evigtok, Greenland, the cryolite of, 140.

INDEX TO THE PROCEEDINGS.

Experimental researches on the granites
of Ireland, by Prof. Haughton, 171.

Felis pardoides from the red crag, 226.

Felis, remains of, in the red crag, 226.

Folded rocks, Mr. Babbage on, 368;
Mr. Scrope on, 345.

-— of Wigtonshire, 362.

Footmarks in the millstone-grit of Tint-
wistle, Cheshire, Mr. Binney on some,
350.

Formation of cones and craters, 327.

—— of craters, and the nature of the
liquidity of lavas, Mr. Scrope on the,
326.

Fossil cranium of the musk-buffalo from
Maidenhead, Berkshire, Prof. Owen
on a, 124.

crustacea from Lesmahago, 26.

—— femur and tibia of the large ex-
tinct bird (Gastornis Parisiensis,
Hébert) found in the lowest eocene
formation near Paris, 204.

foot-tracks from the millstone-

grit, 352.

fucoid from near Bangor, 246.

mammalia from the red crag, 217.

—— remains in the Cambrian rocks of
the Longmynd and North Wales,
Mr. Salter on the, 246.

tracks from Binks, South Scotland,
Mr. Salter on, 243.

Fossils of the upper Keuper sandstone
at Leicester, 369; at Shrewley, 374;
of the Wealden at Hastings, 292.

—— found in the chalk-flints and
greensand of Aberdeenshire, 390;
from Asia Minor, 3; from the
Hastings cliffs, 291; from the tile-
stones of Kington, 93.

Franco-Belgian coal-field, MM. De-
gousée and Laurent on the, 252.

Gastornis Parisiensis, Prof. Owen on

the affinities of the, 204.

General Meeting, Annual, i; special,
384.

Geograrhy of Western Europe at the
coal-growth period, outline of the, 37.

Geology of part of Asia Minor, 1; of
parts of Australia, Mr. Wilson on the,
283 ; of some parts of South Africa,
237; of Trinidad, Mr. Bowen on the,
389 ; of Varna, Capt. Spratt on the,
387.

Gloucestershire, inferior oolite and up-
per lias sands of, 292.

Gneiss and granite, Mr. Scrope on, 345.

Gold district in South Africa, 237; of
Peel River, 286.

veins in quartz and other rocks,

Mr. Ibbetson on the possible origi

of, 384.

Grampus, remains of, in thered crag, 228.

Granite converted into syenite, 197.

Granites of Ireland, Prof. Haughton’s
experimental researches on the, 171.

Graptolitic schists of Wigtownshire,
364.

Greenland, Mr. Tayler on the cryolite
of, 140.

Hamilton, W. J. (President), Address
on presenting the Wollaston Medal
to Sir R. I. Murchison for Sir Wil-
liam Edmond Logan, xxi; Address
on presenting the Donation Fund
Award to Mr. Prestwich for M. Des-
hayes, 25; Anniversary Address, 26.
Notices of Deceased Fellows : George
Bellas Greenough, xxvi; Sir Henry
Thomas de la Beche, xxxiv; Thomas
Weaver, xxxviii; The Right Hon.
Sir H. Ellis, xxxix; Sir William
Molesworth, xxxix; Lewis Weston
Dillwyn,xl; Prof. F. W. Johnston, xli;
M. Jean de Charpentier, xli; Sedg-
wick and M‘Coy’s synopsis of the clas-
sification ofthe British palzeozoic rocks
and fossils, noticed, xliv; Murchison
on the relation of the crystalline rocks
of the North Highlands to the old red
sandstone of that region, and on the
recent fossil discoveries of Mr. C.
Peach, xlvii; Salter on the recent dis-
covery of fossils in the Cambrian rocks
of the Longmynd, xlviii; Murchison
on the upper Silurian rocks and fossils
discovered near Lesmahago by Mr.
Robert Slimon, xlix; Banks on the
tilestones or Downton sandstones in
the neighbourhood of Kington, and
their contents, 1; Sorby on the phy-
sical geography of the old red sand-
stone sea of the central district of
Scotland, li; Sorby on the physical
geography of the tertiary estuary of
the Isle of Wight, li; Godwin-Austen
on the probable extension of the coal-
measures beneath the south-eastern
parts of England, lii; Ramsay on the
permian breccia of Shropshire, Wor-
cestershire, &c., lv ; Hull on the phy-
sical geography and the drift phe-
nomena of the Cotteswold Hills, lvii;
Godwin-Austen and Martin on the
newer tertiary deposits of the Sussex
coast, lvii; Owen on the discovery
near Maidenhead of fossil remains of
the first example of the subgenus
Bubalus yet recognized as fossil in -
Great Britain, and Prestwich on the
gravel in which these remains were
found, lix ; Prestwich on the boring
sunk through the chalk at Kentish

INDEX TO THE PROCEEDINGS.

Town, lix; Haughton and Galbraith
on the granites of Ireland, lx; the
progress of the Geological Survey of
the empire during the past year, and
the publications of the Institution,
noticed, lxi; the monographs of the
Palzontographical Society for 1854,
noticed, Ixii. Foreign Geology :
France and Switzerland, lxvi; Cotteau
on the coral-rag in the department of
the Yonne, lxvi ; Baudouin’s geologi-
cal map of the district of Chatillon-
sur-Seine, Ixvi; Omboni on the sedi-
mentary formations of Lombardy,
and on the structure of the southern
flanks of the Alps, Ixvi; Marquis de
Pareto on the nummulitic formation
at the foot of the Apennines, lxvi;
Pomel’s geological account of the
country of the Beni Bou Said, near
the frontier of Morocco, lxvi; Gras
and others on the age of the an-
thraciferous formations of the Alps,
Ixvii; Barrande on the organic filling-
up of the siphuncle in some of the
palzozoic cephalopoda, lxviii; Haime
on the geology of the island of Ma-
jorca, Ixviii; Bellardi on the num-
mulitic fossils of the district of Nice,
Ixix ; D’Archiac on the geology of the
mountainous district of the Corbieéres,
lxix; Prevost and others on the
Gastornis Parisiensis, xx; Hébert
and Renevier on the nummulitic
formations in Switzerland, Ixx; Sis-
mondi on the nummulitic rocks, lxxi;
Sharpe on some of the more recent
phenomena exhibited in the Alpine
valleys, 1xxi; Morlot on the post-
tertiary and quaternary formations of
Switzerland, Ixxiii; Pictet’s maté-
riaux pour la paléontologie Suisse,
Ixxiv. Germany: Murchison and
Morris on the palzozoic and their
associated rocks of the Thiringer-
wald and the Hartz, lxxiv; Sand-
berger’s list of the fossils of the
Rhenish Devonian system in Nassau,
Ixxvi; Barrande on the parallelism
between the Silurian deposits of Bo-
hemia and Scandinavia, Ixxvii; Gi-
rard on the geology of the North
German plain, lxxviii; Girard’s geo-
logical wanderings, Ixxx ; Sandber-
ger’s account of a species of Cly-
menia in the Cypridina-slates of the
Devonian system in Nassau, Ixxx ;
Beyrich on the shells of the tertiary
formation of the north of Germany,
Ixxxi; Beyrich on the brown-coal of
North Germany, Ixxxii; Koch ona

septarian clay formation underlying
the brown-coal formation, 1xxxiii;
Lipold on the brown-coal of South
Germany, lxxxiii; the Journal of the
German Geological Society, lxxxiv ;
Sandberger on metamorphosed ter-
tiary formations containing fossil
plants in the Kaiserstuhl, Ixxxiv ;
Ludwig on the tertiary formations of
Germany, Ixxxiv; Notes of the Pro-
ceedings of the Imperial Geological
Institute of Vienna, supplied in MS.
by Count Marschall of Vienna to the
Assist. Sec., Ixxxvi; Hauer, Foetterle,
and Hoernes on the fossils of the
secondary deposits of the Alps and
the Carpathians, and of the nummu-
litic and other tertiary beds, Ixxxvi;
Hoernes on the geological position
of the Hallstadt beds, lxxxvii; Suess,
Hoernes, and Hauer on the Hallstadt
fossils, Ixxxvii; Peters on Austrian
tertiary chelonia, lxxxviii; Hauer on
some dolomitic fossils from Monte
Salvatore, Ixxxviii; Rolle on upper
jurassic echinoids of Moravia, lxxxviii;
carbonized wood in the rock-salt of
Wieliczka, Ixxxix ; Lanza on the geo-
logical formations of Dalmatia, lxxxix;
Lipold on the cretaceous and eocene
formations in the north-east portion
of Carinthia, Ixxxix. Norway: D.
Forbes on the Silurian and metamor-
phic rocks of Norway, xc; Kjerulf
on the paleozoic geology of Christ-
jana, xci. Russia: Abich on the
Aralo-Caspian beds, xcii. Jtaly: De
la Marmora on a geological map of
Sardinia, xciii; Montagna on the
coal of Agnana in the southern part
of Calabria, xciii; Scarabelli on the
geology of the province of Ravenna,
xciv; Wright on fossil echinoderms
from the island of Malta, xcv. Spain:
the progress of geology in Spain, and
the labours of M. de Verneuil, M.
Casciano de Prado,and MM. Ezquerra
del Bayo and Pailette, xcv; Botella’s
geological account of the kingdom of
Valencia, xcvi; De Prado on the
geology of Almaden and a part of the
Sierra Morena and the mountains of
Toledo, xcvii. Asia Minor: Poole
on some seams of coal near the Gulf
of Nicomedia in Asia Minor, xevii;
Tchihatcheff on the geology of Asia
Minor, xcviti. Fgypt: Horner on
the geological history of the alluvial
land of Egypt, xcviii; geological ob-
servations by MM. Schlagintweit on
their journey from Cairo to Suez, c.

INDEX TO THE PROCEEDINGS.

India: Hislop on the connexion of
the Umret coal-beds with the plant-
beds of Nagpur in India, and of both
of these with those of Burdwan, c;
Jacob’s account of the examination
of the Nerbudda Valley in Central
India, ci. America: Logan and
Hunt on the geology of Canada, ci;
Dawson’s Acadian Geology, noticed,
cii; Belcher and Salter on the geo-
logy of the Arctic regions, ciii; Is-
bister on the geology of the Hudson
Bay territories, and of portions of the
Arctic and north-western regions of
America, cili; Lea on the fossil
footmarks in the red sandstone of
Pottsville, civ; Norwood and Pratten
on some paleozoic fossils of the
United States, civ ; and on the genus
Chonetes as found in the western
states and territories, civ; Trask on
the geology of the Coast-mountains
and part of the Sierra Nevada, cv;
Dana’s Address to the American As-
sociation for the Advancement of
Science, cv; Marcou on gold in Cali-
fornia, cv; Rogers’s geological map
of the United States and British
North America, cvi; Dana on the
lower Silurian rocks, evi; the geolo-
gical survey of the State of Wiscon-
sin, and of the State of New Jersey,
evii; Whitney on the changes in
mineral-veins near the surface, cvii.
South America: the death of Dr.
Voltz while exploring Surinam, cvii;
fossils from Surinam, cvii. British
Colonies : Garden on some cretaceous
rocks in the district south of Natal,
evili; Sutherland on the geology of
Natal, cvili; Clarke on the geology
of Australia, cviii; Rosales on the
gold-fields of Victoria, cviii; Odern-
heimer on the geology of part of the
Peel River district, cviii. Palgon-
tology, &c.: Jones on paleozoic bi-
valved entomostraca, cviii, cix ;
Wright on a new genus of fossil Ci-
daride, cix; Davidson on the sy-
stematic arrangement of recent. and
fossil Brachiopoda, cix; Dunker and
Von Meyer’s Palgontographica, cix ;
King on the Pleurodictyum problem-
aticum, cx ; Sorby on slaty cleavage
as exhibited in the Devonian lime-
stones of Devonshire, cxi; Lyell’s
fifth edition of the Manual of Ele-
mentary Geology, noticed, cxi; crater
of Palma, cxi; Ehrenberg’s researches
on greensands, cxli; perforations of
rocks by zoophytes and mollusca, as

noticed by M. Cailland of Nantes,
Prof. Long of Grenoble, and by the
President, exii; Murchison and Ni-
col’s geological map of Europe, exiii ;
progress of the geological map of
Germany, cxiv; Von Dechen’s geo-
logical map of the Rhenish provinces
of Prussia and of Westphalia, cxiv ;
Mylne’s MS. map of the geology of
Londonandits vicinity ,cxiv; Powell’s
Essay on the Philosophy of Creation,
noticed and criticized, cexv ; Wallace
on the Law which has regulated the
introduction of new Species, noticed,
CXviil ; conclusion, cxviii.

Harkness, R., on the lowest sedimentary
rocks of the south of Scotland, 238 ;
on the sandstones and breccias of the
south of Scotland of an age subse-
quent to the carboniferous period,
254.

Hastings, Mr. Beckles on the lowest
strata of the cliffs at, 288.

Haughton, S., experimental researches
on the granites of Ireland, 171; no-
ticed, lx.

Hawaii, volcanic eruption in, 171, 386.

Himantopterus and Eurypterus, 27, 28.

Himantopterus acuminatus, 28, 29.

Banksii, 32, 99.

—— bilobus, 28, 30.

—— lanceolatus, 28, 32.

maximus, 28, 29.

—— perornatus, 28, 31.

History of Vesuvius, 335.

Hog, remains of, in the red crag, 222.

Hoplocetus crassidens from the red
crag, 228.

Horse, remains of, in the red crag, 223.

Huxley, T. H.,observations on the struc-
ture and affinities of Himantopterus
by, 34.

Ibbetson, L. L. B., on the possible ori-
gin of veins of gold in quartz and
other rocks, 384.

Igneous rocks of Malvern, 382; of the
district of Lesmahago in Scotland, 21.

Inferior oolite of Dorsetshire, fossils
and sections of, 310; of Gloucester-
shire, fossils and sections of, 292.

Ireland, Experimental Researches on
the Granites of, by the Rev. Samuel
Haughton, 171.

Iron-ore from Cleveland, analysis of,
357.

Isle of Wight, local oscillation of the
coast of, 6; Mr. Sorby on the phy-
sical geography of the tertiary estuary
of the, 137.

Jones, T. R., on the Estheria minuta,
376.

INDEX TO THE PROCEEDINGS.

Kentish Town, a boring through the
chalk at, 13.

Keuper sandstones and fossils at Leices-
ter, 369 ; in Warwickshire, 374.

Kington, tilestones in the neighbour-
hood of, 93.

Laminated or schistose rocks, Mr.
Scrope on, 345.

Lavas, the nature of the liquidity of, 338.

Leicester, section across the river-valley
at, 372 ; upper Keuper sandstone of,
369.

Leinster, granites of, 173.

Lesmahago district, Sir R. Murchison
on the general relation of the rocks
of the, 16.

——.,, the coal-measures of the, 25.

Lias, sands of the upper, 292.

Library Committee, Report of the, iii.

Lignite-deposits of Bovey Tracey, De-
vonshire, 354.

Liquidity of lavas, the nature of, 338.

Liverpool Range, geology of part of the,
286.

Longmynd and North Wales, Mr. Salter
on fossil remains in the Cambrian
rocks of the, 246.

Lower carboniferous rocks near Lesma-
hago in Scotland, 19.

J.owest sedimentary rocks of the south
of Scotland, R. Harkness, on the, 238.

Maidenhead, Berkshire, a cranium of
the musk-buffalo from the lower-
level drift at, 124; Mr. Prestwich on
the gravels near, 131 ; section of part
of the valley of the Thames near, 133.

Malvern Hills, Worcestershire, trap-
dykes in the, 382.

Mammalian bone from the bone-bed at
Lyme, the Rev. Mr. Dennis on a
probable, 252.

—— fossils from the red crag of Suf-
folk, Prof. Owen on some, 217.

Map of the coal-measures, 38 ; country
around Cobre, 146; Franco-Belgic
coal-field, 252; Leinster granites,
172; mineral-field of Cobre, 147;
Ulster granites, 199.

Martin, P. J., on some geological fea-
tures of the country between the
South Downs and the Sussex coast,
134.

Mastodon, remains of, in the red crag,
223.

Matterhorn as seen from the Riffelberg, ©

106.

Mauna Loa in Hawaii, Mr. Miller on
the recent eruption of, 171; Mr.
Miller’s further notice of, 386.

Megaceros, remains of, in the red crag,

26.

Middle eocene tertiaries of England,
France, and Belgium, Mr. Prestwich
on the correlation of the, 390.

Miller, W., on the recent eruption of
Mauna Loa in Hawaii, 171; further
notice of the recent eruption from
the volcano of Mauna Loa in Hawaii
(Owhyhee), 386.

Millstone-grit of Tintwistle, Cheshire,
Mr. Binney on some footmarks in
the, 350.

Moggridge, M., on the section expesed
in the excavation of the Swansea
Docks, 169; on the sunken portion
of Swansea Bay, 170.

Mont Blanc as seen from the valley of
Chamounix, 105; Major Charters on
a section near, 385.

Mont Lacha, section of, 385.

Moore, J. C., on the Silurian rocks of
Wigtownshire, 359.

Moss, bed of, observed in draining a
mere in Norfolk, 355.

Mountain or carboniferous limestone,
range of the, 55.

Mourne, granites of, 188.

Movement of land in the South Sea
Islands, 383.. _

Murchison, Sir R. I., on the discovery
by. Mr. Slimon of Fossils in the Up-
permost Silurian Rocks near Lesma-
hago in Scotland, with Observations
on the Relations of the Palzozoic
Strata in that part of Lanarkshire,
15; noticed, xlix; Reply to the Pre-
sident on receiving the Wollaston
Medal for Sir William E. Logan, xxiv.

Museum Committee, Report of the, iv.

Musk-buffalo, description of a fossil
cranium of the, from Maidenhead,
Berkshire, by Prof. Owen, 124.

Namaqualand, Dr. Rubidge on the cop-
per district of, 238.

New-red sandstone of Leicester, 369 ;
of Warwickshire, 374; range of the,
63.

Newcastle harbour, Australia, geology
of, 284.

Newer tertiary deposits of the Sussex
coast, 4.

Nobby Head, section of, 284.

North of France, coal-field of the, 252.

Notornis Mantelli, tibia of, 210.

Nummulitic rocks, Franco-Belgic, 72 ;
in Asia Minor, 4; of Bulgaria, 387.

Ocean-currents, Mr. Babbage on the
action of, in the formation of the
strata of the earth, 366.

Old red sandstone, range of the, 51;
near Lesmahago in Scotland, 17.

Oolitic series, littoral limits of the, 64.

INDEX TO THE PROCEEDINGS.

Opis carinatus, 324.

Orthoceras from China, Mr. Woodward
on an, 378.

Owen, R., on a Fossil Cranium of the
Musk-Buffalo from the Lower-level
Drift at Maidenhead, Berkshire, 124;
noticed, lix; on some mammalian
fossils from the red crag of Suffolk,
217; on the affinities of the large
extinct bird (Gastornis Parisiensis,
Hébert) indicated by a fossil femur
and tibia discovered in the lowest
eocene formation near Paris, 204.

Paleontological and stratigraphical re-
lations of the so-called sands of the

~ inferior oolite, Dr.Wright on the, 292.

Paleopyge Ramsayi, 249.

Paleozoic rocks in the parish of Les-
mahago, general relations of the, 17.

Paris, fossil bird from the lowest eocene
formation near, 204.

Peat-deposit of Wretham Mere, Nor-
folk, 356.

Peel River district, Mr. Wilson on the
gold-district of, 286.

Permian and triassic sandstones, range
of the, 63.

character of some.of the red sand-

stone and breccias of the south of

Scotland, Mr. Binney on the, 138.

rocks of Scotland, Prof. Harkness
on the, 254.

Phoceena orca, from the red crag, 228.

Phocena, sp. from the red crag, 228.

Physical geography of the tertiary estu-
ary of the Isle of Wight, 137.

Plant, J., on the upper Keuper sand-
stone and its fossils at Leicester, 369.

Plutonic rocks, Mr. P. Scrope on, 342.

Poole, H., notice of a visit to the Dead
Sea, 203 ; on the Coal of the North-
western districts of Asia Minor, 1;
noticed, xcvii.

Posidonomya minuta, Mr. Jones on the,
376.

Potash-granites of Ireland, 187.

Prestwich, J., on the Boring through
the Chalk at Kentish Town, London,
6; noticed, lix; on the correlation
of the middle eocene tertiaries of
England, France, and Belgium, 390;
on the Gravel near Maidenhead in
which the Skull of the Musk-Buffalo
was found, 131; noticed, Jix: Reply
to the President on receiving the
Donation Fund Award for M. Des-
hayes, XXv.

Protichnites Scoticus, 243.

Pteraspides of the tilestones, 98.

Pteraspis Banksii, 100.

truncatus, 100.

Pterygotus of the tilestones, 97.

Raised beaches in Argyllshire, Com-
mander Bedford’s notice of some, 167.

Red crag of Suffolk, Prof. Owen on
some mammalian remains from the,
Palle

Red deer, remains of, in Wretham Mere,
356.

Red sandstones and breccias of the
south of Scotland, Mr. Binney on the
permian character of some of the,

Report, Annual,i; of the Council, 1;
of the Library Committee, iii; of the
Musenm Committee, iv.

Rhinoceros, remains of, in the red crag
of Suffolk, 217.

Rhinoceros Schleiermacheri ?, 218-221.

Ripple-marks in the Longmynd rocks,
250.

Rubidge, R. N., on the geology of some
parts of South Africa, 237.

Salter, J. W., on a new genus of Ce-
phalopoda, Diploceras (Orthoceras
disiphonatum of Sowerby), and on
the occurrence of Ascoceras in Bri-
tain, 381; on fossil remains in the
Cambrian rocks of the Longmynd and
North Wales, 246; on some new
crustacea from the uppermost Silu-
rian rocks, 26; on the fossil tracks
from Binks, 243; on the fossils found
in the chalk-flints and greensand of
Aberdeenshire, 390.

Sands of the upper lias, Dr. Wright on
the, 292.

Sandstones and breccias of the south of
Scotland of an age subsequent to the
carboniferous period, Prof. Harkness
on the, 254.

Santiago de Cuba, copper-lode of, 144.
Sawkins, J. G., on the movement of
land in the South Sea Islands, 383.
Scotland, fossil crustaceans from, 26;
Mr. Binney on the permian character
of some of the red sandstone and

breccias of the south of, 138.

(South), Prof. Harkness on the
permian rocks of, 254.

Scrope, G. Poulett, on the formation of
craters, and the nature of the liquid-
ity of lavas, 326.

Section and fossils at Beacon Hill,
Gloucestershire, 300; Bradford Ab-
bey, 309; Crickley Hill, 297; Fro-
cester Hill, 302; Leckampton Hill,
295; Wotton-under-Edge, 306.

—— of Mont Lacha, 385; part of the
valley of the Thames near Maiden-
head, 133; the boring at Kentish
Town, 13, 14; cliffs east of Hastings,

INDEX TO THE PROCEEDINGS,

290; the lowest sedimentary rocks
at Eskdale, 239; the upper Keuper
at Shrewley, 374; upper permian
sandstones of South Scotland, 139 ;
two terraces of alluvium in the Val-
telline, 115.

Sections and fossils of the inferior
oolite and upper lias sands in Dor-
setshire, 310; in Gloucestershire,
295.

Sections in Cuba, 145; of coal-measures
near Lesmahago in Scotland, 25 ; the
cryolite at Evigtok, 141, 142; per-
mian rocks of South Scotland, 257,
260, 261, 262, 264; Silurian rocks
of Wigtownshire, 369 ; upper Keuper
at Leicester, 371, 372.

Selsea, tertiary fossils from, 4, 5.

Sharpe, Daniel, on the last elevation of
the Alps, with notices of the heights
at which the sea has left traces of its
action on their sides, 102; noticed,
Ixxi.

Shrewley, upper Keuper at, 374.
Silurian rocks of Eskdale, 238 ; of Wig-
townshire, Mr. Moore on the, 359.
Silurian (uppermost) rocks at Lesma-

hago, 15.

Siphuncle in Orthocerata, Mr. Wood-
ward on the, 379.

Slaty cleavage, Mr. Scrope on, 347; of
Mont Lacha, 385.

Slimon, R., discovery of fossils in the
uppermost Silurian rocks near Les-
mahago in Scotland by, 15; sections
of the coal-measures near Lesmahago
in Scotland by, 25.

Soda-granites of Ireland, 187.

Sorby, H. C., on the physical geography
of the tertiary estuary of the Isle of
Wight, 137; noticed, 1.

South Africa, Dr. Rubidge on the geo-
logy of some parts of, 237.

South Downs and the Sussex Coast,
Mr. Martin on some geological fea-
tures of the country between the, 134.

South of Scotland, Prof. Harkness on
the lowest sedimentary rocks of, 238.

South Sea Islands, Mr. Sawkins on the
movement of land in the, 383.

Special General Meeting, 384.

Spratt, Capt. T., on the geology of
Varna and its vicinity, and of other
parts of Bulgaria, 387.

Stigmaria in coal in Asia Minor, 3.

Strata, Mr. Babbage on the action of
ocean-currents in the formation of,
366.

Sus antiquus ?, 223.

—— paleocherus, 223.

Sus, remains of, in the red crag, 222.

Sussex Coast, Mr. Godwin-Austen on
the newer tertiary deposits of, 4;
signs of elevation of the, 6; Mr.
Martin on some geological features
of the, 134,

Sussex, West, drift-deposits of, 3, 134.

Swansea Docks, Mr. Moggridge on the
section exposed in the excavation of
the, 169. ;

Swansea Bay, the sunken portion of,
170.

Swiss valleys, tables of altitudes of the
heads of, and terraces in the, 123.
Sydney, Newcastle, and Brisbane, the

geology of, 283,

Syenite of Malvern, intersected by trap-
dykes, 382.

Symonds Hall Hill and Wotton-under-
Edge, the succession of strata be-
tween, 307.

Symonds, Rey. W. S., on trap-dykes in-
tersecting syenite in the Malvern
Hills, Worcestershire, 382.

Table of the distribution of fossils in
the inferior oolite and upper lias of
England and the Continent, 317.

Tables of altitudes of the heads of
Swiss valleys and of altitudes of ter- .
races in the Swiss valleys, 123.

Tapirus priscus, from the red crag, 222.

Tayler, J. W., on the cryolite of Evig-
tok, Greenland, 140.

Tertiaries of England, France, and Bel-
gium, the correlation of the, 390.
Tertiary estuary of the Isle of Wight,
the physical geography of the, 137.
Terraces of alluvium in the Alpine val-

leys, 113.

Theories of crater-formation, 328.

Tibia of Gastornis Parisiensis, 204.

Tibiz of birds, characters of, 205.

Tilestones, or Downton sandstones, in
the neighbourhood of Kington and
their contents, Mr. Banks on the, 93.

Tilestones, probable age of the, 99.

Tintwistle, Cheshire, footmarks in the
millstone-grit of, 350.

Trap-dykes intersecting syenite in the
Malvern Hills, Worcestershire, the
Rev. Mr. Symonds on, 382.

Trigonia Ramsayi, 323.

Trinidad, Mr. Bowen on the geology
of, 389.

Ulster, granites of, 199.

Unionidz in the Hastings sands, 291.

Upper Keuper sandstone and its fossils
at Leicester, Mr. Plant on the, 369;
of Warwickshire, Rev. P. Brodie on
the, 374.

Upper lias sands, Dr. Wright on the,
292.

INDEX TO THE PROCEEDINGS.

Uppermost Silurian rocks near Lesma-
hago in Scotland, 17; new crustacea
from the, 26.

Upright tree-trunks in the Newcastle
cliffs, Australia, 285.

Ursus, remains of, in the red crag, 227.

Valenciennes coal-basin, MM. Degousée
and Laurent on the, 252.

Valleys, Alpine, lines of water-level in
the, 110; terraces of alluvium in the,
113.

Valtelline, terraces of alluvium in the,
1G

Varna and its vicinity, Capt. Spratt on
the geology of, 387.

Veins of gold in quartz and other rocks,
Mr. Ibbetson on the possible origin
of, 384.

Vesuvius, history of, 335 ; in 1756, 355 ;
in 1767, 336; in 1822, 337.

Volcanic cones, formation of, 327.

Volcano of Mauna Loa in Hawaii, no-
tices of the recent eruption from the,
171, 386.

Warwickshire, upper Keuper sandstone
of, 374.

Wealden series, extent of the,66; strata
at Hastings, 288.

Western Europe, outline of the geo-
graphy of, at the coal-growth period,
57.

vee Islands, raised beaches of the,

167.

Whales, remains of, from the red crag,
228.

Wicklow and Wexford, granites of, 181.

Wigtownshire, Mr. Moore on the Silu-
rian rocks of, 359.

Wilson, S., on the geology of the
neighbourhood of Sydney, Newcastle
and Brisbane, Australia, 283.

Wolf, remains of, in the red crag, 227.

Wollaston Medal, Award of the, xxi.

Woodward, S. P., on an Orthoceras
from China, 378.

Wretham Hall, Norfolk, Mr. Bunbury
on some appearances observed on
draining a mere near, 355.

Wright, T., on the paleontological and
stratigraphical relations of the so-
called sands of the inferior oolite,
A922.

Ziphius, remains of, from the red crag,
228.

END OF VOL. XII.

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