*. 7
AH ben Oe He ee Rotem the

a hehe oh ~
Tye Bodh to Ebi em Phat a Sa me Hat Oe =

ra
est

ss

‘

Be fim db Oita ee
he Petar Rectal
A Snip Hanlin NeeAint ; ate :
Tete OW weer ave AS age ate eee
i o ~ Cin ben te tse

FP -9 Hb alent dada hot

ee —s- i i ;
ree eae ¥ ~ . todo bi y Zi obedient ~ ¢ rare ys we - J eS ee Gain oe . ‘ Ge ee ee cans ee eet eee
nr med te Bs gm Sethe > i . See ee Babe a : 7 ’ ae seo ee a Oy" 9 ‘ ~ Aan ; , HN tel RP PAN IN ed A
Daim a= hn Onl oO ‘ nt ahh 6 A LO Delta tm the tai heh aR - Goat oe Bin Fin Pee Bi teal Sh Gallet Md Onde ee wee : f atid A-ha Poke EP oP FU OP AAP
6 naan Ge on thr fh R= Sag hy NV Hoots Berl pn a nF = meth Ae PR EM A ne PE ES es ina ~ Oty oe eo nik ¥ A I I yay ae
* Ee ee ee ee ae mtv ‘ 7 ad ante Aerie oe “ na , = " : al serine We ah rs betel nb Gdn wok) iAcamaed

es Re Pr Bo bebe tab 0-4 ted dts CN ee eee ee 3 . ps . A .’ q - . 3 > 4 > > x Shinn ar en eeaicatd entity Oh ean 248i
An “ - a ae “tae~ La- Rakhe tient NeW Fale Ff PB BIPM the to - ae oa ¥. - <> > : ae — Maal Pardizer nd Sy , i pune tie eek ee oo
“tev - a : * t : ms ‘ w Leth te niband ae —s 8 . EOSY - - ' rod oe < YS A —_ <ents: Se eae ee ee “ ‘ 5-8 " Apediatatt A adhatenetl
o-2 . . a R= bh Ht Be nif fia Pe PA = Om Ge ON. - rr te ‘ Seti : E aw " ; ee 4 a y en tam ttn tn enh Nn ha 7 + v -! eee

en Be Fe a Aho adhe eae re i gd
. ‘ OPA P DA eho, Balm shal F nnn tant

eae Me Te oe eee oe ae Ce iat 3 vet O-in Penden de> Pin De tne aight al y
BeDa Ve Ape MB toy aM eB Bn Pant 4 Me z a , . Ftd Pot iy ; v meth oe ra : a : —— niet a PS Ne ag EE RT ao aoe ihe a> “
Seb hm en eis OE B P Foe the ho Mea Baie mee 3 _ " - ‘- 3 ms . . _— x . - ~ * a. 2 . ~ oes os i Nw ms Fa ~ to Rinkrtnn ints AM Nalin? a
Vent taritw t= thelr R= nthnt <n o- 4 fr b~ bin RR DMS, erty oo ee aie Fe > ame oldie te Nah AE a ten elt > ~ : ~ ee ag ee r Pur PEAT AS MP

aha Rade Reeth the lho De i Be BB Oe bene Ha we bret nat Pen ne 36<0..4-2- <P Aa MOS bs ' = cA ~A PEEP LETS OA
Fp et oR AFG mle BBD RS * 4 4 / s tn > r 7 pee Sarewr ele
Balle Bi Fett hea a Ga Om ae. - mtr“ ~~ e- Oe ee ee ee we ee ee ee
BO Ne te Het of he Ov Gat te . oe as ; Rn net the thot Fn
SE NES
OE SAM = Ano ie tm admin
ee eee ee ee 2
4 0 HR 0 ym a Font we mae
SE NT pit the Ane ame &
We Bin fiw Sy mate Fe Oe He nde

bettie Ms
Se a eres oar

ta ah hn Eth >

Ohms
Ph he tain Ge TO ob bh
Pe Recintig tual Yet Sa Pom
WDA Beh — te poy

a eo ee
a

ot

er T's we

Beat «

hi) ae . é: ‘
MAT Gihe
pai

cS
to
wo |
’
t

~

BY Roa
iO iia i
WAM ; ivan
# ines ,

et) ea

j, Ohas, CANGHAN, Horr
reso dais VE be LB) 4.
cc ante, AP @zWier.

iad ae oe” Vial ‘és
ont

se y . Ye . senaa
nf alte A a-L y :
Fi Ar Ve
z .
os |

oe

i Ay AL
ven
a
¢.
} 4
ti ie
¥ a
fae)
, i
.
i
; 2
,
{
ay
f
5 M
‘ j
‘ ‘
oi
i
P 7
i j
a T
te!
~s
5
’
i ‘
‘
-
i f . pe
? fret a i {
s , 7 - . ’ i dg
S ‘ Yer el Te t ;
nF iv, is Ly gn J he
‘ Te ‘ute tn A
. ; py [
r p
,
os
i
9
’
i".
aie
j
|
'
{

— fo fan
450, 64

a vA sine Fd
(EEO A é
NH vi

QUARTERLY JOURNAL

GEOLOGICAL SOCIETY OF LONDON.

EDITED BY

THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.

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

se a nn ——

VOLUME THE NINETEENTH. i>
Ke TG
1863. fs

PART THE FIRST.

PROCEEDINGS OF THE GEOLOGICAL SOeiehy) iil Yo

LONDON :

LONGMAN, GREEN, LONGMAN, ROBERTS, AND GREEN,

PARIS :—FRIED. KLINCKSIECK, 11 RUE DE LILLE; J. ROTHSCHILD, 14 RUE DE BUCI;
LEIPZIG, T. O. WEIGEL.

SOLD ALSO AT THE APARTMENTS OF THE SOCIETY.

MDCCCLXIII,

List

OF THE

OFFICERS

OF THE

GEOLOGICAL SOCIETY OF LONDON.

WADARAPE AANA”

Elected February 20th, 1863.

RARALARAASIIYS

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

Wice-PrestVents.

Sir P. G. Egerton, Bart.,M.P.,F.R.S. & L.S. | Leonard Horner, Esq.,
R. A. C. Godwin-Austen, Esq., F.R.S. Sir Charles Lyell, F.R.

P very

Secretartes.

William John Hamilton, Esq., F.R.S.
Warington W. Smyth, Esq., M.A., F.R.S.

PForeiqn Secretary.
Hugh Falconer, M.D., F.R.S.

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

COUNGIL.

John J. Bigsby, M.D. Robert Mallet, Esq., C.E., F.R.S.
George Busk, Esq., F.R.S. Edward Meryon, M.D.

Robert Chambers, Esq. ., F.R.S.E. & L.S. John Carrick Moore, Esq., M.A., F.R.S.
Sir P. G. Egerton, Bart.,M.P., F.R.S.&L.S. | Prof. John Morris.

John Evans, Esq., F.S. A. Robert W. Mylne, Esq., F.R.S.

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

Hugh Falconer, M.D., F.R.S. Prof. A. C. Ramsay, M.A., F.R.S.

R. A. C. Godwin-Austen, Esq., F.R.S. Warington W. Smyth, Esq., M.A., F.R.S.
William John Hamilton, Esq., F.R.S. Alfred Tylor, Esq., F.L.S.

Leonard Horner, Esq., F.R.S. L. & E. Rev. Thomas Wiltshire, M.A.

Prof. T. H. Huxley, F.R.S. & L.S. S. P. Woodward, Esq.

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

Assistant-Decretary, Librarian, anv Curator.
H. M. Jenkins, Esq.

Clerk.
Mr. G. E. Roberts.

Library and fHuseum Assistant.
Mr. A. Stair.

TABLE OF CONTENTS.

PART I.—ORIGINAL COMMUNICATIONS.

ANDERSON, Dr.G. On the Occurrence of a Bituminous Substance
memrvonmieerald, | (UADSURACE DS aws's. or vere sce scene dies seey

APPLEGATH, Capt. F. On the Geology of a Part of the Masulipatam
Me OLIN POR Vice ates oe be cet cnet esis scree tiene sys

Austin, C. E., Esq. Geological Notes on the Locality in Siberia
where Fossil Fish and Estherie have been found; with a Note
on Estheria Middendorfii, by Prof. T. Ruprert Jones, F.G.S.

522

MN Re cca Psa ei uals» Geers, so0 A. a box asate: «ist hears) situs tc Hons eo LE
Biessy, Dr. J. J. On the Cambrian and Huronian Formations.... 36
Curry, T., Esq. On the Gravels and other Superficial Deposits of

Pmtlaw, Hereford, and Slapton.. 6. . ceca e pectic cts seeds ees 175
Darwiy, C., Esq. On the Thickness of the Pampean Formation, near

SORTS et edie ee he dts ce Ons oc ts poe ES ENC ye 8's 68
Davinson, T., Esq. On the Lower Carboniferous Brachiopoda of

ape cOcdL..” CW Ih PE PIgte)ee ise sede se cee ae cbiens 158
Dawxins, W. B., Esq. On a Hyzena-den at Wookey Hole, near

© RSE SACOG DRA eh ee ea ar 4 CPE 260
Dawson, Dr. J. W. Further Observations on the Devonian Plants

of Maine, Gaspé, and New York. (With 3 Plates.).......... 458
——. Notice of a new Species of Dendrerpeton, and of the Dermal

Coverings of certain Carboniferous Reptiles ...........0.005 469
Day, E. C. H., Esq. On the Middle and Upper Lias of the Dorset-

PAS OLE aeRO Ac gn Ale 278
Duncan, Dr. P. M. On the Fossil Corals of the West Indian Islands.

ree eta WEI OE LUGS. ere Sais ca sive ep iadty eels ea.che e's acess 406
Frereusson, J., Esq. On recent Changes in the Delta of the Ganges.

Pe TR yore cease aie ate 79 tinue vain vada iahy OA EMO, 8 321
FisHER, The Rey. O. On the Brick-pit at Lexden, near Colchester ;

with Notes on the Coleoptera, by T. V. WoLuaston, Esq., M.A.,

ROE ee ene, VU nt ee oe Sass tee edocs sultan 394
Gorpvon, The Rey. Dr. G., and the Rev. J. M. Joass. On the Relations

of the Ross-shire Sandstones containing Reptilian Footprints ;

with an Introduction, by Sir R. I. Murcuison, K.C.B., F.R.S.,

TCG Cee i PEROSERAGE: [OU Ritardie ocd aN eit c ks cee ae eee 506

iv TABLE OF CONTENTS.

Page
Groot, Mijnheer C. pr. Notes on the Mineralogy and Geology of
Borneo and the adjacent Islands .....c.ccsecsvecsesssavess 515

Harkness, Prof. R. On the Skiddaw Slate Series ; with a Note on
the Skiddaw Slate Fossils, by J. W. SALTER, Hsq., F.G.8S..... 113

Hopeson, Miss KE. Ona Deposit containing Diatomacee, Leaves, &c.,
in the Iron-ore Mines near Ulverston. [Abridged.].......... 19

Hott, Dr.H.B. On the Correlation of the several Subdivisions of the
Inferior Oolite in the Middle and South of England. { Abridged. | 806

Huxtey, Prof.T.H. Description of Anthracosaurus Russell, a new
Labyrinthodont from the Lanarkshire Coal-field ...........- 56

JAMIESON, T, F., Esq. Onthe Parallel Roads of Glen Roy, and their
Place in the History of the Glacial Period. (With 1 Plate.) .. 2385

JONES, Prof. T, R. On Fossil Estherie and their Distribution .... 140

Konrncx, Prof. L. pr. Descriptions of some Fossils from India, dis-
covered by Dr. A. Fleming, of Edinburgh. (With 8 Plates.).. 1

LEcKENBY, J., Esq. Onthe Sandstones and Shales of the Oolites of |
Scarborough, with Descriptions of new Species of Fossil Plants.
[Abstiract..| ct spasdiousem ok Sens emule ech tiettdnalt easier 519

Ligutsopy, R., Esq. Notice of a Section at Mocktree .......... 358

MacponaLD, J. D., Esq. Description of a new Fossil Thecidium
(ZT. Adamst) from the Miocene Beds of Malta................ 517

Macxenzir, A.C., Esq. On the Occurrence of a Bituminous Mine-
ral at Mountgerald, Scotland. [Abstract.]..............000. 522

Marsu, O. C., Esq. Description of the Remains of a new Enalio-
saurian (Hosaurus Acadianus), from the Coal-formation of Nova
mcotia. . (Abridged.) o.ecedanp ceeding A OLTE Lae CRON COM 52

Moors, J. C., Esq. On some Tertiary Shells from Jamaica; with
a Note-on the Corals, by P. Martin Duncan, M.B., F.G:S. ;
and a Note on some Nummuline and Orbitordes, by Prof. T.
RUPERT JONES, 1, G..0.c-cce 4. > vores fiecamede tc Suen aes ee 510

Murcutsoy, Sir R.I. On the Gneiss and other Azoic Rocks, and on
the superjacent Palzeozoic Formations of Bavaria and Bohemia . 354

——. On the Permian Rocks of North-eastern Bohemia.......... 297
Nicot, Prof: J. On the Geological Structure of the Southern
Grampians 6 33.0 4ac5 «sem ew peenrla ees dh bss teal aol ae 180

OLpHAM, Dr. T. On the Occurrence of Rocks of Upper Cretaceous
Abe in (Mastorm Bengal. 5c itieincta hiaeidele ee sd nae aot 524

Porter, Dr. H. On the Occurrence of large Quantities of Fossil
Wood in the Oxford Clay, near Peterborough. [Abstract.].... 317

PrestwicH, J., Esq. On the Section at Moulin Quignon, Abbeville,
and on the Peculiar Character of some of the Flint Implements
recently discovered there” 24-65... 4. % 22 ag ERRMENe 0» n'y ee 497

TABLE OF CONTENTS. v

Page
Roserts, G. E., Esq. On some Crustacean Tracks from the Old Red
PA SIOHO MCAT UAMMOW NC Wee sass sheng kes cssesvercseveeees 233
—— and Jonn Ranpat1, Esq. On the Upper Silurian Passage-
UU pe eS a a 229
SALTER, J. W., Esq. On a new Crustacean from the Glasgow Coal-
ES ee SE en ee ee ee 519
——. On the Discovery of Paradoxides in Britain ..........e00 274
——. On some Fossil Crustacea from the Coal-measures and Devo-
sen docks of British North America... .......6c000e000008 75
—. On Peltocaris, a new Genus of Silurian Crustacea.......... 87
—. On some Species of Zurypterus and Allied Forms.......... 81
——. On some Tracks of Lower Silurian Crustacea .......... da, 92

——. Onthe Upper Old Red Sandstone and Upper Devonian Rocks 474

Sawxins, J.G., Esq. On the Association of Granite with the Ter-
tiary Strata near Kingston, Jamaica...........ccesececeeees 35

SEELEY, H., Esq. A Monograph of the Ammonites of the Cambridge
ATR fA DCETSLO LY y's ne nie: 4 aig Wi plan (nena oral us aes no eter e s 519

Sorsy, H.C., Esq. On the Original Nature and Subsequent Altera-
PEON eID at creo pec. Sire POP she Lk OWE ee eal se 401

Woopwarp, H., Esq. On a new Macrurous Crustacean (Scapheus
ancylochelis) from the Lias of Lyme Regis. (With 1 Plate.) ., 318

Waieut, Dr. T. On the Fossil Echinide of Malta; with Notes on
the Miocene Beds of the Island, by A. Lerrn Apams, A.M.,

STE ia is Mays she ig are ns einh mun nish donot 9 <2 oe 277
PMR OTG | es eS Seis welale ses eh elele eek Dae we wale eine Fak die gore
TES SST TsO eee peas
Tuist of Foreign Members .............cceeeceeee ee ce ees eeens xix
amt of the Wollaston Medalistes<. 0565 s:0:6 ers e 4 dnareltee yee * ce i oi

Donations to the Library (with Bibliography) .... xi, 96, 210, 372, 527

EXPLANATION OF THE PLATES.

PLATE
I.)
II.
ae PuNsJAUB Fossizs, to illustrate Prof. de Koninck’s paper on
¥ *$ some Fossils from India, discovered by Dr. A. Fleming, of
Midinburphnisy cco. Fear coach neces et erate ees eachee to face page 18
VIL

VIII.

LOWER CARBONIFEROUS BRACHIOPODA FROM Nova Scorta, to
IX. illustrate Mr. Davidson’s paper on the Lower Carboniferous
Brachiopods, of Nova Scotia, «. ..ha:cssesscueteonaes eeseecn eeebeas 175

SKETCH-MAP OF A PART OF LOcCHABER, to illustrate Mr. Jamie-

x son’s paper on the Parallel Roads of Glen Roy, and their place
in the History of the Glacial Period ...........ssscsesenecesoncees 235

SCAPHEUS ANCYLOCHELIS, H. Woopw.,to illustrate Mr. H. Wood-

ward’s paper on a new Macrurous Crustacean (Scapheus ancy-
lochelis) from the Lias of Lyme Reis............cececscseecenseees 318

XI.

Map OF THE RIVERS OF BENGAL, to illustrate Mr. Fergusson’s
paper on Recent Changes in the Delta of the Ganges

West Inpran Fossir Corts, to illustrate Dr. P. M. Duncan’s

XV paper on the Fossil Corals of the West Indian Islands. Part I. 456
XVI
XVHL. EVONIAN Prants, N.E. AMERICA, to illustrate Dr. Dawson’s

pe
sie
Hen aaaq 8

paper on the Devonian Plants of Maine, Gaspé, and New York. 468

LIST OF THE FOSSILS FIGURED AND DESCRIBED
IN THIS VOLUME.

ra

[In this list, those fossils the names of which are printed in Roman type have
been previously described. ]

Name of Species. Formation. Locality. Page.

PLANT. (22.)

Algz. Pl. xix. f. 32,33......000..e0eee-| Devonian...... GASPEs Sires ikesivcus 467
Anarthrocanna Perryana. PI. xviii. ) (

Rca c ncpislns sip siegusng ante wees eee 461

Carpolithes lunatus. Pl. xvii. f.11 . a | 464
—?siliqua. Pl. xvii. f.4 ........000. 465
spicatus. Pl. xvii. f.15 ......00 461

Coniferous Wood. PI. xviii. f. 20, and, :

PONSA fe Pe cages sss cavasuvecsencesavesue : ee 460
Petites. ( Pyenophyllum) Wetivosics: Devonian...... GEE: © hee scones )

PE SVU: £. Oo ines xescccecesccsssedsosseves | 462
Cyclopteris Brownii.. Pl. xvii. f.6 . 463
—— Jacksoni. Pl. xix. f.26 ......... “|| 462

Rogersi. Pl. xvii. f. 17, 18, and

PL. Xix. f.27 ...cccccscevcseece sore | 463
Cyperites......... beta be ae ao i ware ) \ ee
Incerte sedis. PI. xviii. 10, ‘1 an . Z 4

Soe eae one i } Devonian......|Gaspé rae Staecs { 467
Leptophleum eas Pl. xviii. | :

Bear, pavan atone Naan atomic cas actse oss . 462
Teicopniites a fete, Pl xvi fl es Devonian..,....) Perry ..s.e0.s+e0 462

Richardsoni. Pl. xvii. f.1,2 . q a

Nematoxylon crassum. Pl. xix. f. BA . P 4
aus Pi xvii. f. 23. Si cscveneds sete cae gh CRUE es phos 1 467

PSUOPHYTOMN. 2... Jess. .sesscceccsnecs papi Devonian...... PORT Gants acebese sof 461

—— princeps. PI. xviii. f. 22......... Devonian...... GRSNE! See cessv css sec: 465

Sphenopteris recurva. PI. xvii. f. 7, 8. Ae

Stigmaria pusilla. Pl. xvii. f.3 ....... : ee

ie homansine filicula. PI. xvii. f. 12, A oo eee RENE y Meee ounes

13 SCR EOE ERE e eSB ees oees POCERO ode aese eease, 464

vill

Name of Species. Formation. Locality.

C@LENTERATA. (63.)

——, var. nobilis. Pl. xiii. f. 2a,

( Actinozoa.)
ae sabacice ee \ Nivajé shale...| San Domingo ...
Alveolites septosa. Pl.ii. f.1 ......... Carboniferous | Punjaub ..........
Chert - forma -
Alveopora Deedalzea, var. regularis. TION Fives: sos Antigua .........
Plo wivad, 40-405. Js. apoccseveeoeceearer White Lime -
StONE!s. i.ts. Jamaica? 254...

———_ ——, VAT. MINOL veccecssseeecoseees ek SES \ Antigua .........

—— microscopica. Pl. xiv. f.5 ...... Marl - forma - eee

Astrea Antiguensis. Pl. xiii. f.8...... tion. ictal pd tee
ARTAUATUMdactcaaoes caectensse cece Tertiary ........) Montserrat ......

, Mar] - forma -| } Barbadoes ......
Barbadensis. PI. xv. f. 6a, 60... { Kena \ Ae alee
cellulosa. VP. xiii. f. 10 .......... Conglomerate | Antigua .........

Chert - f - ;

— 5 VALs, CUNUAIGs<osccces ns sie'ssisi { Ee saa \ Antena + ..5. ccc
Costata.. PYM. 9 coscescssstinanlensansesaescpcabactechioenasesnceeee eee aee
crassolamellata. P\.xiii.f.1la—le.| \

SS , var. magnetica. PI. xili.| |

POAGL AD weary aecsceeeeoncet ne neens eeetes
a , var. magnifica. Pl. xiii. f. 3 r
pe ar: matnor. Pleat 162: te nS + Antigua ae

POOP OPHSEHEOEE® Pee eeeFHHSH SLES HOH EHFEe

——, var. Nugenti. Pl. xiii. £5] |

26

— » Var. pulchella...ccsccsesseese-

—— cylindrica. PI. xv. £.8....06. pees brane } San Domingo ..

—— endothecata. Pl.xv.f.7a,7b..,| Nivajé shale...| San Domingo ...

— —,,var.l. Pl. xiv. f.9.........

$$ VAL. 2 rieecescececcscnssceveeen i s eae } antigua oe eee

ion.

See a, VAL: B) cwituisacegeasnnetsonmessen

—— megalaxona. P. xiii. f. 12a, 128. ane a

—— radiata, var. infermedia .........4. yas pare Antigua .......
tenuis. Pl.xiii. £1) ..scsscsseee ec Suara }

Astreina? Dendroided ?..........s0cesees Tertiary: cons cacs}e- ae AMIQICR 125508

Astrocoenia ornata. Pl. xiv. f.7 ...... { yes SDs } Antigua’ oo -..0

ASF OFIG GRUAIS © Svaioeices seviascaesnsnaneia
PANT IGUCNSER ino canen see ner arenes kena eee os } Aubigiia:. 2-402.
polygonalis. Pl. xiv. f.6 ......... :

Barysmilia intermedia. Pl. xv. f. 4... aertre } San Domingo ...

Brachycyathus Henekeni. Pl. xv. f.1.| Nivajé shale...| San Domingo ...

Clisiophyllum Indicum. Pl. ii. f.4 ...| Carboniferous} Punjaub ........

Chert - forma -} }

Celoria dens-elephantis. Pl. xiv. f. 8. { ean.

(Jamaica, ..c.28

Cyphastr ea COStata cereccenessseresseeces (fy) Dever yin sscars | | Barbuda

i Antigua’ .......

Page.

1x

Name of Species. Formation. Locality. Page.

C@LENTERATA (continued).

(Actinozoa.)
Dichocenia tuberosa. Pl. xv. f.5a,50.| Nivajé shale...) San Domingo ...| 432
RCH GUUIUME oascccc.cocwscevecseencss Nivajeé shale... San Homined 430
BNF nisls « vidiencs cen acawnanveen's ss Blue shale... 8° ---1) 430
Isastrea arachnoidea. P1. ii. f. 2...... Carboniferous | Punjaub .......... 3
eeatertd, Pl xiv. £2 ocvcossenses Chert - forma - are 422
turbinata. Pl. xiv. f.la—le ... tion. Roe 423
Lithrostrotion irregulare ............0-... Carboniferous | Punjaub .......... 3
Meeandrina filograna. ......s0scseeceeevees HAE 5 vcs s4s San Domingo ...| 433
Lower Forma- :
BEDE cncasecedoeesas eeeciicame aes seee ia Amtifua ~......... 424
Ree eeIa TAVOSA J..6.... 00000000002 seen Carboniferous | Punjaub ......... 4
Montlivaltia ponderosa. PI. xvi. f. 6a,| { Nivajé shale...| San Domingo ...| 433
ari died cin csaukncie ni wee eninoe own asaoe Terigary:.....c.|) Jamaica: sav... 441
Phylloceenia limbata ...ccecccerssovecceees Yellow shale.. Geta caae 433
sculpta, var. tegula ......ccccecseee. Nivajé shale... } oS AEM 432
4 ' Postrero, San
Se leaa ee ae ae } Tertiary Ponce | Domingo ere 428
eeeoeer SCC CeeseFeeseesceeseteesteSetaseoee | Jamaica phish SF 437
Placotrochus alveolus. Pl. xvi. f.2a,25.| Tertiary........ JAMAICA... .<<508 438
Lonsdalei. Pl. xv. f. 2a, 26 eee ate : : 428
Porites Collesniana ....00..ccrseesssseo0e8 Nivaje shale.../ San Domingo ... 437
Rhodar@a irregularis cocecscccssceseseees aaa forename AMeud 2.2.5.0. 426
Siderastrea crenulata, var. dntillarum.| Nivajé shales..| San Domingo ...| 435
grandis. Pl. xvi. f.5a,508 ...... Periiagy.2. 2.5.1 Jamaica J.!.,.... 440
Stephanoccenia dendroidea .............. Miocenes..... 54 San Domingo ...| 432
— tenuis. Pl. xiv. f.3a,30......... Eee forma - | Antipua’’:::.....: 423
Stylophora affinis. Pl. xvi. f. 4...+0+... 436
BARS WENO Sean oan sascae esses Nivajé shale...) San Domingo .../) 436
Thysanus corbicula. Pl. xv. f. 3a, 30. 430
excentricus. Pl. xvi. f.3a—-3e...| Tertiary........ JAMBIGA 2.25005: 439
ECHINODERMATA. (2.)

Cidaris Forbesiana. Pl. iv. £.1, 2s..0+. : |
Philocrinus cometa. P1. ii. f. b. seems ees | } Carboniferous | Punjaub .........
Moxiusca. (54.)

(Bryozoa.)

Dichograpsus. Woodcut, f. 9-12 ...... 139
Phyllograptus. Woodcut, f. 7a, 7 0...| | Skiddaw slates} ..................08. 140
Tetragrapsus. Woodcut, f.8a,80... 140
Fenestella megastoma. Pl. ii. f. 3...... 5

coagerens* (Pini hl. Lonsncite : : 5
Phyllopora? cribellum. Pl. i. £2 .....| [ C@tPoniferous | Punjaub ......... 6
— >? Haimeana. P.i.f.3............ 6
Polypora fastuosa. Pl. i. f. 4 ........... Carboniferous} Moosakhail? ... 5
Retepora? lepida. Pl.i. f.5............ ' Carboniferous} Punjaub ......... 6

Name of Species.

!

| Formation.

Mo.tusca (continued).

(Brachiopoda.)

Athyris subtilita. Pl. ix. f. 4,5.........|

Camarophoria ? globulina? Pl.ix. f.11,
12

Soeeeeeseeseesss SS eeeseerereesesa tees

Productus Cora., Pls ix:.f 22,23... .2t-
semireticulatus. Pl. ix. f. 20, 21.
Rhynchonella Acadiensis, n.sp.? Pl. ix.|

EG ascii
Dawsoniana,n.sp.? Pl. ix. f. 13,
Ue Ee see

RET | Meru
Spirifera acuticostata. Pl. ix. f. 7,8...
glabras Pl ixot. Ol Otecsrecdscass:
Spiriferina cristata. PI. ix. f. 6......... |
Streptorhynchus crenistria. Pl. ix.
Ect D sc Keuniec sndccimaamoncdstetetdanatenees
Strophomena analoga. PI. ix. f.18 ... |
Terebratula sacculus. Pl. ix. f.1-3...| J L |
Thecidium Adamsi. Woodcut, f.1-3.! Miocene........ Malta.....as adeetene
(Lamellibranchiata. )
Anomia Lawrenciana. Pl. iv.f.7,8,9| Carboniferous | Punjaub...........
Curtonotus centralis. Woodcut, f. 4a,| ] ( Enniskeen, co.
BO ncarsiolv de saeaeacaecdees seciisesaducciuitgst Cork
|
elegans. Woodcut, f. 3a, 30...... > Pilton Group.. pire Bay,
elongatus. Woodcut, f. 5a—5d... | | (Co. Cork .citns
CRG Feiss oksnins scacdanawesmeneeaentes | West Angle Bay
Pecten, Asiaticus.” Pl. iv. £.6 ...0.aeere>
erebristria. Pl. iv. f. 5....008 ae . Punjaubigei).sceeee
Flemingianus. PI. iv. f. 4......+6. Cie oniere us
Solenopsis imbricata. Pl.iv.f.3....... Vurchaiiiss..coe:
( Gasteropoda.)
Bellerophon decipiens. PI. iii. f. 1...... P|
Jonestanus.” OPV Me £2: oscecwences
ortentalts,® “Pl. Wivtsio) cs sncecsees

Cepilisssur Pl Will f 3)<csasancsendnsss
INEFINGE 2. N.ISPs 0) aesacenue comnees Bata J
( Cephalopoda.)
Ceratites Buchianus. P\. vi.f. 4. ......| ]
Davidsonianus. Pl. vi.f.2 ......
Flemingianus. Pl. vii. f. 1. ««.....
Hauerianus., Pl. iis £..5....05.50000
latifimbriatus. PI. vil. f.2....... .
—— Lawrencianus. Pl. vi.f.3 ....... Carboniferous
—— Lyellianus. Pl.vi.f.1.......0000.
— Murchisonianus. P. viii. f.1....
planulatus. Pl. ¥.£. 1 ...22.0000..

SOTHO HEESe eee eo eEHOEH ee EEEseee

Macrocheilus avellanoides. PI. iii. f, 4 |

Goniatites ? Gangeticus. Pl.v.f.2 ...| )

Lower Carbo-

Locality.

Nova Scotia...

|
|

"
Punjaub 4
l

eeeeee

Page.

xl

Name of Species. Formation. Locality. Page.
Mo.tuivsca (continued).
( Cephalopoda. )
Nautilus Burtini. PI. viii.f.3 ...... cesle Namnmiphitic?.. Panjaabs: x ccdevsee': 15
—— Flemingianus. PI. viii.f.2....... 15
Orthoceras decrescens. PI. viii. f. 4... ; : 16
PACHIAIUME -osccdacoesseesee Secnideweper Carboniferons |Punjaub ...+..,... 16
= VESICUIOSUM versssecscercerseeccses 15
ANNuLOoSA. (44.)
( Annelida.)
Serpula advena. Woodcut, f.6.........,|Upper Old Red |Caldy Island........| 496
( Crustacea.)
eh eee ee estes} Wineden, \} Devonian...... Db, SOHN 'S evasesc. ss: 76
Apus. Woodcut, POTD icegespiacesss BSi09, CLC senvenlacacvwcceeass eee 90
Argas. Woodeut, f. RR CarbOMilerOus)| nie beascassccescossncvee 90
Caryocaris Wrightii. Woodcut,f.15| SkiddawSlates|.........ccccsesesseees 139
Ceratiocaris. Woodcut, f.6............ Upper Silurian) .:...5/cciscscvseesses. 90
Crustacean, Tracks of a. Woodcuts,| { Old Red Sand-
t Ta bibencbeeae Se chatiecauesecnes¥l stone. } Bouldon ......... —
Upper Silurian
Dictyocaris. Woodcut,f.7 ..........00+ and Lowest | > Joggins ........... 90
Devonian
Diplostylus Dawsoni. Woodcut, f. 6...) Coal-measures)..................00006 77
Dithyrocaris. Woodcut,f.8............ Carboniferous) | e.s 35.0040 asses nsiewes 90
SACS jay TA i aia 8 en 90
PEHPICR 5 or coninssele pa.» = sciesisises vec Lower Oolite |Scarborough ........ 153
Soe te sg aaa Wealden ...... ELANOVER . bawersc005s 154
ERROR fas dansig Gakechesenres se oi0'a clos 0 Permian ....... { eee ee 145
WPTONEL cies cide eSae ore ac accaices'a ae Mesozoic ...... CaChenta cesssicccve 155
Sette MUG UMLICHISIS. 5.050502 0000 sensi cvcnciass Low’ Jurassic?| Kota......00s..-s0s00e 149
IMGMEAHENSIS..52. 2.2205. 00e0e-00-0- Upper Trias ? |Mangali.............. 149
——_ MEMbranacea..........scceeceseeeeeee sane pand: | Caithness........ 142
— Middendorfii ........... Re wesceeNees Miocene ?...... MEDOVIR caus otcedeens 73
; Baden, Wirtem-
Seem MPRISENEY, «ch cv aiws cs cr esicceurescsdebsass Kenper.ss...« berg, a } 146
— , var. Brodieana............ cea aR DEOEO 02) c28se Aust Passage ......| 148
Lower Meso- |N. &S. Carolina,
eo ae ein ceases }is1
—— Murchisoniz................0.ecesee: Oxfordian ..... DEVE roscccenoassocas ss 154
——— Portlockil .........sesccscecscscceess Permian .¢.5.:. Dungannon,Tyrone} 146
SUR EGERAL RSet CA ae muiidu asi; eben vases exe Carboniferous | Bavaria, &c........ a
—— ——,, var. Binneyana ............ Coal-measures|Derbyshire .......... 144
Lower Carbo-
—— g WOKe PALER. by. <sceesendees Rimeias } Lammerton...... 144
TL) Egat GS i nee ee Coal-measures| Astley, &c. ......... 144
Eurypterus. Woodcut,f.5.. Port Hood, Cape 78
ieihan: cee feror. Woodcut, Breton
See ae a Neate eens wane dos seca eae Coal-measures|< N. Staffordshire 86
Pendleton,
mammatus. Wondcut, f. 1-7..... ) = eee } 85

xii
Name of Species. Formation. |

ANNULOSA (continued).
( Crustacea.)

Eurypterus pulicaris. Woodcut, f. 9,10} Devonian......
DGGUIEEL css coos Snedecrs veeauuosa tess Carboniferous
—— (?), tail of. Woodcut, f. 4........ Coal-measures
Hymenocaris. Woodcut, f. 3........006. Lingula-flags |
Leperditia, Beyrichia, &c. Woodcut,

Paradoxides Davidis. Woodcut.......
Peltocaris aptychoides. Woodcut, f. 1.
—? Harknessi. Woodcut, f.2......
— ? Track of. Woodcut ........ eee
Woodent, £450 wec.sccccccsncnne Lower Silurian
Scapheus ancylochelis. Pl. Xi. ..eceees. Lower Lias ...

Liandeilo flags

VERTEBRATA. (6.)
( Pisces.)

.|Carboniferous .
Carboniferous .
.|Carboniferous .

Acrodus Flemingianus. P\. viii. f. 5..
<i SP)- sc cseneddenscoesnscanesnueseet

p-
Saurichthys? Tndicus. Pl. viii. f. 6, 7..

( Amphibia.)

Anthracosaurus Russelli. Woodcut, Galt iaaiees

Locality.

st, John’s:c..04e. ae
Kirkton, Bathgate
J OPPS os aden. cases

eee erases eceereeseeeees

ey

Glasgow «...5.5...0s:

St. David's:.<cve.
Dumfriesshire...
Dumfriesshire ...
Chirbury, Salop

Lyme Regis ....... e

ge) WUTC Bak dons <otanes
so Chedexooy.c.cv< wade
..| Vurcha..... sen aloha

AIPATIC 2 ees cass

Dendrerpeton Oweni..o..scccececcesveeeee Coal-measures ...|Joggins ....... se0.8.

Kosaurus Acadianus ........ cee ee Carboniferous ...

South Joggins......

Page.

LNT

ERRATA ET CORRIGENDA.

Part I.—PrRocEEpInNGs.

Page 42, line 4, for fluates read fluorides.

”
”

68, footnote, add Appendix, by Prof. T. H. Huxley.
79, explanation of woodcut, Fig. 1, after Anthracomya insert (Naiadites) ;
Fig. 2, for Natadites levis read Anthracomya (Naiadites) levis.
358, line 11 from bottom, for newer read older.
405, line 2, for 3 diameters read 2 diameters.
456, line 11 from bottom, for San-Domingan read Central American.
499, transpose line 28 to below line 31.
502, line 28, before occasional insert an.
536, line 30, for Trigen read Triger.

[See also the Appendix to Dr. Duncan’s paper, p. 456. ]

Part II.—MIscEe.LLANeEovs.

Page 3, line 13 from bottom, for Kalakvi (Gulgrud) read Kalakri (Gulgrad).

”

a

’
”
”

5, line 7 from bottom, for Arabio-Caspian read Aralo-Caspian.
6, line 1, for Arabio-Ponto read Aralo-Ponto.

6, line 7 from bottom, before ice-action insert direct.

22, line 25, after have insert been.

a.

ee a

aw
a) . 2 tine br be
a a Wite , ve tot? Ve at Ba. 7

\ ‘
Pe ia e>
‘- >
é
Ls cs Se
P=, “
(eer)
ae
jis ie es
.
‘ 2S
Ck =
> see 2 . ‘er e
it >
-
_
oT |
a 7 7 aw Cos

; toidasne bene
ey nt oe
kp =e Oy" Bein sale

* 2a ‘ig

iinet en

Y any avd

5 «Se pe wag vei
| | . Se ae SP

Pee ee e aes
sa ee aa aioe enc rte
pga) fata fai Sher * igi

mil, ee 'e

GEOLOGICAL SOCIETY OF LONDON,

ANNUAL GENERAL MEETING, FEB. 20, 1863.
REPORT OF THE COUNCIL.

In presenting their Annual Report to the Fellows of the Geological
Society, the Council have again to congratulate them upon the nu-
merical increase in the Society during the past year, and also upon
its financial prosperity.

The augmentation in the number of the Society has occurred
through the election of forty-six new Fellows, forty-two of whom have
paid their fees. These, with seven previously elected who paid their
fees in 1862, make up the unusually large number of forty-nine
new Fellows. This increase is probably attributable to the equali-
zation of subscriptions in accordance with a resolution passed at a
Special General Meeting held on February 26th, 1862, by which
all Fellows elected after March Ist, 1862, pay £2 2s. annually, and
by which those previously on the books as Resident Fellows pay the
same amount, instead of the former scale of contribution.

Against this increase must be placed the loss which the Society
has sustained by the death of fifteen Fellows and the resignation of
five others. Four Foreign Members have died, and the places of
three have been filled up by the election of new Members. The
number of extraordinary Members has also been reduced by the
death of one Honorary Member.

The total number of the Society at the close of 1861 was 940; at
the close of 1862, 969.

No special items have occurred in the expenditure of the year,
but, on the contrary, the expenses of the Museum have been con-
siderably reduced ; consequently the Income has exceeded the Expen-
diture by £227 2s. 9d.

The Funded property of the Society remains the same as at the
last Anniversary, viz. £4350.

At a Special General Meeting held on January 8th, 1863, it was
resolved :—

I. That the number of Foreign Members be in future limited to
forty, instead of fifty as heretofore.

VOL. XIX. a

ii ANNIVERSARY MEETING.

II. That a Class of Foreign Correspondents be instituted, not
exceeding forty in number.

Ill. That the Foreign Members shall be elected out of the list of
Foreign Correspondents.

The Council will take an early opportunity of laying before the
Fellows the names of a number of gentlemen whom they propose to
nominate as Corresponding Members in conformity with the above
resolutions.

At the same Special General Meeting it was also resolved that
the Meetings of the Society shall be held in the Society’s rooms
at Somerset House, on and after the Anniversary Meeting next
ensuing.

The Council have to announce the completion of Vol. XVIII. of
the Quarterly Journal, and the publication of Part 1 of Vol. XIX.

The 8.E. sheet, No. 6, of the Greenough Map is now ready for
publication, and will be issued shortly. The remaining sheets are in
course of preparation, and it is hoped that some of them will be
ready at no distant date.

The Council regret to have to announce the resignation of the
Secretaryship by Professor Huxley, in consequence of the pressure
of his other occupations.

At the end of last Session Mr. Rupert Jones also resigned the
office of Assistant-Secretary, which he could not longer hold con-
sistently with his professorial duties at the Military College, Sand-
hurst. The Council received this resignation with the greatest
regret, having reason to feel the highest satisfaction with the
excellent manner in which Mr. Jones has for a long term of years
performed the duties of his office. Among a great number of candi-
dates for the vacant post, whose recommendations were carefully
considered, the Council selected Mr. H. M. Jenkins, whose assiduity
and experience in the business of the Society, whilst acting as assist-
ant to Mr. Jones, appear in a high degree to qualify him as an
efficient Assistant-Secretary.

The Council have awarded the Wollaston Medal to Professor
Gustav Bischof, of Bonn, in recognition of the eminent services
rendered by him to Geological Science by his long-continued and
laborious chemical investigations on the origin and changes of
minerals and rock-substances, as well as by his numerous publica-
tions on similar subjects, and especially by the production of his
great work on Physical and Chemical Geology ; and the balance of
the proceeds to Dr. Ferdinand Senft, of Hisenach, to encourage him
in the continuation of his meritorious researches in various branches
of geology.

Report of the Library and Museum Committee, 1862-63.
The Museum.

The Foreign Collection has been enriched during the past year by
numerous donations, including a series of specimens of Devonian
Plants and Carboniferous Reptiles from Nova Scotia, presented by

ANNUAL REPORT. 1

Dr. J. W. Dawson, F.G.S.; a complete set of casts of the Climactich-
mites from the Potsdam Sandstone of Perth, Canada West, presented
by Sir W. Logan, F.G.S.; a collection of Fossils from the Estherian
Shales of Phoenixville, Pennsylvania, presented by C. M. Wheatley,
Esq., M.A., &c.; a suite of Rock-specimens from Italy, presented
by Leonard Horner, Esq., F.G.S.; and very recently by a large
number of Echinoderms from the Miocene Beds of Malta, presented
by Dr. Leith Adams, and shortly to be described by Dr. T. Wright,
F.G.S. Specimens from South Africa, South Australia, Mexico, and
Vancouver’s Island have been presented by Capt. J. Grantham, R.E.,
the Rev. J. E. Woods, F.G.S., Signor Gennaro Placci, F.G.S., and
A. J. Langley, Esq.; and smaller contributions have been received
from a number of other donors.

The chief additions to the British Collection are:—A very fine
specimen of Ammonites rusticus from the Chalk, near Chard, Somer-
set, from N. W. Spicer, Esq.; specimens of Fossil Plants from
Hempstead, presented by W. Pengelly, Esq., F.G.S.; and a series
of specimens from the Iron-ore Mines near Ulverston, presented by
Miss Hodgson in illustration of her paper on that district.

The following comparative table will show the extent to which
the Foreign Fossils in the Society’s Collection have been renamed
since the last Anniversary.

Fossils named prior to the last Anniversary.

Drawers.
IOPWaY c.f... ss. SIMU aR cee Ps Loci dace ey ctea cfs \s

Uddevalla, &c..... Besuplocenet i... os. es 5 2
ol is PIMA ton eek s Seis a8 ieee
MAMAVEN Ps. pois ars ENOGORE SG Gee HAP bee ore u
Pouraime-..cn. 0. MG OCERE2 i syeje arecehen soe 2
Paris Basin: ......... OREN Gis porn Re Aeon hen 9
Normandy....... DAVEAR BUC Wi oe Pa apa} sangre ie ate Te &
North America.... Cretaceous. ..........4-. 1

—28

Fossils named since the last Anniversary.

Spitzbergen ...... Carboniferous, &c......... 2
belongs os. Devonian and Carboniferous 1
ROWING. oe. Carboniferous ...' 4.01.0). Paci 1
Rhenish Provinces Carboniferous............ 21
Beeville.) 75. oo oMbotemieii sie ied Se as 1
RulslestiBbamis' ii. Trias ii) ep do bores oo 2
eremmpere ys 3.05) Eas! a) ett. 0 ek 2G cS
LSD a Keuper ersten wir. tld ten &. 1
MET BONE Ae, WARE Y tO beans ae. 1
Stuttgart). 565... (Lit Si es ea i

—32

INRA 85105055 e Fakes 60

iV ANNIVERSARY MEETING.

This progress was made chiefly in the earlier portion of the year,
the reduction in the Staff of the Society by the resignation of Mr.
Jones and the preparation for publication of a new Alphabetical
Supplemental Library-catalogue having, since that time, interfered
with the furtherance of so desirable an end as the complete re-
naming of the Foreign Specimens. It should also be borne in
mind that whereas the Museum-expenses in 1861 reached the sum
of £128 12s. 9d., last year they amounted only to £5 18s. 6d.

The Committee desire to express their opinion that, considering
the reduction in expenses and in the strength of the Staff, the work
in the Museum has been satisfactorily performed, and that an im-
portant step has been made towards rendering the Museum really
serviceable to the Fellows of the Society.

The Council were requested in June 1862, by Dr. P. M. Duncan,
F.G.S., to permit his borrowing the specimens of the Silicified Corals
from the West Indies in the Society’s Museum, for the purpose of
an investigation which he has now nearly completed ; he will, there-
fore, shortly describe them in a paper to be communicated to the
Society, and your Committee view with satisfaction the probability
of this valuable collection being soon completely named and ar-
ranged.

Three boxes, ordered by the Council, have been supplied, at the
cost of £1 15s., to contain the casts of Climactichnites presented by
Sir W. Logan.

The Labrary.

The additions made to the Library since the last Anniversary have
rendered necessary the erection of a new set of Book-shelves, at a
cost of £9 15s. 6d., in addition to the two erected some time back ;
these have been placed in the Meeting-room with the latter, and are
already nearly filled with Periodical Works, the supply of which, by
exchange, gift, and purchase, has continued to increase of late.

The Committee especially call the attention of the Society to the
presentation of about 870 maps of the Ordnance Survey (6-inch
scale) by the Board of Ordnance, through the Director-General,
Col. Sir H. James, F.G.S., &c., for the reception of which a new
Map-case has been provided at a cost of £8.

The Map-collection has also been increased by the usual addition
of a number of French Charts from the Dépot de la Marine, and by
a large Map of the World, geologically coloured by Prof. Jules Mar-
cou, presented by the Publishers.

The Commissioners of the International Exhibition have presented
the Catalogues of the Mining, Metallurgical, and Geological speci-
mens from their respective countries.

A new Alphabetical Catalogue, supplemental to the Library-cata-
logue Supplement published in 1860, is in course of publication, and
will be ready shortly. This Supplement, besides containing the titles

ANNUAL REPORT. Vv

of about 1000 books and pamphlets added to the Library between
June 1860 and June 1862, will also comprise a complete classified
Catalogue of all the Periodical Works (also making about 1000 titles)
in the Society’s Library at the latter date.

When this Catalogue shall have been published, it is in contem-
plation to substitute for the three printed and two MS. reference-
catalogues in the Library a single reference-catalogue which shall
contain all that is now comprised in the older set ; a book has already
been prepared for this purpose in accordance with a recommendation
of the Library Committee last year.

New books and pamphlets have been catalogued and placed in the
Library, as usual, by Mr. Stair, who has also been of much assist-
ance in preparing diagrams for the Evening-meetings, and in com-
pleting the re-arrangement of the Portfolios containing the Society’s
Collection of Sections, Plans, and Drawings.

H. FALCONER.
WM. J. HAMILTON,
R. CHAMBERS.

Comparatiwe Statement of the Number of the Society at the close of —
the years 1861 and 1862.

Dec. 31, 1861. Dec. 31, 1862.

Commounders * 204°... 44/642". LEA Dinter er epee ie 135
OS Sn ir cs a ne 19 Rh Te 306*
Man-residents. ......+.... Sy ete ae 4A76t
886 917
Honorary Members ........ SEE Fates: Seed he, 3
Foreign Members.......... 2A IME ela ae 48
Personage of Royal Blood .. . 1—54 ........ 1—52
940 969

* This number includes all Contributing Fellows, irrespective of their place of
residence.

t Including Contributing and Non-contributing Fellows ;—1in the account for
this year the former have been included with the other Fellows who pay an
Annual Contribution, as explained in the preceding foot-note.

t Comprising only the Non-residents who do not eoababpte; they were elected
prior to November 30, 1859.

v1 ANNIVERSARY MEETING.

General Statement explanatory of the Alteration in the Number of
Fellows, Honorary Members, gc. at the close of the years 1861 and
1862.

Number of Compounders, Residents, and Non-residents,

December od LOOW ees h. Me eee ARC eae eee 886
Add Fellows elected during for- Rasen 9
Pet years sand pan oneret ie one 5
US G2 en hea eke ei Cy: 5 Ms
Contributors™ ). 0 4. o2
Add Fellows elected and paid in } Non-residents elected
SG iat re ee see eee previously to March
iS ttisr. ot fe eee 10
— 42
935
Deduct’ Compounders deceased ...282 2% At ata eee 3
Residents eA” AN PNG Salo cca Sete hoe MRR TN UES ORO ME NL 6
Non=residentsi« iy.) MO ee ed oe 6
Residents resigned 2") /.ie (seh. cohen eee 2
Non-resident resigned), 32202'4o.) 4s Aare eee i
— 18
As aDoven win ec: 917
Number of Honorary Members, Foreign Members, and 54
Personages of Royal Blood, Dec. 31, 1861......
Add Foreign Members elected during 1862 ........... 3
7
Deduct Foreign Members deceased................... 4
Honorary Membervigey bik 005 tec ie eee ey 1
— 65
52

Number of Fellows liable to Annual Contribution, as Residents and
Non-residents, at the close of 1862.

BEING (2 01: a LN SRT eee MN eS aD Baleedye Wh 993,
Won ResiGdon tee jou) fis ote ets ai a a ears an te NE 52
Contributors elected since March Ist .................. 32

306

* Elected subsequently to March Ist, and subject to an Annual Contribution
of Two Guineas.

ANNUAL REPORT. Vil

DercEASED FELLows.

Compounders (3).
J. B. Birch, Esq. | J. H. Deacon, Esq.
S. F. Wilde, Esq.
Residents (6).
J.C. Nesbit, Esq.
W.S. Richardson, Esq.
R. A. Slaney, Esq.
Non-residents (6).
W. Peace, Esq.
Dre 2. 8. Pradll,
R. Trench, Esq.
Foreign Members (4).
Prof. H. G. Bronn. Prof. C. C. von Leonhard.
M. J. M. Bertrand de Doue. Prof. L. A. Necker.
Honorary Member (1).
R. Bald, Esq.

Marquis of Breadalbane.
G. G. Harcourt, Esq.
H. T. Hope, Esq.

Rev. J. C. Cumming.
Rev. J. B. P. Dennis.
A. Hill, Esq.

T he following Persons were elected Fellows during the year 1862.

January 8th.—Robert Harris Valpy, Esq., Enborne, near Newbury ;
William Shepherd Horton, Esq., 10 Church Street, Liverpool ;
Charles Sturtivant Wood, Esq., Geological Survey of Otago, New
Zealand.

22nd.—Samuel Sharp, Esq., Dallington Hall, near Northamp-
ton; George Parkes Wall, Esq., The Hills, near Sheffield.

February 5th.—Captain William Henry Mackesy, 79th Highlanders
(Waterford); Harry Seeley, Esq., Curator of the Woodwardian
Museum, Cambridge; Thomas F. Jamieson, Esq., Ellon, Aber-
deenshire.

26th.—Julius Schvarez, Ph.D., Stuhlweissenburg, Hungary ;
George Charlton, Esq., Dukinfield, near Manchester.

March 5th.—William James Dunsford, Esq., 14 Taviton Street,
Gordon Square ; Charles Henry Gatty, Hsq., Felbridge Park, Kast
Grinstead; George Ford Copeland, Esq., 5 Bays Hill Villas, Chel-
tenham; A. H. Green, Esq., Fellow of Caius College, Cambridge.

19th.—Harvey Buchanan Holl, M.D., Malvern; George W.
Hemans, Esq., 32 Leinster Gardens, Bayswater ; Edward Romilly,
Ksq., 14 Stratton Street, Piccadilly; G. Ernest Shelley, Esq.,
Avington House, Winchester; Elliot Square, Esq., Gresham
House, London; Rt. Hon. Edward Cardwell, M.P., Chancellor of
the Duchy of Lancaster, 74 Eaton Square; George Wilson
Stevenson, Esq., Halifax, Yorkshire.

April 2nd.—Charles Longman, Esq., Hemel Hempstead; Thomas
Wyles, Esq., Allesley Park College, near Coventry.

16th.—Edward Petre, Esq., 388 Brook Street; T. M*Kenny

Hughes, Esq., of the Geological Survey of Great Britain.

Vili ANNIVERSARY MEETING.

May 7th.—Edward Fitton, Esq., 6 Gloucester Crescent, Westbourne
Terrace; Henry Francis Blanford, Esq., late of the Geological
Survey of India; Frederick Hill, Esq., Penhellis, Helston, Corn-
wall; Charles Rogers, Esq., 16 Beaufoy Terrace, Maida Vale;
Rev. Stopford A. Brooke, Fern Lodge, Kensington; John Langley
King, Esq., 56 Wells Street, Oxford Street.

21st.—W. G. Lemon, Esy., B.A., Blackheath ; E. W. Cooke,
Esq., The Ferns, Hyde Park Gate; Edmund Jones, Esq., Basing-
hall Street.

June 4th.—Rev. D. Honeyman, Antigonish, Nova Scotia; Alexander
Macdonald, Esq., Aberdeen.

18th.—John Cumming, Esq.,7 Montague Place, Russell Square;
William Topley, Esq., Geological Survey of Great Britain.

November 19th.—James Brunlees, Esq., 84 Addison Road, Ken-
sington; M. Auguste Laugel, Ex-Secretary of the Geological
Society of France, Orleans House, Twickenham.

December 3rd.—Edward Hesketh Birkenhead, Esq., Master of the
Wigan School of Mines; Alan Lambert, Esq., 2 Portugal Street,
Grosvenor Square; Samuel Higgs, Jun., Esq., Penzance; Antonio
Brady, Esq., Maryland Point, Stratford, Essex.

17th.—Richard Richardson, Esq., Rhayader, Radnorshire ;

John Wickham Flower, Esq., Park Hill, Croydon, Surrey.

The following Personages were elected Foreign Members.
Senor Casiano di Prado, Madrid.
Baron Sartorius von Waltershausen, Gottingen.
Professor Pierre Merian, Basle.

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

British Specimens.

Flint-flakes from Croyde Bay, Devon, and from the South Downs ;
presented by Nicholas Whitley, Esq.

Large specimen of Ammonites rusticus, from the Chalk near Chard,
Somerset; presented by Northcote W. Spicer, Esq.

Specimens of Fossil Plants from Hempstead, Isle of Wight; pre-
sented by W. Pengelly, Esq., F.G.S.

Specimens of Rocks from near Ulverston, Lancashire ; presented by
Miss E. Hodgson.

Specimens of Carboniferous Rocks from Ayrshire; presented by
K. W. Binney, Esq., F.G.S.

Two nodules from the Upper Devonian of West Angle Bay, Pem-
brokeshire ; presented by J. W. Salter, Esq., F.G.S.

Foreign Specimens.

Suite of Nickel-ores; presented by 8S. T. Ayres, Esq.
Suite of Devonian Plants from New Brunswick; presented by Dr. J.
W. Dawson, F.G.S.

ANNUAL REPORT. 1x

A Crystal of Quartz containing a laminated Mineral, from Mexico ;
presented by H. Christy, Esq., F.G.S.

Fossil Wood and other specimens from Quathlamba Mount, Natal;
presented by Captain J. Grantham, R.E.

Tertiary Fossils from Harrow, South Australia; presented by the
Rev. Julian E. Woods, F.G.S.

Suite of Estherian Shales, with Reptilian and Plant-remains, from
Pheenixville, Pennsylvania; presented by C. M. Wheatley, Esq.,
M.A.

Large Plaster-casts of Climactichnites from Perth, Canada West;
and Stand; presented by Sir W. E. Logan, F.G.S.

Specimens of Gold- and Silver-ore from Zacatecas, Mexico; pre-
sented by Sign. Gennaro Placci, F.G.S.

Four specimens of Devonian Plants from Nova Scotia; presented by
Dr. J. W. Dawson, F.G.S.

Six specimens of Crystals of Gypsum containing Sand, from New
Brunswick ; four Photographs of Vertebre of Hosaurus Acadianus,
anda Cast of the Vertebree of Hosawrus Acadianus ; presented by
O. C. Marsh, Esq., M.A.

Specimen of Coral from the Gravel of the Meuse, near Namur ; pre-
sented by Sir F. C. Knowles, Bart., F.R.S.

Specimen of Lead-ore from Monte Vecchia, Sardinia, exhibited at the
International Exhibition ; presented by W. P. Jervis, Esq., F.G.S.

Specimens of Minerals, Rocks, and Nanaimo Coal from Vancouver’s

Island, exhibited at the International Exhibition; presented by
F. J. Langley, Esq.

Specimens of Granite containing Copper-ores, from near Kingston,
Jamaica; presented by J. G. Sawkins, Esq., F.G.S.

Specimens of Rocks from Masulipatam; presented by Captain F.
Applegath.

Specimens of Ammonites, &c., from near Niti Pass; presented by
Col. Strachey, F.G.S.

Specimens of Rocks and Fossils from the Pampean Formation near
Buenos Ayres; presented by C. Darwin, Esq., F.G.S.

Specimen of Carbonate of Lime from the Stalagmitic Floor of the
Rebenac Cave, Pyrenees; presented by H. Christy, Esq., F.G.S.
A large collection of Echinodermata from the Miocene Beds of

, Malta; presented by Dr. Leith Adams.

Specimens of Tertiary Plants from the Upper Val d’Arno; presented
by Sir C. Lyell, V.P.G.S.

Cuarts, MAps, ETC. PRESENTED.

Geologische Uebersichts-Karte von Siebenbiirgen, von Franz Ritter
von Hauer ; presented by F. Ritter von Hauer.

Carta Geologica di Savoja, Piemonte, e Liguria; del Commendatore
Angelo Sismonda, 1862; presented by Professor A. Sismonda,
For.M.G.8.

Geognostische karte des Konigreichs Bayern, herausgegeben auf
Befehl des kon. bayerischen Ministeriums der Finanzen. Erste

x ANNIVERSARY MEETING.

Abtheilung. Das bayerische Alpengebirge und sei Vorland, in
fiinf Blattern und ein Blatt Gebirgsansichten; im dienstlichen
Auftrage aufgenommen und bearbeitet von G. W. Giimbel, Miin-
chen, 1861; presented by His Excellency the Bavarian Minister.

Carte Géologique des parties de la Savoie, du Piémont et de la
Suisse voisines du Mont Blanc, par Alphonse Favre; presented by
M. A. Favre.

Maps of the Gold-fields in the Colony of Victoria: Sheet 1, Ballarat
Gold-field and Castlemaine Gold-field; Sheet of Ballarat Mining
District ; Sheet of Castlemaine Mining District; Sheet of Mary-
borough Mining District; presented by the Hon. G. 8. Evans.

Carta Geologica dei Monti Pisani levata dal vero del Cay. Prof.
Paolo Savi nel 1832, aumentata e corretta nel 1858 ; presented by
Prof. P. Savi.

Geological Map of the World, by Jules Marcou, constructed by J. M.
Ziegler; presented by Messrs. J. Wurster & Co.

First Sketch of a New Geological Map of Scotland, with explanatory
notes, by Sir R. I. Murchison and A. Geikie, Esq. ; presented by
Sir R. I. Murchison, K.C.B., F.G.8., and A. Geikie, Esq., F.G.S.

Ordnance Survey of Great Britain. Maps, 6-inch scale :—Lanca-
shire, Index-sheet, Sheets 1 to 118. Yorkshire, Index-sheet,
Sheets 1 to 301. Ayrshire, Sheets 1 to 14, 16 to 74. Edinburgh,
Index-sheet, Sheets 1 to 25. Fife and Kinross, Index-sheet,
Sheets 1 to41. Haddington, Index-sheet, Sheets 1 to22. Island
of Lewis, Ross-shire, Sheets 1 to49. Kirkcudbright, Index-sheet,
Sheets 1 to 55. Linlithgow, Index-sheet, Sheets 1 to 12. Peebles-
shire, Index-sheet, Sheets 1 to 21, 23 to 27. Wigtonshire, Index-
sheet, Sheets 1 to 37. Durham, Sheets 1 to5, 8,17. Westmore-
land, Sheets 35, 40, 41, 42, 44, 45, 48. Dumfriesshire, Sheets
35 to 37, 45, 46, 52 to 54, 58, 63, 68, 69. Berwickshire,
Sheets 7 to 9,13 to 17, 19, 20, 23, and 26—Ordnance Survey of
England. 1-inch scale :—Sheets 91 to 94,95, N.W., S.W., S.E. ;
96, 97, 103, 8.W.,S.E.; 104, 8.W.—Ordnance Survey of Ireland.
1-inch scale :—Sheet 120.—Ordnance Survey of Scotland. 11-inch
scale :—Sheets 1 to 9, 11, 32 to 34, 40, 41,106. Isle of Lewis,
Sheets 1 to 7. Presented by the Board of Ordnance through the
Director-General, Colonel Sir Henry James, F.G.S.

Forty-nine Maps and Charts published by the Dépot de la Marine
de la France; presented by the Dépot de la Marine.

Carte Physique et Industrielle de la Néerlande. Sheet 15. Veluwe.
Presented by the Minister of the Interior, Holland.

Geological Section through the Tunnels on the Worcester and Here-
ford Railway, by Alan Lambert, Esq., F.G.S.; presented by A.
Lambert, Esq., F.G.S.

Section of a Well at the Tannery of Mr. Lancaster Webb, Stowmarket,
Suffolk, and Sections of the Artesian Wells at Grenelle and Passy,
near Paris; presented by G. R. Burnell, Esq., F.G.S.

Photographs of Somma and Vesuvius, by J. Graham ; presented by
James Graham, Esq.

ANNUAL REPORT. xi

&
Photographs of Sir C. Lyell and Mr. Darwin; presented by L.

Horner, Esq., F.G.S.

The following Lists contain the Names of the Persons and Public
Bodies from whom Donations to the Library and Museum have been
received since the last Anniversary, February 21, 1862.

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

Antwerp. Paleontological So-
ciety of Belgium. |

Basel, Natural History Society of.

Berlin. German Geological So-
ciety.

, Royal Academy of Sciences

at.

Berwick. Natural History Field-
club.

Bogota. Natural History Society
of New Granada.

Bombay Branch of Royal Asiatic
Society.

Bordeaux, Linnean Society of.

Breslau. Imperial Leopold-Car.
Academy of Naturalists of Ger-
many.

Brussels. Royal Academy of
Sciences of Belgium.

Caen. Linnean Society of Nor-
mandy.

Calcutta.
India.

, Bengal Asiatic Society at.

Cambridge (Mass.). American
Philosophical Society.

. American Academy
of Arts and Sciences.

Cherbourg, Society of Natural
Sciences of.

Christiania, Royal Academy of.

Geological Survey of

Darmstadt. Geological Society of
the Middle Rhine.

Dijon, Academy of Natural
Sciences of.

Dorpat,NaturalHistorySociety of.

Dublin, Geological Society of.

Royal Irish Academy.

Royal Dublin Society.

—_—
e

Edinburgh, Royal Society of.

Frankfurt. Senckenberg Natural
History Society.

Geneva, Physical and Natural
History Society of.

Halle. Saxony and Thuringian
Natural History Society.

Hanau. Natural History Society
of the Wetterau.

Heidelberg, Natural History So-
ciety of.

Italy, Commissioners for, at the
International Exhibition.

Kentucky, Geological Survey of.

Lausanne. Société Vaudoise des
Sciences Naturelles.

Lisbon, Royal Academy of.

Liverpool, Philosophical Society
of.

London, Chemical Society of.

Geological Survey of

Great Britain and Ireland.

, Royal Astronomical Society

of.

Royal Asiatic Society of

Great Britain.

, Art-Union of.

British Association.

Royal College of Physi-

cians of England.

. RoyalGeographicalSociety.
Geologists’ Association.

, Royal Horticultural So-

ciety of.

Institute of Actuaries of

Great Britain and Ireland.

. Institute of CivilEngineers.

——, Linnean Society of.

od
.

Xli

London, Mendicity Society of.
, Microscopical Society of.
, Palzontographical Society

of.

, Photographic Society of.
——, Royal Society of.

Ray Society.

Committee of Council on
Education, Science and Art
Department.

. Secretary of State for War.
——., Zoological Society of.
Board of Ordnance.

Madison, United States. Wiscon-

sin State Agricultural Society.
Madrid, Academy of Sciences of.
Manchester, Geological Society of.
, Literary Society of.
Melbourne, University of.

Royal Society of Victoria.
. Mining Surveyors of Vic-
toria.

Commissioners of Public
Works, Victoria.

Milan, Geological Society of.

Montreal, Natural History So-
ciety of.

Moscow, Imperial Academy of
Naturalists in.

Munich, Academy of Sciences of.

Neufchatel, Society of Natural
Sciences of.

New South Wales, Commissioners
for, at the International Ex-
hibition.

New York, State Library of.

, Regents of the University
of the State of.

Nova Scotia, Commissioners for, at
the International Exhibition.

Palermo, Agricultural Society of.
Paris. Academy of Sciences.

. Archeological Congress of
France. —

. Dépot Général de la Marine.
—_—., Geological Society of. .

, Imperial Commissioner for,
atthe International Exhibition.

ANNIVERSARY MEETING.

Paris. L’Ecole des Mines.

. Institute of the Provinces.

. Museum of NaturalHistory.

Philadelphia. Academy of Na-
tural Sciences.

Plymouth Institution.

Presburg, Natural History So-
ciety of.

Puy-en-Velay. Society of Agri-
culture and Science.

Spain, Commissioners for, at the
International Exhibition.

Stockholm, Academy of.

Strasburg, Society of Natural
Sciences of.

Stuttgart. Natural History So-
ciety of Wurtemberg.

St. Petersburg, Imperial Aca-
demy of.

, Mineralogical Society of.

Teign Naturalists’ Field-club.

Toronto, Canadian Institute of.

Turin. International Exhibition
Commissioners.

Royal Institute of Lom-
bardy.

Tyneside Naturalists’ Field-club.

Vermont, State-Legislature of.
Vienna, Geological Institute of.
, Imperial Mineralogical In-
stitute of.

, Imperial Academy of.

Warwickshire Naturalists’ Field-
club.
Washington. United States War
Department.
-. Smithsonian Institution.
Wellington, New Zealand, Com-
missioners of, at the Inter-
national Exhibition.
Wisconsin, State-Legislature of.

Zollverein, Commissioners for the,
at the International Exhi-
bition.

ANNUAL REPORT.

xii

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

Anniversary.

American Journal of Science and | Fournet, Prof.

Arts, Editor of the.
Archiac, Vicomte A. d’, F.M.G.S.
Athensum Journal, Editor of the.
Aucapitaine, Baron.

Baily, W. H., Esq., F.GS.

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

Bathoe, C., Esq.

Bavarian Minister, His Excel-
lency the.

Beardmore, N., Esq., F.G.S.

Beron, M. Pierre.

Bianconi, Prof. G.

Billings, E., Esq.

Binkhorst, M. Binkhorst van den.

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

Blake, E. H., Esq.

Brody, Dr. 8.

Burnell, G. R., Esq.,. F.G.S.

Cheney, T. A., Esq.

Clarke, Rev. W. B., F.G.S.
Colliery Guardian, Editor of the.
Cotteau, M. W. B.

Critic, Editor of the.

Damone, M.

Dana, Dr. J. D., For.M.G.S.

Davidson, T., Esq., F.G.S.

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

Delesse, M., For.M.G.S.

Deshayes, Prof. G. P., For.M.G.8.

Deslongchamps, Dr. J. A. E.,
For.M.G.S.

Desor, M. E.

Dewalque, M.

Dulau & Co.

Eichwald, Dr. E. @’.
Erdmann, A.

Evans, Hon. G. 8., LL.D.
Evans, John, Esq., F.G.S.

Falconer, Dr. H., F.G.S.
Favre, Prof. A.

Francis, Dr., F.G.S.
Freke, Dr.

Gastaldi, B.

Gaudin, Sig. C. T.

Gaudry, Albert.

Geikie, A., Esq., F.G.S.
Geinitz, Prof., For.M.G.S8.
Gibb, Dr. G. D., F.G:S.
Goeppert, Prof., For.M.G.S.
Graham, J., Esq.

Graham, Lieut.-Col.

Haddon, J., Esq.

Haidinger, Dir., For.M.G.S8.
Hall, Prof. J., For.M.G.S8.
Halloy, M.J.J.d0.@’, F.M.GS.
Hauer, Ritter von.

Hayden, Dr.

Heer, Dr. O.

Helmersen, Gen. von, For.M.G.S.
Hornes, Dr.

Horner, Leonard, Esq., V.P.G.S.
Hull, E., Esq., F.G.S.

Huxley, Prof. T: H., Sec.G.8.

India, Secretary of State for.
Intellectual Observer, Editor of
the.

James, Col. Sir H., F.G.8.
Jenyns, Rey. L., F.G:S.
Jervis, .W. P., Esq., F.G.S.
Jones Prof, TE. Ke EGS.
Jouvencel, M. P. de.
Jukes, J. B., Esq., F.G.S,

Karrer, M. Felix.
Kjerulf, Dr.
Korizmics, Dr. L.
Krejciho, Dr.

Lambert, A., Esq., F.G.S.
Laugel, M. A., F.G.S.
ea, Dr.

XIV

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

London, Edinburgh, and Dublin
Philosophical Magazine, Editor
of the.

London Review, Editor of the.

Longman & Co.

Lubbock, J., F.G.S.

Lubbock, Sir John, F.G.S.

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

Maior, Vicomte de Villa.

Marcou, M. J.

Marsh, O. C., Esq., F.G.S.

Mechanics’ Magazine, Editor of
the.

Mining and Smelting Magazine,
Editor of the.

Morgan, Prof. de.

Morris, Prof., V.P.G.S.

Mortillet, M. G. de.

Murchison, Sir R., K.C.B., F.G.S.

Naumann, Dr., For.M.G.S.
Newman & Co.

Oldham, Dr. T., F.G.S.
Omboni, Dr.

Oppel, Dr.

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

Parthenon, Editor of the.
Perrey, M. Alexis.
Phillips, J. A., Esq.
Pictet, M.

Ponzi, Prof.

Power, E. R., Esq.
PrattDreh. By A.
Prestwich, J., Esq., F.G.S.

Quarterly Journal of Microsco-
pical Science, Editor of the.
Quetelet, M.

Ramsay, Prof. A. C., Pres.G.S.
Raulin, M. V.

ANNIVERSARY MEETING.

Reader, Editor of the.
Readwin, T. A., Esq., F.G.S.
Reeve, L., Esq., F.G.S.
Roberts, G. E., Esq.

Rose, Prof. Gustav, For.M.G.S8.
Riitimeyer, Dr.

Salmon, H. C., Esq., F.G.S.
Salter, J. W., Esq., F.G.S.
Sandberger, Dr. F.

Savi, Prof.

Scarabelli, Dr. G.

Schvarez, Dr. J.,. E.G.8
Sculptors’ Journal, Editor of the.
Sedgwick, Prof. A., F.G.S.
Sharswood, Dr.

Sinnett, F., Esq.

Sismonda, Prof., For.M.G.S.
Smith, J., Esq., F.G.S.
Smithe, Rev. F.

Stoppani, Prof. A.

Strozzi, Marq. C.

Studer, M. B., For.M.G:S.
Suess, Prof.

Symonds, Rev. W. S., F.G.S.
Szabo, Dr. J.

Tennant, Prof. J., F.G.S.
Terquem, M.

Triger, M.

Tylor, A., Esq., F.G.S.

Vignoles, C., Esq., F.R.S.

Wallich, Dr. G. C., F.G.S.
War, Secretary of State for.
Watson, Dr.

Weigel, T. O.

White, Dr.

Whiting, G., Esq.

Wood, 8. G., Esq.

Woods, Rev. J. E., F.G.S.
Wiurster, Messrs. J., & Co.
Wyatt, J., Esq., F.G.S.

ANNUAL REPORT. XV

Inst of Pavers read since the last Annwersary Meeting,

; February 21st, 1862.

1862.

Feb. 26th.—On the Drift containing Arctic Shells in the Neighbour-
hood of Wolverhampton, by the Rev. W. Lister, M.A., F.G.S.

On Split Erratic Blocks, by J. Smith, Esq., F.R.S., F.G.S.

On the Ice-worn Rocks of Scotland, by T. F. Jamieson,
Esq., F.G.S.

March 5th.—On the Glacial Origin of certain Lakes in Switzerland,
Great Britain, North America, and elsewhere, by Prof. A. C.
Ramsay, F.R.S., Pres.G.8., dec.

March 19th.—On the Sandstones and their associated Deposits in
the Vale of the Eden, the Cumberland Plain, and the South-east
of Dumfriesshire, by Prof. R. Harkness, F.R.S., F.G.S.

——__— On the Date of the last Elevation of Central Scot-
land, by A. Geikie, Esq., F.G.S.

April 2nd.—On some Reptilian Remains from the Coal-measures of
the South Joggins, Nova Scotia, by Prof. Owen, F.R.S., F.G.S.

On some Fossil Footprints from Hastings, by A.

Tylor, F.G.S.

On some Remains of Chiton from the Mountain-
limestone of Yorkshire, by J. W. Kirkby, Esq. ; communicated by
T. Davidson, Esq., F.R.S., F.G.S.

—_—__—- On the Occurrence of Mesozoic and Permian Faune
in Eastern Australia, by the Rev. W. B. Clarke, F.G.S.

April 16th.—On the Position of the Pteraspis-beds, and on the
Sequence of the Strata of the Old Red Sandstone Series of South
Perthshire, by Prof. R. Harkness, F.R.S., F.G.S.

—_——_———-—— On the Western End of the London Basin; on the
Westerly Thinning of the Lower Eocene Beds in that Basin; and
on the Greywethers of Wiltshire, by W. Whitaker, Esq., F.G.S.

——_—_——— On a Freshwater Deposit beneath the Drift near
Ulverston, by John Bolton, Esq.; communicated by the Pre-
sident.

May 7th.—On new and large Labyrinthodonts from the Edinburgh
Coal-field, by Prof. T. H. Huxley, F.R.S., Sec.G.S.

——_——— On the Flora of the Devonian Period in North-
eastern America, by J. W. Dawson, LL.D., F.RB.S., F.G.S.

—————— On Upper Eocene Fossils from the Isle of Wight, by
Prof. F. Sandberger (in a letter to W. J. Hamilton, Esq.,
For.Sec.G.8.).

May 21st.—On the Metamorphic Rocks of the Banffshire Coast, the
Scarabins, and a portion of East Sutherland, by Prof. R. Harkness,
F.R.S., F.G.S.

On the Geology of the Gold-fields of Nova Scotia, by

the Rev. D. Honeyman ; communicated by the President.

On some Fossil Crustacea from the Lower Coal-

measures of British North America ; on Eurypterus ; on Peltocaris ;

and on some Tracks of Crustaceans in the Lower Silurian Rocks,

by J. W. Salter, Esq., F.G.S.

Xvl1 , ANNIVERSARY MEETING.

1862. ;

June 4th.—On the Disputed Affinity of the Purbeck Mammalian
genus Plagiaulax, by Dr. Hugh Falconer, F.R.S., F.G.S.

—————— On some Fossil Plants from Hempstead, Isle of
Wight, by Prof. O. Heer and W. Pengelly, Esq., F.G.S.

——_——— On some Surface-markings on the Sandstones near
Liverpool, by G. H. Morton, Esq., F.G.S.

June 18th.—On the Mode of Formation of some of the River-valleys
in the South of Ireland, by J. B. Jukes, Esq., F.R.S., F.G.S.

——_———___——— Experimental Researches on the Granites of Ireland:
Part III. The Granites of Donegal, by the Rev. Prof. Haughton,
E.B.S.,.F.G.S:

On the Upper Coal-measures containing a bed of

Limestone in Ayrshire, by E. W. Binney, Esq., F.R.S., F.G.S.

On the Geological Structure of the Southern Gram-
pians, by Prof. James Nicol, F.G.S.

——_—_———— Onsome Natural Casts of Reptilian Footprints in the
Wealden Beds of the Isle of Wight and of Swanage, by 8S. H.
Beckles, Esq., F.R.S., F.G.S.

—_—__—_———— On a Stalk-eyed Crustacean from the Carboniferous
Strata near Paisley, by Prof. Huxley, F.R.S., Sec.G.8.

—— On a Section at Junction Road, Leith, by W. Car-
ruthers, Esq. ; communicated by 8. P. Woodward, Esq., F.G.S.
—_—___—_——— On the Geology of Zanzibar, by R. Thornton, Esq. ;

communicated by Sir R. Murchison, F.R.S., F.G.S.

——-. On the Old Red Sandstone of Fifeshire, by James

Powrie, Esq., F.G.S.

On the Premolar Teeth of Diprotodon and on a new

species of that genus, by Prof. Huxley, F.R.S., Sec.G.8.

On the Death of Fishes in the Sea during the Mon-
soon, by Sir W. Denison; communicated by Sir R. Murchison,
PRSs 2G.5e

Noy. 5th.—Descriptions of some Fossils from India, discovered by
Dr. Fleming of Edinburgh, by Dr. L. de Koninck, For.Mem.G:.8.

On a Deposit containing Diatomacee, Leaves, &c. in

the Iron-ore Mines near Ulverston, by Miss E. Hodgson; com-

municated by the President.

On the Geology of a Part of the Masulipatam District,

by Capt. F. Applegath, Madras Army; communicated by the

President.

On the Association of Granite with the Tertiary
Strata near Kingston, by J. G. Sawkins, Esq., F.G.S.; in a Let-
ter to Sir R. I. Murchison, F.G.8., &c.

Noy. 19th.—On the Cambrian and Huronian Formations, with re-
marks on the Laurentian; by J. J. Bigsby, M.D., F.G.S.

Dec. 3rd.—Description of the Remains of a new Enaliosaurian -
(Kosaurus Acadianus) from the Coal-formation of Nova Scotia, by
O.C. Marsh, Esq., M.A.; communicated by Sir C. Lyell, V.P.GS.

On the Thickness of the Pampean Formation near

Buenos Ayres, by C. Darwin, Esq., F.G.S.

ANNUAL REPORT. XVI

1862.

Dec. 3rd.—Geological Notes on the Locality in Siberia where Fossil
Fishes and Estheriev have been found, by C. E. Austin, Esq., F.G.S. ;
with a Note on Estheria Middendorfii, by Prof. T. Rupert Jones,
F.GS.

Dec. 17th.—On the Skiddaw Slate Series, by Prof. Harkness, F.R.S.,
F.G.S.; with a Note upon the Graptolites, by J. W. Salter, Esq.,
F.GS.

———_——_—— On Fossil Estherie, and their Distribution, by Prof.
T. Rupert Jones, F.G.S.

——_——_— On the Flora of the Devonian Period in North-eastern
America; Appendix; by Dr. J. W. Dawson, F.R.S., F.G.S.

1863.

Jan. 7th.—On the Lower Carboniferous Brachiopoda of Nova Scotia,
by T. Davidson, Esq., F.R.S., F.G.S.

On the Gravel-deposits of Ludlow, Hereford, and
Skipton, by T. Curley, Esq., F.G.S.

Jan. 21st.—On the Upper Silurian “ Passage-beds” of Linley, Salop,
by George E. Roberts, Esq., and John Randall, Esq.; communi-
cated by the President.

———__———. On some Crustacean Tracks from the Old Red Sand-
stone near Ludlow, by George E. Roberts, Esq. ; communicated
by the President.

SEE On the Parallel Roads of Glen Roy, and their place
in the History of the Glacial Period, by T. F. Jamieson, Esq., F.G.S.

Feb. 4th.—On a Hyzena-den at Wookey Hole, near Wells, Part IL.,
by W. Boyd Dawkins, Esq., B.A., F.G.S.

———_——\ On the Discovery of Paradoaides in Britain, by
J. W. Salter, Esq., F.G.S., A.L.S.

—— On the Fossil Echinide of Malta, by Dr. Thomas
Wright, F.G.S.; with Notes on the Miocene Beds of the Island,
by Dr. A. L. Adams, 22nd Regiment.

Feb. 18th.—On the Middle and Upper Lias of the Dorsetshire Coast,
by E. C. H. Day, Esq.; communicated by Robert Etheridge, Esq.,
F.G.S.

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.

Tt was afterwards resolved,—

1. That the thanks of the Society be given to Prof. J. Morris and
J. Carrick Moore, Esq., retiring from the office of Vice-President.

2, That the thanks of the Society be given to Prof. T. H. Huxley,
retiring from the office of Secretary.

3. That the thanks of the Society be given to Sir Charles Bunbury,
the Earl of Enniskillen, J. Lubbock, Esq., Sir R. I. Murchison, and
C. P. Scrope, Esq., retiring from the Council.

VOL. XIX. b

XVili

ANNIVERSARY MEETING.

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

year :—

OFFICERS.
—-

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

VICE-PRESIDENTS.

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

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

Sir Charles Lyell, F.R.S. & LS.

SECRETARIES.

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

FOREIGN SECRETARY.
Hugh Falconer, M.D., F.R.S.

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

COUNCIL.

John J. Bigsby, M.D. Prof. T. H. Huxley, F.R.S. & LS.
George Busk, Esq., F.R.S. Sir Charles Lyell, F.R.S. & LS.
Robert Chambers, Esq., F.R.S.E. | Robert Mallet, Esq., C.E., F.R.S.

& LS. Edward Meryon, M.D.
Sir P. G. Egerton, Bart., M.P., | John Carrick Moore, Esq., F.R.S.
F.R.S. & L.S. Prof. John Morris,
John Evans, Esq., F.S.A. Robert W. Mylne, Esq., F.R.S.
Rev. R. Everest. Joseph Prestwich, Esq., F.R.S.

Hugh Falconer, M.D., F.R.S. Prof. A. C. Ramsay, F.R.S.
R.A.Godwin-Austen, Esq., F.R.S. | Warington W. Smyth, Esq., M.A.,
William John Hamilton, EKsq., PERS:

F.R.S.

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

Leonard Horner, Esq., F.R.S. | Rev. Thomas Wiltshire, M.A.

L. & E.

S. P. Woodward, Esq.

X1xX

LIST OF

THE FOREIGN MEMBERS

OF THE GEOLOGICAL SOCIETY OF LONDON, 1n 1863.

Date of
Election.

1817. Professor Karl von Raumer, Munich.

1818. Professor G. Ch. Gmelin, Tiibingen.

1819. Count A. Breuner, Vienna.

1819. Sign. Alberto Parolini, Bassano.

1822. Count Vitiano Borromeo, Milan.

1823. Professor Nils de Nordenskidld, Helsingfors.

1825. Dr. G. Forchhammer, Copenhagen.

1827. Dr. H. von Dechen, Oberberghauptmann, Bonn.

1827, Herr Karl von Oeynhausen, Oberberghauptmann, Dortmund,
Westphalia.

1828. M. Léonce Elie de Beaumont, Sec. Perpétuel de 1’Instit. France,
For. Mem. R.8., Paris.

1828. Dr. B. Silliman, New Haven, Connecticut.

1829. Dr. Ami Boué, Vienna.

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

1832. Professor Hilert Mitscherlich, For. Mem. R.8., Berlin.

1839. Dr. Ch. G. Ehrenberg, For. Mem. R.8., Berlin.

1840. Professor Adolphe T. Brongniart, For. Mem. R.8., Paris.

1840. Professor Gustav Rose, Berlin.

1841. Dr. Louis Agassiz, For. Mem. R. 8., Cambridge, Massachusetts.

1841. M.G. P. Deshayes, Paris.

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

1844, M. Edouard de Verneuil, For. Mem. R.S8., Paris.

1847. Dr. M. C. H. Pander, Riga.

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

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

1850. Professor Bernard Studer, Berne.

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

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

1851. General G. von Helmersen, St. Petersburg.

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

1851. Professor Angelo Sismonda, Turin.

1853. Count Alexander von Keyserling, Dorpat.

1853. Professor Dr. L. G. de Koninck, Lrége.

1854. M. Joachim Barrande, Prague.

1854, Professor Dr. Karl Friedrich Naumann, Lezpsie.
b2

XX

1856. Professor Dr. Robert W. Bunsen, For. Mem. R. 8., Heidelberg.
1857. Professor Dr. H. R. Goeppert, Breslau.

1857. M. E. Lartét, Paris.

1857. Professor Dr. H. B. Geinitz, Dresden.

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

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

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

1859. M. A. Delesse, Paris.

1859. Professor Dr. Ferdinand Roemer, Breslau.

1860. Professor Dr. H. Milne-Edwards, For. Mem. R. S., Parzs.
1861. Professor Gustav Bischof, Bonn.

1862. Senor Casiano di Prado, Madrid.

1862. Baron Sartorius von Waltershausen, Gottingen.

1862. Professor Pierre Merian, Basle.

AWARDS OF THE WOLLASTON-MEDAL
UNDER THE CONDITIONS OF THE “ DONATION-FUND”
ESTABLISHED BY
WILLIAM HYDE WOLLASTON, M.D., F.RS., F.GS., &e.,

“To promote researches concerning the mineral structure of the earth,
and to enable the Council of the Geological Society to reward those
individuals of any country by whom such researches may hereafter be
made,”’—“ such individual not being a Member of the Council.”

1831. Mr. William Smith, 1850. Mr. William Hopkins.
1835. Dr. G. A. Mantell. 1851. The Rey. Prof. A. Sedgwick.
1836. M. L. Agassiz. 1852. Dr. W. H. Fitton.

Capt. P. F. Cautley. > f M.le Vicomte A. d’Archiac.
win Dr. H. Falconer. i M. E. de Verneuil.
1838. Professor R. Owen. 1854. Dr. Richard Griffith.
1839. Professor C. G. Ehrenberg. | 1855. Sir H. T. De la Beche.
1840. Professor A. H. Dumont. 1856. Sir W. E. Logan.

1841. M. Adolphe T. Brongniart. | 1857. M. Joachim Barrande.
1842. Baron L, von Buch. 1958, { Herr Hermann von Meyer.

1843. M. E. de Beaumont. Mr. James Hall.

M. P. A. Dufrénoy. 1859. Mr. Charles Darwin.
1844. The Rev. W. C. Conybeare. | 1860. Mr. Searles V. Wood.
1845. Professor John Phillips. | 1861. Prof. Dr. H. G. Bronn.
1846. Mr. William Lonsdale. 1862. Mr. Robert A. C. Godwin-
1847. Dr. Ami Boué. Austen.

1848, The Rey. Dr. W. Buckland. | 1863. Prof. Gustav Bischof.
1849, Mr. Joseph Prestwich, jun. wae

6 0 SIISF

...2 ee

9 ¢ ZrOS PCOS Ca EH COREE EE EO OSES eEn08

Aya1v0g ay} JO InoARy Ul doURTeg | J

*punj-jsonbog UmoIg pue Ysnous014
9Y} WO Suurewer QOH JO soueteq oy} Surpnpouy »

“EO8T “G87 WF

—S——— ‘804, “HOIMISAUd HdaSOLr (pousis)
6 O SIISF
— ["‘papnjour asay 2OU $2 suorg
-paygnd pjosun fo y2078 pun ‘aanjwuding ‘havsg
“UT ‘suonjaapog jouampy ayy, fo anjva ay], ‘T'N]
6) 0) OLT Py Ray Cnet ag Ate sre eee ‘suolqynqi413Uu0y jenuuy jo sleol1y
O bF GZ cttteer*""*"9* (HOOT palapISUOd) SadJ-UOISSIUIPY JO SIvalIy
0 O OSEFP —
(0) O xOSEP Seeeeseceoseeree o8eece C6 ye ‘sjosuoy
es ata —: Aysodoig pepuny
P 8 ZG COOCOL SOK OT OHH THHEOHOCHOHEEH EHH OESORESEE spurey $1219 ul soured
OL TI O6F Pr eee see hee me ee Sepa eee eee PALLET, S$ 1oyue qd Ul aoueleq
O 6I ST wrrrtterrsereeeseeees TeUINOL UI SUOIJDIIIO[D ,SloyjNY 10J and
O O OG meereesreeseeeeseeveseeseeeseeeee jeusinor 04 STIqIIOSqNg woody ond
FI LY ia ages a 2 aie Ae Aca seats halk a Sombie tages © “TITAX "lOA
‘jeuinor Jo juN0d0B U0“0ZD pue UeWSUOT ‘sissop] WOT ONG
“pg. ae *ALUAAOUG

"SORT Slaquavag ISTE ‘ ALUAAOUY SALTINOG AHL AO NOILVAIVA

€ Gt GL ‘ITTAX ‘OA “feurmor Jo yunosoe uo 4s9M “AA “IPA 0} ONG

py 6 *sLaaq

a

8 OL 69F

9 FI 6Z ‘°° ZO8T ‘IE °99q S(punj-uoyseTJOM) S.JoyuR_ ye soueleq

9 LET treseeeee Spaa001g JO PlWMY JO SUIOJ Ua}}IM OM} JO {SOD

O Ol OI COSCO OSEOT HOF OSHS THH EET SHOE HTETHHEOHSHH EO SHEE EHT HERE HH EES EEe usjsny
“UIMPOY °D “VY °U “TIAL :0F popieme [epeyT PlOD JO soy

8 FI 0Z COR eetOseesescet OP oseesetesteeseoeses GOST ‘199 F] "Jolg 03 plemy

Di, AB oe *SINAWAVG

8
0)

8
a

Ol GOF

—_

PTUTULERELTTEREU Ee ee *sjU99 Jod € poonpey
poate eee ‘SI P8OLFU0ZOSI A0J puny-uo1jeu0 oY} UO SpuEprAicT

COSCO HCHHHHEEHH SS eEOTHOHTHH HEHE EH OEE EH EER eEe punj-uoryeuocy
ols dias M 24} UO ‘ZQ8t ‘T Adenuer ‘s,Jayueg ye soueyeg
‘$F

*SLdIGOaY

‘LNQODOY-L8N4a J,

-

XX1l
EstTIMATEs for

INCOME EXPECTED.

Due for Subscriptions on Quarterly Journal (con-

BIGETEC: ROU)! sacs sasaccsici<avisan on screaacauccueiects 50}. .0 .0
Due tor Authors’ Corrections </....sssecscsecceeveces 18 19 0
Due for Arrears (See Valuation-sheet) ........ee0. EtO. 6 6

————- 178 19 0
Estimated Ordinary Income for 1863.
Annual Contributions :—

232 Resident Fellows at £2 2s. ....cccccsceeee 487 4 0
51 Non-resident Fellows at £1 1ls. 6d. ... 80 6 6
— 567 10 6
Admission-fees (SUppOSEd) \\.....00secesssseniewescaceneece-ssotue 250). OnsO
Compositions (supposed) \2.ese--c.--.<csaceateren sce aeneedere oes. 200 OOO
Dividends on Consols ...... puis oUadwalcawredesmecmeecemeeies Scsientieee 13f 22220
Sale of Transactions, Proceedings, Geological Map, Library-
catalogues, and Ormerod’s Index ............2sseeses Been aera enerta 50.0 0
Saleiof Quarterly: Jourmtal’ |.22..c.s.esceasateeesateso-e a naaowatsaaa aes 200 0 O
Duelfron: Longman‘and ‘Coc im June sis ceracs cnc cee aswenssncens ere 47 14
Due from Bequest-fund on account of Special Expenditure
on Map, Museum, and Library, in 1861 and 1862.......... 130 ga

£1756 3 4

JOSEPH PRESTWICH, Treas.
Feb. 5, 1863.

XX1il

the Year 1863.

EXPENDITURE ESTIMATED.

Sigs. vOe 8.0
General Expenditure :
Taxes and Insurance ......-..-sseseee Hides b ..0. O
BEEIOUSE-TEPAITS, coc ade nics ose ccanevvsssse 25 0 0
Mame PRRTRAT ARTE 02 a) aiol'a)a.re, = 2.<.sintniw nls iaiaiet ein sine 6 50 0 0
Rims Pe etertWate 1a clio evayeltare?ore)aleib edie, <)0i(sie/mieess 35 0 0
it Fh Dies Sa ae GAR ari a5 05.0
Miscellaneous House-expenses ......+++-02-- 50 0 0
DEMOMEEN | Ghoiaminc iw ie = ~ omnis pidin winrejaisia/sise.c.p' 25 0 0
Miscellaneous Printing (Abstracts) .......... 30 0 0
Mewinr MECWHES. 605 ce ec we asec cnc dese crue 20 0 0
305,.0 #0
Salaries and Wages:
Assistant-Secretary .. 02.0 cccccccccccaccvecs 200 0 0
el Earle 5a oiera. as )v)a, ne, 9 2 51 <, naralapous ofa aaa 120", 0-0
Assistant in Library and Museum ............ 52 0 0
MERMECES s ciutcta rahe; sietala: 9:66 aleis! o's Sula’ shatevahslawiatere-at 90 0 0
RECON UIANE fareies-orein!c\s'el 5 cis -arainiels) a .e'e's sails’ o:ais 40 0 0
Occasional Attendants .......... eras telat 20° 6..0
SAIC OLSE MEET eet a a0. ainissse maida ie Saisie Aoteapane 20 0 0
542 0 O
Library : Ordinary Expenditure ...... Sone 50 O O
Special Expenditure ........... peatecannnes . 100 0 O
156,00
Museum: Ordinary Expenditure ...... mebinteccice eeteaaeisr S-Sece re «. 30 0 ©
Diagrams at Meetings ........... Boe cefatnsn das aoameaantiececisisn’s sieve 10 0 O
Miscellaneous Scientific Expenditure ...........seseccessccecscees 10.0.0
Publications: Quarterly Journal ...........00 needless 550 O O
a PANSACHONS (io. cakdcsh« dcascdenees teeta? TOON
a Geological Map ~.iiivccetvetee. seine DOP? Qi220
ClO. KO
£1737 O O
Balavice tn favour Of the Society .....0.s.scscsssoscssccoscseteces 19 3 4

£1755 3 4

XXIV
Income and Expenditure during the
INCOME.

Bie 85. US RG Sse Ge
Balance at Banker’s, and at Messrs. Longman’s,

SAMUA Yale MSOMc. sis: aie aicdielete~w « cosnats ams eee brs savin LO oe
Balanecesini Clerk’ s hands» o/c). .oae occ aso ee ROE 19 18 I]
Compositions received,’ 16627 371s. ces oon T3910
Avrears of Admission-fees** “2. 3.02 04. 4 aes ae 44 2 0
Arrears of Annual Contributions ...... Dr ated aera 40 19 O
Admission-fees for 1862 ........ Se ART 5, Saco nota le. O
Annual Contributions for 1862, viz.—

224 Resident Fellows ......... £660 19 6
44 Non-Resident Fellows ... 69 6 0
7a0' 5 6
Dividends on Consols ........ COG OS ase aoe ae ee 132 4 4
Publications :
Longman and Co., for Sale of Journal in 1861. 60 9 4
Sale of Transactionsi.. sea 0 «csc ccmee cick 9 @ §
Sale of Journal, Vols. I=6 ...... 0.8 q..- 6 16> 2
x Wale Feat soe eee 13 12 0
As Molds ene eoe 24 17 10
i? Vols Ubu. dscns, doe oT 4
ss Wolk: TF. . la dicuasacaisicier sunstener= G2 4
= Vol 88? 2c at etimatcete 106 7 9
Salevof Geolowical Map) i iccrcicta ccleeiaiateete 6 0
Sale of Library-catalogues ............ee0- re 16
Sale of Ormerod's Index 2420/55. .7-1a)cte'a'sevelorete's 116 0
320 10 O

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

THOMAS F. GIBSON, ,
ALFRED TYLOR, \ AMELIE 21a

Feb. 3, 1863.

* Due from Messrs. Longman and Co., in addition to the above,

Guiilournals Vols XV IEE ecec s « stoic <i svnlsinresclnige 4 oe ataeinsi a £47 14 7
Due from Fellows for Journal-subscription ......-++-+«sees 50 0 0
Balance due from Bequest-fund on account of expenditure on

Map, Library, and Museum........-2+eeeeeeereecceeees 130°.-7 23

£228 1 10

XXV

Year ending December 31st, 1862.

EXPENDITURE.

General Expenditure : £. 8. a. £
Ree Mee ena onl wie oisica( alee 4! weve ae 'si0' ro) a
Fire-insurance ....secccceccecccececees 3.0 0
House-repairs .....eee-ceeecee cece cece 12 18 3
Rete aa ie ic siclola <icie arse Wicipie, sis'a'e'eiee «2 30 14 0
Ramat erate ais ola eel ola ane, a0m'2) #\s, ops. » i 0s 3214 7
Miscellaneous House-expenditure ......-- 20711
BEAGIOMENY .6 os cc ln a cess cece ws veces ce 1915-19
Miscellaneous Printing ........-.se-see+- 4te bk -2Z
Tea for Meetings ........+-seeeceeseees 3 19 1

—_——_ 262

Salaries and Wages:

Assistant-Secretary ......c0ccssesescees 169 10 9
MM atarerel ators ia ieee oo isa ce <2 012 sve haierninvaleh.ase 90 0 0
Assistants in Library and Museum ........ 103: 2° 0
EIpRRRAS EP aoe area! shel nici ote lnintainigtxsaveiatel ata -c. 0 evi 90 0 0
EeEGORIC Tere oferta cic pte Sa-7 ss 5 s'a, cos 40 0 0
Occasional attendants ......-..e-eeseee- 2L-0°.6
MOE CLOE so ichaipie «20 hs sleet oe wos ieh6 Poeeeo 29 16 9
543

KG ielloiiso inn aN tie weld ee a+ 5 76Ke ss 3 Ble © 88

REIMER Ae 28 5 3102 Sco wes 3 SN ape e Bs nee 3 ae ee

Diagrams at Meetings ........ ratiayaa a Ciany ae teeta ee

Miscellaneous Scientific Expenses, including Postages.. 46

Publications :

Geological Map ....... eVsinijoie, shadebs aha telivse)e,/5\0 76, 0078
MIPAMLEETISTAN Sai ce fesse cy tin oe sie cise s.yic ow wos0% PANY
Proceedings and Abstracts .............. i AS: 6
Wanenal Vols, WILMA. seis cesievceecccise = Lb 6.9

a NOS MELE NVivo ecihc s acs eles 18 9

s jy fet eae. Od eet de See aleelsve.'ol Ges 14 6

~ IVI VILL. f craleianeyaisie fieleis cc: #6 ::e 2°19) 13

- Wl ce Vil Rew icianke ostederse.s sata oe 468 13 2*

496

Falance at Banker's, Dec: 31, 1862 ..... .o4:....64. 490

Sranceim Clerk S Hans .7.sie\ss'as beds sees cbse vie 22

£1960

Sills
621k
162.9
19.4
rS.. -6
10,0
2. 0
13. 6
14 10
8 4
2 10

* Since making up this balance-sheet, an account from Mr. W. West of
£72 15s. 3d. for lithograph-printing connected with the Journal (vol. xviii.) has
been received. This increases the cost of that volume to £541 8s. 5d., and reduces
the surplus on the year to £227 2s. 9d., and the cash-balance to be brought for-

ward to £440 7s. 9d.—J. P.

VOL. XIX.

‘ Oa tee i Pas
; h my
-. 4 co : ee
phat, re Ay iriujeranas af

tt Bini

PP Pen rt tie ity al
is aie ;

v Pay wee
Nie haDA 2e esteneg ane "i

al

m ibe ih 4 lbh
7 Z3

Ay a
ae cl fis it

‘ek oy C953 4 Bote highest
33 of as aN Se
y avi

Coe eens 9 vis

‘
=A od *

visi, i brag ye BY pial aga 45 ‘i f
AY hae oe he
i apa fee
£9) eee Lda
Pua}, Ph aie :

PROCEEDINGS

AT THE
ANNUAL GENERAL MEETING,

20TH FEBRUARY, 1863.

AWARD OF THE WoLLASTON MEDAL.

Artsr the Reports of the Council and the Committees had been read,
the President, Professor A. C. Ramsay, delivered to Mr. Horner the
Wollaston Medal, awarded to Professor Gustav Biscnor, of Bonn,
addressing him as follows :-—

Mr. Horner,—It is now my pleasing duty to place in your hands
the Wollaston Medal, and to request that you will cause it to be
conveyed to our distinguished Foreign Member, Professor Gustav
Bischof, of Bonn, in testimony of the high esteem in which the
Fellows of the Geological Society of London hold his services to
geology, more especially as shown in his work entitled ‘ Lehrbuch
der chemischen und physikalischen Geologie’*—a book known and
valued by the physical geologists of the whole world, and which, as
the first great work on the subject, now renders, and in future times
will still render, the name of Bischof classical in geology.

Mr. Horner replied as follows :—

Mr. Presipent,—lIt will give me much pleasure to forward this
Medal to my old and distinguished friend, as an honour so well
merited by long and great services rendered to an important depart-
ment of our science. It is now more than thirty years since I had
the advantage of becoming personally acquainted with Professor
Bischof, during a long residence at Bonn. He was then actively
engaged in those observations in the field, and experiments in his
laboratory, by which, through the labours of many years, he has
thrown so much light on chemical agencies concerned in the forma-
tion of mineral substances, in the phenomena and products of vol-
canos, and in filling mineral veins. It was about that time that he

* A translation of this work has been published by the Cavendish Society,
under the title ‘ Elements of Chemical and Physical Geology,’ 1854-59.
c2

XXVIli PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

published his observations on the emanations of carbonic acid gas in
the district of the Eifel and adjoining lands, and his treatises on hot
and thermal springs and on a natural history of volcanos. In later
years he has shown how all theories on metamorphism, and how the
justice of the application of that term, must be tested by the strict
laws of chemical action; and he is constantly referred to as an
authority by those whose attention is directed to that most obscure
and most difficult subject.

AWARD OF THE Wo.LtAston DoNATION-FUND.

The President next addressed Sir Roprrtck Murcuison, as the
representative of Professor Sznrr, as follows :—

Str Roprerick Murcuison,—Into your hands I now deliver the
balance of the Wollaston Fund, and the diploma of our Society to
that effect, with the request that you will cause them to be con-
veyed to your old and valued friend Professor Ferdinand Senft, of
Eisenach, with the assurance that the Geological Society of London
have specially conferred this honour upon him to testify their sense
of the value of his work in the difficult subject of the classification
of rocks, as shown in his late publication entitled ‘ Classification
und Beschreibung der Felsarten,’ and also in the hope that it may
prove useful in enabling him still further to prosecute his important
researches.

Sir Roperick replied in the following manner :—

Mr. Prestpent,— You have well brought forward the main grounds
on which the Council has awarded the Wollaston Fund to Professor
Senft. On my own part I beg to say that this award has given to
me, and all my associates who are acquainted with that excellent
man, the most sincere pleasure. From visiting, accompanied by
himself, the environs of his residence at Eisenach, some of us have
formed a true admiration of his labours as a field-geologist, as well
as of his powers as an author of valuable works on classification.

As Dr. Senft obtains only a very small pecuniary requital for his
zealous labours in teaching a large school, the pupils of which receive
good lessons from him in our science, our assistance, small as it is,
will, I know, be useful in enabling him to carry out with increased
vigour his scientific researches, the last of which is a work of deep
interest to those who are occupied with the study of the recent
changes on the surface of the globe, and is entitled ‘ Die Humus-,
Marsch-, Torf- und Limonitbildungen, als Erzeugungsmittel neuer
Erdrindelagen,’ or an inquiry into the nature and origin of peat-
and turf-accumulations, and their relations to the newer geological
formations.

As this donation is accompanied by a diploma, signed by you, Sir,
as our President, my friend Dr. Senft will, I am sure, consider that
by this act we confer an honour upon him which, I feel confident, he
will highly value and most gratefully acknowledge.

ANNIVERSARY ADDRESS OF THE PRESIDENT. xxix

THE ANNIVERSARY ADDRESS OF THE PRESIDENT,
Proressor A. C. Ramsay, F.R.S., ke.

It has been a frequent custom with the Presidents of this Society
to pass in review the principal memoirs that have been published
during their years of office, thus giving a sketch of the progress of
the science during that period. I would willingly follow this useful
practice, were it not that the want of leisure induces me to avail
myself of that easier course which some of our Presidents have adopted,
namely, to expound what they considered the best view of an im-
portant or favourite subject; and, in doing so, those who listen to
or read addresses may probably see reason to congratulate themselves
that the method I adopt is one reason why my observations will be
brief. But first it is my duty to read the following obituary notices,
some of which refer to gentlemen who were among our most distin-
guished foreign Members.

Ricuarp Trencu, son of the Very Reverend the Dean of West-
minster, was born at Botley, in Hampshire, on February 18, 1836.
He received his early education at Rugby, and was afterwards
entered at Trinity College, Cambridge, where he took his degree of
B.A., and where, in attendance on the lectures of Professor Sedgwick,
he first acquired a taste for geology. In the year 1858 he was
appointed one of the Assistant-Geologists on the Geological Survey
of Great Britain, and in the following year he was elected a Fel-
low of this Society. During the two years he remained on the
British Survey, he was employed surveying the Oolitic strata near
Banbury, and the Eocene beds on and around Bagshot Heath,
gaining and retaining the esteem and love of his colleagues by his
intelligence and zeal, and the manly frankness, gentleness, and
heartiness of his disposition. When, in 1860, he left us to join the
Geological Survey of India, there was no one of his colleagues who
did not part from him with unwillingness; and the news of his early
death was received with unfeigned sorrow. On the Geological Survey
we still often speak of his pleasant ways, and regret that one who
promised well sunk under a rapid illness ere there was time for
that promise to be fulfilled. He died on the 27th of May, 1861, at
Calcutta, aged twenty-five.

Dr. Cart Casar von LeonnarD, a Privy Councillor, and for many
years a Professor in the University of Heidelberg, was born in 1779,
at Rumpenheim, near Hanau. In early life, after studying at
Marburg and at Gottingen, he was attached to the public service ;
but a strong predilection for the natural sciences led him to change
his career, and devote himself exclusively to their furtherance. In
the first years of this century he was labouring in the field of mine-
ralogical literature, and published at Dresden, in 1805-10, his useful
manual ‘ Handbuch einer allgemeinen topographischen Mineralogie’ ;
whilst a few years later he printed, with Selb, a volume of mineralo-
gical studies (Niirnberg, 1812).

XXX PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

In 1816 he was appointed Professor at Munich, and received the
honour of being elected into the Academy of that place. In con-
junction with Kopp, he then published another work on mineralogy,
‘ Propadeutik der Mineralogie,’ Frankfort, 1817; and soon after his
appointment to the Professorship at Heidelberg, in 1818, he turned
his attention more fully to geological subjects, and wrote at intervals
a series of instructive works which have exercised no little influence
on the studies and thoughts of the young, especially in German
Universities. The ‘Charakteristik der Felsarten,’ 1823, was in its
time a very valuable contribution, as was also, in the unsettled state
of opinion on the basaltic rocks, his work entitled ‘ Die Basalt-Gebilde
in ihren Beziehungen zu normalen und abnormalen Felsmassen,’
1823.

His ‘ Lehrbuch der Geognosie und Geologie, 1835, made its way
to all parts of Germany; the ‘ Handbuch der Oryktognosie’ also
passed through several editions; and his more popular works on
Geology and the Mineral Kingdom have been largely circulated and
translated into foreign languages.

Meanwhile, from 1807 to 1830 as sole editor, and in conjunction
with Bronn from 1830 to the time of his death in January 1862, he
edited the admirable ‘ Jahrbuch fiir Mineralogie und Geologie,’ which
is known throughout the scientific world as a repertory of original
papers, reviews, and interesting letters from some of the most
prominent savants of Europe.

Von Leonhard’s services as a teacher and writer were acknowledged
by the diplomas and honorary titles conferred on him by many learned
societies, and by numerous orders bestowed on him by his own and
by foreign reigning monarchs. In 1817 he was elected a Foreign
Member of this Society, and died last year at Heidelberg, at the
advanced age of eighty-three.

Rozsert Bap was born at Culross,in Perthshire, in 1776, and fora
long time occupied a high position as amining engineer. In 1817 he
became a Fellow of the Royal Society of Edinburgh. He was also
one of the original non-resident members of the Wernerian Society,
and contributed to its memoirs. One of these papers was ‘ On the
Coal-formation of Clackmannanshire,” which was read at three suc-
cessive meetings in 1809-10. Besides an account of the Coal-field,
it contains a careful description of the Boulder-clay and alluvial
deposits of the country. In1819 he read another remarkable paper
on the same district, showing the effect of a series of faults by which
the Coal-measure strata are depressed to the south between the Ochil
Hills and the sea. In 1821 he read a paper before the Wernerian So-
ciety, entitled «« Notices regarding the Fossil Elephant of Scotland,” in
which he described the discovery of a tusk in a cutting in Boulder-clay,
a few miles to the west of Edinburgh. The fossil, when found, was so
fresh that one of the workmen carried it secretly to an ivory-turner,
from whom it was rescued only after it had been cut into three
pieces, which were in process of being converted into chessmen.
This, as far as I am aware, is the earliest record of the occurrence of

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXi

‘organic remains in the Boulder-clay of Scotland. He was also the
author of various other memoirs on geological, engineering, and
mining subjects, some of which were contributed to the ‘ Edinburgh
Encyclopedia.’ In 1810 he was elected an Honorary Member of
this Society, and spent his last years at Alloa, where he died, in
December 1861, in his eighty-sixth year.

The Rev. James Cummine, M.A., F.R.S., Professor of Chemistry,
Cambridge, was born in the parish of St. James’s, Westminster,
October 23,1777; and it is related by one from whom I quote, who
knew him well, that as a child in arms he happened to be present at
Lord George Gordon’s riots. In 1797 he entered at Trinity College,
where he was elected Scholar in 1800, and graduated as Tenth
Wrangler in the following year. In 1803, he was elected a Fellow
of his College, and Professor of Chemistry in 1815; and in 1816 he
became a Fellow of the Royal and Geological Societies of London.
He was a successful experimenter ; and it is said that about the year
1819, when he repeated Oersted’s famous magnetic experiments, he
observed, “ Here we have the principle of an electric telegraph.” His
last course of lectures was interrupted by illness in the spring of 1860,
though he still continued to work in his laboratory. His chief work
was a ‘Manual of Electro-Dynamics’ (1827), and he contributed
various papers to the ‘Cambridge Philosophical Transactions.’ In
1819, Professor Cumming was presented to the Rectory of North
Runcton, where he died, last year, in the eighty-fifth year of his age,
loved and admired by all who knew him for his genuine qualities
both of heart and head.

Joun Corzis Nessrt was born at Bradford, Yorkshire, in 1819.
When quite a boy, he attached himself to chemical pursuits, and at
an early age was placed under the guidance of the celebrated
Dr. Dalton in Manchester, where his family had gone to reside.
When of age, he removed to London, and established at Kennington
his School of Chemistry and Agriculture, and became well known for
his lectures on agricultural chemistry. In 1845 he was elected
Fellow of the Chemical and Geological Societies, and was the author
of several chemical treatises. In 1848 he gave a memoir to this
Society “On the Presence of Phosphoric Acid in the subordinate
members of the Chalk Formation,” in which he showed that on the
Upper and Lower Greensand the use of artificial phosphatic manures
had not proved beneficial for agricultural purposes, for this reason,
that they themselves often contained a sufficiency of phosphoric acid.
Indeed, he specially devoted his attention to the application of
chemistry to geology, and in France he was instrumental in
indicating to the French Government the localities where fossil
manures could be profitably worked—a notice of which appeared in
the ‘Comptes Rendus,’ 1857. In the same year the agricultural
world recognized his labours by presenting him, through the Farmers’
Club, with a valuable microscope and a service of plate. He died
March 30, 1862, aged forty-three.

XXxXll PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Dr. Heryricu G. Bronn, Councillor and Professor at the University
of Heidelberg, Knight of the Grand-Ducal Order of the Lion of Baden-
Zahringen, was born at Ziegelhausen, near Heidelberg, and passed the
greater part of his youth at that place. In his twenty-second year he
published a work on botany, of such excellence that it procured for
him a prize and the degree of Doctor from the faculty of Medicine at
Heidelberg. In the next ten years he zealously employed himself,
while in the Mineral Office at Heidelberg, in paleontological research,
treasuring up materials to be used in his later works. At this time,
too, he commenced his travels, and, hammer in hand, examined the
then little-known formations of Upper Italy. His geological descrip-
tions of that country, combined with his specification of the Tertiary
fossils, show his accuracy as a geologist and critical paleontologist of
no common order. But his first great work was the ‘ Lethea
Geognostica,’ published in 1835-37, which at once placed him in the
foremost rank of European paleontologists of the day.

In this work he laid down the results of the observation and
experience of years, giving a survey of the successive geological
epochs in a manner that powerfully aided the study of our science
in Germany. Its contents have since become common property, from
the numerous popular works that have drawn their materials from its
stores; and though, in the progress of science, the knowledge if
contains has been extended and modified, it still remains one of the
foundations of German stratigraphical geology.

It is needless, in this place, to enumerate all the various works of
which Bronn was the author, embracing, as they do, memoirs on the
geology and paleontology of the Apennines and Pyrenees, and of
various districts in France and Germany; but there is one of them,
‘The History of Nature’ (Geschichte der Natur), which deserves
especial notice. In this work, the first part of which was published
in 1842, beginning at the beginning, in true German style, he first
gives a brief digest of astronomical phenomena, then of chemical and
physical geology, and of the state of physical geography, thus opening
the general subject before proceeding to the second part, where, more
completely in his own domain, he treats of the first appearance of
species and their development in time and space. In one of the
chapters of this work, Bronn, coinciding with Cuvier, maintains the
immutability of species, allowing, at the same time, many instances
of degeneracy, deformity, crossing, and possible mutation. To him
such mutations merely resolved themselves into the development of
races, varieties, and sub-species. Accordingly, he was directly op-
posed to the ideas of Lamarck and Geoffroy St. Hilaire, looking, as
he then did, upon each species as a direct act of creation. The third
part of the ‘ History of Nature’ includes the “ Index (Part I. No-
menclator Paleontologicus, Part IJ. Enumerator Palseontologicus)
Paleontologicus,” published in conjunction with H. von Meyer and
Goppert. By far the greater part of this work was executed by
Bronn ; and it must have required no ordinary amount of enthusiastic
steadfastness of purpose to execute a labour involving the systematic
reduction of all the lists of fossils published in works in many lan-

ANNIVERSARY ADDRESS OF THE PRESIDENT, XXXlil

guages that dealt with geological and paleontological subjects. Not,
however, a thankless task; for the book is in the hands of every
‘geologist—even though, with all his sifting, it was impossible to
avoid multiplying the apparent number of species, which, in different
books and in different countries, went by different names. This
record of scientific labour was recognized by the Scientific Society of
Haarlem, which awarded to Bronn a prize-medal. What is still
more important, it received the universal approval of geologists.

In a later work, on the ‘ Laws of Development of the Organic
World’ (1858), he again reverted to the questions discussed in the
‘History of Nature.’ Reasoning on the entrance, distribution, and
grades of life in the various formations, he arrived at the result that
there has been a gradual development from imperfect to more perfect
forms of life, modified, however, by external conditions of soil, light,
temperature, food, &c., so that the organisms formed by a certain
productive power only endured when capable of adapting themselves
to existing conditions. This power, which he recognized as a means
for the continuous production of individual and original species, was,
according to him, affected by the steady increase of dry land, which
helped to vary the conditions of existence so as to favour a various
and progressive organization. On the whole, then, the later opinions
of Bronn with regard to the development of life seem to have been of
a mixed character (now not uncommon among’ paleontologists since
the publication of Darwin’s great work), which, while it allows a
variation of species so excessive that it may even result in the
production of new genera, says, ‘‘ Hitherto shalt thou come, and no
further.” When leaders go so far, their successors are likely to go
beyond. Notwithstanding these differences of opinion, Bronn exe-
cuted the first German translation of Darwin’s work on the ‘ Origin
of Species’; and, from personal intercourse with my late esteemed
friend, I can testify to his admiration of the wide range of know-
ledge, power of observation, and logical reasoning of the English
philosopher.

Bronn’s last work was ‘The Classes and Orders of the Animal
Kingdom’ (‘ Klassen und Ordnungen des Thierreiches’), in which
paleontology and modern zoology are combined in one system of
natural history. It was interrupted by his sudden death on the
oth of July, 1862, at the age of sixty-two.

In 1851 Bronn was elected a Foreign Member of the Geological
Society, and in 1861 he was awarded the Wollaston Medal. Every
one who enjoyed the privilege of his acquaintance will remember
his amiability, earnestness, and candour. I, for one, shall never
forget the kindness with which he received a wandering geologist,
and, beguiling the time with pleasant conversation, showed him the
geological peculiarities of the neighbourhood of Heidelberg.

BERTRAND DE Dove (Jacques Mathieu) was born on the 28rd of
October, 1776, at Le Puy Cantal, in the old province of Velay.

His father, who destined him for his successor in commerce, sent
him to England, where, having passed three years at school in

XXX1V PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Birmingham, he returned to his own country, and, without neglecting
his commercial career, he took a gratuitous part in many public
offices, thus rendering important services to his native town during
more than half acentury. Science had always for him lively attrac-
tions, and, notwithstanding his public duties, he successfully cultivated
several sciences—the theory and practice of agriculture, archeology,
mathematics, and especially meteorology and geology, in both of
which he made important observations.

The geological description of the neighbourhood of Puy, in Velay,
which he published in 1823, made known to geologists points of the
highest interest in the history of volcanic phenomena, so character-
istic of that part of France. A number of facts, all new at the time,
were then observed by him, with rare penetration, and described with
a clearness, precision, and elegance which make his work still
classical in geology. He was also the author of a memoir on the
fossil bones of Saint-Privat-d’Allier and the basaltic district in which
they were found, published in 1829 in the ‘ Annals of the Agri-
cultural Society of Puy’ and in Brewster’s ‘Journal of Science.’
At the time of his death he was engaged upon a new edition of the
former work.

His power of observation was not less manifest in his meteorological
studies. During a long series of years he observed the currents of
wind both on the surface of the earth and in the region of the clouds,
and he detected in their respective directions a constant relation
which he entitled the law of interversion.

Thus, by the force of native genius alone, Bertrand de Doue rose to
distinction, and, among other honours, became President of the
Society of Agriculture, Sciences, Arts, and Commerce of Puy. In
1828 he was elected a Foreign Member of this Society. He was as
much distinguished by the excellence of his heart as of his head, and
he won the affections of all who knew him by his gentleness and
goodness. He died last year, aged eighty-six.

Dr. Tuomas Stewart Trartt was born on the 29th of October,
1781, at Kirkwall, in Orkney, of which place his father was minister.
He graduated in Medicine in the University of Edinburgh; and in
1832 he was appointed to the Chair of Medical Jurisprudence, which
he filled until his death. He contributed a number of mineralogical
and other memoirs to the ‘ Transactions’ and ‘ Proceedings’ of the
Royal Society of Edinburgh,—and two to this Society, published in
our ‘Transactions, the first entitled “‘Some Observations on the
Salt-mines of Cardona made during a Tour in Spain in the Summer
of 1814,” the second, “On Magnetic Iron-sand mixed with much
Iserine, found at Seacome Ferry, in Cheshire.” He was one of the
oldest Fellows of our Society, having been elected in 1813. He
continued his lectures to within twelve days of his death, and died at
the age of eighty-one.

By the death of the Marevis of BrEapaLBane the sciences of
mineralogy and geology have lost a true friend. Possessed of very

. ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXV

extensive domains in Perthshire and Argyleshire, he employed skil-
ful mineral-surveyors to examine and describe these vast Highland
tracts. One of these surveys was conducted by Mr. Odernheimer, of
Hesse-Cassel ; and it was in consequence of the efficiency of the labours
of this gentleman that he was afterwards selected to be the Surveyor
of the Peel River Company in the extensive grants held by it in
New South Wales. Lord Breadalbane expended very large sums in
improving the machinery and in extending the subterranean works
in his lead-mines of Tyndrum; and though frequently advised as
to the heavy losses he was incurring, he always replied, with a
noble generosity, that the works supported a large body of men and
their families, and must be kept up. ‘These works were for some
time superintended by Mr. Thost, who read before the Society a short
account of the mineralogical features of the Breadalbane rocks, which
was published in the sixteenth volume of the Quarterly Journal.
In these mineral surveys Lord Breadalbane himself took an active
part, hammer in hand, and was often the first to detect the outcrop
of copper-ore, and in one instance of a small portion of gold. Even
when engaged in his favourite amusement of deer-stalking, he always
had an eye to the varied character of the rocks, and never missed a
remarkable junction. ‘Those who, like Sir Roderick Murchison, have
been his companions in the chase can testify to the truthfulness
of this statement.

Whatever Lord Breadalbane intended to do, he did it thoroughly
and, if occasion required, magnificently. Thus, when the Queen
visited Scotland for the first time, his reception of Her Majesty at
Taymouth Castle was truly royal; and again, when the Sovereign
and Her lamented Consort inspected the Volunteers at Edinburgh,
he brought thither such a body of followers that they were con-
sidered the finest and most stalwart men of that splendid review.
In every sense of the word Lord Breadalbane was a great nobleman.
Having for many years served the Queen as Lord Chamberlain, he
was as highly esteemed by Her Majesty and Her Consort as he was
beloved by his associates for his fine social qualities. His unbounded
hospitality will long be remembered by many a foreigner, as well as
by crowds of our countrymen of all classes.

Though he made no pretensions to science, he delighted in sur-
rounding himself with its leading cultivators; and he earned the
praise of naturalists by his endeavours to introduce the animals of
other climes, including the Llama of South America, which he con-
ceived might be useful in Britain. To him also we owe the re-
introduction of the great Capercailzie, or Cock of the Woods.

In the year 1840 he was chosen to preside over the Meeting of
the British Association at Glasgow ; and no one who was present can
forget the success of that vast gathering.

All those persons who knew him well can affirm that he was as
honest and patriotic as he was straightforward and high-minded in
his career through life. Sincere in his attachments, he was natu-
rally so deeply affected by the loss of his accomplished wife, in August
1861, that from that moment he never recovered his former elasti-

XXXYVl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

city of spirit. So, after arranging all his affairs and putting his
house in order, as if he were preparing for the great change, he went
abroad in the autumn of last year, and, after trying a few palliative
remedies in the waters of Germany, he died, at Lausanne, on the
8th of November, in the 67th year of his age.

I propose now to discuss the
Breaks tn Succession oF THE British Patmozorc Srrara.

By breaks in succession I understand those physical interruptions
in stratification marked by the unconformity of an upper formation
to one immediately underlying it, or, when such visible unconformity
is wanting, by a sudden change in the fossils characteristic of the
underlying and overlying formations ; and I therefore only apply my
argument to those cases in which the upper formation is next in
time to that which underlies it, according to our present knowledge
of the order of succession.

In these remarks I lay no claim to originality for the facts re-
corded, which are part of the common stock of knowledge of geolo-
gists; but I am not aware that, in any special memoir, they have
ever been prominently classified. The train of reasoning founded
thereon has also, I suppose, been floating more or less in many
minds. With me it is a result of long personal knowledge of pheno-
mena in the field, and of the memory of what I have thought, read,
and learned in conversation and debate ; and as, in writing what fol-
lows, I have only consulted books when my memory seemed at fault,
if any one finds ideas to which he thinks he can justly lay claim, I
beg he will believe I have borrowed from him.

Before launching into the subject I have only to add that the
species estimated as common to any two formations are from tables
compiled by myself, partly from Morris’s catalogue and others in
various memoirs, and partly, for the Silurian and Devonian rocks,
from data furnished by Mr. Salter, and, for the Permian strata, by
Mr. Davidson. It will not materially affect my argument should these
estimates not be always strictly correct. For a long time paleonto-
logists were busy generally in subdividing, but are now chiefly
engaged in condensing the number of described species ; and though
it is to be hoped they may ultimately diminish the number of
names, and though it is probable they may prove that more are
common to various formations than published lsts now show, yet it
is probable that the mass of the species will still be considered as
essentially distinct in any two formations in which I state that they
are so, according to the common interpretation of the term species.
But constant varieties will do quite as well for my purpose.

Laurentian Gneiss.—First, then, I begin with the more ancient
rocks of the North Highlands, and in doing so I treat the order of
superposition proposed by Sir Roderick Murchison as completely
established ; it happens that the question forms part of my argu-
ment, and I therefore take this opportunity of again bearing testi-

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXVIi

mony to his correct rendering of facts which, in my opinion (and I
know the ground well), only require to be seen to be believed.

The oldest-known rock in Britain is the Laurentian gneiss in the
north-west of Scotland *. On this, certain strata lie which have been
termed Cambrian. They are quite unmetamorphosed, and rest in
the highest degree unconformably on the denuded convolutions of
the intensely metamorphosed gneiss. The interval of time, there-
fore, that elapsed between the conclusion of the formation of the gneiss
and the beginning of the deposition of the overlying conglomerate
was geologically of the longest; for I believe that, in this as in
other cases, Ist, the metamorphic structure was developed deep
beneath the surface, and, 2nd, these rocks were upheaved, contorted,
and greatly denuded before the newer strata were formed above them.
Therefore, except that they occur together, there is no immediate
connexion between the underlying and overlying formations ; and the
vastness of the intervening denudation proves that the interval repre-
sented by the unconformity must have been of extreme length.

The extremely metamorphic state of the Scottish Laurentian rocks
makes it highly improbable that fossils should be found in them.
But in a thick band of limestone in their supposed equivalents in
Canada, Sir Wiliam Logan considers that he has found the remains
of Corals,—an opinion in which I agree. If this be so, the “ Primor-
dial Zone,” in a literal sense, vanishes; and the supposed absence
of fossils in the Cambrian rocks of Scotland f may have no higher
value in paleontology. than the absence of organic remains in the
Bunter sandstone of England.

It is also not quite certain, though it is probable, that the Cam-
brian rocks of Scotland are the equivalents of those of England and
Wales, for this reason, that while in Wales there is perfect con-
formity and a gradual passage from the Cambrian rocks into the
Lingula-flags, in Scotland the Lingula-flags are absent, and the
equivalents of the Llandeilo beds le quite unconformably on the
Cambrian strata. Sir Roderick Murchison has drawn special atten-
tion to this unrepresented interval{; and, as I shall bye-and-bye show
that in Caernarvonshire the Llandeilo beds are probably unconform-
able to the Lingula-series, it is not surprising that in Sutherland
Llandeilo beds should he unconformably on what are believed to be
Cambrian strata. If so, this unconformity is closely connected, as I
shall show, with the great break in the succession of species between
the so-called Primordal Zone and the Llandeilo flags.

LIingula-flags.—The Lingula-flags of Wales § contain a small but
well-marked assemblage of fossils, consisting, as at present known, of
about 6 genera and 20 species of Trilobites ||, 1 Hymenocaris, 3 Bra-
chiopods (2 Lengule and an Orthis), and 1 Bryozoon (Dictyonema)Q.

* See Memoirs and Map by Sir Roderick Murchison and Mr. Geikie.

+ As yet, they have scarcely been searched. t Siluria, 2nd ed., p. 197.

§ From 5000 to 6000 ft., where thickest.

|| Dikelocephalus, Agnostus, Olenus (7), Conocephalus, Ellipsocephalus, and.
Paradoxides.

“| I omit the Annelides, as they do not affect my argument.

XXXVlil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Tremadoc Slate-—Above the true Lingula-flags lie a set of strata
long ago named by Professor Sedgwick the Tremadoc Slate ; and late
researches have brought to light in these beds a series of fossils which
Mr. Salter has proved are mainly distinct from those of the Lingula-
flags below, and of the Llandeilo and Bala beds above them. Thus 11
genera of Trilobites occur in the Tremadoce Slate, which, excepting
4* (Dikelocephalus, Conocephalus, Olenus, and Agnostus), are generi-
cally distinct from those of the Lingula-flags. The species are en-
tirely distinct. At present the Pteropod Theca is first known in
these beds, together with Bellerophon, Conularia, Orthoceras, and
Cyrtoceras; and of all the forms not Trilobitic, Zingula Davisti and
L. lepis are the only species common to the two formations.

Llandeilo and Caradoc Beds.—The community of the ordinary
species in the Llandeilo and Caradoc or Bala beds induces me to
treat them as one group, though it may be possible to subdivide
them in the cabinet, by help chiefly of certain Trilobites, into Lower
and Upper Llandeilo and Caradoc strata. The prodigious develop-
ment of fossils in these rocks has no parallel in the underlying
British formations,—a circumstance of great importance, especially
when we consider that they are to a very great extent new generi-
cally, and almost entirely specifically. But, notwithstanding this
sudden change, no visible unconformity has yet been detected where
(for instance, in the neighbourhood of Ffestiniog and Tremadoc)
the Lower Llandeilo beds le directly on Tremadoc Slate. I shall,
however, presently show that such an unconformity may with reason
be suspected; and though it is difficult, or perhaps impossible, to
separate Lingula-, Tremadoc, and Llandeilo beds (all chiefly slaty) in
mapping, it is not the less evident that in these strata we have three
perfectly distinct zones of organic remains, and therefore, in common
terms, three distinct formations, each much more definitely separated
by fossils from the others than, for instance, the different subdivisions
of the Wenlock and Ludlow beds, each of which can be mapped.

Now all known evidence tends to prove that in Wales the Tremadoc
Slate is an exceedingly local formation, and for various reasons. It
is only certainly known in Merionethshire ; and in Pembrokeshire,
though carefully searched for by Mr. Salter, none of its fossils occur.
Neither is it clearly known in Caernarvonshire ; it is certainly absent
in Anglesey ; and in Scotland, rocks supposed to be Llandeilo flags lie
quite unconformably on supposed Cambrian strata. A fragmentary
formation, such as these Tremadoc beds seem to be, indicates one of
three things.

1st. The formation may have been deposited over the whole area,
but was subsequently disturbed, and in great part removed by
denudation, before the deposition of the Llandeilo flags; or,

2nd. The Lingula-flags were partly upheaved before the deposition
of the Tremadoc Slate, and only those Lingula-beds that still remained
below water had Tremadoc slates deposited above them in direct
succession.

* The remaining seven of these are Angelina, Asaphus, Cheirurus, Ogygia,
Ampyx, Psilocephalus, and Niobe.

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXI1X

3rd. A certain area of sea-bottom had no strata deposited upon it
for a long period of time.

In the first case, so large a denudation implies unconformity and a
great interval between the last Tremadoc bed and the first of Llandeilo
age, and we have thus a coincidence of lapse of time and change of
genera and species.

In the second case, if there were wm places direct succession between
Lingula and Tremadoc beds, why, on a given horizon, does the
Lingula-flag fauna disappear? And the third supposition also by no
means helps us out of the difficulty of a complete change of life in
those areas where the three formations occur in direct order of
superposition.

The question thus arises, why are they so perfectly distinct?
Though in the present state of our science we cannot clearly solve
this question, I hope, ere closing this Address, to lend a little aid
towards its future solution.

One point, if true, is important, and bears strongly on this ques-
tion. I believe that the Llandeilo flags must lie as unconformably
on the underlying strata in Wales as they do in Scotland; and a
close analysis of the structure of the country strengthens this belief.
Thus, in Merionethshire the Lingula-flags are from 5000 to 6000 feet
thick ; in Caernarvonshire, near Llanberris, they are only about
2000 feet thick, having, in a space of about 11 miles, lost 4000 feet in
thickness, either by thinning of the whole mass or by overlap. The
latter seems probable; for in Anglesey, and perhaps even on the
Menai Straits, the Llandeilo and Bala beds lie directly on Cambrian
strata, both Lingula- and Tremadoc Slates being absent. The same
is the case in Ireland.

But the Caernarvonshire and Anglesey areas are so near that
this sudden disappearance of all the Lingula-flags in a few miles
proves an overlap so rapid that I can scarcely doubt that it implies
an actual unconformity of upper on lower strata; and the lapse of
stratigraphically unrepresented time thus indicated is associated,
in my mind, with a total change of fauna between the Tremadoc
formation and the overlying Llandeilo flags; or, in other words, the
period of which we have no fossils preserved, represented by the
unconformity, was so long that all the old life had become, for some
reason, thoroughly remodelled before the deposition of the Llandeilo
flags began.

The same kind of reasoning applies to the difference of species in
the Lingula-flag and Tremadoc beds.

Llandovery or Pentamerus-beds.—The evidence of the physical
and paleontological relations of the Llandovery beds to the under-
lying strata is in part more direct.

In North Wales, in Montgomeryshire and Merionethshire, the
Lower Llandovery beds, being sandy, are easily separable from the
slaty Bala beds beneath, and there is no very direct evidence of un-
conformity between them; but in South Wales, near Llandovery*,

* Observed and mapped by Mr. Aveline.

xl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

there is proof at Noeth-grug of a slight unconformity between them
and the black slates on which they lie.

The Upper Llandovery rocks, however, behave in a very different
manner. ‘These range interruptedly from Marloes Bay in Pembroke-
shire through Caermarthenshire to Builth, the Longmynd, and the
typical Silurian country of Shropshire ; and everywhere they rest
quite unconformably on older rocks, lying sometimes on the denuded
edges of the Lower Llandovery beds, sometimes on Caradoc Sand-
stone, and at Builth and the Longmynd on the highly contorted and
denuded Llandeilo and Cambrian strata.

The lists of the Geological Survey show that about seventy species
of fossils are known in the Lower and Upper Llandovery strata.
These, taken together, are so distinctive that it has been proposed
to elevate the strata in which they occur into a Middle Silurian
series ; and, at all events, their stratigraphical and paleontological
relations are so important that I give the following analysis of
the fossils of the Lower Llandovery beds, followed by more con-
densed statements of the paleontological relations of the Upper
Llandovery beds and Wenlock shale.

go.” | Tankovery: | Handovery. | 8°8dee.
filzenus Bowmannis: <t-cosc--| @ coeeseun | 0) oes x *

Thompson ct seecsssc|) “see ene * *

Calymene Blumenbachii ... * * * *
Orthhisporeatatyco<ces.<cis8ece:|Pmeeseoenn) tare- sete x *

JAG civnculodc-wsgnecnsstededely cecewet Wits imc cess x

calligramma ........0.. * * * *

PELIOLAla)..se2-ee<escesoser x * * x

elegantulla) < cs 2-secseeaes * * x *
Athy pB Crassag te.Lhe-s.ceee cell maestonael |W ete *

PetiCwlaris <..5.<0. -ce ote * x x

marginalis .........-...- # * * *
lhepienassericea ico. sae. .ea| haces se * * *
Tea OCISEA eset ees rre ccc eel meecees * *

transversalis ............ * * * *
Pentamerus oblongus .........| ss... % *

Wpeyisig eee nae Seer * *

UNGA GUS este ne cece er * * *
Strophomena antiquata ...... * * % *
= depressa 2)... 2..cse00sbec- * * * *

IPeGtenises: chee nise aceeare * * * *
Cyclonema crebristria ......| .s.s.. % * *
MUM eMIA yo cc 2k oce nas <cre | pteesates -, lien eee *

AMIGDOSS Sec userse shtenncesesesteeh| Gaaeeceh On temas tes *
Murchisonia Pryce .........| ss... * x
‘Bellerophon, seubus?’.: :7.'-3..22| Mees eemujur eeneee * *

bilobatusi 5.5. Swcenssneees| yu ceute orbs * *

Gilatatus’ ./72.2-.080. 09" * * *

Conuillaria), P. disse. tetisense' * * * *
13 20 28 16

The foregoing Table shows that, according to existing British lists,
there are twenty-eight Lower Llandovery species. Of these, sixteen

ANNIVERSARY ADDRESS OF THE PRESIDENT. xli

have survived from the prodigious numbers (if all were named, pro-
bably more than 500 species) found in the Caradoc and Bala beds;
four are peculiar; twenty pass into the Upper Llandovery rocks,
thirteen of which also pass into the Wenlock shale.

While therefore a fraction more than a half of its fossils are found
also in Lower Silurian rocks, the disappearance of so large a proportion
of Caradoc species proves a very great change of conditions. Con-
sidering the relative numbers in the two formations, it is too much
to suppose that the older fauna was destroyed by the invasion of a few
new species from another area, although, if the beds be conformable
to each other, this is probably an obvious though not the most likely
explanation. The suspicious unconformity between Caradoc and
Llandovery beds in South Wales points in the direction that in reality
there is a gap, due to upheaval and denudation, unrepresented by
strata, between the two formations, and that on re-submergence only
a few of the ancient Caradoc forms survived, to mingle with newer
forms at first almost equally limited in number.

The Upper Llandovery beds have yielded as yet about sixty species,
twenty of which occur in the Lower Llandovery rocks. Eight
species belonging to the latter have disappeared, and only twelve
Upper Llandovery forms are known in the Caradoc Sandstone.

The absolute unconformity of the Upper Llandovery beds on all
below, coupled with a great change of species, is another remarkable
coincidence, and is clearly connected with a lapse of unrepresented
time ; for the Lower Silurian strata were, in our area, in places me-
tamorphosed, intensely contorted, upheaved, and extremely denuded
before the deposition of the Upper Llandovery beds began. Such
events involve the lapse of a period of time (unrepresented by strata)
which it is almost impossible to exaggerate; and I believe that we
see the result in the loss of old species and the appearance of new,
in proportions comparable to the differences between the fossils of
the newest Miocene and oldest Pliocene beds and the life of the
present day. The change in this respect is, however, far less both in
genera and species than that which took place between the Lingula-
and Tremadoc and Llandeilo beds ; and therefore, possibly, the smaller
changes represent shorter periods of stratigraphically unrepresented
time.

‘Wenlock Shale, §c.—If we now examine the relation of the Wen-
lock Shale to the Upper Llandovery beds, we shall find that, out of
fifty-six species, twenty-eight, or one-half, pass upwards into the
former, which frequently overlaps the Llandovery beds in such a
manner as to leave no doubt of an unconformity that must again
indicate a period of unrepresented time, after which we have the
vast development of life of the undoubted Upper Silurian epoch,
during which 5000 or 6000 feet of strata were deposited in a period
of apparently slow and steady depression.

Furthermore it is evident, from the sandy character of most of
the Llandovery strata, from the conglomeratic nature of part of the
upper beds (derived from the waste of the Lower Silurian rocks),
from the comparative thinness, local character, and repeated uncon-

VOL. XIX.

xhi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

formities of its members, extending even to the Tarannon Shale,
that they were formed during an epoch of oscillation of level, and
therefore that its component parts only represent fragments of a
great intermediate epoch that elapsed between the close of the de-
position of the Caradoc Sandstone and the beginning of that of the
Wenlock Shale.

We have now seen that in the whole Silurian series there are six
very distinct sets of strata, and five stratigraphical breaks between
them, as follows :—

Lingula-flags.
Break very nearly complete both in genera and species, an
probable unconformity. : '
Tremadoc Slate.
Break very nearly complete both in genera and species, and
probable unconformity.
Llandeilo and Caradoc beds.
Large break, especially in species, and probable unconformity.
Lower Llandovery beds.
Break and decided unconformity.
Upper Llandovery beds.
Break and strong unconformity.
Wenlock Shale, &c.

Each of these breaks, in my opinion, necessarily implies a lost
epoch, stratigraphically quite unrepresented in our area, and the life
of which is only feebly represented in some cases by the fossils
common to the underlying and overlying formations. But to this
important subject I shall return when I have summed up the evi-
dence respecting the breaks in succession in the higher members of
the Paleozoic series.

Old Red Sandstone and Devonian Rocks—Some of the phenomena
connected with the Devonian rocks and Old Red Sandstone are
more difficult to unravel with precision than those of Silurian age,
for several reasons.

1st. It is understood to be the opinion of one of our best geolo-
gists that in England the true Devonian rocks are the equivalents,
in another area, of the Upper Silurian beds themselves; and this
supposition is not weakened by the circumstance that in Cornwall
the Devonian beds lie directly on Lower Silurian strata. Against
this opinion I think we may urge, with reason, the almost total ab-
sence of the species common in the acknowledged Upper Silurian
districts in this country ; while in other regions, the fossils of which
are almost identical with those in our Devonian beds, the strata
in which these fossils occur are found lying above Upper Silurian
beds, and notably in North America there is an unconformity
between them, which I have seen.

2nd. Though our: Devonian rocks and Old Red Sandstone are
both of dates that come between the Upper Silurian and Carboni-
ferous epochs, it by no means follows that they are throughout of

ANNIVERSARY ADDRESS OF THE PRESIDENT. xiii

precisely the same geological age; for, while in South Wales and
Shropshire the Old Red Sandstone directly succeeds and seems to
pass into the Ludlow beds, the Devonian rocks in the south-west
of England rest on Lower Silurian strata. Again, in our islands,
not only have we few or no terms of comparison between them
derivable from fossils*, but also their lithological characters are
remarkably distinct’.

3rd. In the opinion of several geologists of note, our Old Red
Sandstone proper ought to be broken up as a group and attached
partly to the Silurian and partly to the Carboniferous series.

Under these circumstances, the remarks I venture to make must
be brief for want of definite data, which can only be obtained after
the areas have been carefully surveyed with the light that recent
discovery has thrown on the subject, and with the aid of new and
better topographical maps.

These areas for the Old Red Sandstone are England and Wales,
Scotland, and the south of Ireland, and Devon and Cornwall for the
Devonian rocks.

In Shropshire and in neighbouring districts in South Wales
there is no sign of unconformity, nor any sudden break between the
Ludlow rocks and the Old Red Sandstone. On the contrary, they
pass into each other, this passage being accompanied by a rapid but
not quite sudden disappearance of the uppermost Silurian fossils, in
a manner that suggests, not that there was any disturbance of the
strata, accompanied by unconformity, but rather that, by some lesser
but still broad change in physical geography, the succeeding con-
ditions were in some manner rendered adverse to a plentiful Silu-
rian life +.

Again, when we rise to the top of the Old Red Sandstone round
the Forest of Dean and the greater part of the South Wales coal-
fields, we find that there is no sign of absolute unconformity be-
tween it and the Carboniferous series, although in Pembrokeshire
the limestone does creep across the Old Red Sandstone in a manner
suggestive of overlap rather than of break and unconformity. If then
there be perfect conformity, through the intervening Old Red Sand-
stone, between the Upper Silurian and Carboniferous Rocks, how did
it happen that the life of the two periods was so perfectly distinct ?

Ist. The old reply would have been that the Silurian life was
destroyed at the commencement of the Old Red Sandstone epoch,
and that bye-and-bye, above the same area, the Carboniferous epoch
was ushered in by a special and completely new creation. Lut the
idea that special faunas were created and annihilated periodically
en masse has so long ceased to be the creed of most English geolo-

* In Russia, however, Devonian fossils and Old Red Sandstone Fishes are said,
by Sir R. I. Murchison, to occur in the same bed.

t In North America the Old Red Sandstone of the Catskill Mountains lies
above the Devonian rocks; but perhaps this only represents our Upper Plant-
bearing Old Red Sandstone.

t See Sir R. I, Murchison’s ‘ Siluria,’ and Sir H. De la Beche on the “‘ Forma-
tion of the Rocks in South Wales,” &c., Memoirs of the Geological Survey,
vol. i. p, 51,

a2

xliv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

gists that I need not argue the question, especially with those who
understand the details of the intermediate Devonian fauna.

2nd. Some one geologically quite as heterodox, in the modern
reading of the term, may declare that when the Silurian life was
driven out of this area, it is possible that 1t may have continued
to live elsewhere as late as our Carboniferous epoch ; but when the
latter began, it so happened that our area was repeopled, not from
a Silurian district, but from some other region, where life of a Car-
boniferous type was rife; and this kind of argument has frequently
been enforced by the statement that, if the modern Australian life
were fossilized, we might mistake it for that of part of the Oolitic
epoch *.

Such a statement is most difficult to deal with in the present
state of the science; for the arguments against it can scarcely be
reduced to demonstration, and instinctive feeling must not be mis-
taken for truth. If it be true indeed that, “for anything geology or
paleontology are able to show to the contrary, a Devonian fauna
and flora in the British Islands may have been contemporaneous
with Silurian life in North America, and a Carboniferous fauna and
flora in Africa,’’ there will, in the opinion of some, be a risk that the
very foundations of geological orthodoxy are so sapped and shaken
that the whole column must tumble about our ears, if that column
be based upon a doctrine of paleeontological succession, which, as now
understood, has thus become “ a mockery, a delusion, and a snare.”
I shall return to the question towards the close of this Address, merely
at present remarking that the well-known Australian case vanishes,
when examined, into the region of loose generalization ; for geology
and paleontology deal chiefly with sea-bottoms, and if we compare
that of the Australian sea with those of Oolitic age, we shall find
that, though the former holds Trigonia, Lingula, Terebratula, and
Cestraciont Sharks, yet these form but a very small percentage of a
vast fauna, easily distinguishable as of late Tertiary, that 1s to say,
of modern type. If fossilized, in fact, there would be no more
danger of our confounding an existing Australian and an Oolitic
period because of the T’rigoma, Terebratula, &c. of the former, than
there is of confounding an Oolite and a Carboniferous formation
because of the Terebratule, the Rhynchonelle, the Spiriferw, and the
Nautilr in both.

drd. It may be that mere time had effected the change in species
and genera in other areas, during the period in which the Old Red
Sandstone was deposited under conditions locally unfavourable to
life, such duration of time being much enhanced, if it can be proved
that the Old Red Sandstone consists of two or more unconformable
members.

That the Old Red Sandstone of Shropshire and Wales was not
deposited in an area of general and unbroken depression is almost,
if not quite, demonstrable; and if so, in this case change of life is

* Tuse this argument here at random. It is equally applicable to every

other case of geological superposition and succession of life, but it is needless to
repeat it in each instance.

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlv

connected, as usual, with breaks in stratigraphical succession. It
was long ago stated, by Sir Henry De la Beche, that the upper
sandy and conglomeratic part of the Old Red Sandstone in Wales
overlaps, westward, the lower marly portion, or, in other words,
that the beds which seem to pass into the Carboniferous rocks over-
lap those strata which seem to pass into the Ludlow beds. Though
he does not seem to have considered this worthy of mapping, it now,
in conjunction with other information, seems to indicate actual un-
conformity between the two halves of the Old Red Sandstone—that
is to say, a complete break in succession.

In the south-west of Ireland a physical break of this kind has
been described by Mr. Jukes, where, at the base of the so-called Old
Red Sandstone, from 7000 to 10,000 feet of red beds adhere con-
formably, or nearly conformably, to the Ludlow rocks, and from 3000
to 4000 feet lie upon these beds as unconformably as it is possible
for one set of beds to lie on another, and so pass regularly up into
the Carboniferous Limestone. Here, therefore, is an enormous lapse
of time, of which there is no stratigraphical representative known
in Ireland ; for the Silurian rocks and the unconformable lower por-
tion of the so-called Old Red Sandstone were upheaved and denuded
in the most extreme manner before the deposition of the upper part,
and neither in fossils nor in physical relations is there any connexion
between them.

In Scotland also there is still more ample evidence of strati-
graphical breaks during the deposition of rocks that have all been
massed as Old Red Sandstone.

In Caithness the lowest beds lie quite unconformably on Silurian
gneiss, and therefore the only evidence of anything like the Shropshire
beds of passage is derived from the discovery, at Ulbster, of Ptery-
gotus in the lower strata under the flags—an important fact, only
made known to me two days since by Sir R. I. Murchison.

In the beds next in the Caithness series (so-called Middle Devo-
nian) several of the Fishes are of the same genera with those in the
Upper Old Red Sandstone of Ireland with its Plants and Anodon ;
which division, Mr. Jukes observes, passes conformably into the Car-
boniferous Limestone, and, in his opinion, forms the lowest member
of the Carboniferous strata.

Further south, in Forfarshire, it has been shown that the Ptery-
gotus-beds (supposed to be beds of passage) again occur, and that
these are overlain unconformably by Upper beds of the Old Red
Sandstone.

But recent investigations by Mr. Geikie show that it is in the Pent-
land and Lammermuir hills that the most perfect evidence occurs of
breaks in succession. There certain red strata on the horizon of the
Pterygotus-beds lie conformably on the highest recognized Ludlow
rocks, and these have always, as in Ireland, been massed with the
Old Red Sandstone. On these the red and yellow sandstones, bedded
felstones and ashes of the Pentland hills lie in strong unconformity ;
and on these again the Upper Old Red Sandstone strata (Dura Den
beds?) lie in a second strong unconformity, and pass conformably

xlv1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

under and into the base of the Carboniferous series. The base,
therefore, of this Old Red Sandstone series is, it appears, conformable
to the Ludlow rocks, and the top to the Carboniferous, and there are
two strong unconformities between. The geological succession is
therefore singularly broken and incomplete. I agree with Mr. Jukes
that the classification of the Old Red strata requires to be remodelled ;
but, however this may be, it is clear, from the long-continued denuda-
tions that preceded each unconformity, that enormous gaps exist in
the recognized scale of British Old Red strata, lapses of unrepre-
sented time, the results of which we partly find in changes of life.

Devonian Rocks.—Excepting that they are arranged in a given
order of superposition, there is little to be said respecting the
relation of the fossils to the stratigraphical relations of the Devonian
rocks of the south-west of England. When, many years ago, that
area Was mapped, extreme analyses in geological surveying had
scarcely been introduced ; and in that country, consisting so largely
of granite and gneiss, contorted greywacke and limestone, no one
attempted on maps to split up the Devonian series into distinct sub-
formations. So exceedingly disturbed are the strata, that without
a new survey it is to this day impossible to say what unconformities
may or may not exist among its members. Neither, till the country
is remapped, is it possible to make out accurately the exact zoological
relations of the subdivisions; and the data I now present are only
approximate, being the result of an examination of Devonian lists
with Mr. Salter, who placed his intimate knowledge of the ranges
of palzeozoic forms at my disposal.

First, then, the Devonian fossils are distinct from those of the
Silurian rocks of the district—a circumstance easily accounted for
when we know that they le directly and unconformably on Lower
Silurian strata.

This, therefore, makes it impossible to prove that in Devon or Corn-
wall the lowest Devonian rocks exist. In North America, where
such beds le directly on Upper Silurian strata, it is plain that the
latter suffered extensive erosion before the deposition of the former,
this physical break being accompanied by a marked break in organic
succession. There is thus reason to believe that, if our Upper Silu-
rian strata were in contact with the Lower Devonian rocks of Devon
and Cornwall, the same broken relations would exist between them ;
for, of the several hundreds of Upper Silurian forms, it is said that
only about six species occur in the Lower Devonian rocks, perhaps
not more than 1 per cent. Thus, therefore, we have a zoological
break, all but total, between two formations, accompanied probably
by a vast lapse of time unrepresented by any strata in Devonshire,
and only possebly represented by the so-called unfossiliferous Lower
Old Red Sandstone of Ireland, Scotland, and Wales.

There being, in Mr. Salter’s opinion, no marked zoological line
between our Lower and Middle Devonian rocks, I have massed them,
and divided the series as follows.

1. Marwood and Pilton beds=the Coomhola Grits of Mr. Jukes

and Carboniferous Slate of Sir R. Griffith.

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlvii

2. Upper Devonian strata.

3. Middle and Lower Devonian.

The result of an elaborate analysis from Tables prepared for the
purpose is, that of known Middle and Lower Devonian fossils there
are about 61 genera and 170 species; and of these about 23 species
only pass into the Upper Devonian division, or about 132 per cent.

The Upper Devonian beds yield about 30 genera and 70 species ;
and of these, 24 (or about 34 percent.) pass into the Marwood beds,
which in Devonshire have heretofore given about 31 genera and 65
species, of which 14 species, or about 21 per cent., pass into the
Carboniferous rocks. Judged by the imperfect data of mere per-
centages, it appears then that the Upper Devonian are less intimately
connected with the Lower Devonian than with the Marwood beds,
and that the Marwood beds are zoologically more nearly related to
the Upper Devonian than to the Carboniferous strata. In the south-
west of Ireland the Coomhola Grits and Carboniferous Slate pass
downward into Old Red Sandstone, and upward into Carboniferous
Limestone; and they are considered by Mr. Jukes either to be the
lowest part of the Carboniferous series, or else to form a distinct
group together with the upper half of the Irish Old Red Sandstone,
which is stratigraphically quite unconnected with thé lower half.
Further, it must be remembered that for many years, in Devon and
Cornwall, Silurian and Devonian rocks were all massed together, and
called by one name. But we know that there must be an uncon-
formity discoverable between the Lower Silurian and Devonian rocks,
if properly searched for; and analogy would lead us to expect, from
the strong breaks in organic succession, that the same broken strati-
graphical relations—lapses of unrepresented time—must exist
between the various members of the typical Devonian series, just as
they certainly occur in what geologists consider their equivalents,
the Old Red Sandstones of Scotland and of Ireland.

Carboniferous Series.—I have already stated that, of 65 species
from the Marwood beds, only 14, or about 21 per cent., pass into the
Carboniferous rocks; while, if we take the whole of the Devonian
series, only 11 out of about 240 species, or rather less than 5 per
cent., are common to the Devonian and Carboniferous ages.

If we now analyse the divisions of the Carboniferous series, it is
not easy in Britain at present to get evidence of anything like uni-
versal unconformity of one part on another, though there are proofs
of local disturbances. Thus in South Wales, Lancashire, Derbyshire,
and Yorkshire, the Carboniferous series has generally been described
as conformable from bottom to top. It is true that in Lancashire
Mr. Hull suspects unconformity between his Middle Coal-measures
and the Gannister beds, and that Mr. Marcus Scott has shown an
unconformity in the Coal-measures of Coalbrook Dale. I have also
myself seen the Millstone-grit resting unconformably on the Moun-
tain-limestone of the Forest of Dean ; and overlaps of Upper on Lower
Carboniferous rocks take place in Scotland and almost everywhere.
But in spite of these cases, in a formation like the true Coal-measures,
which evinces frequent oscillation of level, it is at present difficult

xlviii PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

to connect changes of fauna with any special gap in time accom-
panied by extreme unconformity ; for these changes may perhaps be
due to mere local variations of conditions encouraging for a time the
presence of special marine, estuarine, and freshwater or terrestrial
faunas or floras in certain areas. The strongest positive exception
to this seems to be in the rocks below and in those above the
Millstone-grit (where we have at least one unconformity in Dean
Forest) ; for the decidedly marine forms (Brachiopoda, &c.) of the
true Coal-measures in Coalbrook Dale and elsewhere are nearly all
distinct from those of the Carboniferous Limestone. The same kind
of break in organic succession is found in Scotland, where, however,
the coals in the Limestone-series point to a set of conditions closely
resembling those that prevailed during the formation of the ordinary
Coal-measures, and in that country no proof has yet been adduced of
any break in the stratification.

Permian Strata.— When, however, we come to the Permian series,
the proofs of a remarkable physical break are unmistakeable. The
evidence of this in Britain is so well known that to bring it to
recollection I have only to state that the Rothliegende lies as it were
at hap-hazard on all our formations, from the Lower Silurian of
Malvern to the uppermost Coal-measures of the middle and north of
England. In part of the Rothhegende a few of the Plants of a very
meagre flora are common to the Coal-measures ; and when we come
to the marl-slate and limestone, all the Fish are distinct from those
of Carboniferous age. Of more than 170 genera and many more
than 1000 species of Carboniferous forms of marine life, only a few
survive to pass into the Permian series. Mr. Davidson is of opinion
that about half the Permian Brachiopoda are Carboniferous species,
—a much larger allowance than any one else has given. But this
would only give 10 or 11 species, and, adding other forms of shells
still doubtful, probably not 15 per cent. of the whole Carboniferous
fauna is common to the two epochs. As in former cases, I connect
this great break in the succession of species with a lapse of time in
our area, stratigraphically unrepresented, during which most of the
Carboniferous species died out or changed; a few survived, pre-
serving their identity, and the others, according to Mr. Darwin’s
views, are modified descendants of older forms.

It is well known to some that I entertain peculiar opinions
respecting the glacial origin of those boulder-beds which here and
there form so large a part of the Rothlegende; and I cannot help
connecting the smallness of the number of our Permian species, and
their dwarfed character, with a cold episode in this portion of the
geological record, analogous to that which seems to have produced a
dwindling of life in the northern hemisphere during the newer
Pliocene glacial epoch.

After this comes the great break between the Paleozoic and
Mesozoic strata, a part of the subject on which I will not at present
enter.

General Considerations.—If we now review the stratigraphical and

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlix

paleontological relations of the British strata, from the Laurentian
to the Permian rocks, we find that

From the Laurentian to the top of the Silu-

man rocks there gre. Coo eS. 6 physical breaks.
im the Old’ Red Sandstone .............. 2 ‘ Be
In the Carboniferous strata, probably at least 1 3 as
Between the Carboniferous and Permian.... 1 - ‘.
10 in all.

Except in one case where the rocks are almost barren, these
breaks are accompanied by great and remarkable changes in the
number and nature of the fossils, sometimes of the genera, and
always of the species. The coincidence is certain ; and the question
must present itself to every informed mind, Why does this arise ?

Within the memory of most of us the ready answer would gene-
rally have been given, that each formation, the fossils of which are
distinct from those below and above, was complete in itself, and
presented a perfect view of the relics of the marine life of the world
for a given period; that this life, by a distinct act of omnipotence,
was suddenly extinguished, and as suddenly replaced by a universal
new creation when the succeeding deposits began.

The doctrine of per-centages common to two or more formations,
especially in the Tertiary strata, has so completely destroyed this
old notion, that I need not argue it here.

The idea of the sudden destruction of entire faunas has again often
been expressed in another form :—viz., that certain given periods
were brought to an end by tremendous and universal convulsions,
which were the direct means of the destruction of all or nearly all
the life of the globe. Then, this temporary chaos having come to
an end, a new creation and new unconformable formations were
commenced with the return of order. Such opinions, common not
long ago and not yet quite extinct, are founded, often unconsciously,
on the assumption that the succession of known formations, and
therefore of life, is altogether or nearly complete. That it did not
require chaotic convulsions to destroy the old life and usher in the
new, is plain from the circumstance that the Oolitic epoch in a vast
area came to an end without any violent disturbance of the strata ;
for the Oolitic formations seem to have been quietly, and nearly
horizontally raised above the water (whence the origin of the
Purbeck and Wealden beds), and as quietly let down again. But
the diversity of the Oolitic and Cretaceous fossils is as complete
as if accompanied by violent disturbance and unconformity. The
accompaniment of this diversity is t¢me, so strongly expressed in the
old delta, which tells of the drainage of a vast continent, followed
by the swallowing up of that land by the sea. The study of the
Tertiary strata has, however, been the chief means of destroying the
belief in the disappearance of faunas being necessarily accompanied
by sudden convulsions; and therefore the worn-out theory sinks

VOL. XIX. €

l PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

steadily, and will shortly disappear. I need not argue it further
than to indicate the cause of its deserved decline.

The modern school of geology, as I have this day argued, more
and more leans to the opinion that the series of formations is any-:
thing but complete, and that many links in the chain of evidence are
missing. This belief helped to establish the idea that individual
species have died out and been gradually replaced, as slowly as species
are now dying out and now coming in, not only in epochs represented
by the various known formations, but also during those periods of
unrepresented time witnessed by unconformities. This belief equally
applies to the old idea of a special creation for each species, or to
the views so clearly urged by Darwin; but it seems to me to have a
special significance if we believe, with him, that species acted on by
various influences pass slowly from one form into another, and there-
fore that partial or complete diversity of fossils in any two forma-
tions generally marks a greater or less interval of time.

If we now, by way of test, pass the Silurian formations in review, it
is evident that they were deep-sea deposits, with the exception per-
haps of part of the Llandovery beds, which were formed during re-
peated oscillations of level. The Upper Llandovery beds especially
were, in part, formed so near shore that, in the Longmynd country,
they bear almost the characters of a beach. From a consideration of
these circumstances the question easily arises, What relation is there
between the absolute length of time occupied during the deposition of
any one of the greater Silurian formations and the time that elapsed
between its close and the commencement of the formation next in
succession? ‘Take, for instance, the Caradoc or Bala beds, in which
the comparative uniformity of the fauna from bottom to top shows
that the strata were deposited under nearly uniform conditions in a
period of slow and steady depression of the sea-bottom. But where
such conditions were seriously interrupted, we find either direct
evidence of unconformity or strong presumptive evidence of a break
of that nature—phenomena implying a great change of physical
conditions and a long lapse of time. Supposing, therefore, Mr.
Darwin’s hypothesis to be correct, it may be asked whether, under
the changing conditions coincident with disturbance of strata, there
may not have been influences at work that entailed a more rapid
development of new species out of old, and of old species into new
genera, than those that existed during an epoch when the conditions
in a given area remained comparatively unchanged. The notion is
simply this:—A change in the relative distribution of sea and land
took place, so great perhaps that the creatures that inhabited one
area were driven slowly from stage to stage into other latitudes, so
that, under circumstances which varied with comparative rapidity, if
it so happened that their descendants (mingled probably with species
from other stocks) returned into the same area, their forms had
changed entirely or in part. Or, in another possible case, frequent
oscillation of level produced such frequent changes of condition that,
in the end, a like result came about, the intermediate stratigraphical
stages being lost.

ANNIVERSARY ADDRESS OF THE PRESIDENT. li

The question has great weight ; but I do not see that it is likely
soon to be solved, chiefly for want of a sufficient amount of precise
data. The most analogous case that occurs to me at present is that
of the Drift; for there is reason to believe that all, or nearly all, the
Molluscan life that immediately preceded the deposition of the glacial
strata has survived very extensive physical operations which involved
remarkable changes of climate, accompanied by deep submergence
and re-elevation of enormous areas. Both in this case and in that
of the Oolitic and Cretaceous strata formerly cited, one of the elements
of the question involves great elevation and depression of wide areas,
and therefore serious changes of conditions. In the older one there is
no proof of any change of climatal conditions, and yet the change of life
is complete; and in the latter there is the strongest evidence of
extreme variation of climate without extinction of Molluscan species,
Sufficient time to promote the change was perhaps present in the
first case, and wanting in the second.

Contemporaneity of Strata.—I now come to another question con-
nected with physical breaks.

It is stated that over wide European and other areas, even as
far off as North America, the same kind of physical breaks occur as
in the British Islands, and sometimes at what are considered to be
the same points in the geological scale. The question has therefore
often been raised (I have already adverted to it), Are we justified in
considering formations to be altogether or approximately contem-
poraneous that contain the same general assemblages of fossils in

areas wide apart?

' he answer has sometimes been given in the negative, on the
minor ground that the two ends of the same bed are not necessarily
precisely contemporaneous, and on the larger issue that the existence
of the same species in strata far apart proves that they are not of the
same age, because it would take a long time for species that origin-
ated in one area to travel into another. The minor point presents
no serious difficulty ; but the larger one, which is an extension of the
same line of argument, is more difficult to dispose of.

It appears to me, however, that such reasoning is in error simply be-
cause the reasoner is apt unintentionally to consider a whole formation,
perhaps from 1000 to 7000 feet thick (as in the case of the Bala beds
and the Hudson River group), as if it were a bed or a thin set of beds
representing a particular sea-bottom at a particular time, whereas the
Bala beds represent a great many thousands of sea-bottoms more or
less regularly piled on each other very slowly. The question must
therefore arise, in connexion with duration of species, whether under
any circumstances the possible time, for instance, that it might have
taken to transmit species from the English to the American area is
likely to be comparable to the amount of time represented by the
interval between the lowest and the highest Bala strata, or even of a
longer period ; for if formations commonly believed to be approxi-
mately contemporaneous are not so, then the process of transmission
of a group from one area to another might be prolonged indefinitely,
so that, as supposed hypothetically by Professor Huxley, a Silurian, a

hi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Devonian, and a Carboniferous fauna might all exist in different areas
at the same time. Experience, as yet, affords no clue to the
rate of geographical transmission of groups of genera and species ;
but, in the case of a large fauna, such as that of the Caradoc or Bala
beds, I incline to think that the enormous thickness of the formation
represents a range in time probably vast enough within its own
limits to allow (where conditions were good) of transmission, with or
without some amount of modification, over very large areas, so that a
strong family likeness would exist in distant regions, and some of the
strata in supposed contemporaneous formations would run so many
chances of being actual equivalents that the likelihood that none of
them are so is reduced to 4 minimum. Further, if the idea put by
Professor Huxley be just, it appears to me that in the piles of forma-
tions built up in Britain, on the Continent, and in America, the
chances are overwhelmingly strong that in each or in some one area
there might be a recurrent fauna,—which is not the case. To this I
attach great weight.

Furthermore, many considerations, partly stated, lead me to suspect
that we must look to the lapse of time unrepresented by strata,
as the chief cause, or, rather, as the necessary accompaniment, of the
influences that produced the great difference in species between any
two formations one of which lies unconformably on the other,
whether we adopt the old view of gradual extinction and replace-
ment by special creation, or Mr. Darwin’s more philosophical argu-
ment of descent with modification. In other words, believing that the
causes that produced physical changes were much the same in former
times as now, both in kind and intensity (speaking generally, when
spread over long epochs), then the upheaving, contorting, and disloca-
tion of the strata, and the vast denudations they underwent before re-
submergence, generally represents a period of tume longer than that
occupied respectively by the deposition of the formation disturbed, or
of that which overlies it unconformably.

In the present state of knowledge these things cannot be proved,
but we may strongly suspect them to be probably true; and if they
are so, then it follows that the periods of time stratigraphically un-
represented during the Paleozoic epoch were much longer than those
of which the various formations of that epoch bear witness ; and I throw
out these suggestions in the hope that as data accumulate, and thought
is expended, a true solution of the question may be arrived at.

It was my intention when I began this Address to have gone over
the evidence of the same kind that applies to the Secondary and
Tertiary formations, some of the problems to be solved there present-
ing difficulties that do not occur in the Paleozoic rocks of Britain.
Time, however, will not permit me to do so; but, if I find that what I
have now said is not unacceptable, I may return to the subject on a
future occasion.

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS .
tdn

OF

THE GEOLOGICAL SOCIETY.

Novremser 5, 1862.

The followmg communications were read :—

1. Descriptions of some Fossizs from Inna, discovered by Dr. A.
Fiemine, of Eninsures. By Dr. L. pe Konincx, F.M.G.S.,
Professor of Chemistry and Geology in the University of Lidge.

{Puates I.-YIII.]

A memoir by my friend Mr. Davidson, in vol. xviii. p. 25 of the
Quarterly Journal of the Geological Society, contains the description
of the fossil Brachiopoda discovered in the Punjaub by Messrs. A.
Fleming* and W. Purdon. The determimation of these fossils could
not have been confided to better hands. A great number of the
species were susceptible of being identified with European and
American Carboniferous species, some are new, and others do not
possess the paleeozoic aspect which a somewhat experienced paleon-
tologist easily perceives among the fossils of the Carboniferous
period. That which occurs in connexion with the Brachiopoda may
be remarked likewise among the fossils of other classes which
accompany them, and the description of which has been confided to
me by their discoverer. Among these fossils, certain species belong
to genera that have hitherte only been found in the Secondary for-
mations, and occur principally in the lower groups of that great
geological period. Such, above all, are the Ceratites, which appear

* See also Quart. Journ. Geol. Soc. vol. ix. p. 189.
VOL, XIX.—PART I. B

2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 5,
to be tolerably abundant in a rock of the Punjaub Salt-range, ané
are remarkable from the fact that they are all new to science. But
for this last circumstance, one might have entertained serious
doubts relative to their geological position, although Dr. Fleming had
ascertained by personal examination that they occurred in the same
beds as those which contained the Carboniferous Producti and
Spirifere. At all events there is still this remark to make, that the
rock which contains the Ceratites has not shown me (at least, in
relation to the specimens confided to my examination) any traces of
those other Paleozoic genera. It is therefore to be desired that new
observations should be brought to confirm those already made by the
learned Edinburgh Doctor, who was the first to throw some light on
the geological constitution of the ancient kingdom of Rumjeet Sing.
The larger number of specimens that I have had at my disposal
belong to Dr. Fleming, and have been deposited by him in the Cal-
eutta Museum, while the remainder are preserved in the Museum of
the Geological Society of London. Altogether there are forty-nine
species ; but, among these, five were in too bad a state of preservation
to admit of being determined with certainty, and consequently have
neither been figured nor described. The others, which form the

subject of this communication, may be divided in the following
manner :—

I. ANTHOZOARTA.

1. Isastrzea arachnoidea, De Kon.

2. Clisiophyllum Indicum, De Kon.

3. Lithostrotion basaltiforme, Conyb.
§ Phill.

4, Lithostrotion irregulare, Phill.
5. Michelinia favosa, Goldf. .
6. Alveolites septosa ?, Fleming.

II. ECHINODERMATA.
7. Philocrinus cometa, De Kon. | 8. Cidaris Forbesiana, De Kon.

TIT. MOLLUSCA.

A. Bryozoa. 23. Bellerophon Jonesianus, De Kon.
24. Macrocheilus depilis, De Koz.
9. Polypora fastuosa, De Kon. OR ogee Dekon.
10. Fenestella megastoma, De Kon. 26. Nerinxa?, n. sp.?

il. Fenestella? Sykesii, De Kon.
12. Retepora? lepida, De Kon.

13. Phyllopora? Haimeana, De Kon.

D. CEPHALOPODA.

; 27. Ceratites Flemingianus, De Kon.
14. Phyllopora? cribellum, De Kon. 98, Werechieqn eas Wie nee
29. Hauerianus, De Kon.
B. LAMELLIBRANCHIATA. 30. planulatus, De Kon.
15. Anomia Lawrenciana, De Kon. bl. Lyellianus, De Kon.
16. Pecten Flemingianus, De Kon. 32. latifimbriatus, De Kon.
(hy & Asiaticus, De Kon. 33. Buchianus, De Kon.
Hey au Re ae ae 34. Davidsonianus, De Kon,
: Samet Ral ; 35. Lawrencianus, De Kon.
WO Bolencpeats srabaieate, “Yak on 36. Goniatites? Gangeticus, De Kon.
37. Nautilus Burtini, Galeotti.
C. GasTERoPopA, 38 Flemingianus, De Kon.
20. Dentalium Herculeum, De Kon. 39. Orthoceras vesiculosum, De Kon.
21. Bellerophon decipiens, De Kon. 40. rachidium, De Kon.

orientalis, De Kou.

. —— decrescens, De Kon.

1862.] BE KONINCK—INDIAN FOSSILS. 3

TV. PISCES.

42. Acrodus, n. sp., closely related to ; 43. Acredus Flemingianus, De Kon.
A. lateralis, Ag. 44. Saurichthys ? Indicus, De Kon.

All the fossils sent are from the western end of the Punjaub
Salt-range, and from its prolongation down the right bank of the
indus, as far as Kaffir Kote, which is a rich locality for mest of the
fossils.

i. IsastR=A ARACHNOIDEA, De Ken. Pi. II. fig. 2.

This coral is in subgibbous masses, whose subequal calyces are of
a polygonal shape, but more often hexagonal, of small depth, and
terminated by obtuse mural edges: the rays, to the number of from
28-30, are crenulated on their edges, all departing from the centre
of the calyx and radiating towards the margins, where they become
slightly thickened.

It will be interesting to determine by new observations whether
this species really occurs in strata of the Carboniferous period,
because the genus to which it belongs has not been hitherto dis-
covered lower than the Muschelkalk.

2. CristopHytitum Inpicum, De Kon. PI. IL. fig. 4.

The skape of this ceral is that of a very elongated cone, showing
frequent, but slightly marked concentric interruptions, or ruge of
growth..

The vertical ridges or partitions are very thin, and number about
300 all round the circumference. Examined with the lens, one
perceives in the interseptal cells very thin and numerous partitions,
which are marked exteriorly by very fine longitudinal strie. The
floors of the chambers are numerous, and smooth in their central
portions. The oval shape of the transverse section of the specimen
which I have just described appears te depend on a kind of acci-
dental malformation. The diameter is about 6 centimétres. The
large number of partitions with which this species is furnished
allows of its being distinguished without difficulty from all its con-
geners.

3. LirHostRorIoN BASALTIFORME, W. D. Conybeare and W. Phillips,
Outlines of Geol. of England and Wales, 1822, p. 259.
Notwithstanding that the Indian specimen consists only of a sili-
ceous cast, in a very indifferent state of preservation, I do not
think that I can be mistaken in identifying it with the English
species just mentioned.

4, LirHosTRorion IRREGULARE, Phill. Geol. of Yorkshire, 1836, vol. 11.
p- 202, pl. 2. figs. 14 & 15.
This species is represented by a specimen identical in its characters.
with those found in the Carboniferous Limestone of Yorkshire. The

diameter of the calyces is from 14 to 16 millimetres.
B2

4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 5,

5. Micneninia FAvosa, Goldf. Petref. Germ., 1826, vol. 1. p. 4, pl. 1.
fie, 11:

A single specimen discovered by Dr. Fleming is identical in all its
characters with those of this species from the neighbourhood of
Tournay. The only and insignificant difference that it presents
consists in the rather greater extent and the rather more regular
disposition of the vesicular cells. The diameter of the calyces is
between 4 and 10 millimetres.

6. ALvEoLitss sEprosa?, Fleming. Pl. II. fig.1. Brit. Anim. 1828,
p. 529.)

This specimen appears to me to possess all the characters of the
species to which I have referredit; but as I have not had the advan-
tage of being able to compare it with the English examples, there
remains in my mind a slight doubt as to their specific identity.

7. PurLocrinus cometTa, De Kon. PI. II. fig. 5.

While describing this species, I shall indicate the characters of the
new genus which I am obliged to create for its reception. These
characters consist chiefly in the existence of five basal plates of a
quadrangular form, alternating with five rows of radial plates, to the
number of two for each ray. The second plate is cuneate, and sup-
ports two series of brachial plates, also two in number; each of
these, finally, giving support to two series composed of a great
number of brachial plates, thus producing about twenty free arms.
All the other plates are soldered one to the other, and form the
calyx.

In the species which I am describing, the calyx is a little gaping,
the external surface is perfectly smooth, and the arms are composed
of at least fifty articulations. The surfaces of these joints or plates
not being parallel to each other, it results that the dorsal or external
portion of the rays appears to be ornamented by a zigzag sculpture.
I could find no trace of fingers.

Philocrinus has but two radial plates, and is thus distinguished from
the genera Encrinus and Millericrinus, which have three. The dimen-
sions of the Philocrinus cometa are as follows :—length of the calyx
25 millimetres; diameter 24 millimctres; length of the arms 6-8
centimctres.

8. Crparis Forprstana, De Kon. PI. IV. figs. 1 & 2.

T am acquainted with but seven spines of this species, which have
much analogy with those of C. Braunii, Desor, from St. Cassian ; they
are tolerably large, fusiform, terminated by a rather sharp point, de-
pressed on one side, and furnished with from sixteen to eighteen longi-
tudinal series of small spiniform tubercles. They are rather less
marked on the flattened side than on the remainder of the surface.
The tubercles are often connected together by their bases, and
seem then to be derived from parallel keels or longitudinal ribs.
The neck of the spine is large and smooth, the milled ring or annula-
tion does not project much, the head is short and narrow, and the

1862.] DE KONINCK—INDIAN FOSSILS. 5

articulating facet smooth. Length 5-6 centimétres; diameter12-15
millimétres.

Among the Punjaub fossils I have met with some fragments of
stems which seem to have belonged to two different species of Poterio-
erimus, but which it has been out of my power to determine specifi-
cally. One of these specimens was accompanied by the Productus
spinulosus, Sow., the presence of which is a proof of their Carboni-
ferous age.

9. Porypora Frastuosa, De Kon. PI. I. fig. 4. (Description des Anim.
Foss. de la Belgique, 1844, p. 7, pl. A. fig. 5.)

I have not been able to perceive any difference between the Indian
Specimen and those which I discovered in the Carboniferous Lime-
stone of the environs of Ecoussinnes. A portion of the first, acci-
dentally worn by some mechanical agency, has enabled me to see that
the pores, with which its anterior surface is ornamented, served as
orifices to small tubes, which are feebly incurved, have their origin
on the axis of the principal branches, and diverge obliquely upwards
on each side, as shown in the enlarged portion represented by the
figure, 4a. From the Productus-limestone of Moosakhail ?

10, Frenesteria mMEGAstoMA, De Kon. PI. IT. fig. 3.

I am not more certain relative to the generic determination of this
species than I was of the preceding one. I place it by preference in
the genus Fenestella on account of its resemblance to the F. crassa of
M‘Coy. It is composed of rays which are subparallel with each
other, and of which the visible surface (probably the posterior one)
is garnished with very small longitudinal striz, observable by means
of a lens, and similar to those which ornament one of the surfaces of
some other species. The principal branches bifureate at intervals,
and are connected together by means of perpendicularly disposed,
transyerse bars. These accessory branches have the same dimen-
sions as those of the principal ones. The fenestrales so pro-
duced are longer than wide, and their shape is that of a parallelo-
gram with rounded angles. Three radiating series have a length
of 1 centimétre. This species differs from F. crassa by the much
more shortened shape of its fenestrales and the distance of its prin-

cipal branches.

11. Fenestetta? Syxesr1, De Kon. PI. I. fig. 1.

It is with some doubt that I have placed this species in the
genus Fenestella. I have been led to do so from the complete ab-
sence of all trace of pores and striz on the surface of the specimen
examined, although it was perfectly well preserved. This Bryozoon
is fan-shaped, irregularly plaited, composed of a number of rays
soldered one to the other, the direction of which is indicated solely
by a feeble thickening, and especially by the series of small, circular
openings which border them. The arrangement of the openings
demonstrates sufficiently that the rays bifurcated once, or several

6 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

times, during the development of the polyzoarium, and that this bi-
furcation is the principal cause of its rapid enlargement. These
openings are almost all of the same size, and are a little more than
half a millimétre in diameter. One may generally count seven in the
breadth of a centimctre.

12. Rererors? teprpa, De Kon. PI. I. fig. 5.

It is with some doubt that I place this species in the genus
Retepora, because I have been unable to perceive the smallest
traces of pores on the single specimen I have examined. It
is not impossible that it belongs to Fenestellé or to some other
éelosely connected genus. It consists of a kind of very thin fan-
shaped network, composed of a great number of small branches, the
numerous bifurcations of which enable it to widen rapidly; these
small branches, which are all alike, are externally furnished with
small, undulated, longitudinal striz, visible only by the assistance
of a hand-magnifier. They are connected by means of small trans-
verse bars, which are thinner than the branches, and almost per-
pendicular to them, but are rarely parallel to each other, and are
perfectly smooth on their surface. The fenestrales produced by these
intersections are almost all quadrangular, and about as high as wide.
The largest are 1 millimetre wide, each way.

43. Puytiopora? Harmeana, De Kon. PI. I. fig. 3.

The calcareous plate of this species is rather thicker than that of
the following, but its shape is almost the same. The openings, with
which it is covered, are much larger; they are circular, and also
somewhat funnel-shaped. ‘Their disposition is much less regularly
quincuncial ; one can count but 4 or 5 for every centimetre. Only
a single specimen is known.

14, Puyiiopora ? errBpettumM, De Kon. PI. I. fig. 2.

This species is formed of a calcareous plate, irregularly undulated,
very thin, and pierced with a number of small oval apertures tole-
rably regularly and quincuncially disposed ; eight of these apertures,
taken on the same line, occupy a length of 1 centiméctre. The re-
mainder of the surface is entirely smooth. I have seen but a single
specimen.

15. Anomia Lawrencrana, De Kon. PI. IV. figs. 7, 8, 9.

This is certainly one of the most curious shells brought from India
by Dr. Fleming. This gentleman having expressed a desire to dedi-
cate it to Sir H. Lawrence, Chief Commissioner of the Punjaub, who
had so greatly facilitated the exploration of the Salt-range, I have
hastened to comply with this wish ; and the giving it this name will,
at the same time, recall the period of its discovery.

As is the case with the greater number of its congeners, this
species has nothing very regular in its shape. In fact, none of the
three specimens that I have been able to examine resemble each

1862. ] DE KONINCK—INDIAN FOSSILS, 7
other, although it is easy to recognize at first sight that they belong
to the same species. In all of them the upper valve is conical; but
in the first two (figs. 7 & 8) this cone is truncated, while in the
third the summit is slightly inclined on one side, and recalls the shape
of certain species of Pileopsis (fig. 9). The shell is very brilliant, and
has all the appearance of that of a recent species. Its surface is
covered with a great number of irregular striz and wrinkles, pro-
duced by the successive growth of the shell. These wrinkles serve
here and there as a basis for little tubes, similar to those which rise
from certain Producti. The distribution of these tubes is rather
irregular, as one may perceive by a glance at the figures. The test
is laminated and extremely thin.

I have been able to examine the lower valve in a single specimen
only ; it is circular in form, entirely smooth, and feebly grooved in
the middle. This character probably depends on the shape of the
object to which the shell has been attached towards its centre. Four
small, circular tubes (fig. 75) may be perceived, of a rather darker
colour than the rest of the shell; they appeared to me to have been
the bases of small internal tubercles.

The diameters vary too much to be indicated here; they can be
easily taken from the figures, which have been drawn with the
greatest care.

16, Pecren Fremrineranvs, De Kon.. Pl. IV. fig. 4.

This species is of medium size, longer than wide, and suboval in
shape. Its surface is ornamented with a small number (8-9) of
slightly marked, radiating ribs; the space between the ribs is almost
entirely smooth. Nothing can be seen on it besides some lines of
growth, which are hardly perceptible to the naked eye. The ears
are small, triangular in shape, and their surface is smooth.

The length of the only known specimen is 16 millimétres, and the
width 14 millimétres.

17. Pscrmn Astaticus, De Kon. Pl. IV. fig. 6.

This species, which is much larger than the following, is a little
wider than long, and slightly, but rather regularly convex. Its surface
is ornamented with twelve or fifteen radiating ribs, especially apparent
towards the middle of their length, but partially disappearing towards
the margin. In each furrow formed by these ribs there are from three
to five much thinner ribs, less regular than the principal ones, and
also more marked in the lower and central parts of the valves.
The lnes of growth are hardly visible even by the help of a hand-
magnifier. The ears are small and rectangular, and are covered with
small striz parallel with the cardinal edge. ‘The beak is tolerably
prominent. ‘This species possesses at first sight some analogy with
the P. plicatus, Phill.; but, upon careful examination, it is easily
- distinguishable by its small ribs, which are totally absent in the latter
species.

The length is 4 centimétres, and the width 44 centimetres.

8 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Noy. 5,

18. Prcren crespristr1a, De Kon. PI. IV. fig. 5.

The shape of this small Pecten is almost completely circular ; its
valves are slightly, but regularly convex. ‘he surface is covered with
a large number of small, radiating ribs, often bifurcated, of unequal
thickness, and irregularly distributed upon the whole surface of the
valves. The lines of growth are feebly expressed, and are only well
seen with the lens. The ears are small and rectangular.

The length of the only known specimen is 16 millimetres, its
breadth is 14 millimetres.

19. Sorenopsis ImpricaTA, De Kon. PI. IV. fig. 3.

This species is transverse, and almost three times as long as wide.
Its anterior side is very short, and its margin rather regularly semi-
circular; the posterior side is bounded by a curve, approximating to
an ellipse. The ventral edge is feebly sinuated. The beaks are very
small, and hardly project above the dorsal border. The surface is
smooth ; one may observe six or seven imbricated lamelle parallel to
the ventral edge; they have been formed by the successive growth
of the shell. The valves are depressed and very shallow.

The length of the largest of the two known specimens is 17 milli-
métres, and the width 44 millimétres. From the Productus-lime-
stone of Vurcha.

20. Dentatium Hercutevm, De Kon. PI. IV. figs. 10-12.

This species is remarkable on account of its great size and the
considerable thickness of its shell. It has the greatest analogy with
my D. ingens of the Carboniferous Limestone of Visé. Like that spe-
cies, its surface is covered with irregular strie of growth, and is
rendered rugose by their presence; these strie are a little oblique to
the axis, and show that one edge of the aperture of the shell must
have been slightly produced. They differ by the regular, conical
shape, and by the greater thickness of the shell of D. Herculeum, as
shown by the transverse sections represented in Pl. IV. figs. 10a
& 12a, and the longitudinal section, fig. 11. The seetion, fig. 12 a,
offers again another peculiarity, consisting in the presence of a very
prominent longitudinal fold, which transforms the interior of the
shell from a circular into a semicircular form. This shape is merely
accidental, and is exhibited only by a single specimen among the
seven submitted to my examination.

The largest of these specimens was 7 centimétres long, and 14 in
diameter on the side of the aperture; but it is probable that com-
plete specimens attained at least 15 centimétres in length.

21. BetieropHon pecrpiens, De Kon. PI. III. fig. 1.

This is one of the most remarkable of all the species with which I
am at present acquainted; it is a little longer than wide, and its
surface is almost smooth. The dorsal band produced by the buccal
sinus is very narrow, and very slightly apparent. Theribs of growth
are very wide, and it would have been difficult to distinguish them

1862. | DE KONINCK—INDIAN FOSSILS. 9

had not the long exposure to atmospheric agency slightly abraded the
surface of the specimen figured. By this deterioration the ribs have
been distinctly separated by very narrow and shallow furrows, which
one might imagine excavated by a graver, and of which the figure
indicates very well the shape and direction. They number sixteen
on each side, and are curved in the shape of a half-circle, in such a
manner that they join again by a very acute angle to the dorsal
furrow. One may conclude from this disposition that the buccal slit
must have been deep, and that the lower portion of the mouth has
been slightly scooped out by a very well marked sinus. There is no
umbilicus, and the shell is very thick. The height of the only known
specimen is 6 centimetres, its length 53. The ribs are generally
4 millimétres long.

22. BELLEROPHON ORIENTALIS, De Kon. PI. III. fig. 3.

This species is much smaller and rather less globular than the next.
It is higher than wide; its surface is ornamented with small, trans-
verse ribs of growth, produced by very fine and close striz, and form-
ing a tolerably acute angle with the dorsal band. This band termi-
nates in a very narrow and shallow furrow, by which B. orientalis is
easily distinguishable from B. tenuifascia, a species with a promi-
nent band, to which it has in other characters the greatest analogy.
The only specimen I have examined is 15 millimétres long by
12 millimétres wide.

23. BreLtERoPHon Jonestanvs, De Kon. PI. III. fig. 2.

This species is globular in form, and as high as wide. When
young, its surface 1s covered with small, transverse, imbricated ribs,
produced by the successive growth of the shell, as is easily observable
in the specimen represented by fig. 2 a, of which a portion of the last
coil of the spire and the callus of the aperture have been taken off.
The ribs, which on the last whorl are (in the adults) transformed
into large, but slightly marked wrinkles, form an open angle with the
dorsal keel, which projects very slightly, and is but 1 millimétre in
breadth. The several whorls completely overlap each other; the
umbilicus is nearly obsolete ; the lip (peristome) is tolerably thick near
the umbilicus, and slightly reflected. The buccal callosity is very much
extended, and covers over nearly the last whorl of the shell. The
test is thick, and the dorsal slit narrow and deep.

This species has a great analogy with B. hiulcus, from which it
differs by the much narrower form and the more considerable num-
ber of its ribs of growth, as well as by the slight width and the pro-
jection of its dorsal keel.

Of eight specimens examined, the largest are 5 centimetres
high, and as much wide; the opening of the mouth is about 2 centi-
metres high. From the coarse calcareous shale of the Productus-
limestone of Chederoo.

24. Macrocuertus pepiuis, De Kon. PI. VII. fig. 3.
Notwithstanding that I am acquainted with but an internal cast of

10 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 5,

this species, I have not feared to describe it, and to give to it a new
name. In fact, this cast, by its elongated shape, its spiral angle, and
the convexity of its whorls, differs from all its congeners at present
known to me. The only specimen that I have examined is com-
posed of four whorls, but it is probable that it originally possessed
eight or nine.

Its length is 6 centimétres. The last whorl must have occupied,
of itself, almost half the length of the shell. It is 33 centimétres
long, its diameter is 28 millimetres, and the spiral angle equals 39°.

25. MAcRocHEILUS AVELLANOIDES, De Kon. PI. III. fig. 4.

Shell subfusiform, with an acute spire composed of six or seven
inflated whorls, which are rather flattened on the sutural side. The
last whorl is very large, and occupies more than half the total length
of the shell. The aperture is elongately suboval, and possesses no
callosities. The surface is smooth ; the test tolerably thick, especially
towards the sutures. Its spiral angle is about 70°.

Of the two specimens of this species, the one possesses a length of
34 centimetres, and the other of 43 centimetres. The last coil of the
spire of the latter is 27 millimetres in diameter and 30 millimétres
in length.

This species approximates to M. Schlotheimi, d’Arch., but differs
from it by its spiral angle, by the length of its last whorl, and by the
absence of all ornament upon its surface.

26. Nerina ?, n.sp.?

Among the fossils confided to me by Dr. Fleming is the internal
east of a Gasteropod, which appears to possess the characters of
Nerinea, but which I am unable to determine ; none of the species
described by A. d’Orbigny, M. Eudes-Deslongchamps, and others
resemble it.

The Punjaub specimen possesses the last six whorls of the spire,
the total length being 8 centimetres; the diameter of the last coil is
41 centimétres. This last has a siphon parallel to its lower edge,
probably produced by a tooth of the mouth. It is besides adorned
with from six to seven tubercles. The axis of the columella is very
thick ; the angle produced by the spire is 25°.

It is probable that this species is not Carboniferous. - The greyish-
white colour of the limestone of which the cast is formed, and the
crystalline nature and whitish colour of the still-adhering fragments
of the shell, lead me to suppose that there is here an error to rectify,
to which I therefore call the attention of Indian paleontologists.

27. Ceratites Fremineranus, De Kon. Pl. VII. fig. 1.

This magnificent species, which I dedicate to the learned gentle-
man to whom we are indebted for its discovery, is the largest of all
those that are known up to the present time. Unfortunately, Dr.
Fleming found but a fragment, representing apparently the body-
chamber and the larger portion of the chamber behind it. 4

1862. ] DE KONINCK—INDIAN FOSSILS. 11

This shell must have been composed of spiral coils laterally com-
pressed, with a rounded back; the length of the coils equalled about
twice the height. They were feebly embracing, and their transverse
section represents tolerably well the half of an ellipse, of which the
great axis is equivalent to four times the length of the small one (see
Fin VI11, fig: 12).

The surface is covered with a great number of transverse, irregular
ribs, which are sometimes very thin, at others thicker ; they are pro-_
duced by the successive growth of the shell, and are crossed by
small spiral ribs, which are regular and parallel, numbering about
sixty on each side. The result of this disposition is, that the surface
appears as if enveloped by a network composed of meshes of equal
breadth, but of irregular length, depending on the size of the trans-
verse ribs which produce them. ‘The shape of the cells is most
peculiar: the upper lateral lobe is very deep and tolerably wide, and
occupies about one-fifth of the total height of the spiral coil; it is
remarkable from the great number of small denticulations with which
it is provided. The lower labial lobe is acutely funnel-shaped, and
does not present the smallest trace of denticulations. The three
saddles which connect these lobes are rounded, and present nothing
peculiar. The only species of Ceratites, hitherto known, which bears
any affinity with the one here described is the C. parvus, v. Buch.
The transverse ribs of this last are more numerous, and the longi-
tudinal ones are wanting. In addition to this, the conformation of
the chambers is entirely dissimilar in the two species.

The entire diameter of this species is 25 centimétres (10 inches) ;
the height of the mouth is 64 centimetres, and the width 4 centi-
métres. The last spiral coil covers the preceding one to the extent of
half a centimetre. This and the next species occur in a brownish-
yellow sandstone, while the greater number of the following Cera-
tites were found in a rock of a calcareous nature.

28. Ceratites Murcuisontanvus, De Kon. Pl. VIII. fig. 1.

Iam acquainted with but half the shell of this large and fine
species, upon which I have not even been able to discover any traces
of chambers; but these must have borne some analogy with those
of the preceding species. It is probable that the only fragment
known represents in itself the last air-chamber, and that it is from
this cause the septa are wanting. ‘This specimen bears evidence that
the coils of the spire were slightly compressed on their sides, that
their dorsal portions were rounded, that they were feebly embracing,
and that they produced a large umbilicus. The surface is covered
with rather large transverse ribs, which occupy only the sides of the
shell, and are in no way prolonged on the back, which, seen in pro-
file, forms a very regular curve. ‘The ribs are not of equal width ;
they bifurcate or trifurcate without any order, and are eighteen in
number on the specimen figured. As those near the mouth are smaller
than those which precede them, it is probable that the sides of the
first whorls of the spire were strongly ornamented, as may be often
remarked among the Ammonites.

12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

The fragment described possesses a diameter of 18 centimetres ;
the height of the last whorl is 64 centimétres, and its thickness 5
centimetres.

29. Crratrres Havertanus, De Kon. PI. III. fig. 5.

This species, of which I have unfortunately met with but a single
fragment among Dr. Fleming’s fossils, has much resemblance to the
Gonatites Haidingeri, v. Hauer, which may very possibly be like-
Wise a Ceratites, since in the latter the chambers are extremely
numerous, and composed of a great number of very narrow lobes and
saddles; those that occur towards the middle of the spiral coil are a
little wider than the others; they are five in number. Unfortu-
nately the specimen is so much defaced that it is impossible for me to
describe exactly the shape of the parts of its whorls, which have each
eight divisions at least. The back is keeled and tolerably sharp.
The thickness of the shell must have been about 24 centimétres.
The mouth, seen in front, must have had a subtriangular shape, as is
shown in fig. 5 a.

30. CERATITES PLANULATUS, De Kon. PI. Y. fig. 1.

This fine species, of which I have had the advantage of being able
to study one complete and adult example, is distinguished from all
those that follow by the angular shape of its dorsal portion. However,
this shape does not exist in the young specimens, and is only pro-
duced at a certain age of the animal (which is the case also with
some Nautili and Ammonites), as is demonstrated by figs. 1 ¢ and 1d.

The surface is almost smooth and shining, and is ornamented
with fine, radiating strie and undulations produced by the successive
growth of the shell. The umbilicus, in the shape of a very widened
funnel, allows the several coils of the spire of the shell, five or six in
number, to be easily perceived; they mutually overlap each other at
about three-fourths of their height. The number of the chambers is
from 30 to 32 for each coil of the spire; the last chamber is very
large, and occupies one-half of the shell. The lobes are shallow and
finely crenulated; the lower lateral lobe is connected with the umbi-
licus by means of a sinuous curve entirely free from denticulations ;
the dorsal lobe is divided in two by a small elevation, very angular
at the summit, and serving for the passage of the siphuncle. The
saddles are rounded, and of a moderate elevation. The largest dia-
meter of this species is 83 centimetres, that of the umbilicus 18
millimétres; the height of the mouth is 4 centimetres, its thickness
19 millimetres, and the width of the back at the extremity of the
mouth 4 millimétres. The shape of this species bears some resem-
blance to the C. semipartitus, Montf., but differs essentially from it
in the shape and number of its lobes.

31. Crratires Lyettranus, De Kon. PI. VI. fig. 1.

This species is one of the largest among those which have been
discovered by Dr. Fleming; its surface is entirely smooth, its back
is rounded, and the umbilicus large. The number of its chambers

1862. ] DE KONINCK—INDIAN FOSSILS. 13

must have been from eighteen to twenty. The lateral lobes are three
in number, and are similar in shape; their denticulations are rela-
tively small, and number five or six. The whorls of the spire slightly
overlap each other.

The total diameter must have been about 12 centimetres in the
specimen figured, that of the umbilicus 4 centimétres. The height
of the last whorl is 5 centimétres.

32. CERATITES LATIFIMBRIATUS, De Kon. PI. VII. fig. 2.

Shell discoidal, with a strongly rounded back, and remarkable
from the form of the denticulations of its lobes; these are generally
four in number; but in examining them with a lens one distin-
guishes on their edges other supplementary indentations, which
make each joint resemble a little tooth of Carcharias. The coils of
the spire overlap each other from about two-fifths of their height.
The surface is entirely smooth. Besides the dorsal lobe (of which I
have not been able to completely observe the shape, on account of
the bad state of preservation of this portion of the specimen), it pos-
sesses three other sufficiently deep lobes, all of about the same shape.
The corresponding saddles are rounded, and have their sides almost
parallel between the lobes. It is easily distinguishable from C. Zaw-
rencianus by the absence of the auxiliary lobes. The number of the
chambers must have been fifteen or sixteen for each whorl of the
spire. The diameter of the shell is from 9 to 10 centimétres, that of
the umbilicus is 24 centiméctres, and the greatest thickness of the
shell is 3 centimetres. From the Productus-limestone of Vurcha.

33. CERratites Bucnranus, De Kon. PI. VL. fig. 4.

This species is so nearly related to the succeeding one that I
should have willingly dispensed with it, had not its umbilicus
been proportionally much larger; the spiral whorls, also, overlap
each other only to the extent of about one-third, while in C. David-
sonianus they commence to overlap each other at three-fifths of their
height. Besides this, the surface is ornamented with a tolerably large
number of well-marked, radiating undulations, a character not seen
in that species. The shape of the chambers is a little different,
and the sinuosities of its lobes and saddles less deep than those
observed in C. Davidsonianus. The diameter of the largest of the
three specimens that have come under my notice is 53 centimetres,
that of the umbilicus is one-third as much. From the Productus-
limestone of Vurcha and Kaffir Kote.

34, CrratitEs Davrpsonzanus, De Kon. PI. VI. fig. 2.

This species has much affinity to the one following, but differs in
its size, as well as in the shape of its chambers. It is discoid, and
possesses but a small umbilicus. Its surface is smooth, and the
terminal chamber very large, occupying about one-half the last whorl
of the spire. Its lobes and saddles are analogous to those of C. Law-
rencianus, but the former are much less deep, and the saddles much

14 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 5,

more rounded than in that species ; and the part which is connected
with the umbilicus is composed of a larger number of dentations.

Of this species I have been able to examine one perfect specimen,
which is probably adult, and is but 6 centimetres in diameter. The
height of the mouth is about 3 centimetres, and the width 1 centi-
métre. The diameter of the umbilicus is also 1 centimétre. It forms
part of the seriesin the Museum of the Geological Society of London.
From the Productus-limestone of Vurcha.

35. Creratires Lawrencianus, De Kon. Pl. VI. fig. 3.

This fine species is remarkable on account of the form of the lobes
and saddles which bound the chambers. Its general shape is that of
a flattened disc whose margin is rounded. Its surface appears to
have been smooth, the test not having left any trace of strie or fur-
rows on the internal cast, which is all I have here to describe. The
spiral coils are strongly overlapping, and leave but a very small um-
bilicus. The dorsal lobe is very large, and divided into two by a
small median saddle ; it is much less deep than the lateral lobes, but
its width and indentations, which are five or six in number, strongly
resemble those of the last lobes ; it is connected with the upper lateral
lobe by a slightly elevated saddle, narrow and rather acute: the in-
ferior lateral saddle is, on the contrary, very high, but much more
wide at its base than the former, and but little elevated; it is con-
nected with the margin of the umbilicus by seven or eight indenta-
tions, which assume the character of auxiliary lobes.

Tam acquainted with no species with which this one is compa-
rable, unless it be the C. Davidsonianus, which differs from it in the
much more rounded shape of its saddles.

The approximate number of its chambers is about thirty ; the
total diameter is 10 centimétres, and that of the umbilicus 14 milli-
meétres: the height of the last whorl of the spire is 53 centimetres,
and its thickness about 3 centimétres; whilst the height of the pre-
ceding coil is but 28 millimétres, and its thickness 18 millimétres.
The distance which separates the back of the last coil but one of the
spire from that of the last is 34 centimetres.

36. Gonratrres ? GaNncETIcus, De Kon. PI. V. fig. 2

I have placed this species among the Goniatites for the sole reason
that I have been unable to discover any indentations on the edges of
the lobes or chambers. It is highly probable that the denticulations
have been destroyed by the atmospheric agencies to which the speci-
men had been exposed. This species is rather strongly compressed
and planorbiform ; its first spiral whorls are only half overlapped by
those that eueceed them. The umbilicus is wide, and its diameter is
equivalent to about one-third of the entire diameter of the shell ; its
back is very convex, and the surface appears to have been smooth.
The number of its chambers is from twenty to twenty-two; their
height is about twice their width: the dorsal lobe is divided into two
by a little prominent linguiform septum. The lateral lobes are nar-
rower than the saddles which produce them; both are rounded, and

1862. | DE KONINCK—-INDIAN FOSSILS. 15

in no way resemble those of Carboniferous Goniatites, which are
almost always angular.

The specimen figured is but 4 centimétres in diameter; the height of
the last spiral whorl is 16 millimetres, and the width 8 millimétres ;
the diameter of the umbilicus is 15 millimetres.

37. Navritvus Burtt, Galeotti. Pl. VIII. fig. 3. (Mém. couronnés
de l’Acad. de Bruxelles, t. xii. pl. 4. fig. 4, p. 140.)

After comparing this Nautilus with some specimens of the species
described by Galeotti, derived from the Eocene sands of the neigh-
bourhood of Brussels, I have not been able to find any distinguishing
character between them. It is therefore probable that the specimen
figured in this memoir has not been derived from the Carboniferous
system, but from some Nummulitic bed which occurs in the Punjaub.
This is also Dr. Fleming’s opinion, who did not find it im setu, but on
a heap of carboniferous stones destined for road-repairs *.

38. Navritus Fremreranvs, De Kon. Pl. VIII. fig. 2.

This species is remarkable on account of the lateral tubercles with
which the last whorl of its spire is furnished. If I may judge from
the dimensions of the single fragment which I have been able to
examine, its size must have been considerable. At first sight it
presents some resemblance to the NV. tuberculatus, Sow., but is easily
distinguishable by the shape of its tubercles and by the distance of
its chambers. In N. Flemingianus these tubercles are much elon-
gated, and placed on alternate chambers, while in the species de-
scribed by Sowerby the tubercles are more rounded at their base,
forming a kind of crown round the umbilicus ; they are besides more
prominent, and present nothing regular in their distribution with
reference to the chambers. They are very perceptible on the first
whorls of the spire of the latter, but are there scarcely apparent in
N. Flemingianus. The chambers of this species have their lateral and
dorsal margins feebly sinuous, and the fragment figured shows four
coils of the spire. By completing the last whorl, one is able to prove
that it must have been composed of about forty chambers, and that
its greatest diameter was about 19 centimetres ; viewed in front, the
last visible chamber presented an elevation of 6 centimétres, whilst
that of the one behind it was not more than 3 centimétres in
height ; their width is a little greater; their shape in the same
position is that of an oval, irregularly compressed on the two oppo-
site sides (see Pl. VIII. fig. 2a). The siphuncle is scarcely visible,
but appears to be rather large, and is situated towards the upper
third of the height. The coils of the spire do not overlap one
another. From the Productus-limestone of Vurcha.

39. ORTHOCERAS VESICULOsSUM, De Kon.
This species is very remarkable on account of the calcareous
* 'The following note was found attached to the specimen :—

“This fossil was found among the débris of Carboniferous Limestone. It pro-
bably, however, has weathered out of Nummulitic limestone.”

16 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

globules which its chambers contain ; these globules or concretions,
which appear to have been produced by small vesicles, are not very
regular either in shape or number ; their existence might have been
considered as accidental, if several specimens had not presented the
same character.

The shape of this Orthoceras is almost entirely cylindrical; its
length must therefore have been very considerable. The external
surface is completely smooth, whilst the interior of the air-chambers
is rough, and as if covered with shagreen. The chambers are regu-
lar, and the distance between the septa is equivalent to, or rather
more than, a fifth of the diameter of the shell. The siphuncle is
very large and central: I have not been able to assure myself
whether it is cylindrical or moniliform.

The principal fragment observed possesses a length of 7 centi-
metres, and is composed of five equidistant chambers. The diameter
of the shell is 5 centimetres, while that of the siphuncle is 13 centi-
metre. The test which forms the latter is about 2 millimetres thick.

40. OrrHocrRAS RACHIDIUM, De Kon.

The specimens representing this species are deprived of their shell.
The length must have been very great, the growth of the diameter
having been relatively feeble during the development of the animal.
The principal specimen, composed of eleven or twelve air-cells, of
the uniform length of 1 centimétre, measures 12 centimetres. Its
smallest diameter is 33 centimetres, and its largest 4 centimetres.
No ornament or sculpture can be seen on its surface. The siphuncle
is very large, and resembles that of the O. cochleatum, Schl., to
which this species is closely allied.

One of the specimens is accompanied by Productus semireticulatus,
Martin ; there can consequently exist no doubt as to its geological
age. From the Productus-limestone of Subbee.

41. Orrnoceras DEcrEscENs, De Kon. Pl. VIII. fig. 4.

Shell of a very elongated, conical shape. The internal cast alone
is known; it has the surface entirely smooth, the transverse section
perfectly circular, and the siphuncle central and rather narrow. The
diameter of the terminal chamber is 24 centimétres; that of the
sixth chamber is 2 centimétres. The entire length of the specimen
is 12 centimetres, of which the last chamber occupies eight. The
five known chambers are remarkable on account of a regular decrease
in their length, so that, whilst the sixth chamber is 12 millimétres
in length, the fifth is but 10, and the second not more than 5. It
is this conformation, which I have seen in no other species, that has
suggested the name by which I have designated the one here de-
scribed. From the Productus-limestone of Moosakhail. —

42, AcRoDUs, 0. sp.

This species is very closely allied to Acrodus laterals, Ag. Itis
smaller than the one next described, of a much more elliptical shape,
and less transverse at its basis. From the coarse limestone of Che-
deroo.

Cu
| ae

IL

tal
=<

1)

PAA BoE OS

P

ie
ve

1 a
Yi i)
sf X s

;

Se

‘e

by

yee,

: Os ed
. platy

ne

ee pea

a

SS Fa Viale ws 4 ee hee
COMER at Ga aie eS
Pl

o
Pe a

me tale

PUNJAU

LLeve
]

,

H.Wessain

Lith

Lieve.
2

H.Dessatn

ol. XIX.Pl. VI.

/

V
*¥

Lith

Cc

a

eal

(

Journ

juart

PUNJAUB

c—_-

REY

PUNJAU

4

Journ Geol. Soc

Soc. Vol. XIX. PL. V UL

7.

F

teres dl
NARs apm reayr

Lith: H.Dessain Liege.

itn: H.Dessain Lieoe.

PUNJAUB |POSsiz,s

r

hia
ary

*,
es
io

1862. | DE KONINCK—INDIAN FOSSILS. 17

43. Acropus Fiemrneranvs, De Kon. Pl. VIII. fig. 5.

Teeth of a subtriangular shape when seen in front, and sub-
ellipsoidal when seen from above. Enamel very shining, of a dark-
brown colour, occupying almost half the entire length of the tooth,
and producing on it a pointed eminence. The surface is furrowed
by small, longitudinal striz, which are gently bent towards the cul-
minating point of the tooth; they are strongly marked at the base,
and become almost completely obliterated on the crest of the enamel.
The basis is very much compressed, slightly arched in the centre, and
tolerably porous.

Two specimens of these teeth, one 15 millimétres wide by 8 long,
the other 7 millimétres wide, are in the collection of the Geological
Society.

This species has some affinities with the A. Gaillardoti, Ag. They
differ principally by the much more arched shape of the base in this
species. From the Productus-limestone of Vurcha.

44, Savricutuys ? Inpicus, De Kon. PI. VIII. figs. 6, 7.

The teeth which I attribute, with some doubt, to the genus Sau-
richthys (established by Agassiz), on account of their compressed
shape, are very small, very shining, and of a brownish colour. Of
the two specimens examined, one is 2, the other 6 millimétres in
length. This last is strongly striated at its basis, and resembles that
of S. Mougeoti, Ag., and is a little more compressed than the other,
of which the surface is entirely smooth. Both have the upper ex-
tremity very pointed, the sides sharp, and transverse section sub-
oval. From the Productus-limestone of Vurcha.

EXPLANATION OF PLATES I. ro VIII.

(The specimens are in Dr. Fleming’s collection, or in the Geological
Society’s Museum. )

Puate I.

Fig. 1. Fenestella ? Sykesii, De Kon., front view, natural size.
2. Phyllopora ? cribellum, De Kon., natural size.
3. Phyllopora ? Haimeana, De Kon., natural size.
4. Polypora fastuosa, De Kon., natural size.
4a. An enlarged portion of the same.
5. Retepora? lepida, De Kon., natural size.
da. An enlarged portion of the same.

Puate II.

Fig. 1. Alveolites septosa?, Flem., natural size.
la. An enlarged portion of the same.
2. Isastrea arachnoidea, De Kou., natural size.
2a. Two calyces of the same, three times the natural size.
3. Fenestella megastoma, De Kon. Front view, natural size.
4. Clisiophyllum Indicum, De Kon., natural size.
4a. A transverse section of the same.
5. Philocrinus cometa, De Kon., natural size.
VOI. EX ——P An ol. C

18

Fig.

Fig.

Fig.

Fig.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

Puate ITI.

1. Bellerophon decipiens, De Kon., natural size, seen from the side of the
back.

1 a. The same, seen in profile.

2. Bellerophon Jonesianus, De Kon., natural size, seen in profile.

2a. Another specimen, natural size, seen in front, and showing the ribs
with which the species was ornamented when young.

3. Bellerophon orientalis, De Kon., natural size, seen from the dorsal side.

4. Macrocheilus avellanoides, De Kon., natural size.

5. Ceratites Hauerianus, De Kon., natural size, seen in profile.

5a. The same, seen from the side of the mouth.

Puate IV.

1. Cidaris Forbesiana, De Kon., complete spine, natural size.

2. Fragment of a spine of the same species, showing a variety with well-
marked granules, natural size.

2a. Transverse section of the same.

3. Solenopsis imbricata, De Kon., natural size.

4. Pecten Flemingianus, De Kon., twice the natural size.

4a. Line indicating the natural size.

5. Pecten crebristria, De Kon., natural size.

5 a. The same enlarged, twice the natural size.

6. Pecten Asiaticus, De Kon., natural size.

7, 8, 9. Anomia Lawrenciana, Fleming.

7. Specimen of the natural size, seen in profile.

7 a. Another specimen, natural size; upper side.

7 6. The same, showing the lower valve.

8. The same, seen in profile.

9. Another specimen of the natural size, seen in profile.

10, 11, 12. Dentalium Herculeum, De Kon.

10. Specimen of the natural size.

10 a. Upper opening of the same.

11. Another specimen of the natural size, divided in two in the direction of
the length, so as to show the thickness of the shell and the shape of the
cavity.

12. Tita apeeiles natural size.

12a. Upper opening, furnished with a tooth or internal keel.

PuateE V.

1. Ceratites planulatus, De Kon., natural size, seen in profile.

1 a. The same, seen from the side of the mouth.

1d. Lobes of the same.

1c. Another young specimen, seen in front.

1d. The same, seen in profile.

le. Lobes of the same.

2. Goniatites? Gangeticus, De Kon., natural size, seen in profile.
2a. The same, seen in front.

2b. Lobes of the same.

Puate VI.

1. Ceratites Lyellianus, De Kon., natural size, seen in profile.

2. Ceratites Davidsonianus, De Kon., adult specimen of the natural size,
seen in profile.

2a. Lobes of the same.

3. Ceratites Lawrencianus, De Kon., natural size, seen in profile.

4. Ceratites Buchianus, De Kon., natural size, seen in profile.

4a. Lobes of the same.

1862. | HODGSON——ULVERSTON. 19

Puate VII.

Fig. 1. Ceratites Flemingianus, De Kon., half the natural size, seen in profile.

Fig.

la. Transverse section of the same, half the natural size.

2. Ceratites latifimbriatus, De Kon., natural size, seen in profile.
2a. Contour of the same, seen in front.

3. Macrocheilus depilis, De Kon., natural size, back view.

Prats VIII.

1. Ceratites Murchisonianus, De Kon., specimen seen in profile, half the
natural size.

1 a. Transverse section of the same, reduced.

2. Nautilus Flemingianus, De Kon., specimen seen in profile, half the
natural size.

2a. Transverse section of the first two coils of the spire, reduced, and
showing the place of the siphon.

3. Nautilus Burtini, Galeotti, half the natural size, seen in profile.

3a. Back view of the same.

3. Last septum of the same.

4. Orthoceras decrescens, De Kon., natural size, seen in profile.

4a. Transverse section of the same.

5. Acrodus Flemingianus, De Kon., natural size, seen in profile.

6. Saurichthys? Indicus, De Kon., three times the natural size, seen in
profile.

6 a. The same, front view.

6 4. The same, upper side. .

7@ peinichitys! Indicus, var., De Kon., three times the natural size, seen in
ront.

7 a. Transverse section of the same.

2. On a Depostr containing Diatomacrem, Leaves, &c., in the Lron-

orE Mines near Utverston. By Miss E. Hopeson.

[Communicated by the President. ]

(Abridged. )
CoNTENTS.
Introduction. Swallow-holes.
Tarns. a. Lindale Moor.
Cavernous Nature of the Ground. b. Poaka Beck.
Sections.
Diatomaceeé and Plants.

Introduction.—In the ‘ Quarterly Journal of the Geological Society,’
vol. xviii. p. 274, &c., there is a paper by John Bolton, Esq., “‘ Ona
Deposit with Insects, Leaves, d&c.,’’ met with in or near the Iron-ore
Mines of Lindale, in Low Furness, North Lancashire; which deposit,
for reasons stated in the paper, is presumed to be of great antiquity.

Before determining either the age of the deposit, or its origin, it
seems important that geologists should be made acquainted with some
circumstances connected with the district, which would rather induce
one to interpret it as being a cavern-deposit, carried down to these
depths by means of currents,—the currents passing through what
are called “Swallow-holes,”—the cavernous and otherwise open

c2

20 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

state of the ground being favourable to such an interpretation, and
the nature of the deposit itself likewise tending to strengthen that
belief.

The deposit when first brought up is soft, damp, clammy to the
touch, of a dark colour* and nauseous smell, and is capable of
being cut through with a knife. Even after remaining at the mouth
of the shaft of the Water-way (No. 11) four years, the part of it
partially covered with other material retained its soft, moist con-
dition. Kept dry for a time, it assumes a much lighter, greyish
appearance,

Tarns.—The Tarns, or small lakes, laid down on the Ordnance-
map are not wholly unworthy of notice. ‘ Standing Tarn,” a small
sheet of water, situated about a mile to the south-west of Lindale,
has no surface-inlet or -outlet; but it has a very open subterranean
outlet, which is stemmed by the farmers with straw and mud.

A Tarn about two miles south of Lindale, called ‘“ Longlands
Tarn,” has also a wide aperture of escape leading underground ;
chaff thrown in there has been detected in the Stainton-mines, three-
quarters of a mile distant. Such an experiment would prove that
there is an open passage throughout the distance, and this I believe
to be the general character of the ground; water seldom infiltrates,
but courses uninterruptedly on its way. Thus, water pumped into
a ‘“‘Swallow-hole”’ near the Stainton-mines flowed unfiltrated to
Gleaston-mill, a mile further south. Almost all the mines are
troubled with water—not merely top-water, but ‘ under-water,’
rushing along at great depths, over which the engines seem to
have little power.

Cavernous nature of the ground.—The facts above stated will be
no matter for surprise, when the cavernous state of the ground is
taken into consideration.

The caverns occur in the earth or Drift overlying the Mountain-
limestone +. On an accompanying Map (fig. 1), traced from the
Ordnance-sheets Nos. 11 and 16, the situations of the respective
caverns are attempted to be shown.

One marked about a quarter of a mile to the south-east of the
Lindale Railway-station was disclosed by the surface giving way
under the plough, and letting in the horses; this was about 12 feet
deep.

Another smaller cavern is situated close behind the station. This
one I have visited; like the last, it is close to the surface, and was
met with in making a new occupation-road. It was, when discovered,
two or three yards broad; it is now a good deal filled up, but close
to a fence under which it seems to pass, an opening is left. I col-
lected some of the material forming its roof and sides, specimens of
which are in the Society’s Museum.

* Some lately found and brought to me while yet moist could scarcely be
distinguished from bog-peat, and it burned like peat-fuel.

+ For calling my attention to these interesting caverns, and for the informa-
tion connected with them, I am chiefly indebted to Mr. Lawn, of Ulverston,
mining-agent of the Earl of Derby.

1862. | HODGSON—ULVERSTON. 21

Fig. 1.—Map of the Lindale District, near Ulverston.

WHITRICCS Z

{RON MINES
a
Ree Aa ay ee

i GX fs iN
Pa ED 2 het es rag | ae Ue

STANDING
TAA'N

a. Shafts. c. Swallow-holes. . e. Tarns.
b, Caverns. d, Springs.

22 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 5,

Northwards, and a little to the east, is a cavern in the turnpike-
road that leads to Ulverston.

At a short distance above Lindale Tarn, which is situated in the
centre of the village, is a remarkable little cavern, in a field com-
manding a view of the vale. This was formed during one night in
the spring of 1861,—an oval space 26 feet across and 58 feet long,
sinking from 1 to 2 feet. At the south side of this is a cavern open-
ing deep into the ground, apparently for a distance of three or four
yards. I believe it is gradually changing in character, and I have
no doubt the coming winter will alter it much. I send a specimen
of the interior roof. This cavern is nearer to some of the works than
those before mentioned; but it is not considered to be owing to any
workings whatever.

Still further north, upon Lindale Moor, a cavern about 10 yards
in diameter was disclosed, a few years since, by the falling-in of the
surface.

At the distance of a little less than half a mile towards the south-
west, cavernous ground is again met with on Whittriggs. In these
mines, in the year 1843, a very large cavern was discovered, 60
feet below the surface. In sinking the vertical shaft which led to
this discovery, a cavern of small dimensions was opened on one side
of the shaft; but lower down the miners discovered an immense,
dismal vault, 24 feet in depth. In this gloomy chamber a great
mass of rock could be seen resting, as it seemed, on a very slender
pedestal, and threatening every instant to fall down. This cavern,
like the rest, was not in rock, butin the same material as the one
behind the station.

Thus we have a line of cavernous ground proceeding up the
eastern side of the vale, and occurring again on the north-western ;
and there is reason to believe that the miners are acquainted with
many more.

That both kinds of caverns have been long known may be seen by
referring to one of our oldest local writers on the antiquities of Fur-
ness*, from whose statements it appears that the earth-caverns were
supposed to be caused by the sinking in of water. This idea seems
to prevail still amongst the miners, who call them ‘“‘ Water-washes.”

The numerous depressions and inequalities of the surface on the moor
called Carr Kettle, and other localities, would lead one to suspect some
such mining work of nature there. The supposed rock-chasm, after
having been slowly filled or choked by the falling matter, might at
length have formed in it a compact floor, which, receiving constant
additions from the falling roof, would gradually rise; and thus the
cavern of 60 feet depth below the surface might become in time
the cavern of 50 feet, then of 40, and ultimately merely a surface-
depression or deep basin like the cavern on Lindale Moor.

I have very recently received information, from one of the gentle-
men of the Dalton Mining Company, of another “ water-wash ” or
cavern, occurring in their mines near Standing Tarn. It is situated

* Antiquities of Furness, by Thomas West. New edition, by W. Close, 1805,
Supplement, p. 593.

1862. |] HODGSON—ULVERSTON. 23

rather more than a quarter of a mile south-west from that water,
at a depth of about 84 feet from the surface, in strong ‘ Pinel,”
but close to rock ; the pinel of the roof is mixed with large stones.
The cavern is about 9 feet in height, circular, and about 15 feet
in diameter. lJron-ore, apparently of some depth, is found upon
the floor. There is a small quantity of top-water in this cavern,
which drains off into the adjacent mine at the rate of about half-a-
bucket a day, and the pinel of the roof is loosening and falling.
A fissure in the limestone, 16 inches wide, occurs about forty
yards south of the Tarn, at a depth of 8 feet below the surface,
dipping to the east.

It may also be mentioned here, as corroborative of the opinion
given by Mr. Close, that, in a shaft sunk by my brother near to
Stainton, the miners, at the depth of 90 feet, met with a narrow
cavity in the pinel, about 18 inches wide; and, on following it
down, they found, as the cause, a rock-fissure directly under it, and
corresponding to it in width; clearly showing that the pinel had
fallen down the chasm, while the roof remained firm.

Referring back to the cavernous field above Lindale Tarn (at p. 22),
further indications of fissured rock have lately been noticed there.
Another depression, in a line with that of the cavern, may be seen
when viewed from the road below; and, again, the cutting of
a tramway in a parallel line behind this has disclosed what seems
to be a narrow rock-fissure, about 18 inches or 2 feet wide.

Swallow-holes.—I will now refer to what are locally called Water-
sinks or Swallow-holes. In a later work on Furness, by the Rev.
Francis Evans, ‘ Sinks,’ in which the water disappears, are noticed as
oceurring here, ‘‘ as in all limestone districts that abound with iron-
ore*.” I was led to understand these more fully by reading some
remarks on the subject by Sir Charles Lyell in his ‘ Principles of
Geology ’f.

Their position in the Lindale district was first shown to me by
Mr. Bolton, who pointed them out on the Ordnance-map, a short time
previous to the writing of his paper. I at once attached great im-
portance to these Swallow-holes, and, concluding that they might be
found to have connexion with the deposit, I have since endeavoured
to ascertain their accurate situation, antiquity, and nature.

a. Lindale Moor.—I will first notice those on Lindale Moor.
They are situated about a quarter of a mile from the Lindale-moor
Cavern, and a little more to the north.

By the help of an aged miner I have succeeded in noting down
the true natural Swallow-holes,—not as they might appear in 1850,
the date of the Ordnance-map, but as they existed fifty years ago.
A copy of this has been transferred to fig. 1. Some which appear
on the Ordnance-map are omitted, on account of their being only
“< open-top workings,” as they are called, not natural Swallow-
holes.

* Furness and Furness Abbey : or, A Companion through the Lancashire part
of the Lake District. By Francis Evans, 1842, p. 19.
t Principles of Geology, vol. iii. fifth edition, ch. xiv. p. 204.

24 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

The Swallow-holes on Lindale Moor seem to be fissures in the
limestone, which probably comes nearer to the surface here. These
fissures continue open, it is believed, to a considerable depth.

There are numerous springs above the locality of the Swallow-
holes; in dry weather some of them fail, and none remain but
those noted on the sheet ; but in January a field on the side of Carr
Kettle was crossed by a line of numerous small springs. These
unite, and join the larger streams, and the whole are then preci-
pitated down the large Swallow-hole, which may be called “‘ Swal-
low-hole No. 1, Lindale Moor.” Some years since, the earth around
this fell inwards, carrying with it parts of a hedge-row (which it
will be seen on the Ordnance-map is made to cross it), leaving a large,
deep depression, all the material disappearing through the chasm.
The chasm remained open after this for about a year, when it was
gradually choked up, so as to form a deep clear pool in the centre
of the depression. There is little doubt that this remarkable Swal-
low-hole has been receiving the united waters of the several springs
for more than a hundred years.

About 220 yards to the north-west of this there is another
Swallow-hole, and, according to the miner, one equally old. This
also receives a small stream, which is never cut off by dry seasons ;
and it is supposed the two engulfed streams unite, as a continuation
of this chasm, much enlarged, was met with a little further to the
east, proceeding, as it seemed, in the direction of Swallow-hole No. 1,
Lindale Moor.

The other Swallow-holes in this vicinity are simply dry, funnel-
shaped depressions.

Further west, in the ‘ Cross-gates” Iron-mines, which are
situated on the banks of the Poaka Beck, ‘‘ water-sinks ”’ or fissures,
down which water rushes, are frequent. They are known also at
Elliscales, a place still further west, and again at Stainton, to the
south of Lindale. Much open ground, it is believed, of the fore-
going description also lies between Lindale and Ulverston.

b. Poaka Beck.—I now come to a ‘‘ Swallow-hole” which I deem
to have the most connexion with the deposit. This is situated in
the high end of Inman Gill, and until the year 1842 had been re-
ceiving, for an unknown period of time, the whole of the water of
the Poaka Beck*. In very wet seasons, or in thunder-storms, when
the chasm, large as it was, proved too small, the overflowing water
would pass down the Gill on the surface; otherwise the Beck-course
from this spot was usually almost dry. There was said to be an
efflux of part of it about three-quarters of a mile further south,
which, recovering the course from the Gill, flowed onwards along
the south of Dalton. I believe, however, there is no question but
that much of it was lost; and, as it was supposed to find its way
into the neighbouring mines, the course of the stream was altered a
little in the above year, with a view of keeping it on the surface.
I have lately visited this locality. The gulf, for such it appeared

* It has been ascertained that the water entered the ground at this spot in the
year 1802, sixty years ago.

1862. | HODGSON—ULVERSTON. 25

to be*, is close to the steep side of the Gill, and is now strongly
fenced off. The Gill here may be from 14 to 16 feet deep; it is
thickly wooded.

A division of the stream has lately found another entrance about
a quarter of a mile higher up.. Here it filters through, leaving its
sediment on the surface, and forming mud-bankst, through which
the water noiselessly escapes in numerous little eddies. As in the
former instance, the engulfed stream is believed to take an easterly
direction. The Poaka Beck rises by several deep springs on Mean
Moor, about two miles to the north of Lindale Moor, at an elevation
of nearly 1000 feet. Taking rather a south-westerly course, it
runs nearly parallel with the vale of Lindale, separated from it by a
line of hills, but at no point of divergence exceeding the distance of
one mile,

The superior claim of this stream, in regard to the deposit, over
the waters before noticed is, I think, obvious. Its longer course, of
nearly four miles from the rise to the fall, through a tract of varied
country, its thickly wooded banks and gills, its far greater body of
water (which in heavy rains is said to be almost white with mud
and clay from the higher grounds), and especially the remarkable
coincidence of its having been stopped from entering the ground for
the last twenty years, thus leaving time for the deposit to become
drained, are facts which seem to point to the Poaka Beck as the
direct cause of the deposit.

Wherever water is precipitated into the earth through a chasm, it
must take along with it an amount of deposit proportionate to its
volume; and, supposing that such engulfed water may afterwards
escape from the fractured rocks into the adjacent strata, thither it
will carry its mud, Wc., especially if in the adjacent strata it finda
vacuity to receive it.

Sir Charles Lyell, in treating of the phenomena of springs, gives
some extracts from M. Héricart de Thury, and the ‘ Bulletin de la
Société Géologique de France,’ which bear upon this subject.

Although the rocks in Inman Gill are now near the surface, and
the Swallow-hole has been an open rock-chasm for the last sixty
years, the bed of the stream at one time would be higher, and the
gill not so deep. ‘Therefore, however open or cavernous the subter-
ranean region between the Beck and the present seat of the deposit
might be, it is probable that the first influx was by infiltration, as
at present. One is led to this conclusion by the nature of the bluish
clay found underneath the vegetable deposit; this clay, from the
scarceness of any vegetable forms, even in portions lying in close
proximity to the vegetable deposit, may be supposed to have been
collected by filtrated waters on their passage through the various
materials of that region, and so left on the floors of the cavities, indi-

* From the point where I stood; the stream passing between prevented my
getting close to it.

t See Specimen, in the collection of the Society, with probably an alder-leaf
imbedded.

t Principles of Geology, fifth edition, vol. i. p. 306.

26 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

cated by the present position
of the deposit, any disin-
tegrated heavy substances
lying lowest.

In process of time, the
obstruction at the entrance
being removed, the water
would enter in greater vo-
lume, and, carrying in mud
and vegetable matter, would
then, no doubt, pass through
filtrating media to several
points of efflux—namely,
springs, which in former
years were numerous in the
lower part of the vale, and
which are now all cut off.

Sections. —As the position
of the materials in Mr. Bol-
ton’s Section, fig. 1, would
negative the possibility of a
cavern there, inasmuch as
there can be no caverns or
cavities in gravel, Iam com-
pelled to question its ac-
curacy.

Besides the information,
in his own hand-writing,
obtained from the principal
man engaged in sinking the
shaft, the one particular,
that gravel and sand are at
the top, has been corrobo-
rated by three other miners.
The first attempt to sink in
this gravel and sand was, at
the depth of 5 feet, obliged
to be abandoned, it was so
full of water; and the dis-
appointment attending that
loss of time and labour is
well remembered.

In fig. 1 of Mr. Bolton’s
paper, two beds of “ Black
Muck,” with a thin vegeta-
ble clay-bed betwixt them,
are made to he next upon
the limestone in the drift;
whereas I have it on the
authority of four of the

N.W.

No. 12.

Nh yea OB
PI Va BS 28 2
CO
ROG

s. Iron-ore and limestone.

Limestone.

“SPN Wass
- Ye

n. Limestone.

m. Bluish clay.

not reaching the floor of the drift.
lay.

1. Peaty c

c. Peaty clay,

k, Peaty deposit.

Former spring.

j. Pinel.

o
's
fo)
~~
, 2
rs)
£
i

Fig. 2.—Section of a part of the Water-way from Lindale Oote Mines to Urswick Tarn. (Length about 100 fathoms.)

8.E.
2. Gravel or sand.

1862. ] HODGSON—ULVERSTON. 27

miners, one of them being the principal person engaged, that “‘ Pinel ”’
came next to the limestone in the drift.

It would seem from fig. 2 that the deposit in the vertical shaft
(or rather the cavity in it) and that in the drift are not connected,
unless it be by a mere channel of communication, and even that must
remain only a matter of conjecture. The material called “ Pinel,’ I
am told, does not form regular beds.

The absence of bluish clay in the drift (see fig. 2) would lead to
the belief that the first waters had not penetrated this cavity.

So far as I can learn, the material termed ‘‘ Black Muck” was not
present either in the shaft or drift *.

The accompanying section (fig. 2) of the last three shafts of the
Water-way will, I hope, throw much light upon the ground in ques-
tion. It has been drawn from information obtained, in writing, from
two of the chief men employed in the work, neither of whom have
been informed of my views on the subject.

It seems to me that there is a steep precipice (or escarpment) in-
dicated by the abrupt termination of the rock in the Water-way
south of the No. 11 shaft, and that, from this point to below No. 10,
there may have been disturbance and continued change.

Referring to the section of the shaft, fig. 2 of Mr. Bolton’s paper

* The following description of the material called “‘ Black Muck” has been
obligingly given to me by Mr. Cameron, F.C.S. :—

*«* Black Muck’ is a dark-brown substance found in the vicinity of hzmatite-
deposits, and is a very good indication of the neighbourhood of the oxides of iron
and manganese. It is never found of a uniform composition, but consists of
varying proportions of siliceous and aluminous materials, and of the oxide of
iron (hematite) and peroxide of manganese. The hematite iron-ores con-
tain generally a certain proportion of the peroxide of manganese, sometimes
titanic acid, and various other substances. When the hzematite-ores are found
in irregular pockets, the ‘Black Muck’ is very often found surrounding the
ore entirely, like an outward shel!, which peels off from the surface of the iron-
ore, leaving it perfectly clean and glossy. When the ores are found in regular
strata, the ‘Black Muck’ seems to assume a regular form also; for it is then
almost always found overlying the vein of ore, running in the same direction,
and taking the same dip with varying thickness. Sometimes it is found under
the ore-deposit ; and is always a certain indication, when found, of the proximity
of the ores of iron and manganese. This substance, ‘ Black Muck,’ is only found
in connexion with the hzematite-ores of iron ; and its general constituents may
be inferred from the composition of the following examples :—

‘Biack Muck.’

Nook
Oxide of iron (with a little alumina) ..................... 67:00
eraxage Of maneanese oc yc5 aii) web bgees (A) aden seine 5:00
Sad ei AEN cect cr Specs SE ay ctte wha svaruowniees cysen sie 27°50
99°50

No. 2
ase Ot MTOW-ANG ALANIS ooo ie fe yaox bs oda core meee eened: bs 28:00
TPORORIGG OL WAR GAGCRE oc... y ea cc econ ns seep uses cing sansa n ia 17:86
RR MICREMINEEISE earls ee Soliant. come ekesecesce sense. 53°79
99°61

“ Other samples differ a little in the percentage of their constituents, but the
above may be considered a type of the general composition of ‘ Black Muck.’”’

28 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

(p. 276), specimens of the “ yellowish sandy material,” marked d,
lying next upon the vegetable deposit obtained from that shaft,
accompany this paper. (See specimen marked ‘“ Next upon the
deposit, Dalton Road Pit, No. 1.”) It seems sufficiently compact
to form a cavity. (See also other specimens from neighbouring pits.)

In the end of this drift, it appears that this yellowish sandy ma-
terial was never reached. The last man in did not cut through the
vegetable deposit. He informs me that, before abandoning the drift,
they worked directly upwards a short distance, in the hope of find-
ing ore, until the lights became extinguished by bad air, and a great
accumulation of wood was the last material found *.

In the ground-plan of this pit (fig. 3), kindly furnished by Edward
Wadham, Esq., the position of the iron-ore alluded toin Mr. Bolton’s
paper (p. 277) likewise indicates a cavern in the pinel, filled in at
some time by the mineral.

Fig. 3.—Plan of Dalton Road Pit (1862).

KE é,
—SSS SLA
Si j on
rR é . S
a i Ys rom
> wX L/S SKK

Sea

Pinel in the face of the
workings,

Inferior ore ..... oes

Blue clay and sand. .

Peaty shale ..... EZ

The adit containing the peaty or ‘‘ woody ” deposit lies in a north-
easterly direction—not exactly north, as represented in Mr. Bolton’s
section. Mr. Wadham remarks, ‘“‘'The plan now sent is chiefly from
my own recollection, the proper plan having been neglected when it
should have been made; it is, however, correct so far as the differ-
ent substances are concerned, for I have a very vivid recollection of
the whole working when it was in progress. Your view of the case,
as to its being a cavernous deposit, is, in my opinion, perfectly cor-
rect; in fact I have not a doubt upon the subject. The iron-ore,
too, as shown upon the plan (fig. 3), was deposited in the same way,

* On a piece of the deposit-wood in my possession, after removing the blue
paren Dr. Walker-Arnott discovered what he considered to be the mark of a
atchet.

1862. | HODGSON—ULVERSTON. 29

as I can prove; for in workings which have been abandoned, the
small particles of ore, which exist throughout the whole of the district,
have, by the action of the water, been washed through the cavities
in the limestone, and been deposited in quantities sufficiently large
to be worked.”’

Diatomacece and Plants.—At the risk of some recapitulation, I
must not omit acknowledging that the idea of the clay having been
very lately deposited did not entirely originate with myself. The
opinion of one or two eminent microscopists, that the species of
Diatomacee might confidently be expected to occur in its neighbour-
hood in a living state, served to suggest the possibility of its having
been in some way conveyed below ground; whilst the remarks of
equally eminent botanists, who detected for me the presence of
rushes and other familiar water-side plants, further tended to
strengthen the idea, and to impose the necessity of discovering its
impracticability, before yielding to the deposit that antiquity which
its position would appear to claim for it.

After ascertaining with accuracy the species of Diatomacee con-
tained in the deposit, and noting to what conditions of growth they
might be referred, it was found that not only did they belong to a
peaty and subalpine district, but also to running streams (the
peculiar habitat, if I do not mistake, of the species of freshwater
sponge found in the deposit); all clearly indicating the hills and
moors north of Lindale, and the streams and peat-bogs which occur
there, as their source; and thus, without any previous knowledge of
the district, its interesting features, as I have detailed them, became
successively disclosed, and seemed to invite close and persevering
investigation.

All the waters on Lindale Moor that could find access to the
Swallow-holes were examined, and also the dry soils in the vicinity.
All yielded Diatoms, including a few of the deposit-species, just
sufficient perhaps to prove the correctness of altitude, but failing in
some, from the absence of peaty or boggy ground; a result at once
acting as an unerring guide to the district further west, towards the
channel of the Poaka Beck, where the interesting facts connected
with that stream soon after developed themselves, and tended indu-
bitably to confirm, in all points, the preconceived idea.

Much of the arable and pasture land on the sides of the Beck, near
Stewnor Park, was, thirty or forty years back, nothing but peat-bog.

With a view of obtaining the Diatomacee which might have lived
upon the surface at that time, samples of bog were taken up by means
of aniron rod from the depths of 2, 4, and 5 feet, on different parts
near the Beck-course.

The following tabular list of the Diatoms found in the deposit will
at one view show its character, and also with what success the repre-
sentatives of the Diatoms have been searched for in the Poaka Beck.
Allowing for the lapse of years, and the great changes that have been
effected in what may be called the principal Diatom-ground on the
course, the few species yet undiscovered ought not to negative the
belief that the deposit has been supplied from thence; for there can be

30 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

little doubt that the banks of the stream about Stewnor at one time
presented most favourable conditions for the growth of the Diato-
Macece.

At the same time the Diatomacee are not abundant in the deposit.
There is a great preponderance of vegetable and earthy matter,
which renders it troublesome and difficult to prepare for the micro-
scope. It is very likely that many of the Diatoms were lost on the
passage. Their scarcity and broken state would indicate their having
been carried a great distance by a current.

Dratomacecee of Inndale Cote Deposit.
List of Species. Localities where they are found living. | Other deposits in which they occur.

Epithemia Hyndmannii ...J;Pond at Shooting-lodge, Glen|Lough Mourne. Cantyre peat.
Tilt, Loch Leven.

—— turgida...............6.. Poaka Beck. Subalpine streams,/Lough Mourne. Cantyre peat.
Kirby, Furness, Lancashire.
granulata ..........5. Poaka Becks io.5: soc csomunt Sepa anes Lough Mourne.
—w— Zebra, vars. ......... Poaka Beck. Near Ulverston.
——— APOE 2.600.001). ec cune Poaka Beck.
—— ocellata .........u5. Poaka Beck crs ta2 sce. Cantyre peat.
— longicornis.
SOLER cckcndlsnwng tewamer hag. estae as Seabee eink ety. weer eee ee Lough Mourne. Cantyre peat.
SIDS, © cee stes cent Poaka Beck. Near Ulverston ...|Lough Mourne. Peterhead.
VEDUICOSA, <2 spose sc Ponka BeGke.. sactndsonn sp ce Peterhead.
PRODOSEICEH “5 Se Taeraltec tech ote ceamieanet dec enacine Actas ae Raasay earth.
Cymbella Ehrenbergii ...... Poaka Beck. Tarn near Ulverston|/Lough Mourne. Premnay peat.
maculata .........ss0c0 Poaka Beck. River Frome, Dorset|Cantyre peat. Peterhead.
—— Helvetica ............ Poaka Beck. Subalpine bogs, U1-|Peterhead.
verston.
Cocconeis Placentula ...... Poaka Beck. Frequent in streams|Lough Mourne. Peterhead.

about Ulverston.
Cyclotella minutula, Kiitz.|Peat-trenches. Ulverston. Carr
Kettle Moor.

—— operculata ............ Poaka Beck. Subalpine bogs, Ul-|Cantyre peat.
verston.

Campylodiscus costatus ...|/Poaka Beck. Rivers and springs Lough Mourne. Peterhead, &c.

Cymatopleura elliptica...... Rivers, frequent. Near Ulverston. ;

Nitzschia amphioxys ...... Poaka Beck, Rivers, common.

Navicula elliptica, Kitz. .../Poaka Beck. Subalpine bogs, Ul-/Lough Mourne. Peterhead.
verston.

—— levissima.............., Poaka Beck. Peat-trenches, U1-
verston.

—— gibberula............... Poaka Beck. Subalpine bogs, Ul-/Lough Mourne. Dolgellyearth.
verston.

SCiiaatyaccesseth eras Poaka Beck.
varians(Pinn.?), Greg.

Pinnularia major ............ Poaka Beck. Subalpine bogs, Ul-/Cantyre peat. Dolgelly earth,
verston. &e.

—— -VITIGIS 2.654.500 8 Poaka Beck. Subalpine bogs, Ul-|Cantyre peat. Dolgelly earth,
verston. &e.

—— oblonga ............... Poaka Beck. Subalpine bogs, Ul1-|Peterhead.
verston.

Stauroneis Phoenicenteron |Poaka Beck. Subalpine bogs, Ul-|Cantyre peat. Lough Mourne,
verston. Peterhead.

Pleurosigma attenuatum ...{Common in streams ............... Lough Mourne. Peterhead.

1862. ] _ HODGSON—ULVERSTON. 31

List of Species. Localities where they are found living. | Other deposits in which they occur.
Synedra radians ............ Poaka Beck. Near Ulverston, in}/Lough Mourne. Peterhead.
springs.
Cocconema lanceolatum ...|Poaka Beck. Common in streams,/Lough Mourne. Cantyre peat.

Ulverston. Peterhead.
cymbiforme ............ Leola )2c Se ae ee ae Lough Mourne. Peterhead.
Gomphonema acuminatum|Poaka Beck. Subalpine bogs, Ul-|Lough Mourne. Peterhead.
verston.
Mab eee. OMA MISCO. . 5. ctkycacsecedicvetitess Lough Mourne. Peterhead.
dichotomum ......... Poaka Beck. Levers Water, “ Old|Premnay peat.
Man” Mountain, Coniston.
= WIEMEREAM 65... 5..++ Poaka Beck.
Himantidium bidens ...... Poaka Beck. Hills, Ulverston.|Dolgelly earth. Mull.
Levers Water, “ Old Man”
Mountain.
—— pectinale ............... Poaka Beck. Levers Water, ‘‘ Old/Dolgelly earth. Mull.

Man” Mountain.
Odontidium Harrisonii 8...|River Thames.

Ci) fear Wiyorstom |... sqeucsecccsnast Lough Mourne. Peterhead.
Denticula sinuata.
Tetracyclus lacustris ..... UNIV/GiN Ss] U2) an Maps lee Aan ones Dolgelly earth.
emarginatus............ Rivers, “ mountain-streams, and
cascades.”
‘Fabellaria flocculosa......... Poaka Beck. Road-sides north o
Lindale Moor.
Mastogloia Grevillii......... Mossy springs, Ulverston.

Taking for a moment Mr. Bolton’s view of the deposit, a ques-
tion would arise respecting the ‘“ Leaves of Beech” said to have
been discovered in it.

Now there is no record, I believe, of the Fagus sylvatica occurring
truly wild so far north. Therefore, if correctly identified, the spe-
cimens would seem to have belonged to a cultivated tree; otherwise,
we have yet to learn why the beech has, since that period, become
extinct as a native.

Returning to my own views, [ cannot say that there are no beech-
trees all along the banks of the Poaka Beck ; none were observed ; the
alder, oak, ash, maple, hazel, thorn, &c. occur—the first, perhaps,
predominating.

Great quantities of very fine mosses grow in and about all the
springs; we find their débris in all the diatomaceous gatherings. I
also found, by careful washing, fragments of moss still adhering to a
pebble from the deposit.

Rushes grow in great abundance; also ferns, especially the Hard
Fern (Blechnum boreale) and the Common Bracken (Pteris aquilina).
Spores of the latter have been detected in the deposit, with a frag-
ment of a frond of the same.

32 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 5,

3. On the Gzotoey of a part of the Masutrpatam District.
By Captain F, Arpruearn, Madras Army.

[Communicated by the President. ]
(Abridged.)

Tue country west of the Palair River, and north of the Kistnah
River, is covered with a thinly stratified limestone (E) of a dark blue
or black colour, which is about 150 feet thick, and alternates some-
times with dark purple slates (A), sometimes with a lighter-coloured
speckled slate, and occasionally with some cubical pieces of clay iron-
stone. The extent of this district is 24 square miles*. The lime-
stone here has a strike due north, and a dip about 19° east: this
description mainly applies to all the limestone west of the Palair
River. The slates are considered old, and have attracted much
attention at Madras. No quarries have been opened in these lime-
stone-fields ; but the stone is burnt for lime by the natives, who use
the slates extensively for the floors of their houses and verandahs.
The slabs are usually about 6 feet long, 53 feet wide, and from 2 to
8 inches thick.

The dark-coloured limestone contains casts of shells, and rings
when struck by a hammer. A similar limestone in appearance at
Kurnool, Province of Ballaghaut, on the Toombuddra River, 250
miles N.W. of Madras, contains large quantities of lead; and in
every ton of lead there are 400 oz. of pure silver ; at least, a speci-
men analysed showed this per-centage.

The limestones on the east side of the Palair differ much in colour,
appearance, and position from those on the west side, indicating
great disturbance of strata; they are principally of a pale yellow,
salmon, or red colour, sometimes brown, and occasionally black or
blue; they are very thinly stratified, and feather out. The general
strike of the yellow limestone is 70° N.E.; the dip varies from 11°
to 80° 8. The strike of the dark blue or black limestone here is
K., and the dip N.

The black limestone alternates with red schist, which is found on
undulating hills, which are frequently covered by rounded, quartzose
pebbles, and occasionally by small masses of clay-ironstone. Each
red-schist hill seems an independent basin, as the strata on the top
are vertical, and those on the lower portions of the hill dip from
20° to 40° towards the centre. There is an evident intrusion of the
same igneous rock as that which extends from the banks of the
Kistnah for almost two and a half miles in a north-easterly direc-
tion. This intrusion appears to divide the red-schist area into two
parts; and the red schist is finally overlain by a long ridge of varie-
gated schist, which extends from the Kistnah banks, in a due
northerly direction, for five miles. This schist attains an elevation
of 400 feet above the river-bed, being most probably the last deposit ;
it has a uniform N.E. strike, and the dip varies from 15° to 50°.

* A sketch-map and several sections illustrating this paper are deposited in the
Society’s library.

1862. ] APPLEGATH——MASULIPATAM,

33

There is another remarkable feature in this locality,—-several oliye-

coloured slate hills, with nearly
horizontal strata. The variegated
schist and olive slates appear to lie
unconformably upon a kind of flag-
stone ; the latter rests on a hard,
quartzose sandstone (O); and the
base-rock is massive gneiss. The
last-named rock is joined at the
Fort of Juggiah Pettah by the
limestone already described, the
variegated schist extending as a
ridge down the centre, and attain-
ing an elevation of 400 feet in a
conical hill called Noonacondah, or
Oily Hill, which has been scarped
by the river, and where a few
traces of fossils have been found.

I must not omit to mention
that in the bed of the Kistnah,
accompanying the schist C, is a
large mass of rounded, water-worn
pebbles (a specimen of a reddish
one is sent, D). They vary in size
from 1 inch to 1 foot in diameter.
They are principally of a pale-grey
colour, weathering to brownish
grey, and are composed of a very
fine sandstone; their internal
structure is perfectly crystalline,
corresponding to that of the rock
due north, at the Fort of Juggiah
Pettah, where the sandstone as-
sumes a tessellated form, and dips
9° §., strike 70° N.E.

On the eastern side of these
fields the same description of sand-
stone 1s met with, but more mass-
ive and coarser, more like a grit,
and dipping to the W., strike 65°
N.E. It has a uniform strike
along the ridge for about four
miles, and an olive shale or slate is
always found close adjoining.

An attempt was made some
years ago to sink No. | shaft for
coal through the red schist in the
southern part of these fields. The
red colour appears to be super-
ficial; for at a depth of 10 or 15

VOL, XIX,—PART I,

=

Section from Vadadry, eastwards (about two miles),

Kistnah River.

Olive-brown schist.
O. Coarse sandstone.

wx. Gneiss.

ING

M (?). Flagstone.

Ochre
L. Ironstone.
(The capital letters correspond with those on the specimens.)

K.

Hf. Pink and variegated schist.
I. Arenaceous limestone.

G. Red schist.

C. Dark-coloured sehist.
D. Quartzose pebble.
E. Black limestone

a, Grey micaceous shale,

34 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 5,

feet it changes from red to greenish grey, blue, and sometimes black.
In the bed of a natural ravine I commenced a shaft in the blue
schist, which, in descending, was found to be more thinly laminated
and of a greyer colour.

I also commenced shaft No. 2 on the northern boundary of this
red schist, and, at a depth of 80 feet, a pale-brown sandstone was
met with. However, no blue or grey schist was seen in this shaft ;
but the variegated schist was found immediately beneath the red
surface, and continued for about 80 feet. This shaft was evidently
sunk on the outer edge of the red schist. The pale-coloured, brown
sandstone resembled that which I found in the Wells, but, not being
provided with a pump of any sort, the water overpowered my
attempts to pierce it.

The red schist often assumes a hard, fissile, unevenly stratified
character, and appears occasionally to be traversed by veins of
quartz, and probably is quite of a different age from the pink schist
(H), which is much softer, and has invariably a very thin foliation ;
with the latter is also associated a cream-coloured arenaceous schist.

The schists are situated on a ridge of hills varying from 100 to
400 feet in height. Excavations, which can scarcely be called shafts,
both horizontal and vertical, have been commenced; and the notes
taken on the spot are herewith recorded. In gallery No.3 (hori-
zontal), white and reddish-brown schists were found. In sinking
No. 4 shaft, commenced at the bottom of a ravine, about 200 feet
below the top of the hill, thinly laminated, pinkish-coloured schist,
indurated clay, 24 feet thick, and, at the bottom, finely laminated
schist were found.

No. 5 shaft was sunk at right angles to the dip, through fine-
erained, white, thick schist.

In shaft No. 6 were seen speckled white, brown, and yellow
schists, and, beneath them, hard brown schist.

It is perhaps essential that I should attempt to describe the
difference of the immediately underlying rock occasionally found
under these pink and cream-coloured schists. Itisa hard, arenaceous
limestone (1), which is accompanied with a soft, dark, purple-coloured
substance (ochre) (K), and iron-sandstone (L), in rectangular pieces,
very abundant; in fact, the whole ground in this locality for a
considerable distance is coloured brown. The ironstones run in
bands, varying from 1 to 3 inches in thickness, and have a geodic
structure. In consequence of the great labour and expense required,
I have not sunk any shaft in this rock, but, at the depth of 5 feet,
layers of white sand and blackish powder were found intermixed
with it.

There is also another point of interest (a true limestone-basin) in
this locality. On the north, south, and west sides there is a dark-
coloured limestone, dipping towards a common centre, at angles
varying from 5° to 52°; and on the east side there is a thicker lime-
stone, more of the dolomitic kind, which dips 14° west, and strikes
north. It contains numerous large, circular holes, about 8 inches in
diameter, apparently the casts of some fossil, as the rock is not in a

1862. ] SAWKINS—GRANITE, JAMAICA. 35

position to have been acted upon by water. The pink and cream-
coloured schists are situated within the limestone-basin, attaining an
elevation of 250 feet, the limestone forming a thin belt at the foot of
the hill, on the north, south, and west sides. That on the east side
occupies a higher position, and at the north-east corner of the basin
graduates in step-like terraces, till it joins, or nearly joins, the lime-
stone at the foot on the south side. The area of this limestone-basin
is not less than 40,000 square yards ; but outside it three other rocks
are seen, the highest being a silver-grey, micaceous schist; secondly,
a sandy, brown-coloured schist ; and, thirdly, a hard, massive, blue
schist, with innumerable circular impressions.

4. On the Assoctatton of Granite with the Tertrary Srrata near
Kriyeston, Jamaica. By J. G. Sawxins, Esq., F.G.S.
[In a letter to Sir R. I. Murchison, G.C. St.8., F-R.S., F.G.S., &e. Dated
Kingston, July 29th, 1862.]

TuE object of my writing at present is to inform you that, during
the last few months, I have been tracing out a very interesting
eranitic formation traversing this island from the 8.E. to the N.W.,
the direction of our earthquake-shocks.

My interest in the investigation was enhanced because it was
generally supposed that lower rocks of this intrusive class did not
appear on this island, and also by frequently observing small crystals
of the carbonate of copper associated with it, by which I was
encouraged in the belief that I should find this metal accompanying
the granitic formation.

This formation first appears in the parish of Port Royal, piercing
through the carbonaceous series; then west of the Hope River, in
the parish of St. Andrew, between the white limestone and con-
glomerates. It is consequently of Tertiary age. It sinks below
the white limestone at Stony Hill, rises again through the same
to the N.W., and trends off into the parish of Metcalfe, where I found
the copper associated with the granitic series in the manner the
specimens sent with this note will ulustrate, which I consider an
interesting fact to lay before you.

The character of the granitic rock differs materially in the quantity
of each constituent, and it is more frequently accompanied with
hornblende than mica, the amount of felspar being greater than
the quartz. It has, in many instances, undergone decomposition to
so great an extent that it is recognized with difficulty.

After I surveyed Anguilla, some of the Americans engaged at Tom-
brero examined and experimented on the bone-breccia I found there ;
they abandoned it in a few days, and found no phosphatic rocks on
the island worthy their attention.

D2

36 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

[Nov. 19,

Novemser 19, 1862.

James Brunlees, Esq., C.E., 5 Victoria Street, Westminster, and
M. Auguste Laugel, Ex-Secrétaire de la Société Géologique de
France, Orleans House, Twickenham, were elected Fellows.

The following communication was read :—

On the CAMBRIAN and Hurontan ForMATIONS,
By J. J. Brassy, M.D., F.G.8.

ConTENTS.

Part I.
1. Introduction.
11. Characters of the Cambrian Rocks.
a. Typical Form and Distribution.
6. Stages in the Cambrian Epoch.
ec. Stratigraphical Characters.
d. Organic Elements.
e. Paucity of Fossils.
III. Abundance of Life above the
Cambrian.
a. Tracks of Crustaceans.
b. Phosphatie Coprolites
Lingule.
c. Primordial Zone.
Table I. Synopsis of the Cambrian.
Table II. Fossils of the Primordial

with

Part IT.
I. Introduction.
II. Characters of the Huronian Rocks.
. Geological Position.
Geographical Distribution.
¢. Lithological Characters
Typical Form.
d. Connexion with the Laurentian.
e. Igneous Intrusions.
Ill. Huronian of various Districts.
a. South Shore of Lake Superior.
b. Norway.
IV. Relations of the Cambrian and
the Huronian.
V. Conclusion.
Table III. Synopsis of the Huronian.

~sS

and

Zone.

Part I,—Remarks oN THE GrocrapnicaAt ConpdITIONSs OF THE
CAMBRIAN SYSTEM,

I. Introduction.—Some of the following statements, and the con-
clusions to which they have given rise, were originally intended to
refer, in chief, to the presence or absence of organic remains in the
Cambrian rocks; but, led on by points of interest that gradually
presented themselves, the inquiry has been conducted further than
was at first anticipated.

I may perhaps be allowed, for the present, to take for granted
that the Cambrian of Western Europe passes conformably upwards
into the Silurian series, with certain changes introduced by altered
conditions. Usually these two sets of rocks are mutually conform-
able, and pass into each other, sometimes by insensible gradations *.

It is also true that their unconformity is very frequent, from the
local operation of plutonic forces. I shall not stop now to bring
forward proofs of these several assertions.

I have given as a Table a synoptical list of all the Cambrian
deposits known to me, and also other Tables of some use. On these
Tables is grounded much of what is advanced in this paper.

* T ought, however, ex “imine, to say that the published proofs of this con-
nexion between Cambrian and Silurian beds (some of them at least) need
revision.

1862. | B1GSBY—CAMBRIAN AND HURONIAN, 37

II. Characters of the Cambrian.—The Cambrian formation is so
varied in its particulars, and so familiar as a whole, that a definition
of it need not be attempted.

We find in it, however, the following characters :—

§ 1. In Northern and Western Europe alone (or nearly alone) it
consists principally of purple and black clay-slates, often chloritic
and micaceous, together with conglomerates, grits, and sandstones,
placed almost indifferently on any horizon.

§ 2. This schistose constitution is elsewhere absent, except in one
or two localities ; and usually if any rocks exist intermediate between
the Silurian beds and a crystalline base, those rocks are derived
from the latter, and have no mineral or paleontological connexion
with the Silurian series.

§ 3. Immediate contact (transgressive) between the Silurian and
the metamorphic rocks may be said to be more general and more
extensive than between either the schistose or the simply conglome-
ratic rocks above mentioned, which are themselves, perhaps, about
equal in extent.

§ 4, The Cambrian has a tendency to assume a local character,
inclining perhaps to the mixed schistose character mentioned in $ 1,
the typical form as heretofore considered.

§ 5. The various beds, argillaceous, arenaceous, &c., are incon~
stant in their succession, 7. ¢. they have different horizons ; and some
may be absent altogether.

§ 6. They vary also in their thickness, both as a whole and in
the individual beds.

§ 7. Some of the mineral substances essential to organic struc-
ture, such as lime, phosphorus, fluor, azote (?), are absent, except a
httle of the first, and that rarely.

§ 8. With a large and varied assemblage of highly organized life
in the lowest Silurian deposit, we find this older, but kindred set of
rocks to be almost totally wanting in evidences of animal and vege-
table existence. Such forms as do appear are of low organization, and
do not indicate a fauna differing essentially from that of the Silurian
scheme: life is not here another, and an original, conception.

§ 9. The Cambrian is not the Huronian.

a. Typical Form and Distribution.—The description given in § 1
may be taken as representing very briefly the typical form of the
Cambrian as generally understood, and as first seen in Wales by
Professor Sedgwick. It has since been traced, with modifications,
into Ireland, Brittany, Dép. Loire Inférieure, &e., in France, as well
as into Thuringia and Bohemia, and less distinctly in a few other
districts.

Many of the leading facts in Cambrian geology may be learnt by
consulting the large Table at the end of this part of the paper; and
still more satisfactorily by recourse to the original authorities, as
set down in the footnote*,

* The principal authorities on the Cambrian Formation are as foliows :—
EnGuanp AND WaEs.—Professor Sedgwick. Proc. Geol. Soc. and Quart. Journ.

38 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 19,

In § 2 a very different state of things is revealed: there is not a
shred of Cambrian schist, nor of its grits and peculiar conglomerates,
throughout vast spaces in America, as far as 1s yet known, embracing
many degrees of latitude and longitude, throughout the Arctic Seas,
Hudson’s Bay, North-east America, with Texas, Nebraska, and
Wisconsin.

We see the same absence of Cambrian schist through vast
breadths of Northern Europe, that is, in Scandinavia, the north-
west end of Scotland, and in Sardinia. In fact, the larger part of
the schistose rocks of examined countries, though apparently Cam-
brian, is really Huronian.

From all these countries, as I have said, schists are either
altogether absent or extremely rare. Where there is an inter-
mediate mass of rock, it is a conglomerate supporting the Silurian
base, and resting transgressively on the crystalline rocks. To take
the following cases: a gneissic conglomerate is seen at and about
Whitehall, on Lake Champlain, New York, in this position; also on
the River San Saba, in Texas ; in Nebraska, among the Black Hills ;
on Granite Island, Black Bay, Lake Superior *; and in the north-
west of Scotland and the neighbouring isles.

The mineral constitution of all these conglomerates is much the
same, but wholly dependent on that of the rock below. Thus the
red Scottish conglomerate is totally derived from the underlying
Laurentian rock, and, though in contact, has no mineral con-
nexion with the Silurian above. It is both coarse and fine, and
small portions of it are triturated into fine red or purplish sandstone.

Geol. Soc., passim; Philosophical Magazine.—Professor Sedgwick and
Professor M‘Coy. British Palzeozoic Rocks and Fossils, 1855.

Great Brirary, &c.—Sir R. I. Murchison. Siluria, 2nd edit.; Quart. Journ.
Geol. Soc., vols. xvi., xvil., e¢ passim.

Wass, &c.—Prof. A. C. Ramsay. Lectures at Government School of Mines;
Lectures at Royal Institution ; Quart. Journ. Geol. Soc. vol. ix. pp. 162,
172; Geologist, vol.i. p. 171.—W. T. Aveline, Esq. Geol. Survey Sections,
sheets 36, 37.—J W. Salter, Esq. Quart. Journ. Geol. Soc. vol. xi. p. 246,
and vol. xiii. p. 200.

Scortanp.—G. Tate, Esq. Geologist, 1860, p. 240.—D. Page, Esq. Brit. Assoc.
Rep. 1858.—Professor Harkness. Quart. Journ. Geol. Soe. vol. viii. p. 393 ;
ea p. 239.—Professor J. Nicol. Quart. Journ. Geol. Soe. vol. xiii.
OS .

ga eeT . B. Jukes, Esq., and Messrs. Wylie and Kinahan. Journ. Dublin
Geol. Soe. vol. v. &e.

France.—MM. Elie de Beaumont et Dufrénoy. Explic. de la Carte Géol. de
France, pp. 130, 158, 204, 251.—M™M. Lorieux et de Fourcy. Carte Géo-
logique de Morbihan.—MM. Dalimier. Bull. Soc. Géol. France, N. S.,
vol. xviii. p. 664; Comptes Rendus, vol. xlvi. p. 636 (Cotentin and Pyre-
nees).—MM. de Verneuil, d’Archiac, Rouault, Triger, &c.; also Siluria,
2nd edit. p. 444.—Rozet, Ardennes.

Aurs.—MM. von Hauer et Feetterle. Annales des Mines, 5™ sér., vol. viii. p. 180.

Grrmany.—Barrande. Syst. Sil. de Bohéme; Bull. Soc. Géol. Fr. vol. viii. &e.
&c.—Sir R. I. Murchison and Professor J. Morris. Quart. Journ. Geol. Soc.
vol. xi. pp. lvi, 412.

S. America.—D’Orbigny. Cours de Paléontologie, pp. 111, 169.

N. Ameritca.—Roemer. Bull. Soc. Géol. Fr., N. S., vol. xviii. p. 216.—B. F.
Shumard. Bull. Soc. Géol. Fr., N. 8., vol. xviii. p. 220.

* Sir W. E. Logan, Geol. of Canada, 1862, p. 78.

1862. | BIGSBY—CAMBRIAN AND HURONIAN, 39

These conglomerates and sandstones, sometimes 1500-3000 feet
thick, are local; and they are called Cambrian because they occupy
the place of that formation in the geological series; but they have
no affinity with the Cambrian of Wales, for, both in Europe and
America, they are merely the re-cemented fragments of the crystalline
rock on which they repose. The same is to be said of the bed near
Kinnekulle, in Sweden, which lies between the granitic gneiss there
and the Silurian strata; it consists in like manner of re-adhering
fragments of the metamorphic rock below—the “ arkose” of Bron-
geniart. These are important facts, and they derogate not a little
from the high rank at present held by the Cambrian as a system.

The schistose form of Cambrian and the local puddingstone variety
do not form constant and widely diffused strata, like those of many
kinds of rocks in the palzeozoic and mesozoic series, the conglomerate
being native, the other comparatively foreign.

According to our present information, the direct superposition of
Silurian upon metamorphic rocks, mentioned in § 3, prevails over
considerably more space than the schistose or conglomeratic inter-
mediates, We find them in close adhesion for 2000 miles, from
Labrador westward to Minnesota beyond the Mississippi River. At a
multitude of points along this line they have been examined by
Logan, Murray, Chapman, Richardson*, myself, and others,—on the
shores of Labrador, Lake St. John (L. Canada), near Quebec,
Montreal, Kingston, Lake Simcoe, on the Great Lakes, and so on.

Professor Haughton, in the Appendix to M‘Clintock’s ‘ Fate of
Sir John Franklin,’ broadly states that “the Silurian rocks of the
Arctic Archipelago rest everywhere directly on the granitoid rocks,
with a remarkable red sandstone, &c.;” and, I suppose, transgres-
sively, seeing that the Professor finds the Upper Silurian beds there to
be horizontal. The same immediate contact takes place in the
Appalachians and on the Upper Mississippiy.

In the excellent account of the geology of Bolivia and Southern
Peru, by David Forbes, Esq., F.R.S.f, the word ‘ Cambrian” never
occurs. Silurian beds of enormous thickness, with Cruziana Boli-
viana and Annelid-tracks, are said to rest directly on granite. Nor
does the Cambrian show itself in either of Mr. Forbes’s two sections
(335 and 328 miles long respectively) through these countries,
abounding in paleozoic strata. In the neighbouring province of Chi-
quitos M. d’Orbigny observed the same facts ; and also on the flanks
of the lofty Iimani, a part of these Cordilleras $.

This direct contact obtains also in Scandinavia, as at Andrarum,
&c., in Scania, and in the Silurian trough of Christiania, Norway |j.
As regards Bohemia, M. Barrande expresses himself very satisfac-
torily on this point in ‘ Bulletin Soc. Géol. de France,’ n. s. vol. x.

* Logan and Murray, Geol. Reports, passzmm ; Chapman, Canadian Naturalist ;
Richardson, Geol. Reports, Canada, 1857, p. 78.

t Rogers and D. D. Owen, Reports on Pennsylvania and Minnesota.

t Quart. Journ. Geol. Soc. vol. xvii.

§ Travels in South America, vol. iii. pp. 146, 225.

|| Sir R. I. Murchison, Quart. Journ. Geol. Soc. vol. xi. p. 162.

40 PROCEEDINGS OF THE GEOLOGICAL SOCTETY, [Nov. 19,

General Portlock, also, states* that in Londonderry coarse arenaceous
schists, containing Orthis grandis, &c., rest directly upon, and skirt
granite and hornblende-rock (sce section, p. 230). Mr. Jukes
observed a similar fact among the Cambrians of Wicklow Tf (see
section); and Professor Ramsay informs me that he has seen it in
Scotland.

b. Stages in the Cambrian Epoch.—The Cambrian epoch then is
marked by three distinct conditions, which perhaps represent stages
caused by changes in the relative level of land and sea; and hence
the want of constancy in its constituents.

These conditions are :—

1. The under rock, Laurentian or Huronian, having been ex-
posed above water, no deposit whatever took place until the Primor-
dial epoch of the Silurian period arrived; in some places with
abundance of life.

2. The parent rock having been submerged in shallow and dis-
turbed waters, native conglomerates were produced by well-known
processes (Scotland, North America, &c.).

3. These parent rocks having subsided into great depths, arcna-
ceous, argillaceous, and other deposits took place, sometimes to the
thickness of 25,000 feet and more; such deposits becoming after-
wards more or less metamorphosed.

ce. Stratiqraphical characters.—Passing by § 4, we find in reference
to § 5, on examining the Synoptical Table, that the succession of beds
in this group of strata (schists, grits, conglomerates, &c.) is quite
irregular. This arises from local causes; and the want of stratigra-
phical agreement, it is remarkable to notice, is as strong in contiguous
districts as in those more remote.

In considering § 6, which treats of the thickness of the Cambrian
strata, I believe that unusually great accumulations have no great
ecological importance. I deduce from them that a change of level
has oceasioned heavy denudations somewhere, followed, of course, by
loaded currents, which have been suddenly arrested at the place of
accumulation. One effect is, that this thick deposit has few or no
fossils, for more than one obvious reason. We sce this exemplified
by the ten or twelve thousand feet of Devonian Sandstone (without
organic remains) in Kerry and Cork, Irelandt; and in the three
thousand feet of the same rock, forming the Catskill Mountains,
New York, containing few animal remains, but many plants. The
thickening of the middle Carboniferous Limestone in Derbyshire and
Yorkshire is another similar instance. We must not, therefore, ex-
aggerate the importance of thickening in the Cambrian.

d. Organic elements—As regards $ 7, the absence from this set of
beds of phosphorus and such elements is generally believed, but upon
what authority I know not. Instead of numerous analyses in sup-
port of this opinion, I only recollect a very few by Mr. D. Forbes and
by Dr. Lyon Playfair. But we must not forget Professor Daubeny’s

* Survey of Londonderry, p. 303.

t Jukes and Wylie, Journ. Dublin Geol. Soc. vol. vi.
t Jukes, Student’s Manual, p. 409.

1862. ] BIGSBY—CAMBRIAN AND HURONIAN. 41

curious experiments, which consisted of sowing barley in powdered
rocks ; he found that whatever might be the age of the rock, provided
only that it belonged to a series in which organic remains were
present, the amount of phosphoric acid present in the crop exceeded
considerably that existing in the barley from which it was derived.
In Cambrian rocks Dr. Daubeny found no trace of phosphorus.

We know that calcareous matter in Cambrian beds seldom occurs,
and only in small infiltrations, as in Wales, or in a thin and solitary
seam, as in Brittany. Where one or more large calcareous beds,
unfossiliferous, are observed in a group which seems to belong to this
epoch, the strong probability is that it belongs to the Huronian
series.

e. Paucity of Fossils—We also know that § 8, marking the im-
poverished life of the Cambrian, contains an important fact which
we are authorized to state, after a most pertinacious and skilful ex-
amination of its beds, in Wales and Ireland especially. Nor need
we expect any traces of life in the contemporary conglomerates of
Scotland and America.

The frequent occurrence of conglomerates, grits, and sandstones in
this series forbids our attributing the absence of life in it to any
permanent abyssal depths, as was supposed by the late justly lamented
Daniel Sharpe*.

The remains of organized beings in the Cambrian are few, both
generically or specifically, and they are mostly related to certain low
forms in the primordial zone of various countries; for instance, the
Arenicola didyma, which corresponds to the Scolithus (Annelid-tubes) ;
Paleopyge Ramsayi, corresponding to the Trilobite (a high form,
however); the Oldhamia is a sea-weed (Goeppert); the plant Chon-
drites occurs also in the Silurian as a genus‘.

I repeat, then, that in this period we are not introduced to any
set of living creatures wholly unknown in later periods, as we are in
some other parts of the great sedimentary succession.

Some of the reasons for the absence of organic remains from this
group of beds may be stated as follows :—

1. The general absence of carbonate of lime, and the probable ab-
sence of phosphorus and other elements of organization.

2. The great, continued, and occasionally tumultuary deposition of
sediment, in which few or no animals could haye lived (James Hall).

3. The deposition of substances unfit to support life, whether di-
rectly poisonous or because consisting of any unmixed material, as
clay, lime, silex, &e.

4, Plutonic action, which was frequent in the Cambrian, operated
by modifying or destroying rocks and their contents ; metamorphism,
which need not haye been caused by subterranean heat, has the same
effect.

5. Shells in porous or permeable strata are often removed by the
infiltration of solvent fluids.

* Quart. Journ. Geol. Soe. vol. id. p. 208. f Jdid. vol. xii. p. 246,
{ See Mr. Prestwich’s remarks, 207d. vol. viii. p. 240.

42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Noy. 19,

However we may seek to account for the absence of a varied fauna
in the Cambrian strata, the fact is rendered the more remarkable
by the occasional abundance of the phosphates, sulphates, and
fluates, as well as of graphite, in the Silurian basement-rocks, which
immediately followed the Cambrian by tranquil deposition.

III. Abundance of Life above the Cambrian.—Not a few natural-
ists are inclined to believe that in the molluscan form of life, from
the earliest times, instead of an ascendant movement in their order
of development, a decadence even has affected them ; and that these
organisms of distant date do not yield in specialization to the like
forms of today. A tendency to concur in such opinions may well arise
from a consideration of the following facts, which show at the same
time how abrupt and great must have been the change from life in the
subjacent strata, to life in the Silurian ; from a state, that is, of great
comparative sterility, to one singularly prolific.

a. Tracks of Crustaceans.—First, the occurrence in the Potsdam
Sandstone (the oldest Silurian) about the mouth of the Ottawa, that
noble river, and about Lake Louis into which it flows, of footprints
and tracks of several species of large Crustaceans. They have been
faithfully described by Sir W. E. Logan and Professor Owen, be-
sides having been most generously illustrated by the former. These
appearances carry the existence of complex forms of life very far
down.

b. Phosphatic Coprolites with Lingule.—Secondly, while James
Hall, the great paleontologist of America, found in the Delthyris
Shaly Limestone (Upper Silurian) coprolite-like, phosphatic nodules,
full of crushed Lingule, the Geological Commission of Canada met
with facts more remarkable still. They discovered that a large
breadth of country on the Ottawa River, from Lake Allumettes to,
at least, Grenville, a distance of 80 miles in the south-east direction,
is more or less sown with coprolites in calciferous sandstone. This
rock, at the Falls of the Allumettes, is a conglomerate, and rests
directly on Laurentian gneiss.

These coprolites are sometimes 23 inches long by 4 an inch broad,
and are filled with a large species of Lingula; in one case a frag-_
ment of this shell was found lying crosswise in the nodule. Besides
the Lingule, a few Pleurotomarie or Holopewe are met with in these
reniform masses.

The Grenville coprolites are smaller and more compact than those
of Lake Allumettes. They give off an animal odour when heated,
and principally consist of phosphate of lime, as do those of the
Township of Hawksbury, close by. These latter are yellowish brown,
and smell like burnt horn when heated. Dr. Lyon Playfair proved
that similar bodies from the Bala Limestone, in North Wales, were
foreign bodies of animal origin*, All phosphatic nodules may not
be coprolites ; but these from the Ottawa have every appearance of
being so.

The coprolites of Lake Allumettes, &c., seem to be the excretions of

* Quart. Journ. Geol. Soc. vol. vii. p. 267,

1862. ] BIGSBY—CAMBRIAN AND HURONIAN, 43

large animals, and are probably those of the large Crustaceans whose
footprints have just been alluded to. So that we may now-a-days
have some small perception of the antique and mysterious interest
which is attached to these relics, dragged out of the abysses of time
by a young science.

D. D. Owen and others after him have mentioned, with great
surprise, the countless myriads of phosphatic Zingule buried in the
Potsdam Sandstone which forms the walls of the River St. Croix,
in Minnesota, not far from its junction with the Mississippi. In
the same way Trilobites in incalculable numbers occupy a bed of
Trenton Limestone at Beaufort, Quebec ; all in fragments, and lying
flat upon each other.

e. Primordial Zone.—I have, finally, to request your attention to
the great and unexpected abundance of life in the Primordial rocks,
the immediate successors of the inhospitable Cambrian.

About ninety genera of Mollusca, and 250 species (allowing for
regional duplicates) met with regionally, are found in this one set of
beds (called indifferently Potsdam Sandstone, Lingula-flags, Pri-
mordial zone, or, as I believe, Taconic). The Molluscan orders
and genera are well represented in this initiatory basement-bed,
even up to the most highly organized—excepting the Cephalopoda,
which are entirely absent.

In this Primordial zone alone, there are twenty-five genera of Tri-
lobites, and 114 species; seventy-three species have been found in
Scandinavia alone, partly because this region has been thoroughly
examined (by Angelin).

It must be remembered that vast spaces of the earth’s surface have
received no attention, and that extensive Silurian districts, such as
Russia, Germany (exclusive of Bohemia), Scotland, and Sardinia,
have as yet furnished not one indisputable basement-fossil ; while
from others, Australia, France, Spain, we have received but one
or two.

We cannot but feel and express great astonishment to see a rich
and well-balanced fauna thus spring forth from a Cambrian barren-
ness which was nearly absolute, and with a quickness not yet fully
explained. Indeed this barrenness is in all probability more ap-
parent than real, for, according to Mr. Salter, we are dealing with
shore-deposits only, which generally present few species. There
may have been, and probably was, a deep-sea fauna*.

All that has now been stated may well prepare our minds to re-
cognize a living nature in the Laurentian, or fundamental gneiss-
rocks, equally diversified and plentiful. We may not have found, at
this moment, the very forms themselves, but their residuary elements
are there in vast abundance.

* With a group or commonwealth of living creatures in the Primordial zone,
so well furnished and peopled in every department of Molluscan life, some re-
quiring deep or shallow waters, some only flourishing in moist sands or tangled
seaweed, and others on rocks above low water, is it not probable that the univer-
sal, shallow levels frequently attributed by continental authors to the earliest
Silurian period have only existed in imagination ?

[Nov. 19,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

44

eciotle | lore 9 \cotzcle celor tetlors &

@ [refeee) ee soon @ uophepy| rere eereteeteeeeeeese* eyepada NT

x |p Ig eglgclp erie [ittrrecerecscesesneeneenelatastnnreareneeres Teagiy

"a G

I eal 9 e I ainib)|ietete]|(e:ni0\e\e/siaisie/Bieipyels 59) TRH eoace pele nema rarer ssnntie * TTR OOS DAN
I

G eeeleooe wooleee paeumnyg ‘TOULIOY re eee ee ee SUXOT,
sie/ei|(etsiei|\exeveil(aiare]|/leuwia\e@/slele\clnieterels DRO UMAR? tet PN Saar: BeOS a dossouua y,
Pispilinit| oak Pc ores TOON 6 oTrey [gee tine ns ene oa ee ABAD ASELULO
I 9 1 Se ee POO TTORD | eee as et aiene gear NON
Spolsou||oga| (oo tsle 6 sereineiacine ssurT[iq Botha incu nme Me ese a “WUOULLO A
I pe ling eee e eee eee coer SOUT [LG . *puB[pUNOFMO NK ‘OTSIOT[O_ JO SJIV.4S

So) G rr SUNT | saris” eae ‘VN ‘seqont)
sra[eea[ees|eceeceeceeseereees tA MIQg| tetttsresteeeereeecccerrerere BITBIISNYT

sselverleeesoomrrogary Gunaaly| ttt setter sseenneee ‘+ BLABUIpPURIG
eleeeleceleer[eereoe “Oxy STLOSUMTOSUTLTA ee tat” 2 NS eS eit ebie BISSNY
7 |ecr|pealnerensceenay= o prrectarugy lpg” sag aes conan name tee CUTE Oy
tr apes eye emongr a akees a sae sone apse cane gere fuewiey
rOlUtO| Nl ae So moeen tat anh taneNs | de edtyeoit-nisee aeaisagedeni eu aes TON)

N

ON ky
DOM NAA

io @)
a
SS
i
SN
_

|
N
i)
a
I~
N
AN
6
me
l=!
N
re
oD
aS
S
EON

steeee cong ‘LOSTIPIN TAL POLO OSCUE GORE ey SI CIE oy vd alo py
Pi eae Oo ‘COSTYyOIN A, SES ia (=) (AV Ws O18 purpouny
aoallounaa tance TIMOUTO A O@ice sees ts escapee mad restore soured
Olt ecouaeyy Bad artes estas he eee OTE TE
“le opetg ep OUBISUD| ttre teeter erste ersten uTedg

a

eocleeoieeri|eee|~ 19 pr jeceiers

Si

re

N

io. @)

09

rei

—

—
: O° .
eS.

=

‘|Su) 1} Six)

"epodorsysey | nN

—
re

[RIO] | Set as

“*sploony |

‘wapysig | 7:

‘epypeuny |
“eaousniy | Bit

‘ewozoAg |
90, |
‘sproong |

“BozosIg

‘eyAqdooz, |
‘epododoyg |

‘S10 Y ‘SO1IGUNOD

‘vpodoieyse-y | aes :

‘epodomprag | 12
‘epodorpovag | o

‘SIpes @ytoouy |
-epodoyeydeg |
‘SIpes @j1o0uy |
‘epodoreydag |

“SaIOgdS “VUANHD

‘spossoyy qoupsounlg fo hunmuny jp.avag—TT ATAVy,

ties, pp. 37 & 38.

| Quart. Journ. Geol. Soc. vol. xix., to face page 44. |

ee ——

1. W/LAND.

is, Quart. Journ.
From Menai Straits. 360. Sir R. I.
to the North of Sno

aart. Journ. Geol.
ee |

W. Coast, Quart.
Prof. Ramsay, Hopl. xvi. p. 219.

Survey of Great Bri ane a
ol. xvii. p. 175.

Cri ghlands.

=e Le stone,) 2000-2500
seamed ek
a oe, ee

Slate and grit........

Grit and conglomer

Conglomerate and gVrath.
‘red, hard.
bjacent gneiss.
ul.

Ross-shire.
pebbles of the rock

al.

Coast ; also Isle of

5. IRELAND.

Wicklow, Wexford, and Dublin
Counties.

Messrs. J. B. Jukes & Wyley, Journ.
Geol. Soc. Dublin, vol. vi. p. 28.

Chiefly green and purple grits, shading

off into quartz-rocks.

Grits, bright red, green, grey, coarsely
granular, hard.

Sandstones, compact, close - grained,
white mica-flakes occasionally.

Slates, green, red, olive-brown, yellow-
ish, often chloritic, or a fine roofing-
slate or flagstone.

(Stratification very confused.)

These rocks are identical with those of
Barmouth, Wales.

6. FRA: AMERICA.

10. AusTRALt (?).

Cotentin ? (Norm:

Dalimier, Bull. So

vol. xviii. p. 664. Saba. B.F.Shu-
Granville, Cancale]. Fy. ns. vol. xviii.

Bull. Soc. Géol. Fr. Ip, 4
Ardennes, Slate-7, Hayden, Trans.

mogne. Rozet et Du, yol. ‘xii. p. 23, &c.
mont et Dufrénoy, E

Géol. de France.

Cotentin? (Norias,

Sandstone, compact,

Sandstones, purple. se granitic, 150 ft.

Cong'omerate, felsfnounted by fossili-
Limestones, thin. Sandstone. )

Clay-slates at St. Zo.
Schists, micaceous an_,
Schists, macliferous. shea.
brian.

rests extensively
ly on Azoic (Hu-

Granville, Cay

Schists, macliferous,
and conglomerates,

Ardennes (R

Quartzite, thick-bed
Psamumite, alternatin
Schists, pale.

Schists, shining ; thi
Schists, argillaceous

Sandstones, ferruginous, micaceous.

Victoria, on Rivers Loddon and
Campaspe ?

A. Selwyn, Quart. Journ. Geol. Soc.
vol. x. p. 299.

Grits, felspathic, red, grey, brown.
Slates, clay, arenaceous, felspathic,
Flagstones, fine arenaceous.
Quartz-rock } er
Conglomerate f * hair
Direction N. and $., dip high.
Gold in quartz-veins.

No organic remains.

Thickness 35,000 feet.
(N.B. Probably Lower Silurian.)

1. WALES.

Tasiu I.—Synopsis of the Cambrian Formation.

The order of succession in this Table is descending.—or further information see List of Authorities, pp. 37 & 38.

[Quart. Journ. Geol. Soc. vol. xix., to face page 44.)

2. TINGLAND.

3. ENGLAND.

4, Scornanp.

From Menai Straits over Glyder Fawr
to the North of Snowdon.

Longmynd, Shropshire.
Thickness probably not more than
14,000 ft., as it is exaggerated by folds,
the curves being cut off by denudation,

Prof. Ramsay, Horiz. Sect. 81, Geol.
Survey of Great Britain.

W. T. Aveline, Horiz. Sect. 36 & 37,
Geol. Survey of Great Britain.

Longmynd, Shropshire.

J. W. Salter, Quart. Journ. Geol.
Soe. vol. xii. p. 247.

Slate and grit
Grit and conglomerate #900
Conglomerate and grit, obscure 1650

5100

Feet.
Sandstone, coarse red ......... 7,000
Shale, sandy, red, micaceous... 300
Sandstone and shale, hard, 4.500

coarse, red
Sandstone, hard, gritty, grey... 1,500

Shale, purple, sandy ............ 100
Sandstone, coarse, reddish- 2,000
‘DYOW lives squcheoces eves tence Q

Shale and sandstone, purple... 4,000
Grey rock, very hard............ 1,000.
Conglomerate .......-..0.:01+010+- 200
Sandstone, hard ..............--++ 400
Shale, greyish-blue, slaty ...... 2,000

23,000

No base seen. (No lime.)

. Sandstones and conglomerates, red.

. Slates and sandstones, grey, alter-
nating.

. Sandstones, hard, grey, greenish.

. Slates and sandstones, grey and red,
alternating.

. Slates, red, and hard.

Sandstones, hard, ereenish, very fine-

grained, or micaceous, rippled.

. Schists, harder, rippled, felspathic ;

thin shale, greenish, alternating.

. Schists, dark olive, with few lines
of crystalline limestone.

wo Ne

Oo TI an

North Highlands, Quart. Journ.
Geol. Soe. vol. xv. p. 360. Sir R. I.
Murchison.

Cape Wrath, Quart. Journ. Geol.
Soe. vol. xvi. p. 216.

Durness and N. W. Coast, Quart.
Journ. Geol. Soc. vol. xvi. p. 219.

Isle of Lewis and Ross-shire, Quart.
Journ. Geol. Soc. vol. xvii. p. 175.

5. IRELAND.
fae

Wicklow, Wexford, and Dublin
Counties.

Messrs. J. B. Jukes & Wyley, Journ.
Geol. Soc. Dublin, vol. vi. p. 28.

North Highlands.
Conglomerate-sandstone, | 2000-2500
chocolate-brown. feet.

Gneiss, fundamental, grey, with red
granite-veins.

Cape Wrath.

Sandstones, purple-red, hard.
Conglomerate of subjacent gneiss.
Gneiss, fundamental.

Chiefly green and purple grits, shading
off into quartz-rocks.

Grits, bright red, green, grey, coarsely
granular, hard.

Sandstones, compact, close - grained,
white mica-flakes occasionally.

Slates, green, red, olive-brown, yellow-
ish, often chloritic, or a fine roofing-
slate or flagstone.

(Stratification very confused.)

These rocks are identical with those of
Barmouth, Wales.

Durness and N. W. Coast ; also Isle of
Lewis and Ross-shire.
Conglomerate, red, pebbles of the rock

below.
Gneiss, fundamental.

6. FRANcE.

7. FRANCE.

8. BonEmia AND GERMANY.

9. Nort AMERICA.

10. Ausrratta (?).

Cotentin? (Norman Bocage). M.
Dalimier, Bull. Soc. Géol. Fr. n.s.
vol. xviii. p. 664.

Granville, Cancale, &e. D’Archiac,
Bull. Soc. Géol. Fr.n.s. xviii. p. 664.

Ardennes, Slate-quarries of Ri-
mogne. Rozetet Dumont. De Beau-
mont et Dufrénoy, Explic. de la Carte
Géol. de France.

Départ. Loire. Brevenne, &e., in
patches. Grimer, Ann. des Mines,
3™° sér. vol. xix. p. 89.

Near Maletroit, Guers, &c. Lorieux
and De Fourcy, Geol. Map of Morbi-
han.

Upper Garonne. Ia Pique. Ley-
merie, Compt. Rend. vol. xlvi. p. 636.

Central Bohemia. Barrande, Sil.
Syst. Bohéme, p. 66.

South Thuringia and Saxony. Mur-
chison and Morris, Quart. Journ. Geol.

Soe. vol, xi. p. 412.

Texas, River San Saba. B. F.Shu-
mard, Bull. Soc. Géol. Fr. n.s. vol. xviii.
p. 218. F. Roemer, ~

Nebraska. F. V. Hayden, Trans.
Amer. Phil. Soc. n.s. vol. xii. p. 23, &e.

Victoria, on Rivers Loddon and
Campaspe ?

A. Selwyn, Quart. Journ. Geol. Soc.
vol. x. p. 299.

Cotentin? (Norman Bocage).

Sandstone, compact, intermixed with
Sandstones, purple. [schists.
Congiomerate, felspathic materials,
Limestones, thin. [granitic.
Clay-slates at St. Zo.

Schists, micaceous and satiny.

Schists, macliferous.

Granville, Cancale, §.

Schists, macliferous, with quartzites
and conglomerates.

Ardennes (Rimogne).

Quartzite, thick-bedded.

Psammite, alternating, thin-bedded.
Schists, pale.

Schists, shining ; thickness great.
Schists, argillaceous and roofing.

Département de la Loire.

Schist, argillaceous, with felspar-cry-
stals. Gneiss, micaceous or talcose.
Granite, slaty.

Schist, green, satiny, argillaceous.

Sandstone, green, quartzose, schistose.

Lydian quartz, in small beds.

Conglomerate of quartz-pebbles in si-
liceous cement.

(Much disturbed by porphyry.)

Near Maletroit, Guers, &c.

Schist, extensive, talcose.
Granite, porphyritic.

Upper Garonne. La Pique.

Schists, fine, satiny (extensive).
Gneiss.
Granite.

Bohemia.

Schists, granular and conglomeratic,
with quartzose boulders.
Slates, argillaceous.
Schist, taleose, chloritic, micaceous.
Granite.
Total 22,000 feet.
(No lime.)

South Thuringia and Saxony.

| Schist, chloritic, greenish, and with

hornstone.
Schist, dark-coloured argillaccous.
Quartz-rock.

All these beds are in great mass, and
are overlain conformably by Silurian.

Teaas.

Sandstone, granitic.

Conglomerate, coarse granitic, 150 ft.

Granite. (All surmounted by fossili-
ferous Potsdam Sandstone.)

Nebraska.

[Generally no Cambrian.

Potsdam Sandstone rests extensively
and unconformably on Azoic (Hu-
ronian?) rocks. ]

Sandstones, ferruginous, micaceous.
Grits, felspathic, red, grey, brown.
Slates, clay, arenaceous, felspathic,
Flagstones, fine arenaceous.
Quartz-rock
Conglomerate \ CMSA W EAL
Direction N. and &., dip high.
Gold in quartz-veins.

No organic remains.

Thickness 35,000 feet.
(N.B. Probably Lower Silurian.)

Midst ei
i iby i
ent enn! wll

” ned eg i | ‘

Ty

ee joa ia Aart say) oh
“ie mre oy a aii nes ae
o aae Pay 7 mp ee wi
Bi ih : ee Dat Da hy

1862. ] BIGSBY—CAMBRIAN AND HURONIAN, 45

Part II.—Tse Hvuronran Formation oF CANADA NOT CAMBRIAN;
witH Remarks on rts RecronaL AFFINITIES.

I. Introduction.—The Huronian formation, one of the several
great discoveries of the Geological Commission of Canada, will pro-
bably be found to be an important member of the fixed rocks of the
earth ; for on the north side of the Great Lakes of Canada, where it
was first detected, it occupies a district 710 miles long, and there
is a considerable area of it on the south-east side of Lake Superior.
It is largely and variously developed also in Norway, and probably
in other parts of Europe.

This set of rocks is therefore of great importance, geologically as
well as economically, and is fully entitled to be called a formation if
we adopt Deshayes’s definition of the term, that is, “‘ a certain num-
ber of beds laid down under the influence of the same phenomena’’*.

The general feeling of geologistst is that the Huronian of Canada
is the same as the Cambrian of Western Europe ; but careful exami-
nation into all the circumstances seems to provoke more than a doubt
as to the correctness of this view.

No true Cambrian exists in North America according to Danat;
and, as far as my experience goes, the Huronian constitutes a group
of beds which may be said to be its substitute in place, if not in time.
It has received a name from Sir W. E. Logan because it has a new
and distinct character, and needed a designation; and by him and
Mr. Murray, his able and enterprising coadjutor, it has been minutely
described.

As I have paid three visits to the greater part of this formation,
in Canada, I may be permitted to make the following brief comments
upon it; my object being, first, a summary account of its place and
relations, with some small additions of my own; secondly, to point
out an all but perfect identity in the members of this formation in
Europe and America; and thirdly, to show that it is not Cambrian.

II. Characters of the Huronian.—a. Geological position —The
Huronian of Canada occupies a stratigraphical horizon not far from
that of the Cambrian of Wales, between the Laurentian gneiss and
the Silurian ; but it is older, for the Cambrian is continuous into,
and conformable to the base of the Silurian, when the latter is in
an undisturbed and normal state, while the Silurian is invariably
transgressive as regards the Huronian formation in both hemispheres.
I have seen this exemplified in numerous instances in Lake Huron
and Lake Superior. ‘That the traces of life are not found in this
formation affords but moderate aid in fixing its date, for this happens

* Deshayes, Bull. Soc. Géol. de France, N. S., vol. ii. p. 89.

+ Sir W. E. Logan, American Journ. Science, N. S., vol. xiv. p. 227. Sir R,
TI. Murchison, Siluria, 2nd edit. p. 19. Coquand, Traité des Roches, p. 299.
D’ Archiac (as I understand), Bull. Soc. Géol. de France, N.8., vol. xviii. p. 664,
Morris, Geologist, vol. i. p. 139.

+ Dana (Address, Rhode Island), Canad. Journ. 1855, p. 386.

§ At the Twin Falls, River Menomonee, south side of Lake Superior ; see
Foster and Whitney, Geol. of Land District, p. 24. Also between the Rivers
Missassaga and St, Mary, Lake Huron; see Sir W. E, Logan, Geol. of Canada,
1862, p. 56,

46 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 19,

in all the stages of the sedimentary series ; and the not uncommon
marks of ripples, cracks, and mud-flows§ in its quartzites and fine
grits render it possible that signs of animal or vegetable existence
may eventually be met with. Neither do we learn much from its
extraordinarily agitated and metamorphosed condition in many
places, for the same may occur at any epoch.

b. Geographical distribution—The geographical position of the
true Huronian beds may be broadly stated in the following words.

With a breadth often small (10-20 miles), but often concealed by
jungle and morass, the northern mass extends 710 miles, as already
stated, along the north-west watershed of Upper Canada, and prin-
cipally along the borders of Lakes Huron and Superior. We trace
it for 150 miles from near Lake Tematscaming (R. Ottawa), 80
miles north-west of Lake Nipissing, south-westwards, to Shebahah-
ning, on Lake Huron; and from thence westward for 120 miles to
Gros Cap, in Lake Superior. From this well-marked headland,
northerly and westwardly, the whole edge or coast of the latter lake,
with small and uncertain exceptions, consists of this formation as far
as the Pigeon River, near Grand Portage, about 440 miles ; and it is
amply exposed by the bare and hilly nature of the country *.

Another aggregate of these beds occupies more than 3000 square
miles of the region south-east of Lake Superior, on the River Meno-
monee (a tributary of Lake Michigan), and the districts north and west
of that river. It is anarea of very irregular shape, 80 miles wide in
one place, and having its highest points 1800 feetabove thesea-level +.

There is good reason to believe, according to my own recorded
observations, that the only three contiguous lakes in South Hudson’s
Bay at all known geologically—the Lacroix, Lapluie, and the Lake
of the Woods—each a few hundred miles round, consist largely of
this formation. Besides being extensively developed in the Adon-
dirock Mountains of the State of New York, and probably also in
Missouri and Arkansas, the Huronian is seen to great advantage in
Norway, and is not wanting in France; but of its occurrence in
these countries more will be found in the sequel.

c. Lithological characters and typical form.—Table III. is a
Synopsis exhibiting the leading features of the Huronian beds,
wherever they are known with tolerable certainty. It enables us
to keep facts separate and distinct from suppositions.

For the minuter details, the several authorities named in the foot-
notes may be consultedt. Of these I am most indebted to the mi-
nute and truthful reports of the Geological Commission of Canada; but
my obligations to the other investigations are neither few nor small.

By reference to the Synopsis (Table III.) at the end of this paper,
it appears that, on the large scale, the characteristic beds of

* Sir W. E. Logan, Geol. of Canada, 1862; Murray, Canadian Reports.

t+ Foster and Whitney, Geol. of Land District of Lake Superior, p. 31.

+ Sir W. E. Logan. Geology of Canada, 1862, p. 50, &. Alexander Murray,
Geological Reports of Canada, 1849, 1857, &c. Thomas M‘Farlane, Canadian
Naturalist, &c., vol. vii. p. 1. Foster and Whitney, Geology of Land District,
Lake Superior. Durocher, Mémoires de la Société Géol. de France, vol. vi.

1862.] BIGSBY-—CAMBRIAN AND HURONIAN. 47

the Huronian formation in America, whether in Canada, Wisconsin
(U.8.), or elsewhere, consist of :—

1. Slate; chloritic, siliceous, and hornblendic.

2. Slate; conglomeratic, matrix impurely argillaceous ; the pebbles
and boulders being granitic, syenitic, and slaty.

3. Conglomerates; quartzose, with white quartzose and red jasper
pebbles.

4, Trap and pale greenstone, both conformable and intrusive.

5. Granite; red, moderately porphyritic, intrusive.

6. Crystalline limestone; with some serpentine.

All these rocks are set down in the order of their abundance, the
most prevalent first ; Nos. 2 and 3 being very thick compared with
the other beds individually, 2. e. 7900 feet out of 16,700 feet (be-
tween the Rivers St. Mary and Missassaga, Lake Huron*), if we add
up the separate beds.

d. Connexion with the Laurentian.—The connexion of the Huro-
nian set of rocks with the Laurentian is not so fully made out in
America as in Norway; but we are not without some good materials,
and time will do the rest. Sir William Logan met with a conformable
junction of these two formations on the River Kaministiquia, on the
north side of Lake Superior, in the rear of Fort William. At the
lower end of the Second Portage, above the Grand Falls, the Lauren-
tian appears as a massive syenite or, rather, as a hornblendic gneiss,
Resting on it conformably, there occurs a series of dark, greenish-
blue or greenish-black slates (Huronian); the one rock almost running
into the other. The section extends for a quarter of a mile along the
river-bank. The Huronian has been observed to rest on granite in
two places,—on Spanish River in Lake Huron, and again on the same
granite 100 miles to the west, near Gros Cap, on Lake Superiorf.

No particular succession of individual beds has been, as yet, made
out, either in Europe or America; not but that there are, in parts,
long lines of distinct stratification, but because there are scarcely any
dips to be depended on. On Lake Huron, in the district just men-
tioned, this may well happen, through the occurrence of two enor-
mous downthrows in a wild and marshy country; and then again
from the inextricable confusion created by the violent intrusion of
molten rocks at five distinct epochs, the last of which produced large
deposits of cupper-ores.

e. Igneous intrusions.—Any description by words of the mutual
penetration, interweavings, and delicate inosculations of bright-green
greenstone and red granite, over considerable spaces of the mainland,
between the Rivers Missassaga and Thessalon, has been abandoned
in despair by Mr. Murray$. And Messrs. Foster and Whitney have
been equally foiled by similar blendings of granite and greenstone
on the Menomonee, between Sandy Point and Sturgeon Point ||.

* Murray, Canadian Geological Report, 1858, p. 76.

+ Canad. Geol. Report, 1849, p. 8.

t Murray, Report on North Shore of Lake Huron, 1849, p. 14.

§ Canad. Geol. Report, 1858, p. 76.

|| Foster and Whitney, Geol, Surv. of Lake Superior Land District, 1851, p. 19.

48 PROCEEDINGS OF THE GROLOGICAL SOCIETY. Nov. 19,

Many years ago I published in the ‘ American Journal of Science ’
a coloured representation of these capricious mutual infoldings on
the east of the mouth of the Thessalon River (Lake Huron). In
the middle, too, of a naked islet in Lake Huron, opposite the river
just mentioned, but three miles off, a boss of granite pushes its bare
red mass from beneath a paste-like envelope of fine-grained green-
stone, just as occurs in Carp River, on the south side of Lake
Superior*, but the mode of contact is not stated.

III. Huronian of various districts.—a. South shore of Lake
Superior.—With respect to the Azoic Series of the south shore of
Lake Superior, already alluded to, I beg to refer the Society to
columns 8, 9, and 10 of Table III., and here quote Foster and Whit-
neyy as saying that this series “is in alternating beds, of great
thickness, of gneiss, of chloritic, talcose, argillaceous, and siliceous
slate, of quartz, of saccharoid and crystalline limestones, and ser-
pentines—all much contorted, highly inclined—nowhere having a
sedimentary aspect, and most nfetamorphic near the lines of igneous
outburst,” so powerful and numerous hereabouts.

I look upon the Huronian or Azoic Rocks, here spoken of, as
belonging to the Huronian of the north of Lake Huron and Lake
Superior, for the following stratigraphical and mineralogical reasons :

1. The transgressive relation of the Potsdam Sandstone to both.

2. The same strike East and West in both; dip high.

3. The great prevalence in both of chloritic, dioritic, and horn-
plendic slates.

4, The abundance of trappean and hornblendic rock, sometimes
in brecciated masses composed of jasper, slate, felspar, and horn-
blende.

5. The extraordinary and extensive intermixture of the beds of
greenstone and granite, which defy description and classification.

6. The same quartzites, occasionally becoming a conglomerate,
with red jasper and other pebbles.

7. The occasional bands of white, grey, and red crystalline lime-
stone.

8. The presence in both of greenstone-dykes.

9. The absence of organic remains in both.

The quartzite of the country south of Lake Superior, unlike that
of Lake Huron, contains vast beds of magnetic iron-ore.

Besides the Huronian beds, as already treated of, Sir W. E. Logan
has described with great care a new formation, which he calls ‘ the
copper-bearing rocks.” They are of great interest, and their more
prominent characters may be best seen in columns 10, 11, 12 of the
Synoptical Table III. They repose on the Huronian, unconformably
to the crystalline rock below and to the Potsdam Sandstone above.
This subformation occupies about 250 miles of the north shore of
Lake Superior—that is, from Michipicoton to Pigeon River. It is
very naturally divided into a lower and an upper group; the lower
group, consisting of bluish slates or shales, with sandstones and
interstratified columnar trap, extends from Thunder Head to Pigeon

* Op, cit. p. 14, t (Op. cit. po 14,

1862. ] BIGSBY—CAMBRIAN AND HURONIAN, 49

River, a distance of 42 miles. The upper group consists of sandstones,
limestones, indurated marls, and conglomerates, interstratified with
columnar trap.

b. Norway.—Leaying without remark the deposits in Arkansas
and Missouri mentioned in column 12, because, although probably
Huronian, they require further study*, I now proceed to Europe,
where, at present, it is more than probable that the Huronian forma-
tion exists in Norwayf in great quantity, and very clearly shown,
as well as in other parts of that quarter of the globe.

In Norway, to a consideration of which country I shall first apply
myself, it has received from M. Durochert the name of * the semi-
crystalline schists,” or ‘the second group of Azoic formations,” the
lowest or first being Fundamental or Laurentian Gneiss§.

M. Durocher has called the first-named formation semi-crystalline
because in Norway, as in Canada, it consists of two associated por-
tions, the amorphous (sedimentary) and the crystalline (metamor-
phic); but it is a name very easily misunderstood.

M. Durocher professes himself unable to fix upon the age of these
rocks with precision, but believes them to form a transition between
the Fundamental Gneiss and the fossiliferous paleozoic rocks
(Mémoire, p. 61), and that it corresponds in part to the Cambrian of
Sedgwick.

This set of rocks does not, as in Canada, spread out in one mass
continuously to great distances, but is in distinct tracts and basins
within and upon the Fundamental Gneiss, which is the general base
of all the rocks of the north of Europe.

There are six of these basins according to M. Durocher: viz. (1)
at Nummendal and Haut-Tellemark; (2) in Central Scandinavia ;
(3) on the South-west coast of Norway; (4) on the sea-coast be-
tween Drontheim and Sogne Fiord; (5) in Finmark ; and (6) near
Tornea, at the head of the Gulf of Bothnia.

There is no difficulty as to the relations of this Huronian, if we
may so call it, to the Fundamental Gneiss. It is seen to rest on it
conformably in many places ||; on the gneiss of Schneehatten, in the
Dovrefield ; on the south side of the Sogne Fiord ; in the Fiord of
Urland, &c. And it is often unconformable, as in the valley of
the Beine and Elv4{, in the Fillefield, and other places; but these

* Engelmann, Foster and Whitney’s Geological Survey of Lake Superior Land
District, p. 31.

t+ To Thomas Macfarlane, Esq., of Acton, Eastern Townships, L. C., belongs
the credit of associating the Huronian of Canada with the semi-crystalline schists
of Norway, in a most valuable memoir published, in February 1862, in the ‘ Cana-
dian Naturalist.’ Ihave laboured independently to the same end, upon materials
gathered from other sources.

{ The author of a survey of Norway, most elaborate as far as is within the
power of an individual. His paper in the sixth volume of the ‘ Mémoires de la
Société Géologique de France’ is a model of geological description.

§ Von Buch, Sir R.I. Murchison, Keilhau, Kjerulf, Naumann, and Macfarlane
have also done good work in this country.

|| Mémoires de la Soc. Géol. de France, sér. 2, vol. vi. pp. 61, 90.

{ Op. cit. p. 92.

VOL. XIX,— PART I. E

50 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 19,

M. Durocher considers local phenomena. But, as we learn from this
author, the contact of this formation with Silurian is only seen with
perfect distinctness on Lake Miosen*, where the latter 1s transgressive
in a moderate degree, because, in the course of its undulations,
the Huronian at that spot has not a high dip. The meeting of the
Silurian beds of Hedemark, on the south of Losness, with the Huro-
nian or semi-crystalline Azoic rocks is rendered not so clear on
account of the undulations of the latter, which have only a moderate
dip, and are but feebly crystalline. Nevertheless it is here that it
- truly takes place. As in Canada, no very clear order of succession
has been made out in the individual beds of the Norwegian forma-
tion. How could there be, when in both countries plutonic action
has been intense, prolonged, and minute in its effects ?

While these deposits present in their composition notable varia-
tions, from place to place, they nevertheless possess in every part of
Norway the following common characters.

This second Azoic, or Huronian, formation is for the most part
essentially a schist, argillaceous, chloritic, and micaceous by turns ;
changing often also from the foliate and crystalline condition to the
amorphous or sedimentary, and this either suddenly or insensibly.

These schists frequently become siliceous, and then they may be
accompanied by granular, compact, and subcompact quartzites ; the
latter being translucent, and with a conchoidal fracture. The Gous-
tafield quartzitet is remarkably like that of Lake Huron. It is in
mountain-masses, as in Canada, where it forms hills, whose sides
shine bright and white from amid the dark pines. It is translucent,
glassy, and clear; grey, greenish or bluish grey; and brittle,
granular, or compact. It is also schistose; a tendency to which
structure is increased by interspersed lamine of talc, chlorite, or
mica. Certain varieties on the east side of Altenfiord and elsewhere
are red, green, violet, and white. Others assume the form of rib-
boned jasper (near Hjardal Church) or of hornstone, and become
conglomerates and breccias, with a dark-coloured paste, and con-
taining boulders of red and white jasper (on the Mandela River),
of quartz, chlorite-slate, and hornblende. Porphyritic intrusions
are common among the quartzites, and those of Nummendal and
Tellemark yield much sulphuret of copper, specular iron, and mag-
netite. |

Besides these schists and quartzites, we have, in Norway, grau-
wackes (grits and conglomerates, in fact), conformable to the schists,
&c., with a dark-green base, and pebbles of gneiss, granite, quartz,
and porphyry; being the nearest approach, as far as I am aware,
to the pecular greenstone-conglomerate of this age in Canada. We
must not always expect identities.

The Huronian limestone here is not quite equal in quantity to
that in Canada, with the exception of that in Finmarkt, where it is
pretty well developed. It is not white, but dark grey or blackish,

* Mémoires de la Soc. Géol. de France, sér. 2, vol. vi. p. 62.
t Op. cit. p. 63. 1 Op? ete: pee:

1862. ] BIGSBY—CAMBRIAN AND HURONIAN, 51

and both granular and compact. For details the Society is referred
to the admirable descriptions of Durocher ; for general information,
necessarily limited, the column in the Synoptical Table III., under
the head “‘ Norway,”’ may be consulted.

My reasons for believing the Norwegian Second Azoic Group to
be Huronian are as follows; and it is believed that they are not
without great force :—

1. Its place—lying on the Fundamental Gneiss, and covered by
Silurian.

2. The discordance of the paleozoic rocks above in regard to it.

3. Its resolving, as in Canada, into several distinct and important
parts, not altogether dissimilar to those of Canada.

4, The schistose rocks, the same in kind and proportion in both
countries.

5. The immense prevalence in this formation of diorite or green-
stone, and of hornstone, both in Norway and Canada.

6. The peculiar, greenish-grey, talcose quartzite, and quartzite-
conglomerates, with aphanite and red jasper pebbles, in these countries.

7. The dark-coloured slaty conglomerates, with boulders of gneiss,
granite, and greenstone, in both.

8. The limestones in the two regions, similar in kind, and much
So in quantity, but few in comparison with the other members, though
large in comparison with the Cambrian limestones. Here they are
dark, perhaps from graphite.

9. The total absence of life in both regions.

10. The presence in both countries of certain ores of copper and
iron. I shall content myself, for the sake of brevity, with referring to
Table III. for information regarding the probable Huronian of France.

IV. Relations of the Cambrian and the Huronian.—Having now
sketched the leading features of the Huronian series, while those of
the Cambrian have been treated of in Part I. of this paper, I am
at length enabled to exhibit such of their geological differences as
point to a difference of epoch, and they are as follows :—

1. The Huronian is unconformable to the Silurian both in
America and Europe :—ndét so the Cambrian.

2. The Huronian in Norway is conformable to the Fundamental
Gneiss formation ; and confidently believed to be so in America :—
not so the Cambrian.

3. Its mass is principally conglomeratic, such conglomerate being
of a special and typical kind :—not so the Cambrian.

4. It contains large and prolonged beds of marble :-—not so the
Cambrian, which is nearly destitute of limestone.

5. Its plutonic invasions and disturbances are quite different in
quantity and intensity from those of the Cambrian period, being of
five distinct epochs *.

6. The Huronian is more highly metamorphosed than the Cambrian
(containing gneiss, &c., Foster and Whitney) ; notwithstanding that
in Anglesea the latter formation has been completely changed into
gneiss.

* A. Murray, Canada Geol. Report for 1849, p. 14.
E 2

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 3,

Oi
bo

7. It contains large deposits of copper, native and in a state of
combination :—not so the Cambrian*.

8. The Upper Huronian of Logan (his copper-bearing rock) has
no resemblance to, or affinity at the Cambrian (see Synopses,
Tables I. and III.).

9. It is destitute of the traces of life :—not quite so the Cambrian.

V. Conclusion.—It is now time to conclude by observing that the
Ist, 2nd, 4th, and 9th of these points appear to be fatal da any idea
of the Huronian and Cambrian being the same formation, while the
rest are not without weight.

Three circumstances create in my mind a strong feeling that the
Huronian is greatly the older deposit. These are :—

1. Its marked similarity, lithologically, to the Fundamental
Gneiss formation.

2. The conformity of these two sets of beds.

3. The great interval of time which must have elapsed between
the periods of laying down the Fundamental formation and the
Silurian, if we are to judge from the occasionally vast thickness of
the Cambrian.

Beyond all comparison, the Huronian is more wide-spread and
extensive, a8 well as more uniform in its mineral constitution, than
the Cambrian group. It is, perhaps, also more important economi-
cally.

DEcEMBER 3, 1862.

Edward Hesketh Birkenhead, Esq., Master of the Wigan School
of Mines; Antonio Brady, Esq., Maryland Point, Stratford, Essex ;
Samuel Higgs, Jun., Esq., Assistant-Secretary of the Royal Geo-
logical Society of Cornwall, Penzance; and Alan Lambert, Esq.,
2 Portugal Street, Grosvenor Square, London, were elected Fellows.

The following communications were read :—
s

1. Duscrrption of the Remarns of a new Enatiosaurtan (Kosaurus
Acadianus), from the Coat-Formation of Nova Scotia. By O. C.
Marsu, Esq., M.A.

(Communicated by Sir Charles Lyell, V.P.G.S.)

[‘The Regulations of the Society do not admit of this important communica-
tion being printed in full in the ‘ Quarterly Journal,’ because, owing to an unfor-
tunate misunderstanding, it was not received until after it had been published
in the ‘ American Journal of Science and Arts’ for July 1862, New Series,
vol. xxxiv. p. 1, to which paleontologists are referred for a more detailed descrip-
tion of the fossil bgnes alluded to. |

[ Abstract. }

Introduction.—The Reptilian remains from the Coal-measures,
hitherto described, were stated to be few in number, and mostly of

* There is some copper in the Longmynd.

‘£akydaod osozyaenb
Aq pasxOAVry 1B PUB ‘OYJOUR OO YALA
oyVUtoy[e spoq YP pur ‘pare ‘pug oy,
“OSOYSTIPOS ‘OYTUB.L
"SSTOUL)
‘9800 BJ-O9OLTIIGAB ‘SnOsoKvOTUR “4sIT[OG
‘guUOyspuRg
“zyaenb
oyIgM pus ouojys uvrpATT jo solq
-qod yytm ‘osozjtenb ‘oyeroutopsu0g
"9U04s URIpPATT
JO spoq |[VUls YIIM ‘OlLLOTYO ‘systyog

(‘Tey ‘d *xtx ‘10a "@ “gs ‘souTTT Sop soreu
“uy ‘tounty 009) ‘odtoy aoddq

"HONVU

‘SHOAOWINU STOISBAUL OIUOIN,
‘oGp mnoge digg ‘snortea oylayg
‘oye]s
pue ‘zjaenb ‘aodsef pot jo solq
-qod osozjivnb yim ‘oyesoutopdu0g
"SOME 4O9F OOGZ-OOOL “OFOTCT
‘osozyrenb ‘stow
YIM Suyvusojye “aepnuead ‘ouoysouvy
‘omy ‘osOoTRy ‘OLLLOTY ‘soqeTg
‘rodsel
oyut Sutissed Arkydaod - ouoysuxozy
"9UOJSULOFT
*‘poureas-ourp ‘SstouLy
‘osozjaenb “YstqyoSs-vor AL
‘spoq
yoryy ut “ow ‘osoore, ‘Aasoqurtds
‘Kors ‘oyeyps-zjaenb =.10 opt zyren'}
‘UMOUYUN Spoq oY} JO UOIssedONS ONL,

‘OW “YAVULUT 489 AA.
‘KUMION YOY ‘uoyrwuusj[pay, UT

“AVMUO NT

"yIOX MONT puv

SVSURYLV UL 4STX9 0} pocopisuoo oq Avut
Solos OY} ‘SUOUTUIA “AQZ puw (OLS,
pur ‘aormedng oyey ‘foox ‘Aouqty AA
pue 104s0,7) uuUeUtfosuA 04 Surp.aoo
-oy ‘suttvoq-soddoo st puv ‘aumyoo
4xoU Ol} UL poyeromMNuUS osoT} 07 9[q¥
-ULLOJUOOUN SI Spoq JO SoLJOS STIL],

x

ioe B = os

=

4 ; = .
LQuart. Journ, Geol. Soc. vol. xix., to face page 52.) _

Tasre IIl.—Synopsis of the Huronian Formation.
‘The order of succession in this Table is descending or unknown.

Dare Huron.

8. North shore, between the Rivers |

1. From Lake Tematscaming S.W. 2. North shore of Georgian Bay; Missassaga and St. Mary, near Lake

to Lake Huron, 150 miles. from Collins Inlet, westward, 70 miles?

Superior,
ith j Feet.
erate of quartz, with jasper ie 2
Saas { uo Greenstone! ..<c.ss..sstsesceeeee 700 Seeley pitel rc
E faite white and pale sea-| Quartzite-conglomerate mestone, like that 4 3 cco
ee 3 with red jasper pebbles. 1000 | Quartzite, white, mottle A
F Quartzite alternating with Quartzite, whitish-grey : daniesione) Breen, greyelanel
| Slates, chloritic and siliceous. Quartzite, alternating er 500 Gee red san a0
Conglomerate, like the one below. Slates, blue os iElaek 6 800 @ i Perea ae Pe ane
Limestone, pebbly. onglomerate-s F Sool Gare ee ae
erate, ith boulders | Limestone (very long) 25 glo < BE
eres Conglomerate-slate . 1000 red jastanen ott pebbles 2,150
Slat 3 iliceous, chloritic Quarizite, pale green . 1200 Diorite, alternating wit a per
Be kee head : Slates, green argillaceous = Quartzite, iron - stained, he
‘No regular succession detected; the Greenstone vipple-smarke; or ..1......

total thickness is 10,000 feet.

Slates, chloritie Conglomerate, like the one

¥ above 20
Limestone, grey

greatly disturbed ... ;

ic intrusions very frequent. Diorite, alternating with

| pea rate vei Conglomerate-slate, argil-

laceous, with boulders of > 1,280

gneiss, syenite, jasper,

quartz:
Diorite .. alterna-
Quartzite - con - nating. + 1,000

glomerate...... |
Quarizite, white, yitreous
‘Drap, interstratified .. :
Slates, epidotic, chloritic
rp Qu +
Gneiss,

16,650

| Extreme confusion ; two great faults,
Plutonic invasions very frequent.

Take Surerior.

1. North and North-east shores ; 2. North and North-east shores 5 3. South shore; between Lakes Supe-
from River St. Mary to Pigeon River, | from River St, Mary to Pigeon River, | rior and Michigan. (See Foster and
440 miles. miles, Whitney, op. ci? p. 19.)

Upper Hurontan of Logan. Quarizite, slaty and conglomeratic, | Potsdam Sandstone, transgressive,
Upper Group containing pebbles of jasper and Conglomerate, quartzose, with

. : quartz.
Sandstones, red and white, with Slate-conglomerate.

calcareous shales: trap interstra- Slates, like No. 7.
tified. Quartzite.
Limestone, reddish-white, 120 feet, Mica-slate.
Sandstones, conglomeratic, with red

quartz-pebbles.
Slate, siliceous; Novaciulite.
Slate, chloritic.
@rap, Hornblendic and felspathio,
caring Potsdam Sandstone in

u a r Diorite, alternating with denuded spots.
Jasper pebbles and limestones in- Slate, dark grey, and! green. Dip, ‘Drap-dykes, Hisar
termixed. N.and §. 70°. —

Grit, white, with jasper pebbles.

Veins numerous, containing ores of
copper.

Dykes of diorite, syenite, and por-
phyry, abundant.

Trap, amygdaloidal and columnar,

Taurentian gneiss, 4. Same region nearer Lake Superior.

Limestone, crystalline; on seyeral
horizons, with clay-slate,

Magnetic and Specular iron-ore,
with white quartz.

Lower Group, Hornblende-rock, compact,
qi e Slates, chloritic, talcose,
Slates ee with sandstone Quartzite, felspathic,
sou U ALOTLG Granite, intrusive,
Chert and Dolomite, with specks of
Anthracite. ae
Conglomerate green, with jasper The same section is seen on Chocolate
and quartz pebbles, River and Carp Riyer,

Trap, in conformable bands, on
several horizons,

This series of beds is unconform-

able to those enumerated in the next
column, and is Copper-bearing, Ac-
cording to Hngelmann (Foster and
Whitney, Geol. Lake Superior, Land
District) and Dr. Emmons, the series
may be considered to exist in Arkansas
and New York.

Norway, France.

In Tellenmarken, South Norway, Upper Loire. (See Griner, An-
West Finmark, &c. nales ats Mines, sér. 3. vol. xix, p. 151.)

True succession of the beds unknown, Schists, chloritic, with small beds of
Quartzite or quartz-slate, grey, Tydian stone. : |
splintery, talcose, &e., in thick Conglomerate, quartzose, with peb-

beds, bles of Lydian stone and white }
Mica-schist, quartzose, quartz. |
Gneiss, fine-grained, Sandstone, 4 i
Hornstone, Schist, micaceous, argillaceo-talcose,
Hornstone - porph jassing into | Gneiss,

Jasper. ETO 3 Granite, schistose,

Slates, chloritic, taleose, &e. ‘The 2nd, 3rd, and 4th beds alternate
Cae alternating with with one another, and are trayersed by
h 0,

Diorite, 1000-2500 feet thick, ear ob) Porphyry.

Conglomerate, with quartzose peb- |
bles of red jasper, quartz, and }
slate.

Strike various. Dip about 45°.

Plutonic inyasions numerous.

1862. | MARSH—EOSAURUS ACADIANUS. 53

Batrachian or Amphibian affinities ; and it was observed that, previous
to the year 1844, the evidence of even this low form of reptilian
life during the Carboniferous period was unsuspected by most geo-
logists, and its first appearance upon the earth confidently referred
to the Permian epoch. The author gave a short résumé of the
reptilian remains discovered since that date in rocks of the more
ancient period, especially alluding .to the joint discoveries of Dr.
Dawson and Sir Charles Lyell* and the mére recent researches of
the former geologist.

The remains which form the subject of the present communica-
tion consist of two centra, or bodies of vertebre, which were discovered
by the author in August 1855. Their resemblance in form and
appearance to the vertebre of Ichthyosaurus was considered by him
to be so marked that, at the time of the discovery, he referred them
to that genus. A subsequent and more careful examination and
comparison, though it confirmed his idea of their Enaliosaurian
character, showed some important differences; consequently, as
every endeavour to procure further remains met with no success, he
proposed for the fossil the name of Hosauwrus Acadianus in a short
notice which appeared in the ‘ American Journal of Science ’ for
March 1862, N.S., vol. xxxui. p.278. In a subsequent number of
the same journal a full description was given, illustrated with figures
and microscopic sections of the vertebre.

Locality whence the fossil was obtained.—The fossil was found at
the South Joggins, in Nova Scotia, on the southern shore of the
Chiegnecto Channel, a branch of the Bay of Fundy, in a bed of
argillaceous, chocolate-coloured shale, which forms part of group
Xxvi. in the elaborate section of this formation made in 1852 by Sir
Charles Lyell and Dr. J. W. Dawson.

Mr. Marsh then gave some stratigraphical details respecting the
coal-measures of this locality, noting the more fossiliferous beds and
the principal organic remains found in them.

Osteological description.—The vertebre, as already stated, are two
in number, and when discovered were attached to each othert. Their
uniformity in size and appearance, as well as their collocation when
found, would indicate that they belonged to the same animal, and
were contiguous in the vertebral column. They are remarkably
well preserved, a result of their complete ossification in their natural
state, and of their being imbedded in the peculiar matrix which has
since contained them, and furnished the material for their minerali-
zation. ‘The posterior vertebra, in fact, with the exception of a small
fracture, seems to be nearly as perfect as in its original condition ;
and from it the description and measurements given§ were mainly
taken.

A detailed account of the osteological characters of the fossil was
then given, and the points in which it agrees with, or differs from,

* Quart. Journ. Geol. Soe. vol. ix. p. 58. + Op. cit. vol. xvi. p. 273.
{ See Am. Journ. Science, pl. 1. figs. 1 & 2, n.s., vol. xxxiv.
§ Op. cit. p. 4, &e.

o4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dees;

Ichthyosaurus were particularly described, and contrasted in a table
of the measurements of the vertebre in the two Enaliosaurians.

In the margin of one of the vertebre there is an angular notch,
about a line in depth, which Prof. Agassiz, after a casual examination,
considered to be organic rather than accidental, and to indicate an
inferiority of structure, as a similar character is common in Fishes.
Prof. Jeffries Wyman, on the other hand, regarded the notch as
purely accidental, and the result of a fracture, which has also displaced
the articular pits of the superior arch. He is also of opinion that
the notch would not be sufficiently important, if it were organic, to
affect at all the Enaliosaurian character of the remains.

Microscopie structure.—A microscopic examination of the osseous
structure of these vertebrae revealed well-marked reptilian charac-
ters, which were fully described and compared with the characters
exhibited by microscopic sections of the vertebrae of Ichthyosaurus

and Plesrosaurus.
Comparison with other vertebre.—The author then stated that
the vertebre of Hosaurus, in their biconcave centres, exhibit a struc-
ture which prevails in the class of Fishes, in the Labyrinthodonts,
as well as in a few genera of extinct Saurians, and which is seen in
existing reptiles only in the Geckos and the Perennibranchiate divi-
sion of Batrachians.

Amongst Fishes, the Plagiostomi were stated to possess vertebree
having more in common with those of Hosaurus than others of the
class, but that the latter show a much higher degree of ossification
in all their parts than the former; also that the osseous structure
differs in the two cases, and that these vertebrae do not possess, on
their articular faces, any traces of those concentric rings which so
generally exist on the vertebre of fossil and recent Sharks.

Mr. Marsh also alluded to the persistence of the notochord in the
Paleozoic Fishes, and the incomplete ossification of the vertebree in
Mesozoic species ; also to the general difference in the osseous struc-
ture of these vertebree and those of Fishes. He therefore rejects
that class, and places the Hosauwrus among the Reptiles.

The differences between the fossil in question and reptilian bicon-
cave vertebre, other than those of the Ichthyopterygia, were then
pointed out, the author remarking that in the orders Ganocephala
and Labyrinthodontia of Owen, either the notochord was persistent or
the neurapophyses were anchylosed to the centrum, neither of which
characters is to be observed in Hosaurus. The Crocodilia of the
Secondary formations differ from it in having the superior arch
united to the centrum by suture; and in the only genus of Sauwro-
pterygia whose vertebre resemble it in their proportions (cervical
vertebrae of Phosaurus), the articular faces were flat, or but very
slightly concave.

The characters of the vertebrae of Hosaurus were contrasted at
length with those of Ichthyosaurus, and a very close resemblance
was found to exist between them, especially in their flattened
and subhexagonal form, in their deep and regular terminal cavi-
ties, and in the separate state of the neural arch. The most marked

1862. | MARSH—EOSAURUS ACADIANUS. 55

differences are seen in the absence of costal articular surfaces from
the sides of the centrum, in the deeper concavities at the vertebral
extremities, and in the form and dimensions of the superior arch
in this fossil. It was therefore concluded that the points of simi-
larity between it and the Ichthyosauri, which it most resembles,
clearly indicate that they belong to the same natural group of
marine reptiles, and to the same order; while the differences
which exist between them seem to be sufficiently numerous and
important to authorize the conclusion that they are generically
distinct, as might naturally be expected from the vast periods of
time that separated their existence.

Habits of the Eosaurus.—These vertebre of the Hosaurus, although
the only remains of the genus at present known, are so characteristic
and well preserved that Mr. Marsh considers them sufficient to indi-
cate that the animal, like the later Enaliosaurians, was of great size,
air-breathing, cold-blooded, and carnivorous; that it was aquatic,
and probably marine, inhabiting the sea or estuaries, or, possibly, as
might be inferred from the place of its entombment, the mouths of
rivers flowing into the sea. The flattened form of the vertebree, the
great depth of their terminal concavities, the separate condition of
the neural arch, and its short longitudinal extent at the base, were
stated to be all consistent with the conclusion that the Hosawrus was
capable of rapid progress through the water in pursuit of its prey,
which was probably fishes ; and since it had then, according to our
present knowledge, no superior in point of size, it probably reigned
supreme in the waters of the Carboniferous era.

Chemical examination.—Mr. Marsh observed that a comparison
of the composition of recent and fossil bone is interesting, both in a
chemical and a physiological point of view, and bas already attracted
some attention. As he considered it desirable to add to the limited
data on this subject hitherto collected, he analysed a portion of a
vertebra of the Hosaurus, and the results were given in full.

A preliminary qualitative examination showed the presence of
iron, manganese, copper, alumina, lime, magnesia, potash, soda,
organic matter, and water, as well as fluorine, chlorine, and sulphur,
with silicic, carbonic, phosphoric, and sulphuric acids. The com-
plete separation of these various constituents was necessarily attended.
with some difficulty, and the methods resorted to were therefore
fully described, and a table showing the percentage of each consti-
tuent substance was given.

A nitrogen-determination was made with a portion of the fossil of a
rather different character, which gave -776 per cent. for the amount of
that substance init. This corresponds essentially with the results
obtained by M. Delesse, who has made some extensive researches
on this point, and who considers that the quantity of nitrogen
in fossil bones is, within certain limits, a reliable indication of their
age. The above-mentioned percentage of nitrogen is much greater
than that indicated by the analysis, and was probably due in part
to the substance used in the two cases being somewhat different ;
but part of the nitrogen in the determination may have been derived

56 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 3,

from ammonia, which is sometimes introduced into fossils by infil-
tration. A want of sufficient material prevented fuller investigations
of the organic elements in these remains.

The fossil bones hitherto analysed appear to have been all from the
more recent formations; but it was remarked that the results of
this analysis of a Paleozoic fossil did not differ materially, in most
respects, from those previously obtained by analysing fossil bones
from much newer deposits.

2. Description of ANTHRACOSAURUS RUSSELLI, a new LABYRINTHO-
pont from the LANARKSHIRE Coat-FIELD. By T. H. Huxtey,
Esq., F.R.S., F.G.S., Professor of Natural History in the Royal
School of Mines.

In September last, Mr. James Russell, Mineral Surveyor, of Chapel-
hall, near Airdrie, called at the Museum of Practical Geology to
make some inquiries respecting the probable nature of a fossil (sup-
posed to be a fish) lately brought to light by the workmen engaged
upon the Monkland Iron and Steel Company’s estate, about a mile
from Airdrie and twelve miles east of Glasgow, and found in what
is known as the Airdrie or Mushet’s black-band Ironstone*. I was
at that time absent from London; but Mr. Etheridge, to whom Mr.
Russell described the fossil, strongly advised that a careful drawing
should be made and sent up to London, for my examination. This
was eventually done, and the sketch, faithfully executed in its
general characters, which reached me on the 6th of November, ap-
peared so conclusively to indicate the Labyrinthodont nature of the
fossil, that I at once requested Mr. Russell to permit me to have it
sent up to the Museum for closer examination. Mr. Russell very
obligingly consented to this proposition, and the specimen reached
me in perfect safety on the 27th of November, my interest in it
having in the meanwhile been greatly heightened by the reports
respecting its characters which had reached me from Professor
Rogers, Mr. David Page, and Mr. Armstrong of Glasgow.

A glance at the fossil was sufficient to satisfy me that these reports
had not unduly exaggerated its merits. It exhibited, in fact, the
greater part of the contour of a skull, 15 inches long by 12 inches wide
at the widest part. That the under or palatine surface of the skull
was turned towards the eye was obvious from the numerous stumps
of broken teeth which followed the anterior moiety of its contour ;

* The President has kindly furnished me with the following note respecting
the stratigraphical position of the Airdrie black-band Ironstone :—

‘The fossils described in this memoir were found in, or else close to the ‘ Airdrie
or Mushet’s black-band’ Ironstone, which at this point changes into Coal. Ac-
cording to Mr. Ralph Moore’s published section, this stratum lies about 564 feet
below the topmost Coal-measures, and about 666 feet above the ‘ Moorstone
rock,’ which I believe to be the general equivalent of the English Millstone grit.
The bones were therefore found in the true Coal-measures, far above the Gil-
merton Limestone series (the equivalent of part of the English Carboniferous

limestone, in which Lozomma was discovered), and probably 2000 feet or more
above the horizon of the Burdie House limestone.’

1862. ] HUXLEY—CARBONIFEROUS LABYRINTHODONT. 57

but almost the whole of this surface was obscured by a thick coat
of the matrix, in which were partially imbedded many of the
long and pointed crowns of the teeth. These had been broken off,
and lay not very distant from their stumps, with their points all
directed inwards, towards the middle line of the palate. Their
arrangement was just such as might have been expected if the axes
of the teeth had naturally been turned somewhat inwards, and the
vertical crush of the superincumbent strata, after the fossilization
of the skull, had consequently caused them all to fall inwards as
they broke. The same pressure has produced a slight asymmetry of
the whole skull.

From the proportional size and structural features of the teeth, and
from the general contour of the skull, I concluded this to be a new
genus of Labyrinthodonts ; but in order to make sure of the point, I
proceeded to develope the fossil, from the hard matrix in which it was
imbedded, with much care; removing some of the teeth and, on one
side, even a portion of the bony palate, in order to obtain a view of
those parts, such as the orbits and posterior nares, which would enable
me to decide the question.

The skull, as it now appears (fig. 1), presents almost the whole
of its palatine or inferior surface to view, with the exception of the
right temporal region. Its greatest length, measured along a me-
dian line drawn from the middle of the premaxillary region to a level
with the posterior and external points of its prolonged and broad
temporal prolongations, is 15 inches. Its greatest width, obtained
by doubling the distance from the left posterior and outer margin to
the middle line, is 12 inches. Opposite the great vomerine tusks (d),
the skull measures 5:3 inches in width. It diminishes slightly from
this point to the rounded snout, and gradually increases in breadth
posteriorly to the level of the supratemporal foramina (c), where it
measures about 10 inches in width. Beyond this point it widens
suddenly by about half an inch on each side, and the lateral contours
continue to diverge from hence to a point about 23 inches distant
from the hinder extremity of the temporal prolongations of the
skull. The external contour of the temporal prolongation now
becomes rounded off, and sweeps evenly inwards, until it meets the
internal contour, which appears to be nearly straight. The epiotic
processes are not visible.

In the middle line of the base of the skull, extending as far back-
ward as the level of the posterior part of the supratemporal fora-
men, is the well-ossified basisphenoid, 1:7 inch broad, and slightly
excavated posteriorly. The basisphenoid narrows anteriorly, so that,
at 1:4 inch from its posterior extremity, it is not more than 0:9
inch wide; beyond this point it suddenly widens to form the
lateral processes, like those commonly exhibited by the basisphenoid
of fishes, and then rapidly tapers forward, having, at 2-8 inches
from its hinder extremity, a diameter of not more than 0°25 inch,
and continuing straight and style-like as far as it can be traced,
which is to a distance of about 6 inches from its hinder extremity.

The limits of the vomers cannot be accurately defined ; but they

58 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 3,

are very broad plates, separating the large anterior palatine fora-
mina (a) from the comparatively small posterior nares (6), which are
round apertures, 1 inch in diameter, and 5 inches from the anterior
end of the snout, situated between the vomer, the maxilla, and the
palatine bones on each side. The vomers unite in the middle line
with one another and with the prolonged anterior extremity of the
basisphenoid. Posteriorly they are connected with the palato-ptery-
goid arcade, the separate components of which cannot be accurately
defined. The palatine portion, however, is a broad, flat plate, measur-
ing 3°5 inches between the posterior nares and the palato-temporal
foramen. It is united externally with the maxilla. Internally it
is separated by a narrow interval from the basisphenoid. Posteriorly
it passes into the pterygoid portion, which is narrow and curves out-
ward, beneath the inner contour of the temporal prolongation of the
skull, to be lost about the posterior and internal angle of that region.
Externally the margin of the pterygoid portion is arcuated, to form
the boundary of the palato-temporal foramen. Through this fora-
men the under surface of the upper wall of the skull in the temporal
region becomes visible. The sutures separating the component bones
of this region are not visible ; but on the level of the posterior end
of the basisphenoid it presents an elongated aperture, or supratem-
poral foramen (c), 1:3 inch long by 0-4 inch wide. The long axis of
this foramen is directed obliquely forwards and inwards, and it is
nearer the pterygoid than the external boundary of the palato-tem-
poral foramen.

Although I worked out this region of the skull with extreme care, I
was in doubt whether the aperture in question was really a natural
one, until I cleared away the matrix from the opposite side, and
there found a foramen of quite a similar character, though distorted
by the crushing of this part of the skull.

The premaxillary bones, strong and arched, send back two pro-
cesses from their apposed ends, which run upwards and backwards
in the middle line (in the manner common in Amphibia) towards the
junction of the vomers. As the anterior portion of the vomerine
plate is inclined upwards and forwards, it follows that the most
anterior region of the palate has a somewhat arched roof, as in the
Frog. The anterior palatine foramina (a), included between the
recurrent processes of the premaxillaries, their dentigerous processes,
and the vomers, appear to be about 14 inch long by 1 inch wide; but
it is difficult, from the condition of the fossil, to define their limits
with exactitude.

Thirty-seven teeth, or remains of teeth, are visible. Of these, on
the left side, thirteen are situated in the premaxilla and maxilla, and
three on the palatine bone; while, on the right side, nineteen are
attached to the premaxilla and maxilla, one to the vomer, and one to
the palatine bone. On the whole, the maxillary teeth decrease in
size from before backwards, but not very regularly. The first tooth
on the left side was 1-7 inch long when entire, by about half an
inch thick at the base. The second immediately follows it, and is
somewhat larger. The third, of about the same size as the second,

1862. | HUXLEY—CARBONIFEROUS LABYRINTHODONT. 59

Fig. 1.— Palatine aspect of the skull of Anthracosaurus Russelli.
(One-third of the natural size.)

a. Anterior palatine foramen. d. Place of attachment of left vomerine tusk.
6. Posterior nares. e. Vomerine tooth.
¢. Supratemporal foramen. f. Palatine teeth and alveolar plate.

60 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 3,

is separated from the latter and from the fourth, by spaces about
three-quarters of an inch wide. The fourth tooth, broken short off,
must have been a very large one, being not less than three-fourths
of an inch in diameter at the base. It is separated by a deepish
fossa, 0:7 inch wide, from the succeeding tooth. This, the fifth, is
close to the sixth, and both are small, the base of neither attaining
more than 0-3 inch in diameter. The seventh and eighth teeth,
rather large, are situated at tolerably equal intervals from one an-
other, and from their predecessors and successors, in the interspace
of about 2 inches which separates the sixth from the ninth tooth.
There are marked fosse, as if for the reception of the points of man-
dibular teeth, between them. The bases of the ninth and tenth teeth,
close together, occupy 0:7 inch. They are separated by a space of
about half an inch from the eleventh tooth, and this by a somewhat
smaller interval from the twelfth, which 1s close to the thirteenth.
The bases of these last-mentioned teeth do not exceed 0:4 inch in dia-
meter. The last tooth is nearly on a level with the anterior margin of
the palato-temporal foramen. There is a fossa of nearly the same size
as its base behind it, but no trace of the attachment of any other tooth.

The premaxillary and maxillary teeth on the right side by no means
exactly correspond, either in position or in size, with those on the left.

The tooth nearest the middle line in the right premaxilla is six-
tenths of an inch in diameter, and its base and its several fragments,
when put together, show that it had a length of at least an inch and
three-quarters. The two succeeding teeth are about half an inch in
diameter at the base, and are not more than a quarter of an inch apart.
Then follows an interspace of 0-9 inch, in which I think I can trace
the remains of the attachment of a great tusk. Then comes a large
tooth, 0-7 inch in diameter at the base ; and then four small ones, none
of which exceed 0:3 inch. The crowns of the succeeding teeth are all
broken off, and lie with their points inwards upon the matrix, which
covers this region and obscures their broken roots. None of them,
however, have a basal diameter of more than 0-35 inch, and the last
measures hardly more than 0-2 inch at the base. The anterior of
these teeth are about 1:3 inch in length, while the hinder ones
become shorter, until the last was probably not more than half an
inch long when entire. The right vomer gives attachment to an im-
mense tusk, 0-8 inch in diameter at the base. It could hardly have
been much less than 3 inches long, but it is unfortunately broken
short off. The left vomer presents the surface for the attachment
of a similar tusk, but the tooth itself is entirely detached. There is
not the least trace of the existence of any other vomerine teeth besides
these.

On the left side, the palatine bone, eight-tenths of an inch behind
the posterior nasal aperture, supports a tusk 0-6 inch wide at the
base, which, when entire, was very nearly 2 inches long. The pala-
tine bone is raised up into a ridge, so as to form a sort of alveolar
wall on the outer side of this tusk, and the wall is continued back-
wards asa thin plate of bone directed almost horizontally inwards (f).
At a distance of three-quarters of an inch from the great anterior

1862. |] HUXLEY—CARBONIFEROUS LABYRINTHODONT. 61

tusk, the alveolar plate, the margin of which is excavated in the
interval, affords support to a tooth 0:35 inch in diameter at its base,
and this is immediately followed by another of the same dimensions.
These teeth are about 0:9 inch long.

On the right side, the base of a similar palatine tusk and part of an
alveolar plate are visible; but there are no small teeth, and the tusk
is situated nearly an inch further back than on the left side. But
the alveolar plate extends forward in front of this tusk, and pre-
sents a deep sinus, in which I suppose a tusk corresponding to that
on the opposite side may have been developed. If the sinus upon
the palatine alveolar plate of the opposite side has the same signifi-
cation, it would appear as if there were normally two great palatine
tusks on each side, but that the anterior and posterior of opposite
sides are shed simultaneously.

The fossil was broken into two pieces when it reached me; the
fracture passing obliquely between the third and fourth teeth on the
left side, and through the fourth on the right. The fractured surface
shows the roof of the skull, or rather the snout, and proves that it
was raised into a broad longitudinal ridge, so convex as to be almost
semicircular, about 1:5 inch broad and 0-6 inch above the general level
of the facial bones. From the sides of this convexity, the sides of the
face slope with a gradual curve towards the alveolar margin. The
depth of the skull, immediately over the centre of the maxillary
alveoli, is rather less than one inch. From the centre of a line
joining the margins of the alveoli to the top of the central ridge is a
distance of about 1:9 inch; and in the occipital region the skull is
not deeper: considering its breadth and length, therefore, the skull
is extremely flat.

The teeth are round, or slightly oval in section at their bases,
and throughout the greater part of their length. They taper gradu-
ally to sharp points and become slightly incurved towards their
apices. Their bases are not grooved, but, on the contrary, are marked
by numerous delicate and sharp longitudinal ridges, so that trans-
verse sections appear to be very slightly polygonal. Towards the
apex of the tooth, two of these ridges, an anterior and a posterior,
become more distinctly marked, and, combined with a very slight
flattening of the tooth, give it a double edge.

In one of the anterior teeth, the front face towards the point is
much worn, as if by attrition against one of the mandibular teeth.

Transparent transverse sections of the teeth exhibit a singularly
beautiful and complex structure. The relatively small pulp-cavity
sends off primary radiating prolongations, which pass straight to the
circumference of the tooth, and at a small distance from it terminate
by dividing, usually, into two short branches, each of which gives off
from its extremity a wedge-shaped pencil of coarse dentinal tubuli.
These spread out from one another, and terminate in a structureless
or granular layer, which forms the peripheral portion of the dentine,
and, from the small irregular cavities scattered here and there
through its substance, reminds one of the ‘ globular dentine’ of the
human tooth. An extension of this peripheral layer is continued

62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 3,

towards the centre of the tooth, between every pair of primary pro-
longations of the pulp-cavity. The short secondary processes which
are sent out from opposite sides of the primary prolongations of the
pulp-cavity, give off in the same way, from their ends, pencils of con-
spicuous dentinal tubuli, the ends of which terminate in the inward
extensions of the peripheral layer. The secondary processes of ad-
jacent primary prolongations alternate and, as it were, interlock
with one another, so that the inward extension of the peripheral
layer takes a sinuous course between them. A thin layer of dense
and glassy enamel invests the tooth continuously, but sends no
processes into its interior ; and, of course, under these circumstances
there can be no cement in the interior of the tooth, nor can its surface
be said to be plaited or folded. It will be understood that this de-
scription gives merely the principle of arrangement of the parts of the
tooth: its details could only be made intelligible by elaborate figures.

In Rhizodus and in Ichthyosaurus the principle of construction of
the complex tooth is totally different, the surface of the tooth being
really folded, and prolongations of the cement being continued into
the folds.

Addendum, January 14, 1863.

The Referee, to whom the preceding description of the skull of
Anthracosaurus was sent, has suggested that it is desirable I should
express some opinion respecting the systematic relations and affinities
of the fossil. Iam glad that I am in afar better position to comply
with this suggestion now, than I was when the description of the
cranium was sent to the Society; for at that time I was not in
possession of the valuable evidence regarding the characters of the
vertebral column, which has come into my hands within the last
few days through the exertions of my indefatigable correspondent,
Mr. Russell.

For some years past, I have been acquainted with well-ossified
vertebre and ribs from the Carboniferous formation; but the ver-
tebree have always been devoid of their arches and processes; and
though the ribs presented characters suggestive of their belonging to
a higher division of the Vertebrata than Fishes, I thought it better
to wait for further evidence as to their real nature before giving any
account of them.

More than a year ago, I brought away with me from the collection
of the Earl of Enniskillen, at Florence Court, a remarkable rib and
vertebral centrum. I have seen similar remains in the admirable
collection of Dr. Rankin, of Carluke ; and, more recently, Mr. Rus-
sell has sent me up a number of vertebral bodies of different kinds
from the Airdrie workings. I had every reason to believe some of
these vertebre to belong to Anthracosaurus, and it was with that
conviction in my mind that I ventured to caution the members of
the Geological Society, on the occasion of the reading of Mr. Marsh’s
paper on “ Hosaurus Acadianus,’’* against too hastily concluding that
the vertebral centra, which he had found in the Nova-Scotian coal-

* See anteé, p. 52.

1862. ] HUXLEY—CARBONIFEROUS LABYRINTHODONT. 63

field and then described, were necessarily Ichthyosaurian,—seeing

’ that I had much reason to suspect that they might belong either to
Labyrinthodonts, or to some genus of intermediate characters, be-
tween Labyrinthodonts and Ichthyosaurians.

Within the last few days Mr. Russell has sent me the vertebra of
which an outline-view is given in fig. 2 (one-half the natural size).
It was found in the same bed as that which yielded the skull of
Anthracosaurus, and corresponds very well in size with what one
might expect would be the dimensions of a dorsal vertebra of that
animal. Associated with it on the same slab are several other less
complete vertebre and the remains of two ribs.

Fig. 2.

A. Dorsal vertebra of Anthracosaurus, viewed from behind.
B. Red of the same Amphibian.

A.—a. Body of the vertebra.
b. The longer division of the transverse process, and
e. The shorter division. f. Spinous process.
d. Anterior zygapophysis. g. Neural canal.
e. Posterior zygapophysis.

B.—a. Capitulum. b, Tuberculum.

The body of the vertebra is greatly flattened from before back-
wards, as the subjoined measurements will show. The exposed
articular surface is concave, and a section which I have had made of
a similar vertebral body shows that it was equally concave upon both
sides. The concavity, however, is not conical in section like that of
a fish’s vertebra, but its sides are a little convex, rising slightly, within
the margin. Hence the section of this vertebra has very much the
same appearance as that of Mr. Marsh’s problematical vertebra repre-
sented in the figure which accompanies his paper*.

The contour of the vertebral body is not circular, but is slightly
angulated, so that it would tend to be octagonal were not the place of

* Am. Journ. Science, n.s., vol. xxxiv. pl. 2. fig. 2.

64 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 3,

the uppermost angle of the octagon occupied by the excavated floor of
the neural canal. The short sides of the vertebral body are concave
from before backwards, and in other specimens exhibit a slightly
rugose marking.

The neural arch is very small in proportion to the size of the body
of the vertebra, and its contour is nearly that of an equilateral tri-
angle with a curved base.

The very stout sides of the neural arch are continued upwards
into a strong spinous process, which is broken off a short distance
above its origin and nearly on a level with the upper parts of the
zygapophyses. Of the latter the posterior pair are turned towards
the eye, and are much broken. The hinder face of the right anterior
zygapophysis is visible (at @), and its curved contour is nearly entire.

The transverse process of the right side (the only one preserved)
springs by a long line of origin from the lower part of the neural arch
and from the upper half of the circumference of the vertebral body.
It is greatly flattened from before backwards, and its lower half (c)
ends, at a distance nearly equal to half the diameter of the body of
the vertebra, in a rounded edge, which appears to be complete and
unbroken. The upper half, on the other hand, terminates in an ob-
viously rough and fractured extremity. I conclude from this cireum-
stance, and from the characters exhibited by the proximal ends of the
ribs, which I shall immediately describe, that the upper division of
the transverse process extended much further outward than the lower,
and I have indicated this in the dotted restoration of the left side
of the vertebra.

inch.
Height of body of vertebra .......... 1:6
‘Transverse: diameter! SS Adies 0 3. 0502s 1:6
Tienes 5 seen era pie nt errs 0-47
Heigh tof meuna rarer Sates 0-3
Depth of transverse process .......... 0-8
Thickness of transverse process ........ 0-2

The best-preserved rib is 63 inches long* and half an inch broad,
measured in a direction perpendicular to its length. It is, however,
much flattened from before backwards, so that its thickness does not
amount to more than one-sixth of an inch. The face of the rib is
not flat, but it is somewhat excavated, so that the bone is thinner
in the middle than at the edges. At its proximal end the rib
exhibits a very distinct tuberculum and capitulum. The former
projects, so as to disturb the sweep of the curve of the convex
side of the rib and to convert it for a short distance into a
concavity, and it is abruptly truncated posteriorly. The capitulum
of the rib continues the line of its general curvature for half
an inch beyond the tuberculum, and ends in a rounded ex-
tremity. I presume that the capitulum articulated with the lower
half of the transverse process (c), and that the tuberculum articu-

* The sternal end of the rib is broken off. It was certainly much longer when
perfect, as the rib from Lord Enniskillen’s collection, though more slender,
measures 84 inches along its curve, and still presents a fractured extremity.

1862. | HUXLEY—CARBONIFEROUS LABYRINTHODONT. 65

lated with its upper half, in which case the distance (a, 6) on the
rib would be practically equal to the excess of length of the upper
division of the transverse process over that of the lower.

The skull, a dorsal vertebra, and a rib of Anthracosaurus being
known, I now return to the question, what are the affinities of that
Labyrinthodont ?

The large size of the teeth, the comparative solidity of their bases,
and the complex character of the labyrinthic ramifications of the pulp-
cavity are all characters in which Anthracosaurus resembles the
Mastodonsaurus of von Meyer and Plieninger and its allies, and differs
from Archegosaurus. Whether Anthracosaurus had well-ossified occi-
pital condyles like Mastodonsaurus, or cartilaginous ones such as
were probably possessed by Archegosaurus, does not appear, the
fossil being defective in this region. In the large size of the an-
terior palatine foramina, the extent to which the palate-bones are
united with the maxillaries, in the form of the pterygoidean arch
and that of the basisphenoid, Anthracosaurus is nearer to Archego-
saurus and Dasyceps than to Mastodonsaurus.

But the vertebre are altogether Mastodonsaurian. The vertebrae
of Mastodonsaurus were described and figured in 1844 in the well-
known work of von Meyer and Plieninger, ‘ Beitriige zur Paliaonto-
logie Wirtembergs.’ No fewer than seventeen vertebra were dis-
covered in one slab, together with the skull of this remarkable
Labyrinthodont; another block contained eight vertebrae, belonging
to the same animal, but not immediately succeeding the former ; and
a third slab of stone contained five more trunk-vertebre, besides
three others which were caudal. Dr. Plieninger seems inclined to
think that all these cervico-dorsal vertebrae belonged to one animal:
but even the fact that seventeen vertebrae were found together in one
block, and the existence of caudal vertebra, must be amply sufficient
to satisfy every anatomist of the untenability of the hypothesis that
the Labyrinthodonts were frog-like or toad-like in form.

The trunk-vertebre of Mastodonsaurus are biconcave, and much
flattened from before backwards. The neural arch ends above in a
strong spinous process; there are well-developed zygapophyses, and
the stout transverse processes exhibit a division into an upper longer
and a lower shorter portion. So far they are very similar to those
of Anthracosaurus. The ribs again are strikingly similar to those
of Anthracosaurus, as may be seen by comparing plate 5. figs. 1 & 2
of the work cited with fig. 2, B.

On the other hand, the vertebrae of Mastodonsaurus, according to
Plieninger, presented characters which I do not meet with in An-
thracosaurus. Thus, the articular surfaces of the bodies of the vertebrz
of the Triassic Amphibian are inclined towards one another superiorly,
while those of Anthracosaurus are parallel ; and the upper and lower
portions of the transverse process, which are said by Plieninger to be
separated by a suture, so that the neural arch, with the upper longer
transverse processes, readily separates itself from the body with the
lower and shorter transverse processes, are, so far as I can observe,
perfectly continuous in the Carboniferous Amphibian.

VOL. XIX.—PART I. x

66 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 3,

Double transverse processes, the upper more particularly connected
with the neural arch, and the lower with the body of the vertebra,
are to be found, though the circumstance does not seem to have re-
ceived much notice from paleontologists, in several genera of Sawro-
batrachia, or Salamandroid Amphibians.

In Salamandra maculosa, for example, each cervico-dorsal vertebra,
except the atlas, has, on each rib, a prominent transverse process
inclined backwards ; and all these processes, except perhaps the very
last, are deeply bifid, so as to be divided down nearly to their origin
into two more or less divergent processes. The upper division comes
off distinctly from the neural arch, while the lower arises for the
most part below the level of the upper margin of the articular face
of the body of the vertebra. The transverse processes of the three
or four anterior caudal vertebre are also bifurcated at their ends, and
at the eighth or ninth caudal the transverse processes cease to be
distinguishable.

The proximal ends of the four anterior pairs of ribs are divided
into capitular and tubercular processes of nearly equal length, and
possess a distinct ‘angle,’ whence a process is given off upwards and
outwards*. In the hinder ribs the tuberculum becomes a Little
shorter and more slender than the capitulum. In Plewrodeles Waltli,
the vertebral column and the proximal ends of the ribs resemble
those of Salamandra maculosa, though the division of the transverse
processes is less marked, and the capitulum and the tuberculum of the
ribs are not so deeply separated ; indeed, posteriorly, the separating
cleft becomes almost obsolete. In Huproctes the division of the trans-
verse processes is hardly discernible ; nevertheless there is a rudiment
of the angular processes in the anterior ribs. In other Saurobatrachia,
a groove on each side, indicating an incipient division of the proxi-
mal end of the rib, is not uncommon. In all these cases, 1am not aware
that the single or bifid character of the transverse processes is cor-
related with any notable differences in other parts of the organization.

It appears to me, then, that the characters of the certainly
Labyrinthodont vertebree+ made known by von Meyer and Plie-
ninger, and in the present paper, are in perfect accordance with the
view originally put forward by Professor Owen, that these animals
are more closely allied to the Batrachia than to any of the Reptilia
proper. But I conceive that the affinities of the Labyrinthodonts
are clearly with the Saurobatrachia (and, in some cranial cha-
racters, with the Cecilie), and not with the Anura as was at first
suggested ; and, with every deference to the opinion of so great an
authority on all that relates to the Labyrinthodonts as von Meyer,
T must venture to doubt whether, in any characters, these Amphibia
exhibit a real approximation to the Reptilia.

* Plieninger notes what appears to be a process of a similar character to this
in the ribs of Mastodonsaurus.

+ It does not appear that there is any evidence to show that the vertebra
ascribed to Labyrinthodon by Professor Owen in his paper on the Warwickshire
Labyrinthodonts (Geol. Trans. 1841) are such, while there is much reason to
believe they are not.

-

1862. | HUXLEY—CARBONIFEROUS LABYRINTHODONT. 67

At present we are acquainted with two apparently very distinct
types among the Labyrinthodonts—that of the ArcuEcosauRia (Ar-
chegosaurus),at present known to occur onlyin the Carboniferous rocks,
and that of the Masroponsavuria (Mastodonsaurus, Labyrinthodon,
Capitosaurus, Trematosaurus), which seem to have flourished in re-
markable abundance during the Triassic epoch. Both groups exhibit
the sculptured and polished* surface of the crania, the vomerine and
palatine teeth, the forwardly situated posterior nares, the permanently
distinct epiotic bones, the divided supra-occipital, the three sculp-
tured pectoral plates, the elongated, caudate, salamandroid body, and
the comparatively short limbs and weak feet which are distinctive
features of the Labyrinthodont Amphibia, as well as the more or less
complex ramifications of the pulp-cavities of the teeth, which they
share with Fishes and Ichthyosauria.

But the Archegosauria have imperfectly ossified vertebral bodiest,
while the Mastodonsauria have them thoroughly well ossified, though
still biconcave ; and the Mastodonsauria have double ossified occipital
condyles, which have not been found in Archegosauria.

Of the other distinctions, if such there were, of the two groups,
we know very little. It is true that the Archegosauria had, as von
Meyer has proved, in his splendid monograph ‘ Die Reptilien des
Steinkohls,’ a persistent branchial apparatus and a very remarkable
sealy ventral armature. But what do we know with certainty about
the presence or absence of corresponding structures in the Triassic
Mastodonsauria? Whatever may be the nature of the doubtful
Anisopus or Rhombopholis, it is certain that the African, probably
Triassic, Micropholis was protected by ventral scutes; and until Mas-
todonsaurian Labyrinthodonts are found preserved as favourably as
the Archegosauria have been, I think it will be hazardous to take it
for granted that they had neither ventral scutes nor even persistent
branchial arches.

If we adopt these two divisions and endeavour to range the known
Carboniferous Labyrinthodonts under one or the other,—Archego-
saurus, of course, takes its place among the Archegosauria; and Pho-
lidogaster t, I suspect, must go with it, though its vertebre are far
better ossified, and the condition of the cranial condyles is not known.
Baphetes and Parabatrachus are too little known to justify us in
arriving at any conclusion respecting them; and the like is true of
Loxomma. As regards the Raniceps of Wyman (Am. Journ. of Sci.
and Arts, 1858), the Dendrerpeton and Hylonomus recently discovered
by Dr. Dawson in the Nova-Scotian coal-field, and the new genus
Hylerpeton instituted by Professor Owen, from the same locality, I
do not think we are even in a position to say that they are Labyrin-
thodont, much less whether they have Archegosaurian or Masto-

* Whence the term ‘ Ganocephala’ as a distinctive appellation of the Arche-
gosauria is inadmissible.

+ Itseems to me probable that the vertebral centra of Archegosaurus may really
have been osseous rings, such as are found in embryo frogs and salamanders, and
as persisted in Megalichthys and probably in Rhizodus, and that they have broken
into the separate pieces described by von Meyer in the process of fossilization.

t Quart. Journ. Geol. Soc. 1862.

F2

68 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 3,

donsaurian affinities. Among the many remains discovered by the
zealous research of Dr. Dawson, I do not know that a single specimen
of one of the pectoral plates, so characteristic of all Labyrinthodonts,
has made its appearance. ‘They may possibly have been Amphibia ;
but their skulls, their cycloid scales, and their deeply biconcave,
fish-like, vertebral centra appear to me to indicate a closer affinity
with the Ophiomorpha (Caeciha, Ichthyophis, &c.) than with the
Labyrinthodontia.

Of the unquestionable Labyrinthodonts which occur in the Car-
boniferous rocks, then, Anthracosaurus is the only genus regarding
the vertebral column and ribs of which there is any information ; and
the description and comparisons which I have given seem to me to
necessitate the conclusion that, side by side with the Archegosaurian
type, the Mastodonsaurian type of vertebral organization, hitherto
known to occur only in the Trias*, was well developed in the An-
thracosaurus of the Scotch coal-field. At the same time, the anchy-
losed condition of the neural arches, the supratemporal foramina
(which may, however, be parts of the ‘mucous grooves’ common upon
Labyrinthodont skulls, the floor of which was very thin, or merely
membranous in the temporal region of <Anthracosawrus), and the
strong median convexity of the snout, separate Anthracosaurus from
any known Triassic Labyrinthodont. And though, in the general
form of the cranium and in some other respects, Anthracosaurus has
a certain resemblance to the Permian Dasyceps, it differs as widely as
possible from it in its dentition.

3. On the Tuicxness of the Pampran Formation, near Burnos AYRES.
By Cuarzes Darwin, Esq., M.A., F.R.S., F.G.8., &e.

M. Sovrpgavux and J. Coghlan, Esq., C.E., have had the kindness
to send me, through E. B. Webb, Esq., C.E., some excellent sections
of, and specimens from, two artesian wells lately made at Buenos
Ayres. I beg permission to present these specimens to the Geolo-
gical Society, as they would be of considerable service to any one
investigating the geology of that country. The Pampean formation
is in several respects so interesting, from containing an extraordinary
number of the remains of various extinct Mammifers, such as Mega-
therrum, Mylodon, Mastodon, Toxodon, &c., and from its great extent,
stretching in a north and south line for at least 750 geographical
miles, and covering an area fully equal to that of France, that, as
it appears to me, a record ought to be preserved of these borings.
Southward, at the Rio Colorado, the Pampean formation meets the
great Tertiary formation of Patagonia; and northward, at Sta. Fé
Bajada, it overlies this same formation with its several extinct shells.

In the central region near Buenos Ayres no natural section shows
its thickness ; but, by the borings there made in two artesian wells
(figs. 1 & 2), the Pampean mud, with Tosca-rock, is seen to extend

* Nothing is at present known of the vertebre of Dasyceps Buck/andi, from
the Bunter sandstein of this country. See Memoirs of the Geological Survey of
Great Britain :—The Geology of the Warwickshire Coal-field ; by H. H. Howell,
F.G.S. 1859.

1862. ] DARWIN—BUENOS AYRES. 69

downwards from the level of the Rio Plata to a depth of 61 fect,
and to this must be added 55 feet above the level of the river.
These argillaceous beds overlie coarse sand, containing the Azara
labiata (a shell characteristic of the Pampean formation), and at-
taining a thickness of about 93 feet*. So that the entire thickness

Fig. 1.—Comparative Sections of the Artesian Wells of Barracas
and Buenos Ayres. (Distance 3} miles.)

Barracas. Riachuelo. Buenos Ayres.

the princi-

Level of equi- \
librium of
pal spring

High-water level.

Ist spring .. .

2nd spring.... = 2nd spring.

h ord spring.
4th spring. 245 feet.

drd spring....
4th spring....

=

ky
470 feet.
Thickness at Thickness at
Barracas. Buenos Ayres.
Feet. Feet.
eer, BM DR fj. 22k. ease ck Ped suse Uh- onenemee Se Ah ae ae d7
MEE 555s Uses do So acfacn dein sacs d a sabinher Che dunes ee Pt abi pew Set 51
é. Weryisandyclay <...0.0.-...0.-
d. Dark-bluc plastic clay......-1.:> sssnvie-ivececeveeoet Brey Smisabiese 52
e. Tosca with calcareous nodules
f. Yellow sands, very fine and fluid ................. SS ae 45
So 2S EL Sr ee en EA eee ee oo ee 62
h. Tertiary clay and sandstone (for details see fig.2) 34 ......... 33
k,. Hard sandstone at the bottom of the Barracas
ML RS ey ee ee ae Resa Te Oy aee 43
ky. Very calcareous red clay, becoming more marly
beneath ; bored through to a depth of............ A) £0 225

* The following extract from the Report of the borers relates to this bed :—
** The bed of yellow, fluid sands between 18°60 aud 47"°20 below the ground

70 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 3,

of the great estuarine or Pampean formation near Buenos Ayres is
nearly 210 feet.

Fig. 2.—Detailed Section of the Artesian Well at Barracas.

Thickness
in metres.
hp ANC ard va nraeps ola seecragdomaenie@egansaeed saneeee eee ;
0: Very arenaceOUs Clay | Joc... c.s-donssmar ee eee 8:02
LUG |) SSOP Re PRP OR NR A RAS Sree pe 1:05
{ Blue plastie:clay --aes1 Suet ecm catcnane ee 2:90
d. Tosca with calcareous nodules ...................+- 2:30
é. Yellow sand, very fine and fluid, with quartz-
pebbles and fluviatile shells .............cc0.e00e 28°60
f. Green clay, more or less plastic and calcareous,
with iron-pyrites, marine shells, and nodules
ot iithographicstone: 5.0. 2.1..22 eden eee 20°30
g. Green sand, with shells and quartz-pebbles...... “80
he Shelly: lamestone sic. .<--6. ocssaetasa ie eee 45
ti Calcareous Clay s.cscassssasec- sacs eek ee eee Oe 2-00
&. Shelly sandstone). swass:.-dsce-s< 02s .cee eee see "25
i. Green arenaceous clay ......... Baers i nae 2:00
a: Shelly ‘sandstone 2 .s-stesas. care sae eee ‘30
Pa SPECK EAHBANG sade sso eaisinn AR ce eee eae ‘70
o. Very compact arenaceous clay ..................0+. 2°25
p;, Coarse sandstone: “5 .eke wees senbe sn ceo eee eee 1-40
g. Green sand, very fine and fluid, with quartz-
pebbles andishellson, 055.20 cine. 4 eee ee ee 2°35

This formation rests on various marine beds of indurated green
clay, sand with corals, sandstone, and limestone, altogether 107 feet
in thickness. These beds contain fragments of the great Ostrea
Patagonica, O. Alvarez (?), Pecten Paranensis, and other shells,
apparently the same (but they have not been rigorously compared)
with those enumerated by M. A. d’Orbigny and by myself as found
at Sta. Fé Bajada, as well as at various points on the coast of Pata-
gonia. The already enormous continuous extension of the Pata-
gonian Tertiary formation is thus largely increased. Beneath these
beds a mass of red calcareous clay, becoming in the lower part more
and more marly, containing layers of sand, and of the thickness of
213 feet, was bored through to a depth of 470 feet from the level of

contains a subterranean ascending current, the level of which has not varied by
a centimétre for three years. The level is 0°60 (2 feet over the level of the
wells at Barracas). This bed (‘napa’) is powerfully absorbent. At 68™°30 a
second subterranean current (‘overflowing’) was met, which rose one foot
over the surface of the ground at Barracas. The discharge was about 50 pipes
daily, but the water was salt and undrinkable. At 73"°30 was found a third
subterranean current (‘ overflowing’), which reached with difficulty the level
of the ground. The discharge might be calculated at 100 pipes daily. The
water was very salt, and absorbed that of the first overflowing current. The
great spring was met with at 77"°65.”

As regards the quality and abundance of the water, Mr. Coghlan remarks that
“The quantity of water discharged per hour through a tube of about 44 inches in
diameter, at a level of 6 feet above high-water mark, was 2658 gallons. Its tem-
perature was 21° Cent., and it had avslightly disagreeable taste, from its being
impregnated with salts of lime and magnesia and a small quantity of sulphu-
retted hydrogen.”

1862. | . AUSTIN—SIBERIA. 71

the Rio Plata. This lower mass contained no fossils, and its age
is of course unknown* ; but, I may add, that I saw at two points in
Western Banda Oriental, beneath the marine tertiary strata, beds
of red clay with marly concretions, which, from their mineralogical
resemblance to the overlying Pampean formation, seemed to indicate
that at an ancient period the Rio Plata had deposited an estuarine
formation, subsequently covered by the marine tertiary beds, and
these by the more modern estuarine formation, with its remains of
numerous gigantic mammalia; and that, finally, the whole had
been elevated into the present plains of the Pampas.

4, GrotoeicaL Notes on the Locality in Stperta where Fossit Fisu
and Esturr1a have been found. By C. E. Austin, Esq., Mem.
LC.E., F.G.8. With a Note on Kstuer1a MippEnporFir; by
Professor T. Rurrrr Jonzs, F.G.S.

(Abridged. )

In 1858 I had the pleasure of presenting to the Society some slabs
of fossiliferous shale, containing specimens of the fossil fish men-
tioned by Dr. von Middendorft as having been obtained by him at
Nertchinsk, during his last journey in Siberia, and named Lycoptera
Middendorfii by J. Miller ¢.

The slabs also contain the remains of a number of Estheria,
referred to by Miller as Limnadie§, as well as portions of reeds and
stems of plants, some lignite, and two imperfectly preserved shells
which probably belong to a species of Zimneus, but may possibly be
Paludine. They were taken by me from the bed, zn situ, in the year
1848.

The bed lies about 160 versts south by east of Nertchinsk, at the
base of a cliff from 6 to 10 feet high, extending north and south, and
forming the west or right bank of a small clear stream, called the
Toorga, which flows southward into the River Onon. The bed dips
westward about 25°.

The east bank of this stream, where it flows by the fossiliferous
strata, rises gradually, and extends, above the level of the water,
into a plain, on which conspicuous masses of igneous rocks are dis-
tributed.

At a point eight versts to the south of that where the fossils were
found, an abrupt hill of augite-porphyry rises from the plain to an
elevation of more than 100 feet. Its southern face is composed of
rhomboids cemented together by quartz into one solid mass, and
thus a rock is formed which is not uncommon in the mountainous
districts of Siberia.

* It was supposed by Dr. Burmeister to be Silurian.

+ A. Th. von Middendorf’s ‘Siberische Reise,’ Band i. Theil. 1. Hinleitung ;
Klimatologie ; Geognosie. Fossile Fische, bearbeitet von Johnnes Miller: 4to.
St. Petersburg, 1847. See also Quart. Journ. Geol. Soe. vol. vi. part i1. Miscell.
pp. 45-48.

f Op. cit. p. 262, pl. 11. § Op. cit. p. 261.

72 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 3,

The strata forming the cliff were found, where they were cut
through by a shaft sunk, by the direction of the author, for the pur-
pose of examining their relations and position, to lie in the following
order :—

Ft. in.
1. A small quantity of alluvium between the cliff and the
steep part of the hill.
2. Gravel composed of the detritus of trap-rocks, containing
soft clay and lamine of indurated shale ............ 2 6
3. Gravel of indurated shale in an argillaceous matrix .... 1 6
4. White porcelam-clay: -.)2.cis ie anics cr eclw Gere aes ier 2 0
5. Clay containing pieces of the indurated fossiliferous shale 1 6

About 300 yards to the north of the excavation, where the course
of the stream has a direction from N.W. to S.E., the cliff is higher.
At its base occurs a dome of basalt, which has bent the beds
upwards into the form of a parabolic arch. Immediately above lies
a gravel formed of the rounded detritus of trap-rocks, resembling that
found in the shaft, 6 feet in thickness ; and above this gravel, beds of
indurated shale, in thin leayes, alternate with clay, forming a bed
1 foot 6 inches thick. Above this lies a gravel composed of disin-
tegrated trap-rocks.

The laminz of shale in the thin beds of clay just mentioned re-
semble in substance and colour the fossiliferous strata below, but
they are too disintegrated to contain perceptible traces of fossils.
They are very distinctly seen in the cliff for a considerable distance
to the north, but eventually disappear beneath the bed of the stream,
about one verst to the north of the excavation made to examine
the position of the strata.

The surface of the plain where the igneous rocks are seen seems
to be composed of a detritus formed by their disintegration. It is
bounded eastward by a high ridge of hills rising gradually from the
plain, and extending northward and southward. This ridge is com-
posed of fine-grained granite, and is covered in places with fragments
of lava and scorie. Remnants of metamorphic rocks occur to the
east of this ridge amongst fragments of basalt, and further eastward
ridges of clay-slate crop out with a westerly escarpment.

At the foot of the ridge of fine-grained granite, and about 20
versts south of its southernmost extremity, lies Odon Tchalon, the
‘Variegated Mountain.” The summit of this mountain is formed of
three cone-shaped hills, composed of a very crystalline garnet-
bearing granite, containing abundant nests of yellow topaz and
aquamarine. Beryl and amethyst are also found in it, some of the
latter being very valuable.

The inference it seems most natural to draw, on consideration of
the general position of the strata which appear on the surface of the
surrounding country, and from the dip of their beds, is, that the
garnet-bearing granite of Odon Tchalon represents the nucleus or
centre of this eruption; and that the ridge of fine-grained granite,
commencing immediately to the north of it, and running nearly north
and south, is the line of the eruptive force that formed the Nertchinsk

1862. ] AUSTIN—SIBERIA. 73

ridges, which together compose a branch or spur, or what may be
termed a parallel wave, of the great Daourian chain,

With regard to the age of the fossiliferous strata, some Ammo-
nites and Ceratites were given to me in Siberia, which were said
to have come from the neighbourhood of Yakootsk and the banks of
the Lena. Mr. Etheridge has had the kindness to examine them, and
he assigns the Ammonites to the ‘“ middle division of the Oolites’’*,
and the Ceratites to the Trias. Another Ammonite appears to be the
A. virgatus of von Buch, and is therefore undoubtedly from the Lower
Oolite. The cliffs forming the right bank of the Angara, about 30
versts below Yakootsk, are formed of sandstone containing beds of
coal several inches in thickness. A specimen of Fern taken from
these beds renders it probable that they are of Oolitic age.

Several specimens of Rhynchonella cynocephala, found in what
appeared to be a bed of alluvium near Verchne-oudinsk, and which
are nearly perfect, having still a soft coat of shelly matter, appear to
show the occurrence of the Inferior Oolite there.

The connexion, however, between the shale containing the Fish
and LHstherie and the other fossiliferous deposits is not apparent.
Dr. von Middendorf must therefore have pronounced the former to be
Lias through the evidence which he derived from these fossils. It is
possible that the striped schist found in the neighbourhood of Nert-
chinsk may be a continuation of the same strata in an altered form,
as 1t very much resembles them in many respects.

It may be presumed, from the presence of the fossil fish associated
with Hstherie, and two shells which appear to be a species of Lim-
neus, or possibly Paludina, as well as from the relation of the fish
(as determined by Sir Philip Egerton) to Aspius, that the shale is of
lacustrine origin.

Note on Estoerta Mippenporrit.
By Professor T, Ruprrr Jonzs, F.G.S.

Tus is a well-marked species of that interesting genus of Phyllo-
podous Crustaceans which appears to have its representatives in the
freshwater or brackish deposits of nearly all the great geological
groups of strata, from the Devonian to the existing period.

Estheria Middendorfiit occurs in great numbers in grey shale
found on the River Toorga in Siberia, and was first regarded by Mid-
dendorf as a shell, and then noticed and figured by J. Miller as a Zxm-
nadia (see references in Mr. C. Austin’s paper, above). The carapace
agrees well in its characters with that of Hstheria, both in contour,

concentric ridges, and sculptured interspaces. It is relatively large
among its congeners, recent and fossil, being 3ths of an inch long;
few of the known forms attaining the length of half an inch (ex-
cepting the somewhat Limnadioid Estheria Birch of Australia, which

* The species appear to be Ammonites cordatus and A. planula? ; but the
former resembles in some respects 4. Chamusetti.

+ Described and figured in my ‘‘ Monograph of Fossil Estherze,” Palzonto-
graphical Society.

14 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 3.

is an inch long, and Hstheria striata of the Coal, which is as large).
The valves are frequently (if not mostly) in pairs, closely adpressed,
as if the animals had been suddenly imbedded ; and this is apparently
the case on the several planes of bedding which their abundant
presence makes so readily apparent in the fissile shale. Rarely,
however, are the valves perfect; their tenuity and a slight lateral
shift, which oblique pressure has given them, have led to their being
crushed and wrinkled, and the two separated faces of a bed-plane
divide unequally between them concentric portions of the light-brown,
glossy, thin, corneous valves, The umbones are usually wanting.

Putting aside the wrinkles (mechanically formed) that affect the
carapaces, we see, with a low power of the microscope, a delicate,
raised reticulation between the concentric ridges, the meshes often
passing into irregular, anastomosing riblets, perpendicular to the
ridges. The usual ornamentation of Estheria is some reticulate
sculpturing of the interspaces between the ridges; and this is not
unfrequently modified by passing into vertical riblets: still, different
patterns or modifications are recognizable in the several species of
Estheria; and the bold freedom of the delicate reticulo-linear orna-
ment in this case differs from all the other patterns that I know of.
The carapace of #. Middendorfic approaches in general appearance
that of H. Dahalacensis (Durckheim), from the freshwater marshes
of Dahalae, off the coast of Abyssinia, and found also in stagnant
water on the banks of the Tigris by the late W. Kennett Loftus ;
and the reticulation of the two species would be similar, did it not lose
itself in riblets in the former. Though the carapaces seem to have
been, at least in many instances, imbedded whole, yet they do not
appear to contain any limbs or remains of the body, with the ex-
ception, in one or two individuals, of what may be ova; these are
numerous little globular bodies, occasionally somewhat crushed, and
about 54th of an inch in diameter.

The slightly indurated condition of the shale gives it a modern
appearance; but there is a want of collateral evidence as to its
geological age, excepting in the case of the little Fish that occurs in
considerable abundance in the deposit, both with and without the
Estheria. This Fish is termed Lycoptera Middendorfiu by J. Miller ;
but Sir P. Egerton informs me that he has no doubt of its being
either an Aspius or some closely allied genus. -Aspzus (a Cyprinoid)
is found in some Miocene freshwater strata in Europe.

LIimneus seems also to have been found with the Hstheria, both
by von Middendorf and Mr. C. Austin, as well as a few fragments
of Insects and some remains of Plants; and hence there is here, as
in most other fossil occurrences of Estheria, every reason to believe
the deposit to be of freshwater formation.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.
POSTPONED PAPERS.

On some Fosstzt Crustacea from the Coat-MEAsuRES and Devonian
Rocks of British Nortn America. ByJ. W. Satter, Esq., F.G.S.,
A.L.S8., of the Geological Survey of Great Britain.

[Read May 21, 1862*.]

Dr. Dawson, so well known for his researches in the Coal-measures
of Nova Scotia, has entrusted to me several fragments of Crustacea
from the Coal-measures and Devonian rocks of that region for
description. These form a most welcome supplement to the late
discoveries in Scotland, recorded in the last volume of the Society’s
Journal}, which Dr. Dawson could not have seen when he kindly
sent these specimens for examination.

Accompanying the Crustacea, there are eight specimenst of other
fossils, of which three are shells (see further on, p.80) agreeing
closely in character with some from our own Coal-measures, and
tending to confirm, if proof were needed, the age of the Crustacean
fragments. They are numbered by Dr. Dawson from 1 to 5.

Of these, No. 1 is most probably the abdomen of an Isopodous
Crustacean, and is from arich plant-bed in the Coal-measures of the
Joggins, Nova Scotia. No.5 is part of a large species of Hurypterus,
also from the Coal-measures. Nos.3 and 4 belong to a small species
of Eurypterus, a genus already well known in the Devonian. They
are from St. John’s, New Brunswick.

Of No. 2, from the Devonian slate of St. John’s, I know no
analogue, and can only guess that it has some relation to the Sto-
mapods. It is well preserved, however, and there can be no doubt
of its general structure. I have here called it Amphipelts.

I am obliged to propose new generic terms for some of these
Crustacea, even though the specimens are imperfect. I will describe
the large Devonian species first.

AMPHIPELTIS » gen. Nov.

Carapace oblong-oval, rounded in front, and more truncate be-
hind, with a thorax of (probably) nine segments, five of which project
beyond the carapace, and four are concealed beneath it. Tail-piece

* For the other communications read at this Evening-meeting, see Quart.
Journ. Geol. Soc. vol. xviii. p. 331.

T Vol. xviii. p. 528.

+ All the specimens noticed are in the Colonial Collections of the Museum of
Practical. Geology, except Nos. 1 and la, which have been returned to Dr. Daw-
son’s cabinet.

76 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

semicircular, as wide as the abdomen, and as long as the last three
segments taken together.

AMPHIPELTIS PARADOXUS, spec. nov. Fig. 11.

The length of the carapace is fully ? of an inch ; its breadth some-
what less. Itis gently convex in the middle, and, if the appearance
be not deceptive, it has the central area subtriangular and raised
above the flattened sides. But I can see no trace of definite orna-
ment on the surface, nor any eyes. The margin shows a minute
serration. Beneath the carapace the thorax-rings, four in number,
are very narrow at their origin, but they attained their full width
before leaving the shield; and the hinder seven rings are all about
dan inch broad, smooth, or with scattered punctations, and regularly
arched from side to side. The pleura are somewhat oblique, bent
backwards, and a littlerounded at the tips; they are not distinguished,
except by the remote fulcral point, from the broad axis.

Looking for the analogues of this fossil among recent forms, one
is obliged to neglect the whole of the Isopod order, on account of
the great size of the carapace in the fossil before us. This becomes
a point of agreement with the Phyllopoda, to some of the Apodoid
forms of which there is a general resemblance ; the few segments
of the body do not prove otherwise, since in the Paleozoic forms of
the group (Ceratiocaris, é&cc.) the number is much less than in the
recent forms. But the expanded, broad shape of the segments is
unlike that of any Phyllopod. Again, although the recent Apus
productus has a large, spatulate, terminal joint (other species have a
short notched one), yet the great caudal styles are much more im-
portant than the telson. These styles, however, in the Paleozoic
forms are always elongate, sometimes greatly so; and hence, if
Amphipeltis be a Phyllopod, it is of a group yet unknown, and should
form the type of anew family. I should prefer comparing it (as Dr.
Dawson did in his letter to me) with the Stomapoda ; among these,
Squillerichthys and Erichthys have a large caudal shield, but their
carapace is both angular and spinose. I confess I am not at all
_ satisfied with this analogy, but consider it at all events preferable
to that of the Phyllopoda.

Locality. Devonian rocks near St. John’s. Fragments of a Fern
and of a Cardiocarpum occur here on the same slab of black glossy
slate. These plants have been described by Dr. Dawson, Quart.
Journ. Geol. Soc. vol. xviii. pp. 296, &e.

DieLostTyLvs, gen. nov.

Carapace unknown. Body-segments (in number —?) arched,and
with minute pleura. Tail-segment large, triangular, spinose, with
two pairs of simple, ovate appendages.

It was not till I had tried hard to find analogies with Squilla that
I could persuade myself that this was not the abdomen and tail-flaps
of a Crustacean allied to that genus. The shape, ornaments, and
spines of the broad telson cannot fail to remind the observer of
Squilla (fig. 8); andif I could have believed that the palettes (fig. 6a)

SALTER—BRITISH NORTH AMERICAN CRUSTACEA. 77
were portions of a concealed, three-jointed appendage, this analogy
must have been received. But the more the specimen is studied, the
more clear it is that there are two pairs of appendages attached (one
pair to the sides, another near the tip) to the terminal joint. Squilla
and its allies, like all the higher Crustacea, have, of course, no ap-
pendages to the broad telson. And for the same reason, the affinity
of Diplostylus with the Macrura is out of the question.

But when reference is made to the Jsopoda, the resemblance is
much greater; and none are better suited for comparison than
Spheroma (fig. 7), which has a large, tuberculo-spinose, terminal
joint, and a two-jointed, palette-shaped style on each side. In
Spheroma the appendages are higher up on the sides; in Serolis
they are nearer the apex.

But in no case that I have yet seen or heard of, among Isopod
Crustaceans, are there two pairs of appendages to the last joint.
The Jsopoda have all a single pair only*.

Dirtostytus DawsonI, spec. nov. Fig. 6.

The portion preserved consists only of five rings and the broad
telson ; and these together are # of an inch long, and less than } an
inch broad at the widest part. The telson is somewhat narrower
than the body-rings, broad above, and pointed behind, where it is
notched into three spines, the centre one very short, the two on
each side of it broad, and on their outer sides covering the attach-
ment of two small obovate palettes. These palettes are a little oblique,
narrower than their length, rounded at their posterior margin, and
striated distinctly. Outside these, and much higher up on the sides,
are a pair of broader notches, which give origin to a pair of small
palettes, ovate and not broader at their ends, and striated obliquely.
And above the insertion of these are a pair of broad, flat spines on
the surface of the tail-joint.

The body-segments are transverse, the axis not much distinguished
from the short, pointed, recurved pleura; with a narrow, articular
furrow, and strongly punctate on the exposed portions. The puncta-
tions (in the hinder segments only) are overhung by short plications:
such punctations are observable in many Isopod Crustaceans.

Locality. Coal-measures of the Joggins, Nova Scotia, in a plant-
bed in the middle of the series.

Having looked in vain for a similar pygidium among the large-
tailed Isopods, and consulted Mr. Spence Bate with a like result, he
referred me to a group of parasitic Amphipods (the Hyperina), among
which there are a few formsy (such as fig. 12) with tail-segments
coalesced and bearing appendages. These show a sufficient resem-
blance to warrant our referring Diplostylus provisionally to the

* Lest it should be thought I had overlooked their occurrence, I may mention
that there is sometimes a pair of moveable spines at the extremity of the tail-
joint in Sguzl/a, which might represent the terminal palette-like styles. Still
this would not account for the lateral appendages ; and I do not think there is
any real relation to Sguzila.

t Anchylomera, Typhis, Brachyscelus, &c.

78 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Amphipod order. I am very much obliged to Mr. Bate for this
analogy (which would certainly have escaped me in Milne-Edwards’s
work). Mr. Bate’s late papers on the Amphipods (Ann. Nat. Hist.
1861) admirably illustrate this peculiar group.

EURYPTERUS PULICARIS, spec. nov. Figs. 9, 10.

This minute form (sent under the name of “ Stylonurus or Eury-
pterus”’ by Dr. Dawson) can only be compared with such species as
I have described and figured in the 15th volume of our Journal.
The small Z. pygmeus (op. cit. p. 232, pl. 10. figs. 5, 6) resembles
our species in size; but the tail-joint, fig. 18 (Z. abbreviatus), figured
from the Downton Sandstone (Uppermost Ludlow Rock), is the
nearest in point of shape.

The tail-joint is a characteristic portion, and is sufficiently pre-
served in the specimen from Nova Scotia to show that it is a distinct
species from the British one. I hope that better material will soon
occur to Dr. Dawson’s search. The entire length of the more per-
fect specimen (including nine body-joints and the telson) is less than
4+ an inch. These nine body-joints taper rapidly backward, from
ith of an inch to quite a narrow base in the penultimate joint above
the telson. The telson is broader than the penultimate joint, swelling
rather rapidly from its origin, and then suddenly contracting into
the serrate tip.

Locality. Devonian rocks; St. John’s, New Brunswick. Dr.
Dawson desires me to add, that the rare Devonian forms from near
St. John’s were collected and given to him by Messrs. Matthew,
Hartt, and Payne, of that city.

Evryrrertvs ; a large species allied to H. Scouleri, Hibbert. Fig. 5.

A mere fragment of a large body-ring, which nevertheless indicates

a species nearly as large as the great Scotch Hurypterus (E. Scouleri,
Hibbert).
' The large “ teardrop-tubercles’’ along the hinder margin suffi-
ciently show the nature of the ornament. These, in all probability,
were replaced by spines on the carapace, as in our own Coal-mea-
sure species (to be described in a succeeding paper).

The carbonaceous film which remains in part on the surface,
cracked (by shrinking) into minute areole, represents evidently a
corneous substance, from which the animal matter has been dissolved
away. The suggestion of Professor Huxley, that the large Hury-
pteride had a thick crust like that of Limulus, with but little cal-
careous matter, is most probably true.

Locality. Coal-measures ; Port Hood, Cape Breton.

Evryrrervs (?), tail of. Fig. 4.

This small specimen, found with the Diplostylus in the Joggins
plant-bed, has evidently nothing to do with that genus. It is im-
perfect, but can hardly be supposed to be other than the caudal joint
(broken) of a Eurypterus or allied form. It is, as usual in that
genus, contracted at its origin; but swells out afterwards, in the

SALTER—BRITISH NORTH AMERICAN CRUSTACEA. 79

Figs. 1-12.—Fossils from British North America.

CoAL-MEASURES,

. REE
S 2 Z > Y

Aa

Fig. 1. Anthracomya elongata. Fig. 7. roma. re
: 2. Natadites lone § Gain } outtines.
3. Anthracoptera carbonaria. 9,10. Eurypterus pulicaris.
4. Eurypterus, tail of : nat. size. ll. Amphipeltis paradoxus.
3. Eurypterus, sp. 12. Tail-piece of Typhis (recent).
6. Diplostylus Dawsoni.

80 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

manner of the tail-joint of Slimonia (Pterygotus) acuminata. (See
Quart. Journ. Geol. Soc. vol. xii. p. 28.)

There are no surface-markings nor marginal serrations.

Locality. Coal-measures ; Joggins, Nova Scotia (cabinet of Dr.
Dawson).

While dealing with Crustacea of the Carboniferous rocks, I may
be permitted to make a correction in reference to my last paper*,
and to alter the term Paleocrangon to Crangopsis. I had overlooked
the fact that the term “‘ Paleocrangon” was applied to the small
Isopod Crustacean in the Permian rocks described long ago by
Schauroth (see Quart. Journ. Geol. Soc. vol. xii. p. 214). It is true
my correspondent, Mr. Kirkby, would replace that name by a more
satisfactory term, as Palewocrangon suggests a wrong affinity. Most
naturalists, however, are agreed that a generic name once given is
entitled (like a specific one) to priority, unless utterly erroneous in
meaning, or accompanied by a manifestly imperfect description.

Fossil Shells from the Coal-measures of Nova Scotia.

I have added figures of three species of shells sent to me by
Dr. Dawson. They are from the Coal-measures, and are specially
interesting as being the genera common in our own Coal-deposits,
and which I cannot but regard as of marine origin. There are three
species, which I find Dr. Dawson has named respectively Naiadites
elongatus, NV. carbonarius, and NV. levis, in the Supplementary Chapter
to his ‘ Acadian Geology.’

The first and last are species of a genus which I have described
and figured as Anthracomya in the Memoirs of the Geological
Surveyy. They are thin equivalve shells, wider behind, and with a

byssal ?) sinus on the anterior ventral edge. A wrinkled epidermis
shows that the animal probably had a closed mantle and respiratory
siphons; and the ligament is external, as in Panopea, which is
essentially one of the Myade.

As Dr. Dawson had only proposed the name Nazadites without
description, perhaps these shells may be allowed to retain the name
I have giventhem. The Anthracomya (Naiadites) levis (fig. 2) is, I
believe, identical with a shell from the Upper Coal-measures of
Manchester.

For the second species, however, WV. carbonarius (fig. 3), no generic
name has yet been proposed, though Professor King had long ago
noticed the genus (Ann. and Mag. Nat. Hist. Jan. 1846, vol. viii.).
It includes the so-called Myaline. Nor can they be described as
species of Dreissena,as has been done by Herr Ludwig, in his recent
descriptions of Coal-fossils in the ‘ Paleeontographica,’ vol. ix.

Meantime, until Professor King or myself describe some of the
Coal-fossils of this group, I shall employ the name Anthracoptera
for these triangular shells. They are abundant in our Coals.

* Quart. Journ. Geol. Soc. vol. xvii. p. 533.
t “ Iron-ores,” 1861, p. 229, pl. 2.

SALTER—-EURYPTERUS. 8]

On some Species of Evuryprerus and Allied Forms. By J. W.
Satrer, Esq., F.G.S., A.L.S., of the Geological Survey of Great
Britain.

[Read May 21, 1862.]

Since the appearance in 1859 of the memoir by Prof. Huxley and
myself on Pterygotus and its allies, the great work of Prof. Hall, of
Albany, has appeared (‘ Paleontology of New York,’ vol.iii.), containing
the fullest material for the illustration of this genus ; and following,
as it did, upon the very full account given by Dr. Wieskowski,
it has completed our knowledge of the structure of this remarkable
genus. And there seems to be now no doubt whatever that the ano-
malous plates and processes about the position of which Prof. Huxley
and myself were compelled to guess, and which for many obvious
reasons were compared with the under portion of the head, really
belong to the under part of the thorax.

All this was as satisfactorily made out by the Russian author as by
Prof. Hall’s independent researches. We had also arrived at the
same conclusion before Wieskowski’s admirable paper reached us.
For previous to the Meeting of the British Association at Aberdeen
in 1859, I was sent by the Director-General of the Geological
Survey to examine the collections made by Mr. Simon, of Lesma-
hago; and in that fine series (which was sent to the Meeting for
exhibition) we found abundant proofs of the true position of the
sternal plates, such as Wieskowski and Hall have figured, and of the
place of the post-oral plate, previously assigned by Prof. Huxley to
the hinder margin of themouth. The position of the chele in these
new specimens also confirmed the Professor’s judgment in assigning
them to the antennz or antennules; and they supported my own
view too as to the existence of three pairs of appendages to the head,
exclusive of the chele and the large swimming-feet, which are also,
as we learn from the new and more perfect specimens found both in
America and Russia, included with the appendages of the mouth.

The chief new points, I take it, in Prof. Hall’s beautiful series are,
first, the larger number of joints in the great maxillary appendages
than was supposed from analogy with Pterygotus, where there are
certainly only seven; and secondly, the existence of ocelli on the
dorsal surface of the shield, such as give it a wonderfully limuloid
aspect. But some of the Copepoda have similar ocelli; and as to
the affinities, it would be out of place in every way to give my
opinions, when the naturalist is by who first truly studied these
relations. Whatever corrections better specimens may have led to,
the main credit is due to him who from fragmentary materials con-
structed a true hypothesis. The business of the paleontologist—
half-naturalist, half-geologist—is to collect, arrange, and describe the
material, giving to and receiving from both naturalist and geologist
all the aid he can.

The kindness of some friends in Scotland has lately enabled me
to examine, for the purpose of description, the rare Crustacea, from
the Glasgow coal-field, published in the last volume of in Society’s

VOL. XIX.—PART I.

82 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Journal*. Immediately after, others exerted themselves to obtain
for us the loan of the great Scotch Hurypterus, made so famous by
Dr. Hibbert, and which was found, not in the Coal proper, but in the
Carboniferous Limestone of Linlithgow.

No sooner had the Scotch Hurypterus been taken in hand, than I
found a new one in our own Coal, almost as large. A friend in
Staffordshire sent me a unique form from the coal-measures of
that district, the remarkable spined Hurypterus described below.
A new Shrimp turned up from the Millstone Grit of Yorkshire, under
the hammer of the well-tried Collector of the Geological Survey,
Richard Gibbs. A beautiful Crustacean, illustrating new points in
the Paleozoic history of the class, came to light in Dumfriesshire ;
and, while considering what to do with all this material, Dr. Dawson
of Montreal sent me his Carboniferous and Devonian novelties to
describe for the Society.

Evryptervs Scouteri, Hibbert.

Eurypterus Scoulert, Hibbert, Trans. Roy. Soc. Edinb. vol. xii.
p. 179, pl. 12. figs. 1-5; Etdothea, Scouler, Cheek’s Edinb. Journ. of
Nat. and Geograph. Science, vol. iii. p. 352, pl. 10.

For an opportunity to examine this fine head, long ago described
by Dr. Hibbert in the ‘ Transactions of the Royal Society of Edin-
burgh,’ I am indebted to Mr. James Smith, of Jordan Hill, Glasgow,
and Dr. Rankin of that place. It was kindly lent me by the
Council of the Andersonian Institution for a fresh description and
figure, that of Dr. Hibbert being incomplete. The large carapace
is all but perfect (a portion of the right side only being absent), and
in its natural condition uncompressed ; so that the great convexity
of the form is manifest. The carapace and the two front body-
rings (preserved so as to show both their dorsal and ventral surfaces)
are retained in this specimen, attached to one another; and, bent
upward beneath it, is a large fragment of a swimming-foot, con-
sisting of the first four joints, all imperfect.

The dimensions are as follows :—Carapace, forming more than a
quarter of a sphere, 43 inches long by fully 6? broad, and the con-
vexity such as to follow the shape of the body-rings, which are
43 inches broad and 3 inches deep from back to front. The greatest
convexity is in the region behind the eyes, which are placed, not
quite halfway up the head, near together, only an inch and a quarter
apart. They are divided from each other by a pair of inflated tri-
angular lobes, with a small central process lying in the deep hollow
between them. This central prominence, the round approximate eyes,
together with the rough, hirsute, spinous character of the convex
region behind the eyes, give the whole head much the appearance of
a deformed human countenance.

The outline of the carapace is about two-thirds of a circle, the
short, broad, spinous ears being curved inwards, not outwards; and
the posterior edge is only gently arched. A very distinct depression
indents the front, but does not affect the actual anterior margin.

* T have, however, since seen another fragment in the Hope Collection at Oxford.

SALTER——EURYPTERUS. 83

The round prominent eyes are also set in depressions, which run
from them ina curved line to the inner margin of the broad posterior
spines on each side, and thus enclose the convex, semicircular space
which, lying behind the region of the eyes, is covered with thick-
set spinous squame. Another deep triangular indentation lies
between two thick lobes, diverging backward, which separate the
eyes; and, as these lobes are much swollen, the depression is really
greater than any of the others. In the midst of it lies a short, tri-
angular, prominent mass, broken in our specimen. Above, in front
of this depression, is a slight boss (which would very probably be
the place of the minute stemmata, were they preserved); but there
are no wrinkles nor elevations of any kind in front of the eyes.
The whole surface is evenly convex, divided by the semicircular
furrows from the rugose portion behind the eyes, as above men-
tioned. The margin is narrow, thickened, and raised all round.
The ornament of the surface is minute in front, and consists of small
prominent tubercles, with minute granules between them; further
down the sides the tubercles become triangular squame, with others
interspersed ; and these squamee become larger and larger towards
the ears (with raised borders and generally a strong central tubercle),
and attain their largest size on the posterior area, where they are
also narrower and more pointed, as well as stronger, than elsewhere.
On the extreme hinder border they become linear ridges; and in
this form they also occur on the free edges of the body-segments.
The crust is not thick; and the squame, except in the largest,
appear to be more convex and prominent beneath the crust than
above it, so as to indent the cast. This is particularly the case with
the smaller squamz, which are so concave above as to be truly convex
below : the margin shows this conspicuously (fig. 5) ; and wherever
the surface has been abraded or weathered, the hollows are much
deepened and exaggerated.

The body-rings have a great convexity, as above stated; the two
anterior rings are very short, not more than half an inch long even
in this large specimen. On the under side they expand into
the broad sternal flaps so characteristic of this family of Crustacea.
One of the swimming-feet is preserved. The basal joint is either
very small, compared with that of Pterygotus, or is imperfect.
The shape of the other three is not well defined; but they are
evidently thick, carinate at the edges, and have the usual triangular
or wedge-like shape alternately in the lower joints.

In Dr. Hibbert’s description of Hurypterus Scouleri, he says
(p. 281):—“The Eurypterus Scowert is to be distinguished from
other species by the prolonged eminences intervening between the
eyes, which, at their apex, form an angle wherein appears a central
tubercle; also by the small, acutely angular protuberances, like spines,
which are diffused over the surface of the head beneath the eyes. The
characters of the feet cannot be given, as no vestiges of them, except
very slight ones, have turned up.” In truth, there is no known spe-
cies with which it can be confounded, nor any approaching it in size.

Hall’s beautiful specimens have enabled him to show, what was

G 2

84 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

not clear in any figures before, that Hurypterus had more than seven
joints in the limbs.

I would gladly have given a natural-sized figure of this fine fossil,

Figs. 1-8.—Mew Species of Kurypterus.

Figs. 1-7. Eurypterus mammatus, natural size.
8. EL. (Arthropleura) ferox, natural size.

had the arrangements of this Journal permitted it. I hope to figure
it at some future opportunity.

Localities. Carboniferous Limestone of Kirkton, Bathgate; and
also in Upper beds of Old Red Sandstone, at Kiltorkan Hill, Kil-
kenny. (See Quart. Journ. Geol. Soc. vol. xv. p. 282, pl. 10. fig. 3.)

SALTER—-EURYPTERUS. 85

On the general characters of the species here described, it is to
be observed, first, that von Meyer evidently thinks Z. Scouleri should
be regarded as a new type, distinct from Hurypterus, and that
Scouler’s old name, Hidothea, should be restored. Its great size (fully
1} foot long), round convex carapace, the processes between the
eyes (to which might be added their approximate position), and the
large sculpturing seem to him sufficient to distinguish it. These are
certainly good characters; and, if we only knew more of the species
of the genus, I should be disposed to unite in this opinion. But very
few of the known species show enough to decide that ornamentation,
or a slightly different position of the eyes, is accompanied by positive
characters in the other parts, so as to warrant the distinction. I
should say the same of his proposed genus Adelophthalmus; for
scarcely enough is left of the carapace to prove that it had no eyes,
on which character the genus is founded. <Arthropleura is probably
distinct ; but as the known specimens have neither a whole carapace,
nor eyes, nor appendages, it would be premature to separate it gene-

rically.

Evryprervs (ARTHROPLEURA ?) MAMMATUS, Sp. nov. Figs. 1-7.

I have fragments of the head, of the lateral portions of the body-
segments, and parts nearer to the tail, but not of the central surface
of the carapace, of the eyes, nor of the appendages of this species.

The first fragment occurred to the Collectors of the Geological
Survey, when they were breaking the rubbish of the mine-tip from
Pendleton Colliery, Manchester. Others were obtained afterwards by
Messrs. Gibbs and Rhind; and the exact bed proves to be the
«Ferny Metal,” under the “ Big Coal” or “‘ Rams Mine.”’

In this bed many plants are found, viz.,

Lepidodendron obovatum. Neuropteris gigantea.

Sternbergii. Cyclopteris flabelliformis.
elegans. Sphenopteris obtusiloba.

Neuropteris Loshii. latifolia, &e.
heterophylla. |

The bed lies rather high in the “‘ middle coal” series.

The lateral portions (fig. 1) of the head of this large Crustacean,
which must have been at least 8 or 9 inches broad, show a strongly
arched border, running out into a short, acuminate, broad spine,
into which a strong, curved, sharpish ridge runs from about the
upper central portion of the head (probably from the eye itself).
The space outside and above this ridge is flat, and is covered with
prominent squame ; beneath it the surface is tolerably smooth and
concave, until near the hinder border, at a short distance within
which at least six (and probably more) large, mammillated, tuber-
cular spines are ranged in a tolerably even line. They are directed
backwards, and are full a third of an inch in length, and as much
in diameter, at the swollen base. Another portion of the head
(fig. 2) shows large and small tubercles instead of squame. Then we
have a fragment (fig. 3) which I suppose to be the hinder margin of
the head, with the first body-segment, showing one or two of the

86 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

‘“‘tear-drop’”’ ornaments characteristic of Huwrypterus. Such have
been figured in my monograph of the genus, Quart. Journ. Geol.
Soc. 1859, vol. xv. p. 229, pl. 10. figs. 3, 11, 12.

The remaining pieces are evidently parts of a great Crustacean,
and almost certainly belong to this one; for they have the same
ornaments on the hinder edge; but they differ remarkably by having
a curious set of short, wavy, interrupted ridges (or furrows,—it is
impossible to say which), lying transversely to the length, and which
are equally distributed over the whole segment. They are not all
of the same size, small rounded ridges being mixed with those of a
more linear shape. On some of these body-segments (figs. 4 & 5)
large spines occur on the hinder edges; and these I suppose to have
been the rings nearest the head. On others a large spine is rare, as
fig. 6; and on fig. 7, which was probably nearer the middle of the
body, only the linear “ tear-drop ” ornaments are present.

Locality. Pendleton Colliery, near Manchester. In the “ Ferny
Metal,”’ beneath the ‘‘ Seven-foot Coal” or “ Rams Mine.”

Although I have supposed figs. 1 and 2 to belong to the head,
I have really little else to recommend this view than the great com-
parative size and breadth, and the general form, which is like
that of the hinder angles of the head of the Scotch Hurypterus. If
the original figure, given by M. Jordan (‘ Paleontographica,’ vol. iv.
pl. 2. figs. 4& 5, p. 13), of the Arthropleura armata be consulted, a
somewhat similar piece, having a similar arrangement of tubercles,
will be seen to occur in contact (not joined) with a fragment, which
would make the pointed portion more like the pleuron of a trilobed
segment. I do not believe this is the case, but still itis worth while
to call attention to the circumstance. M. Jordan evidently does not
know to what part of the animal he is to refer this plate; and as it is
not certain, according to his own showing, that the two portions of
his fig. 5* belong to the same piece, while in his fig. 4 there is a
large plate like a carapace connected with tubercular body-rings, I
think we may interpret our own fragments without reference to the
Saarbruck fossil, except to identify the genus. The authors von
Meyer and Jordan have failed to give a generic character, and, in
the absence of any proof that it is distinct from Hurypterus, I do
not feel justified in referring the British fossil to any other genus.

The fragment next described carries still further the strange
ornamentation with spines and tubercles, and may belong to a
distinct genus.

EvurypTEervs ? (ARTHROPLEURA) FEROX, sp. nov. Fig. 8.

A fortunate blow of Mr. Charles Ketley’s hammer has yielded one
of the most curious Crustacean fragments on record. He found it
in the Staffordshire Coal-measures, at Tipton, and states that it
came from the shale over the “ Thick Coal.” Abundance of coal-
plants were with it.

At first sight, 1t would strike an entomologist as a fossil caterpillar
of the Saturnia genus, so strong is its resemblance in size, form, and

SALTER—-PELTOCARIS. 87

ornament to the larve of that group. Unlike most Crustaceans*

from the old rocks, it is extravagantly ornamented, with long forked

spines. Were it not for the figure of von Meyer quoted above,
which shows a considerable amount of ornament in a species of the

Eurypterus group, it would have been impossible to have so assigned

it. I believe it to be the central lobe of the abdomen of a trilobate

Eurypterus or allied genus, and shall so describe it.

E. horridus, axi corporis (solum conservato) subcylindrico, annulis rugosis
spinosis; tubercula in utroque segmento 4, quorum 2 centralia brevia, lateralia
longispinosa, spinis bifurcatis et ad basin bispinulosis.

The length of the fragment, including five rings, is 13 inch; and
the breadth of the axis, without the long forked spines, is 2ths of an
inch. The forked spines are #ths of an inch each, and have at their
base, front and back, two other smaller spines.

Locality. In ironstone, North Staffordshire (Museum of Practical
Geology). Another specimen, as above noted, occurs in the Hope
Cabinet, Oxford; its locality is uncertain.

On Purtrocaris, a new Genus of SruRtAN Crustacea. By J. W.
Satter, Esq., F.G.S., A.L.S., of the Geological Survey of Great

Britain.
[Read May 21, 1861.]

Iv a paper on Graptolites from the Anthracite-shales (Llandeilo-
flags?) of Scotland (Quart. Journ. Geol. Soc. vol. viii. p. 391), a
figure (pl. 21. fig. 10) was introduced of a minute Crustacean, the
affinities of which were doubtful, but which nevertheless had much
resemblance to Dithyrocaris, a Carboniferous fossil. That specimen
was imperfect; but one or two since collected in Dumfriesshire are
more complete ; and, lastly, a beautiful and perfect example has been
given to the Museum of Practical Geology, through the kind offices
of Mr. James Young, of Glasgow.

Fortunately, since I described the above-mentioned little Crus-
tacean as Dithyrocaris? aptychordes, I have had occasion to study a
large series of Silurian Crustacea, which have, in their turn, furnished
the data whereby to connect this old Phyllopod with the modern
Nebalia and Apus; and I propose in describing this genus to notice
them, as chronological as well as zoological links, believing that such
illustrations of the theory of Mr. Darwin may best serve to give the
data whereby to confirm or refute his masterly hypothesis.

PELTOCARIS, gen. nov.

A small Phyllopod, with a round, shield-shaped carapace ; bivalved,
the valves open and imperfectly joined along the dorsal line; deeply
emarginate in front, the excavation so formed being filled up com-
pletely by a parabolic plate, which is the analogue of the rostrum,
and completes the broad oval shield.

* There are only a few living Crustaceans which show such an ornament;
the Lithodes described by De Haan, in the ‘ Fauna Japonica,’ is one of them.

88 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

PELTOCARIS APTYcHOIDES. Fig. 1.

Dithyrocaris aptychoides, Salter, Quart. Journ. Geol. Soe. vol. viii.
p. 391, pl. 21. fig. 10.

The broad, rounded-oval shield measures only 5 lines in length,
by about 47 lines in breadth; so
that it is not a true circle, but ap-
pears nearly like one. The rostrum,
as broad as long, and of a para-
bolic shape, is just one-third the
whole length. The body and ap-
pendages have not yet been found.

The division along the dorsal line
is continued as an open fissure for
a part of the length, then as a
narrow line; but the valves seem
to have been so far connected (by
membrane ?) that they occupy their
original place; and in one case only,
I think, have I seen the valves dissevered, never bent down. Imme-
diately behind the rostrum, in this specimen, what should be the
apex of the valve is circumscribed (a) and apparently cut off by a
deep furrow, or suture, from the rest. The two umbones, if they
may be so called, are in this way isolated. It may not be so in all
specimens ; but this notched umbone existed also in the larger speci-
men, figured as above quoted, and which is also, by favour of Pro-
fessor Harkness, in the collection of the Museum of Practical Geology.

Locality. Anthracite-shales (Llandeilo-flags), Dumfriesshire. Mu-
seum of Practical Geology.

Fig. 1.—Peltocaris aptychoides,
natural size and enlarged.

Pettocaris? HARrKkNEssI, sp. noy. Fig. 2.

A fragment, 2 inches long, in the same black Anthracite-shale
which afforded the Peltocaris aptychoides, was sent me by my friend
Professor Harkness many years back; and I then made the accom-
panying drawings (fig. 2) and description. I hope the specimen is
still safe in his cabinet.

It is a fragment of a much larger carapace than that of P. apty-

- choides, probably 33 inches at least in length. Only the ventral edge is

shown, and that for a short distance, covered by oblique marginal lines,
» which run backwards, while these are crossed by ventral strie,
=transverse to the general direction of the carapace. The latter are

aes

more remote than the marginal lines, and meet or cross these at an
angle of about 85° or 90°; while in the region unoccupied by the
marginal striae, the cross lines are themselves interrupted and fre-
quently decussated by short strize in an opposite direction. These
short strise may possibly be structural. But they are all exhibited
on the fossil; and I have introduced them accurately in the figure.
Fig. 2, B, is a magnified portion. The marginal lines are closer than
the vertical, and more wavy, and they oceupy the undefined border to
the exclusion of the others; but they are distinctly traceable for a

SALTER—PELTOCARIS. 89

short space across the vertical lines on the general surface (just as
these are continued also faintly towards the margin). The vertical
lines, though more distant than the marginal ones, are still very
close together—eight or nine of them at least in the space of 4th of
aninch. They are notso regular as they appear to be at first sight.
Most of them, after proceeding a short distance, turn obliquely and
abruptly forwards, or else are crossed by short oblique striations, to
join the next vertical line, which is generally, but not always, obli-
terated above the point of junction (as at a). Very rarely these
oblique lines cross the space of two vertical lines (6); and, as they
are all strictly in the same direction, they give the appearance of a
third set of parallel striz ruled across the other two.

Fig. 2.—Peltocaris? Harknessi. A, natural size. B, enlarged.

hare

\\ \ :
\ \
i) Ny, pM

will

Wy

Wil
Hii Ti

i ‘NM

Ui

na Bi fist
bhi

ei A
Nt Mh,

eh \
i

The faint transverse lines above mentioned are, I believe, due to
mineralization only ; but three sets of lines are certainly present, viz.
the strong, vertical ones, the oblique, close, marginal striz, and, lastly,
theshort, oblique lines in the opposite direction to those last mentioned.
I do not remember such a complication of lines on the surface of any
other carapace*. Peltocaris aptychoides is so small and smooth, that
there is no opportunity of judging whether it may be the young state of
this larger species. Its nearly uniform size in the half-dozen speci-
mens [ have seen would seem to be in favour of its being distinct.

Locality. Anthracite-beds (Llandeilo-flags), Dumfriesshire. Pro-
fessor Harkness’s collection.

And now a word or two regarding the affinities of this curious
Crustacean.

Before the structure of Ceratiocaris was known, of which genus a
reduced figure is here given (fig. 6), the rostral portion of Peltocaris
could not have been understood. But a reference to the accom-
panying series of woodcuts will show that a tolerably broad rostrum,
placed in the same relative position, occurs in Ceratiocarist. In the
recent Nebalia (fig. 12) it is fixed; and in Dithyrocaris (fig. 8) and

* The margin of Argas testudineus (fig. 9) is striated, but in the same direction
as the transverse lines on the rest of the shield.

t+ More complete figures are given in the Ann. & Mag. Nat. Hist. for March
1860, p. 154.

Concentration of shield, increase of abdomen, &c.

90 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

other genera it is perhaps yet to be discovered. Again, Ceratiocaris,
together with its moveable rostrum, has a bivalved shell, yet habitu-
ally keeps its valves half closed, as I learn from perfect specimens.

Figs. 3-12, a to i.—Geological distribution of Phyllopoda.

Recent.

Carboniferous. Trias.

Devonian.

Lower Upper
Silurian

Silurian.

Lingula
Flags

Fig. 3. Hymenocaris, Saiter. Lingula-flags or Primordial zone.
4, 5, Peltocaris, Salter. Lower Silurian (Llandeilo or Caradoc).
6. Ceratiocaris, M‘Coy. Upper Silurian.
7. Dictyocaris, Salter. Upper Silurian and Lowest Devonian.
8. Dithyrocaris, Scouler. ?
9. Arg e Sooner: } Carboniferous.
10, 11. Apus. Trias to Recent.
12. Nebalia. Recent.
Figs. 3-12 are somewhat reduced ; fig. 7 is less than one-tenth the natural
size.
a-d. Estheria, Strauss. Natural size.
e-t. Leperditia, Beyrichia, &e. Natural size.

Division of shield, diminution of abdomen, &ce.

SALTER—PELTOCARIS. 91

In Peltocaris this habit was certainly absent, and the whole contour
indicates a flat, shield-shaped carapace, though divided into three
parts. In Dithyrocaris (fig. 8) the sutures themselves are lost, as
they are in Nebalia (fig. 12).

Peltocaris would seem to be, in some sort, intermediate between
the shield-bearing Dithyrocaris, whose valves are soldered into one,
and the bivalved genera. And, if we had the body preserved, we
might probably find a still nearer relation to a more ancient genus,
found in the Lingula-flags, I mean the Hymenocaris (fig. 3), now
becoming pretty well known.

I beg leave to express what appears to me to be the series of
affinities of this and other known Phyllopodous forms in a diagram,
which shall at the same time give their chronological order. The
numbers correspond with those on the woodcut.

Fig. 3. Beginning with what I must call the more generalized
type, Hymenocaris. In this the shield is neither flat nor bivalved,
but simply bent; and without any rostrum. There is a medium
number of free body-segments ; while the appendages of the taz/ are
irrelatively multiplied. (Lingula-flags or Primordial Zone.)

Fig. 4. A form (Peltocaris) in which the carapace is marked out,
as it were, into three portions, not yet intended to enclose the
animal. The body and appendages are not known ; but a Crustacean
certainly existed in the Llandeilo-flags in some respects intermediate
between Hymenocaris and Ceratiocaris, and we may perhaps be justi-
fied in provisionally referring to Peltocaris such tracks as those de-
scribed below (page 93).

Fig. 5. Peltocaris (?)*.—Known only by tracks made by a double
instrument which may have been part of a more complex tail (see
p. 93).

Fig. 6. Ceratiocaris.—Here the rostrum is narrowed, but still not
soldered to the carapace. And the valves have free motion, and
partly enclose the body. The tail-appendages are three; the telson
being enlarged to make the third and larger prong.

Fig. 7. A very imperfectly known form of immense size occurs in
the Lower Devonian. and Upper Silurian ; but all that is known of it
is that the carapace is undivided and reticulate (Dictyocaris).

Figs. 8 to 12. From this point the larger Phyllopods (for, though
I have inserted them, figs. a to2, it may be a question yet whether
Leperditia and its allies be undoubted Phyllopods) diverge (in a
geological sense only) into two groups; the one becoming more
decidedly shield-shaped, and with exserted abdomen and large caudal
styles ; the other starting at once with a bivalved carapace, com-
pletely enclosing the small abdominal segments and their minute
appendages (Estheria).

I do not pretend to have shown every link, but have given all I

* IT hope I may be allowed to insert in this figure (which is only a diagram)
the caudal appendages at least of the hypothetical Crustacean whose existence in
the Llandeilo strata I cannot doubt (see next paper). It might be too much
to surmise that it belonged definitely to Peltocaris, or that the P. Harknessi, a
Llandeilo species, actually produced the tracks.

92 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

could find of published data, and here exhibit the series in a dia-
grammatic form, that the naturalist may judge for himself whether
it bear out the view of Darwin, or no.

I do not think, judging by the carapace only, that many links are
wanting between the Llandeilo-flag Peltocaris and the Upper Silu-
rian Ceratiocaris. But there is evidently a still nearer connexion
(probably we want an intermediate Devonian form) between Cera-
teocaris and Dithyrocaris. The Argas of the Lower Carboniferous
rocks, and a huge bivalve Crustacean not here described*, were close
relations of the Dictyocaris and Ceratiocaris of the Upper Silurian,
differing only in having the anterior joints of the abdomen concealed,
and the rostrum minute or possibly (but not probably) absent.

The links between these Coal-measure forms and those of recent
times are many of them wanting; but in Nebalia we have a good
representative of the compact, shield-shaped form of Ceratiocaris, the
two valves soldered into one, and the rostrum attached,—the eyes
being still beneath the carapace. -Apus is the most complete and
decided form, and it is one of the latest of this group, as it commences
in the Trias. The abdomen is not only greatly increased, and the
caudal styles elongated beyond the telson, but the styles are jointed
appendages; and the feet and antenne have also taken on a de-
velopment wholly beyond that of the rest of the order.

The other group, the truly bivalved and enclosing Phyllopods, do
not present the same variety of forms. From the period of the
Middle Devonian, where Estheria first makes its appearance, till
now, there has been but little change, except a gradual increase in
size. And, as I do not feel sure that we have in the Estheria or
Leperditia the oldest member of the series, I will only place them
as they stand in the diagram, and abstain from discussing the affini-
ties of any but the larger and shield-bearing Phyllopods.

I may be permitted to say, that even of these the series, as here
exhibited, is not quite satisfactory in a Darwinian point of view.
The transition, if it be such, from Hymenocaris, with an entire shield,
to a form with sutures, and then valves, returning afterwards to a
more completely soldered and compact form, may be regarded as an
oscillation of character by those who do not see a more embryonic
representative in the thin undivided carapace (without rostrum,
suture, or external eye) in the primordial form. Apus, however, is
unquestionably the most highly developed ; and it is the latest.

On some Tracks of Lower Siturtan Crustacea. By J. W. Satter,
Esq., F.G.8., A.L.S., of the Geological Survey of Great Britain.

[Read May 21, 1862.]

Tas short communication seemed hardly worth the Society’s
notice, and would have been long delayed, but for the appearance
of a most interesting photograph-plate in the ‘ Transactions of the

* Dithyrocaris Pholadomya, MS., a species with a carapace 7 inches long, from
the Carboniferous Shales of Berwickshire.

_ SALTER—LOWER SILURIAN CRUSTACEA. 93

Linnean Society of Normandy,’ 1861. This shows the entire sur-
face of a slab of sandstone, observed by the author of the paper,
M. de Brébisson, in a small quarry at Noron, in the Falaise ; which
sandstone, overlain by beds of red and brown schist, the author is
disposed, with M. Moriére, to consider of Cambrian rather than of
Lower Silurian age. The geologic position may be somewhat
doubtful ; but at least these sandstones and schists are overlain by
the quartzose rocks referred to the age of the Caradoc sandstone,
which is now tolerably well known in Normandy.

The surface of the sandstone is split up by a compound cleavage,
and the slabs could not be detached; casts only and photographs
could be taken, but these are quite sufficient to show the whole
nature of the imprints. These, though doubtfully referred by M. de
Brébisson to gigantic Algw, are (by the consent of four British
paleontologists) clearly referable to the tracks of some Crustacean.
I shall endeavour, after describing a similar track from British rocks,
to show in what respects the two differ, and in what way the tracks
were formed.

Track oF PELTocaRis (?).

The track to which I would first draw attention was presented to
the Museum of Practical Geology* by the late Rev. T. T. Lewis, of
Aymestry. He found it ina picturesque glen (Wilmington Dingle),
near Chirbury, Salop, in beds of the age of the Llandeilo-flags, which,
in various localities near, contain abundance of the characteristic
Ogygia Buch and Lingula granulata. In these beds, up to the pre-
sent time, no other Crustaceans than Trilobites have been discovered.

The surface of the slab, broken unfortunately in two by some
meddling collector, was evidently once continuous, and must have
been fully 2 feet long by 1 foot broad. On this surface three
broad ripple-ridges, with intervening shallow depressions, may be
seen; and the ridges are cut in all directions by the marks to be
presently described, while the depressions are left untouched.

I draw attention to this striking feature, because it at once shows us
that the creature swam so near the bottom, that every stroke of the
extremity of the tail impinged upon the muddy ridges, and not so close -
to the bottom but that the instrument, whatever it was, did not strike
it when the animal passed over the more depressed surface.

The tracks vary not a little in length. The deeper ones are often
2 inches long, and occasionally even more ; the shallower ones some-
times not more than 13 inch to less than 4 an inch. But all are of
the same breadth ; and all, without exception, have been made by the
same instrument. They are very numerous, as many as twenty-
three being crowded (and crossing each other at all angles) in a space
of 4 inches on one ridge. In other portions not above a dozen
occupy the same space. ‘They are broad and shallow at the abrupt
end, deep and narrower in the middle, and taper a good deal toward the
smaller end; and at both extremities the mud has been driven up

: S.1
* Wall-ca j
all-case IV. Noo:

94 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

into a ridge by the stroke; while along the deeper middle portion
the matrix has fallen in after the instruments (there were two of them)
had passed, and appears as a rounded, tumid border.

SALTER—-LOWER SILURIAN CRUSTACEA. 95

That there were two instruments or styles used to produce the
stroke is clear from the shape of the indent. In very shallow
imprints the marks of the two prongs (set rather widely apart) are
visible along the whole length of the indent, and keep at an equal
distance along this space. When the indent deepens, the prongs
appear to have been pressed together as the stroke proceeded, for
the imprint is narrower at the deeper part; and then, as the stroke
was ended, they did not in all cases spring open to their full width,
but remained half closed until the prongs were withdrawn. But at
the first impact they are always about two lines apart; and, as
before stated, when the stroke has been a shallow one, this breadth
is preserved to the extremity of the imprint.

The mud must evidently have been very soft when these impres-
sions were made; for there seems to have been no resistance, save
that which the natural density of the substance would readily account
for. That two prongs were used in the operation is equally clear ;
and we must look, therefore, for a Crustacean which must have
possessed such a pair of caudal appendages. There is no probability
whatever of the markings having been produced by lateral feet, for
the stroke has in every instance been unique.

The question next arises, what Crustacean could have formed such
a track? We know of many large forms in the Upper Silurian rocks
which have strong prong-like tails; and it is to these I should natu-
rally look for comparison, were it not that all the species of Ceratio-
caris known, besides being strictly Upper Silurian, have the median
prong, or telson, of the tail so strong and large that it alone would
have made the imprint. Such a creature might indeed easily drag its
long telson along with a wriggling motion, and produce the wavy,
zigzag trail observed on the slab of Normandy sandstone. The
wavy line is just what would be produced by a weapon trailed slowly
along a ridge of muddy silt, which detained it, while the intervening
hollows would not be even touched by the instrument. I refer that
track to Ceratiocaris, or an allied genus. But the double imprint
of our specimen is to be interpreted differently. Either we must
conceive a genus allied to Ceratiocaris, but with the median tail-
prong abortive and the two lateral ones only developed, or we must
look to rocks of a higher antiquity than the Llandeilo-flags for its
analogue. I have lately learned that the caudal appendages of
Hymenocaris, from the Lingula-flags of Wales, were composed of six
pieces, four short and two long ones (fig. 3, p. 90). If we have not
yet discovered the large Crustacean which made these broad and
vigorous imprints, we may feel pretty certain, from analogy with
forms found both on higher and lower horizons, that if was a great
Phyllopod, with a prong-like tail, intermediate (in all probability)
_ between the two genera above named. A single track becomes in
this way the witness of an undiscovered form. It may possibly
belong to Peltocaris (p. 90).

DONATIONS
TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From July st to September 30th, 1862.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

American Journal of Science and Arts. Second Series. Vol. xxxiv.
No. 100. July 1862. From Prof. B. Silliman, For. Mem. G.S.

O. C. Marsh.—New Enaliosaurian (Kosawrus Acadianus) from the
Coal-formation of Nova Scotia, 1 (2 plates).

J. S. Newberry.—American Fossil Fishes, 73.

C. P. Williams and J. F. Blandy.—Constitution of the Copper Range
of Lake Superior, 112.

Mastodon Tooth in Amador Co., California, 135.

KE. Billings’s ‘New Species of Silurian Fossils,’ noticed, 186.

C. Rominga.—True position of the Waukesha Limestone of Wis-
consin, 136.

R. P. Whitfield—Description of Lingula polita, 186.

F. B. Meek and F. V. Hayden’s ‘New Lower Silurian (Primordial),
Jurassic, Cretaceous, and Tertiary Fossils collected in Nebraska,
&e.,’ noticed, 137.

Meteorites, 152.

California Geological and Natural History Survey, 157.

Assurance Magazine. Vol. x. Part 4. No. 48. July 1862.
Atheneum Journal. Nos. 1810-1822.

Notices of Meetings of Scientific Societies, &c.

J. Mallet’s ‘Cotton: its Chemical, Geological, and Meteorological
relations,’ noticed, 14.

S. J. Mackie.—Human bones at Leicester, 23.

J. B. Jukes’s ‘Manual of Geology,’ noticed, 117.

G. R. Burnell’s ‘Annual Retrospect of Engineering and Architecture,
noticed, 214.

G. P. Scrope’s ‘ Volcanos,’ noticed, 234.

H. W. Bristow’s ‘Glossary of Mineralogy,’ noticed, 296.

DONATIONS. G4

Atheneum Journal. Nos. 1810-1822 (continued),

‘Memoirs of the Geological Survey of India. Palseontologia Indica,’
noticed, 280.

J. Schvarez’s ‘Failure of Geological Attempts in Greece,’ noticed,
370.

Basel. Verhandlungen der naturforschenden Gesellschaft in Basel.
Dritter Theil. Drittes Heft. 1862.

Berlin. Zeitschrift der deutschen geol. Gesellschaft. Band xiii.
Heft 4. August—October 1861.

Proceedings, 523-526. General Meeting, 526-529.

A. Oppel.—Ueber die Brachiopoden des untern Lias, 529 (4 plates).

K. v. Seebach.—Die Conchylien-Fauna der weimarischen Trias,
551 (2 plates).

O. Volger.—Beitrage zur Theorie der Hrdbeben, 667.

J. G. Bornemann,—Ueber Pflanzenreste in Quarzkrystallen, 675

1 plate).

up Geinitz.—Die Dyas, oder die Zechsteinformation und das Roth-
liegende, 692 (1 plate).

F. Roemer.—Notiz tiber das Vorkommen von Nautilus bilobatus, Sow.,
im Kohlenkalke Schlesiens, 695.

Band xiv, Heft I. 1861.

Proceedings, 1-16.

T’, Scheerer.—Die Gneuse des sachsischen Erzgebirges und verwandte
Gesteine, 25.

D, Gerhard.—Ueber lamellare Verwachsung zweier Feldspath-
Species, 151.

Senft.—Der Gypsstock bei Kittelsthal mit seinen Mineral-Kin-

_. schhissen, GO (1 plate).

F, Roemer.—Bericht iiber eine geologische Reise nach Russland im
Sommer 1861, 178.

Breslau. Abhandlungen der schlesischen Gesellschaft fiir vaterlin-
dische Cultur. Philosophisch-historische Abtheilung. 1862,
Hefte 1 & 2,

—, Abtheilung fur Naturwissenschaften und Medicin.,
1861, Heft 3.

——, 1862, Heft 1.

——, Jahresbericht der Schlesischen Gesellschaft fiir vaterlindische
Caitur. Vol. xxxix. 1862.

Roemer.—Ueber die im Sept. 1860 in Besancon abgehaltene Ver-
sammlung franzosischer Geologen, 37.

~~, Hine Notiz iiber die Auttndung von Postdonomya Becheri in
der Grauwacke von Oesterreichisch-Schesien, 38.

—. Ueber seine geologische Reise nach Russland, 39.

Stache.—Uebersicht iiber die geologischen Verhiiltnisse Istriens, Sie-
benburgens, und des Bakonyer Waldes, 43.

Goppert.—Bemerkung rucksichtlich der Auffindung der Posidono-
mya Bechert unweit Troppau, 52.

—. Entdeckung yon Thierfahrten im Gebiet des Rothliegenden, 52,

VOL. XIX,— PART I, H

(Ctr 8
e

- ~ e

98 DONATIONS.

Canadian Journal. NewSeries. Nos.39&40. May and July 1862.

T. C. Keefer.—Anchor-ice, 173.

J. De Cew.—Age of the Oriskany Sandstone, 190.

Meteoric Stones 3 in India, 193.

‘Catalogue of Canadian Minerals at the London International Ex-
hibition,’ noticed, 215.

W. Boyd Dawkins. “Hy eena-den at Wookey Hole, 377

Notices of Books, 200, 347.

Chemical Society. Journal. ‘Nos. 63-65. Vol. xv. Parts 7-9.
July-September 1862.

T. L. Phipson.—Sombrerite, 277,
HK. Riley.—Titanic Acid, 311.

Colliery Guardian. Vol. iv. Nos. 80-91.

Notices of Meetings of Scientific Societies, &c.

W. Green. —Origin and Formation of Coal, es

The International Exhibition, Class L., 8, 91, 129.

Safety-lamps, 9.

T. J. Taylor.—Archeology of the Coal-trade, 11, 29, 49, 69, 89.
Coal-mines of Michigan, 17.

Discoveries of Ccal in Nevada, 27.

The Mineral Section of the International Exhibition, 30.
Discovery of valuable Minerals in North Northumberland, 33.
D. T. Ansted.—The Coal-fields of Hungary, 51.

Dudley and Midland Geological and Scientific Society, 105, 147.
H. Cossham.—The Natural History of Coal, 108.

E. Hull.—The North Staffordshire Coal- field, 181.
Self-extinguishing Safety-lamp, 151.

EK. Hull.—Marine Fossils at Dukinfield, 166.

KE. W. Binney.—Geology of Manchester and its neighbourhood, 166,
Accidents in Mines, 169, 189.

Coal at Redhead, Australia, 173.

Coal-mining in New Zealand, 174.

Fuel, 206, 260.

E. Hull.—Carboniferous Strata of Great Britain, 211.
Geological Survey of the United Kingdom, 227.

H. T. James. —Mining i in the County. of Leitrim, DSz.

Frogs in Coal or Stone, 247, 249, 256.

Government Inspection of Mines, 262.

Copenhagen. Questiones que in a. 1862 proponuntur a Societate
regia Danica Scientiarum cum premii promissu.

Critic. Vol. xxv. Nos. 627 & 628.
D. G. F. Macdonald’s ‘British Columbia and Vancouver's Island,’
noticed, 50.
H. Holland’s ‘ Essays on Scientific and other Subjects,’ noticed, 75.
B. y. Cotta’s ‘ Geologische Bilder,’ noticed, 77.

Darmstadt. Notizblatt des Vereins fiir Erdkunde und verwandte
Wissenschaften zu Darmstadt und des mittelrheinischen geologis-
chen Vereins. Nos. 3-8. May—August 1862. Folge ui. Heft 1.

R. Ludwig.—Braunkohlenablagerungen im Tertiiirbecken yon Teplitz
in Bohmen, 88.

DONATIONS. 99

Darmstadt. Notizblatt des Vereins. May—Aug. 1862 (continued).

Siebert.—Aus der Section Worms, 41, 112.

Delesse’s ‘Recherches sur ]’eau dans l’intérieur de la terre,’ noticed, 78.

R. Ludwig.—Die Steinkohlenformation zwischen Prag und Pilsen,
101. |

A. Groos.—Geognostische Beobachtungen in der Umgegend von
Nieder-Ingelheim, 107.

Dijon, Mémoires de l’Académie Impériale des Sciences, Arts et
Belles-lettres de. 2™° Série. Tome ix. 1861.

A. Perrey.—Bibliographie seismique (2° partie), 87.

Dorpat. Archiv fiir die Naturkunde Liy-, Esth-, und Kurlands’
Erste Serie: Mineralogische Wissenschaften. Band ii, Dritte
(Schluss-) Lieferung. 1861.

C. Grewingk.—Geologie von Liv- und Kurland mit Inbegriff einiger
angrenzenden Gebiete, 479 (4 plates and map).

——. ——. Zweite Serie: Biologische Naturkunde. Band iy.
1861.

Dresden, Sitzungsberichte der naturwissenschaftlichen Gesellschaft
Isis zu. Jahrgang 1861. 1862.

Voigtlinder.—Skelette eines Riesenhirsches (Cervus Hibernicus), 31.

H. Blochman.—Ein Theil von Indien, wohin ja die Wiege der
Menschheit versetzt wird, 32.

Schaufuss.—Ueber die Minen und Gruben der Real Compania Astu-
riana in Nordspanien, 62.

Geinitz.— Untersuchung der Zechsteinformation und des Rothlie-
genden, 63.

K. Fischer.—Die Urschieferformation des Eulengrundes, 113.

H. B. Geinitz.—Ueber die neuesten Aufschliisse im Gebiete der Stein-
kohlenformation Sachsens, 114.

Von Abendroth.—Abriss des bayerischen Chiemgaues, 116.

E. Fischer.—Bohrung des artesischen Brunnens neben der Dresdener
Papierfabrik, 120.

Geologist. Vol. v. Nos. 55-57. July-September 1862.

G. V. Du Noyer.—Glacial Action in South of Ireland, 241 (2 plates).

W. King.—Origin of Species, 254.

Anon.—M. Gras on Flint Implements, 281.

W. H. Bensted.—Geology of Maidstone, 294, 334 (4 plates).

Geological Notes in the Great Exhibition, 306, 344.

Proceedings of Geological Societies, 262, 309, 351.

Notes and Queries, 272, 312.

Foreign Intelligence, 273, 317.

Reviews, 274, 318, 354.

J. Taylor.—Supposed footprints in the Cambrian Rocks of the Isle
of Man, 321.

C. C. Blake.—Past Life in America, 323.

G. D. Gibb.— Excursion to Reculver, 330,

Giessen. Neunter Bericht der oberhessischen Gesellschaft fiir
Natur- und Heilkunde. 1862.
To

100 DONATIONS,

Hanau, Jahresbericht der Wetterauer Gesellschaft fiir die gesammte
Naturkunde zu. Session 1860-61.

Intellectual Observer. Vol. i. No.6. July 1862.

Notices of Meetings of Scientific Societies, &c.

—. Vol.u. Nos.7&8. August and September 1862.

Notices of Meetings of Scientific Societies, &c.
Minerals at the International Exhibition, 64, 144.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xxiv. Nos. 158-160. July-September 1862.

RR. Harkness.—Pteraspis-beds of Scotland, 75.

W. Whitaker.— Western Extremity of the London Basin, 74.

J. Bolton.—Clay-deposit with Insects, Leaves, &c., near Ulverstone, 74.

T. H. Huxley.—Two New Labyrinthodonts, 75.

J. W. Dawson.—Land-flora of the Devonian Period in North-eastern
America, 75.

I, Sandberger.—Upper Eocene Fossils from the Isle of Wight, 76.

Ri. Harkness.—Metamorphic Rocks of the Banffshire Coast, 165.

D. Honeyman.—Gold-fields of Nova Scotia, 165.

J. W. Salter.—Crustacea from the Coal-measures and Devonian Rocks
of New Brunswick, &c.; some species of Eurypterus and allied
forms; Peltocaris; Crustacean Track in the Llandovery Flags, &c.,
166.

J. Tyndall.—Conformation of the Alps, 169.

H. Falconer.—Affinities of Plagiaulax, 240.

O. Heer.—Fossil Plants from Hempstead, 241.

G. H. Morton.—Glacial Surface-markings near Liverpool, 241.

London Review. Vol. vy. Nos. 105-117. July 5-August 23, 1862.

Notices of Meetings of Scientific Societies, &e.

Rearrangement of the minerals in the British Museum, 88.

R. Owen’s ‘ Extent and Aims of a National Museum of Natural
History,’ noticed, 195. _—-

Zoological Collections of the British Museum, 220,

The Kirkdale Cavern, 231, 242.: -

ik. Melena’s ‘ Calabria and the Lipari Islands,’ noticed, 240.

Longman’s Notes on Books. Vol. ii.. No. 30. August 30, 1862.

Manchester, Geological Society of.. Transactions. Vol. iii. No. 15.

1861-62.
FE. Hull.—Marine fossils at Dukinfield, 348.
K. W. Binney.—Geology of Manchester, 350.
Manchester, Memoirs of the Literary and Philosophical Society of.
ord Series. Vol.i. 1862.

W. S. Jevons.—Australian Gold-fields, 115 (1 plate).

i. Hull.— Vestiges of Extinct Glaciers in the Highlands of Great
Britain and Ireland, 131.

Proceedings of the Literary and Philosophical Society.

Vol: ii. 1862.

E. W. Binney.—Nodules ‘in Coal, 71.
-—, Peat from Mosses near Southport, 73,

————————

DONATIONS. 101

Manchester, Memoirs of the Literary and Philosophical Society of
ord Series. Vol. ii. 1862 (continued).

EK. W. Binney.—Drift-deposits near Blackpool,133.
—. Permian Beds of South Lancashire, 137,

—. Markings on the Kerridge Flags, 153.

F, C. Calvert.—Sulphur in Pyrites, 135.

R. D. Darbishire.—Fossil Shells at Capell Backen, 21.
-—. Deposit of Bones at Great Orme’s Head, 184.
T. Davies.—Crystallization, 210.

W. Fairbairn.—Temperature in Dukinfield Coal-pit, 15.
—. Temperature of the Earth’s Crust, 64.

E. Hull.—Geological Surveys, 32.

—. Glacial Striations near Liverpool, 155,

P. Pauli.—Production of Graphite, 97.

J. A. Ransome.—Selenium in Coal, 97.

—. Arsenic in Sulphur, 13.

R. A. Smith.—Arsenic in Coal-pyrites, 4.

S. Peter.—Arsenic in Coal, 6.

——. Arsenious Acid in Pyrites, 125.

——, Proceedings of the Literary and Philosophical Society of.
Session 1859-60, No. 15. pp. 253-261.

——— =———, lPreface and Index to Yol.1. 1860.

——. Rules of the Literary and Philosophical Society of Man-
chester, 1861.

Mechanics’ Magazine. New Series. Vol. viii. Nos, 184-196.

Notices of Meetings of Scientific Societies, &c.

South Australian Mines, 32.

The International Exhibition, Class I., 52, 63, 115, 142, 158.

C. F. Chandler.—New Metal in the native Platinum of Rogue River,
Oregon, 96.

Tronstone- and Coal-mining in a sanitary point of view, 108,

Remains of British Tin-works, 160,

Indian Coal-fields, 164.

Conformation of the Alps, 176, 196.

Melbourne. Transactions of the Philosophical Institute of Victoria,
Vol. i. Aug. 1855—Dec. 1856.

L. Becker.—Age of Animal and Vegetable Kingdoms of Australia, 15,
—. Native Zinc in Basalt, 166.

C. Hodgkinson.—Geology and Soil of the Upper Murray, 37.

F. M’Coy.—Museums in Victoria, 127,

——. Transactions of the Philosophical Institute of Victoria.
Vol.u. 1858.

R. B. Smyth.—New Mineral from MclIvor, 17.

W. Blandowski.—Infusoria-deposits on the Lower Murray River,
Victoria; and the presence of Fucoide in Silurian Rocks near
Melbourne, 141.

J. E. Woods.—Metamorphic Rocks in South Australia, 168,

102 DONATIONS.

Mining and Smelting Magazine. Vol.i. Nos.’ 4-6. April-June
1862.

M. Fryar.—Faults, Dislocations, and Disturbances in Coal-mines,
240, 312.

FE. Hull.—Coal-fields of North Wales, 295.

W. W. Smyth.—Gold-mining at Clogau, North Wales, 359.

Abstracts and Reviews, 245, 319, 388.

H. C. Salmon.—lIllustrated Notes of prominent Mines, 314, 384.

Correspondence, Notes and Queries, &c.

—. Vol.u. Nos. 7-9. July-September 1862.

D. T. Ansted.—The Coal-fields of Hungary, 1.

i. Hull.—The North Staffordshire Coal-field, 65.

The International Exhibition, 87.

H. W. Bristow.—Auriferous Deposits of the Spanish and Portuguese
Estremaduras, 97, 132.

H. C. Salmon.—Illustrated Notes of prominent Mines, 14, 40, 74.

Abstracts and Reviews, 39, 100, 149.

Correspondence, Notes and Queries, &c.

Montreal. Canadian Naturalist and Geologist. Vol. vii. No. 3:
June 1862.

T. Macfarlane.—Primitive Formations in Norway and in Canada, and
their mineral wealth, 161.

T. Sterry Hunt.—Chemistry of the Earth, 201.

O. C. Marsh.—New Enaliosaurian from the Coal-measures of Nova
Scotia, 205.

J. W. Dawson.—Land-flora of the Devonian Period in North-eastern
America, 223,

Munich. Abhandlungen der Math.-phys. Classe d. k. bayer. Akad.
der Wissenschaften, Vol.ix. Part 2. 1862.

A. Wagner.—Monographie der fossilen Fische aus den lithographis-
chen Schiefern Bayerns. Erste Abtheilung: Plakoiden und Pyk-
nodonten, 279 (4 plates).

——. Sitzungsberichte d. k. bayer. Akademie der Wissenschaften.
1862. Vol. i. Heft 1.

———. Verzeichniss der Mitglieder d. k. bayer. Akad. der Wissen-
schaften. 1862.

Neo-Granadinos (Bogota). Contribuciones de Colombia a la Ciencias
ialas Artes. Ano Segundo. 1861. pp. 1-48.

E. Uricoechea.—Las minas de los Andes, 46.
F. A. de Humboldt.— Memoria razonada de las salinas de Zipaquira, 47.

Paris. Annales des Mines. 6™¢° Série. Vol. i. 2° livr. 1862.

Bulletin de la Société Géologique de France. Deuxiéme Série.
Vol. xvii. Feuill. 44-52. 1861.
Réunion Extraordinaire 2 Saint-Jean-de-Maurienne (Savoie), 693.

DONATIONS, 103

Paris. Bulletin dela Société Géologique de France. Dexicme Série.
Vol. xix. Feuill. 21-32. 1862.

Terquem et Piette.—Le lias inférieur de la Meurthe, de la Moselle,
du grand-duché de Luxembourg, de la Belgique, de la Meuse et
des Ardennes, 322 (2 plates).

Deshayes.—Sur la Monographie des gastéropodes de la craie supé-
rieure du Limbourg, par M. de Binkhorst, 394,

De Roys.—Sur une précédente communication de M. de Rouville
(p. 91), 397.

A. Paints. De Vazote et des matiéres organiques dans l’écorce
terrestre, 400.

Eug. Deslongchamps.—Développement du deltidium chez les bra-
chiopodes articulés, 409 (plate).

A. Damour.—Examen minéralogique d’une roche désignée sous le
nom de lherzolite, 413.

Descloizeaux.—Présence du zine carbonaté, de la lherzolite et de la
fluorine dans la chaine des Pyrénées, aux environs des Eaux-
Bonnes, 416.

A. Boué.—Lettre sur divers sujets, 420.

Melleville.—Sur les terrains de transport superficiels du bassin de
la Somme, 423.

Ed. Hébert.—Argile a silex, les sables marins tertiaires et les calcaires
d’eau douce du nord-ouest de la France, 445 (plate).

Arnaud.—La craie de la Dordogne, 465 (plate).

A. F. Nogués.—Terrain jurassique des Corbiéres, 501.

Académie des Sciences. Comptes Rendus. 1861, Deuxicme
Sem. Vol. liii.

Jackson.—A érolithe tombé 4 Dhurmsalla, dans l’Inde, 1018.

H. Ste.-Claire Deville et Damour.—Véritable nature des columbites,
et sur le dianium, 1044.

Jenzsch.—Polarisation circulaire du quartz et autres cristaux du
systéme 4 base hexagonale, 1262.

Terreil—Analyse des scories provenant de travaux métallurgiques des
anciens, 1275.

Jacquelain.—Etude chimique de l’eau d’une source de Neubourg, 672.

Frangois.—Eaux minérales de La Malou (Hérault), 1007.

Guyon.—Eaux thermales de Bou-Chater, dans la régence de Tunis, 44.

Boussingault.—Présence de l’azote dans un fer météorique, 77.

Fournet.—L’abus de l’emploi des expériences chimiques en géo-
logie, 82.

L’age des filons stanniféres, auriféres et de quelques autres

catégories, 695.

Du role de la persolidification en géologie, 179.

Sismonda.—Observations faites dans une excursion récente en Mau-
rienne, 113.

Terreil—Analyse de cinq roches de la vallée de Tarentaise, en
Savoie, 120.

S. Gras.—Séparation géologique des marnes 4 Ancyloceras du terrain
Néocomien dans les Alpes, 195.

Gaudry.—Résultats géologiques des recherches faites en Gréce, 372,
1018, 1126.

Hébert.—Terrain Jurassique de la Provence, 836.

Marcou.—Roches fossiliféres les plus anciennes de ’Amerique du
Nord, 803, 915.

Jourdan.—Terrains sidérolitiques, 1009.

104 DONATIONS.

Paris. Académie des Sciences. Comptes Rendus. 1861, 2™° Sem.
(continued).

Laur.—L’origine et la distribution de l’or dans les divers terrains de
la Californie, 1096.

Marcel de Serres.—Des gouttes d’eau fossiles des grés bigarrés de
Plombiéres-les-Bains (Vosges), 649, 927.

Haidinger.—Nature et le mode de formation des météorites, 456.

Kuhn.—Deux bolides observés le 7 septembre, & Gaillon (Eure),
482.

De Luca,—Matiéres minérales et organiques contenues dans la pluie, )
153.

Becquerel.—Production électrique de la silice et de Valumine hy-
dratées, 1196.

H. Ste.-Claire Deville-—Reproduction de )’étain oxydé et du rutile,
Ton,

Reproduction du fer oxydulé, de la martite et dela périclase :
protoxyde de manganése cristallisé, 199.

Descloizeaux.—Modifications temporaires et une modification per-
manente que l’action de la chaleur apporte & quelques propricétés
optiques du feldspath orthose, 64.

B. de Lom.—Nouveaux faits minéralogiques et géologiques recueillis
dans les cing départements volcaniques frangais, 288.

Pisanii—Analyse de la dufrénite de Rochefort-en-Terre, 1020.

Analyse de la pholérite de Lodéve (Hérault), 1072.

Radoszkovski.—Description d’un nouveau minéral de VOural, la
wagite, 1071.

Laugel.—Découverte d’un Castor & Auneux, prés Lumeau, et sur le
terrain falunien dans Eure-et-Loir, 35.

Jourdan.—Restes fossiles de deux grands mammiféres, 959.

Gervais.—Mesoplodon Christollii, grande espéce éteinte de Cétacés
Ziphioides, 496.

Bertherand.—Ossements fossiles trouvés dans les environs de Poligny
(Jura), 1246.

Valenciennes.—Une téte de grand Ichthyosaure trouvée dans largile |
du Kimmeridge au Cap la Héve, 267.

——. Nouveau reptile voisin de l’Ichthyosaure, trouvé dans Vargile
du Kimmeridge prés le Havre, 999.

Gervais.—Grandes empreintes végétales trouvées & Armissan (Aude),
TU ke

Marcel de Serres.—Des pierres de fronde trouvées dans les habita-
tions lacustres de la Suisse et dans les terrains d’alluvion de |
Amérique du Sud, 1123.

Dumas.—Influence exercée par la mise en activité du puits foré de
Passy sur le débit du puits foré de Grenelle, 571.

Gueymard.—Dosage du platine que se trouve 4 l’état de diffusion,
dans les gites métalliques ou dans les roches des Alpes du Dau-
phiné et de la Savoie, 98.

Jenzsch.—Systémes formés de différentes piéces d’un cristal d’apatite,
1262.

Gaudin.—Puits artésiens, 675.

Moyen expéditif pour accroitre le débit du puits de Passy,

672.
Pelouze.—Nouveau procédé de dosage du soufre contenu dans les
pyrites de fer et de cuivre, 685.
Pourian.—Comparaison de la marche de la température dans l’air et
dans le sol 4 2 métres de profondeur, 647.

DONATIONS. 105

Paris. Académie des Sciences. Comptes Rendus. 1861, 2™° Sem.
(continued).

Prost.—Trépidations du sol a Nice pendant le premier semestre de
1861, 638.

Commandant du navire la Félicie.—Effets d’un tremblement de terre
ressenti en mer le 20 février 1861, 1005.

Marchand.—Appareils pour l’étude des tremblements de terre, 1259.

P. de Tchihatcheff.—Nouvelle éruption du Vésuve, 1090, 1236.

A. Le Play.—Une des sources de la chaux assimilée par les produits
agricoles des terrains primitifs du Limousin, 1054.

Fagant.—Les minerais de fer magnétiques, 73.

Parthenon. Vol.i. Nos. 10-22.

Notices of Meetings of Scientific Societies, &c.

Antiquity of the Human Race, 372.

EK. Peacock.—Antiquity of the Human Race, 402.

J. Evans.—Antiquity of the Human Race, 403.

C.C. Blake.—Antiquity of the Human Race, 403.

J. Schvarcz’s ‘Failure of Geological Attempts in Greece,’ noticed, 404.

‘Transactions of the Philosophical Institute of Victoria,’ noticed, 467.

A. Massalongo e G. Scarabelli’s ‘Studii sulla Flora Fossile e Geologia
Stratigraphica del Senigalliese,’ noticed, 468.

W. B. Carpenter, W. K. Parker, and T. R. Jones’s ‘Introduction to
the Study of the Foraminifera,’ noticed, 530.

D. T. Ansted’s ‘Hungary and Transylvania,’ noticed, 675.

Photographic Journal. No, 123-125. July-September 1862.

Presburg, Verhandlungen des Vereins fiir Naturkunde zu. 4. Jahr-
gang. 1859.

F*. Hazslinsky.—Beitrag zur Kenntniss des Karpathensandsteins, iii.
A. Kornhuber.—Mineralien des Quarzgeschlechtes, 5.

——. Vorlage ungrischer Minerale, 49.

—. Geognostische Beschaffenheit des Bakony-Gebirges, 51.
Geognostische Verhiltnisse der Trentschiner Gespanschaft, 61.
A. Schneller.—Lignitspuren in Presburg, 59.

A. Richter.—Ueber Torfmoore, 75,

Band v. 1860-1861.

Ueber das geologische Alter der Thonschiefer von Mariathal, 69.

E, E. Lang.—Untersuchungen der Mineralquellen von Bajméez und
Belitz im Neitraer-Comitate, 86.

A. Kornhuber.—Vorkommen yon Braunkohle bei Bruznik und des
Basaltes bei Suschanowetz im Temeser Banate, liii.

——. Ueber die geologische Beschattenheit von Nord-Ungern, lxxix.

Suess.— Ammonites bi/rons, Brug., in Schiefern von Mariathal,
lxxxvlii.

Quarterly Journal of Microscopical Science. New Series. No. 7,
July 1862.

W. W. Stoddart.—Microgeology, 147.

Royal Asiatic Society of Great Britain and Ireland. Journal.
Vol. xix. Part 4.- 1862.

Royal Dublin Society. Journal. Nos. 24 & 25. January and April
1862.

Scott.—Fossils from Dresden, 269.

b

106 DONATIONS,

Royal Geographical Society. Journal. Vol. xxxi. 1861.
R. Alcock.—Hot Sulphur-baths of Atami, Japan, 321 (map).

——. Proceedings. Vol. vi. Nos. 3 & 4.

Royal Horticultural Society. Proceedings. Vol. ii. Nos. 7-9.
July-September 1862.

Royal Society. Proceedings. Vol. xii. Nos.50 &51. 1862.

W. Hopkins.—Motion of Glaciers, 110.

G. Forchhammer.—Constitution of Sea-water, 129.

J. Prestwich.—Loess of the Valleys of the South of England, and of
the Somme and the Seine, 170.

W. Mitchell.—Geometrical Isomorphism of Crystals, 190.

Society of Arts. Journal. Vol. x. Nos. 512-514.
Notices of Meetings of Scientific Societies, &c.
New South Wales, 575.
Structure of Copper, 646.
Products of India, 651, 665, 673.

Tyneside Naturalists’ Field Club. Vol. v. Part 3. 1862.

Vienna. Bericht iiber die zweite allgemeine Versammlung von
Berg- und Hiittenmiinnern zu Wien, 1861. 1862.

F. Schott.—Ueber geognostich-bergminnische Verhaltnisse im Kra-
kauer Gebiete, 47.

Jahrbuch der k.-k. geol. Reichsanstalt. 1861 und 1862.
No. 2. Jan.—April 1862.

F. y. Richthofen.—Der Kalkalpen von Vorarlberg und Nord-Tirol.
Zweite Abtheilung, 87 (plate).

A. Marschall—Aus Herrn Joachim Barrande’s Schrift: ‘ Défense
des Colonies. I. Groupe probatoire,”’ 207.

J. Krejci.—Bericht iiber die im Jahre 1859 ausgefiihrten geologischen
Aufnahmen bei Prag und Beraun, 228 (1 plate).

D. Stur.—Die neogen-tertiaren Ablagerungen von West-Slavonien,
285,

Verhandlungen der k,-k. geol. Reichsanstalt, 135.

——. Sitzungsberichte der k.-k. Akad. der Wissenschaften. Math.-
nat. Classe. Band xlv. Heft 1. Jahrgang 1862, Janner. Erste
Abtheilung (Mineralogie, Botanik, Zoologie, Anatomie, Geologie
und Paliontologie).

F. Stoliczka.—Oligocane Bryozoen von Latdorf in Bernburg, 71
(5 plates).

F. Rolle.—Ueber eine neue Cephalopoden-Gattung Cyclidia aus den
Tertiarschichten von Siebenburgen, 119 (1 plate).

Sitzungsberichte d. k.-k. Akad. Math.-nat. Classe. Band
' xiv. Heft 1. Zweite Abtheilung (Mathematik, Physik, u. s. w.).

V. v. Lang.—Die Krystallformen des unterschwefelsauren Baryts und
des traubensauren Kali, 27 (2 plates).

W. Haidinger.—Das Meteoreisen von Cranbourne im k.-k. Hof-
Mineralien-Cabinet, 65 (1 plate).

DONATIONS. 107

Vienna. Sitzungsberichte d.k.-k. Akad. Math.-nat. Classe. Band
xlv. Heft 2. Februar. Erste und zweite Abtheilung.

—, —. ——. ——. Heft 3. Marz. Zweite Abtheilung.

4 Heft 4. April. Zweite Abtheilung.

F. C. Schneider.—Chemische Analyse einiger Mineralquellen Oester-
reichs, 483.

G. Tschermak.—Die Dichte im Verhaltnisse zur Form und chemis-

chen Beschaffenheit der Krystalle, 603.

Zoological Society of London. Proceedings. 1861. Parts 2 & 3.

ee

II, PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 3rd Series. Vol. x.
Nos. 55-57. July-September 1862.

J. Prestwich.—Drift Deposits containing Flint Implements, and
their geological age, 57.

W. B. Clarke.—Age of the New South Wales Coal-field, 81.

R. T, Lowe.—Discovery of the fossil Helix coronula recent, 93.

H. Seeley.—Notes on Cambridge Geology: I., 97.

Discovery of Microscopic Organisms in the Paleozoic Rocks of New
York, 160.

J. W. Kirkby.—Additional Species common to Carboniferous and
Permian Strata, 202 (1 plate).

A. Newton.—Ancient Remains of Lmys hiraria in Norfolk, 224
(1 plate).

R. Owen.—Hyvracotherian Characters of the supposed Macacus from
the Eocene Sand of Kyson, Suffolk, 240.

Bronn und Leonhard’s Neues Jahrbuch fiir Mineralogie, Geologie
u.s.w. Jahrgang 1862. . Hefte 3 & 4.

C. Ribiero.—Die Steinkohlen-Grube von S. Pedro da Cova im Con-
celho de Gondomar, Distrikt von Porto, 267 (1 plate).

C. W. Giimbel.—Reyvision der Goniatiten des Fichtelgebirges, 285
(1 plate).

F. Roemer.—Notiz iiber die silurischen Schichten der Gegend von
Zaleszczyky in Galizien, 327.

Krauss.—Der Schadel des Halitherium Schinzi Kaup, 385 (2 plates).

H. G. Bronn.—Bemerkungen iiber das zu dem alteren Haltherium-
Schadel gehorige Skelett, 416.

R. Blum.—Der Epidot in petrographischer und genetischer Bezie-
hung, 419.

F Neha s-Aleber das Vorkommen yon Prehnit, Datolith und Rutil bei
Freiburg in Baden, und iiber die Bedingungen zur Zeolith-Bildung,
432.

Letters; Notices of Books, Minerals, Geology, and Fossils.

Edinburgh New Philosophical Journal. New Series. No. 31.
Vol. xvi. No: Ly duly 1862.

J. Duns.—A Recent Sandslip, 25.
W. Carruthers.—Geology of Moffat, Dumfriesshire, 33.
M. Thompson and M. Binney.—Composition of a Pseudo-steatite, 55.

108 DONATIONS.

Edinburgh New Philosophical Journal. July 1862 (continued).

J. A. Smith.—Meteorite at Newstead, Roxburghshire, 108 (plate).

M. Thompson.—Analysis of Meteorite described by Dr. Smith, 125,

J. H. Balfour.—Bark of Araucaria imbricata, 141.

A. Geikie.—Carboniferous Volcanic Rocks of the Basin of the Forth,
145. |

W. Thompson.—Secular Cooling of the Earth, 161.

L’Institut. 1 Section. 30¢ Année. Nos. 1469, 1483-1489, 1494.

Valenciennes.— Machoire inférieure de dauphin fossile trouvée a
Montfort, prés de Dax (Landes), 170.

G. Dewalque.—Systéme eifélien dans le bassin de Namur, 182.

Van Beneden.—Réflexions a propos de restes de Cétacés et d’autres
animaux fossiles trouvés sur la céte d’Ostende et prés d’Anvers,
185, 193.

G. Dewalque.—Non-existence du terrain houiller 4 Menin, 191.

A. Pissis.-—Vulcanicité aux differentes époques geologiques, 208.

A. Schrauf.—Théorie du systéme cristallographique rhomboédrique,
228,

Hébert.—Formations d’eau douce du bassin de Paris, 238.

Descloiseaux.—Dispersion des axes optiques dans les cristaux a
deux axes, 244.

E. Dumas et P. Rouville.-—Carte géologique de l’arrondissement de
Lodéve (Hérault), 245.

F. Pisani.—Grenat octaédrique de Vile d’Elbe, 246.

E. de Beaumont.—Systémes de montagnes du département de la
Haute-Marne, 255.

i. Beguyer de Chancourtois.—Distribution générale des gites miné-
raux, 271.

A. Dejardin.—Terrains d’Anvers, 275.
——. 2°Section. 27° Année. No. 317. 1862.

Paleontographica: herausgegeben von W. Dunker. Vol. ix. Part 3.
August 1862.
C. Speyer—Die Conchylien der Casseler Tertiarbildungen, 91
(5 plates).
——. ——. Supplement-Band. July 1862.

A. Hellmann.—Die Petrefacten Thtiringens nach dem Materiale des
herzoglichen Naturalien-Kabinets in Gotha, 1 (4 plates),

——: herausgegeben von H. vy. Meyer. Vol. x. Part 3. July 1862.

HI. v. Meyer.—Tertiare Decapoden aus den Alpen, von Oeningen und
dem Taunus, 147 (4 plates).

R. Ludwig.—Paleontologie des Ural’s: Actinozoen und Bryozoen

aus dem Carbon-Kalkstein im Gouvernement Perm, 179 (6 plates).

DONATIONS. 109

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italies.

Archer, W. H. Statistical Notes on the Progress of Victoria from
the foundation of the Colony (1835-1860). First Series, Parts
I. and II. Second Edition. 1862. From the University of Mel-
bourne.

, F. Mueller, R. B. Smyth, M. Neumayer, F. M‘Coy, A. R. C.
Selwyn, and W. Birkmyre. KEssais divers, servant d’introduction
au Catalogue de l’exposition des produits de la colonie de Victoria:
mettant en relief les progrés, ressources et caractere physique de
la colonie, 1861. From the University of Melbourne.

Aucapitaine, H. Mollusques terrestres et d’eau douce observés
dans la Haute Kabylie. 1862.

Baily, W. H. On the occurrence of some characteristic Graptolites
and other fossils indicating certain divisions of the Lower Silurian
Rocks in the counties of Meath, Tipperary, and Clare. 1862.

Béron, P. Chronologie du monde. 1862.

Capellini, G. Le Schegge di diaspro dei monti délla Spezia e l’epoca
della pietra. 1862. From Sur C. Lyell, V.P.GS.
Carpenter, W. B., W. K. Parker, and T. R. Jones. Introduction to

the Study of the Foraminifera, (Ray Society.) 1862. From
the Ray Society.

Catalogue. A Catalogue of the Contributions to the Ceylon Court
at the International Exhibition of 1862. 1862. rom the Com-
Mrssrioners.

——. Catalogue of the Articles exhibited by the Imperial and
Royal Geological Institute of the Austrian Empire, at the London
International Exhibition of 1862, From the Commissioners.

——. Exposicion Internacional de 1862 en Londres. Departamento
Espanol. Catalogo Oficial, 1862. From the Commissioners.

Catalogue of the Melbourne Public Library for 1861, 1861.
From the Unversity of Melbourne.

Catalogue of the Victorian Exhibition 1861, with prefatory
essays indicating the progress, resources, and physical character-
istics of the colony. 1861. rom the University of Melbourne.

Official Classified and Descriptive Catalogue of the Contri-
butions from India to the London Exhibition of 1862, forwarded
through the Central Committee for Bengal. Compiled by A, M.
Dowbeans, Esq. 1862, From Dr. Watson, FGA,

110 DONATIONS.

Cotteau, G. Apercu d’ensemble sur la géologie et la paléontologie
du département de ’Yonne. 1859,

——. KEchinides nouveaux ou peu connus. Art. 1-4. 1858-61.

. Etudes sur les échinides fossiles du département de ’Yonne.
ler volume: Terrain Jurassique. 1849-56.

——, ——, 2éme yolume: Terrain Crétacé. 1862.

——, Note sur la famille des Salénidés. 1861.

Note sur le genre Heterocidaris, nouveau type de la famille
des Cidaridées. 1861.

Notes sur les échinides recueillis en Espagne par MM. de
Verneuil, Triger, et Collomb. 1860.

——. Notice? bibliographique. Synopsis des échinides fossiles,
par E. Desor.

Notice géologique sur la formation des grottes d’Arcy-sur-
Cure. 1859.

——. Rapport sur le progrés de la géologie en France pendant
Pannée 1858. 1859.

1859. 1860.
1860. 1861.

——, et Triger. Echinides du département de la Sarthe. 1-8.
livraison. 1861.

Delesse et M. Laugel. Revue de géologie pour l’année 1860. 1861.

Deshayes, G. P. Description des animaux sans vertébres découverts
dans le bassin de Paris. 29. et 30. livraison. 1858.

Deslongchamps, E. E. Note sur la présence du genre Phorus dans
le Dévonien supérieur du Boulonnais. 1862.

Note sur le développement du deltidium chez les brachiopodes
articulés. 1862.

Dewalque, G. Notice sur le systéme eifélien dans le bassin de
Namur. 1862.

Die Colonie Victoria in Australien; ihr Fortschritt, ihre Hilfsquellen
und ihr physikalischer Charakter. 1861. From the University
of Melbourne.

Gastaldi, B. Nuovi cenni sugli oggetti di alta antichita trovati nelle
torbiere e nelle marniere dell’ Italia. 1862. From Str C. Lyell,
VPA.

Geinitz, H. B. Dyas oder die Zechsteinformation und das Rothlie-
gende. Heft 2: die Pflanzen der Dyas und Geologisches, 1862.

DONATIONS. 111

Halloy, J. J. @O.d’. Abrégé de Géologie. Time édition. 1862.
Heer, O. Beitrige zur Insektenfauna Oeningens. Coleoptera. 1862.

—. Ueber die von Dr. Lyall in Gronland entdeckten fossilen
Pflanzen. Sendschreiben an Herrn Dr. Jos. D. Hooker. 1862.

Hofmeister, W. On the Germination, Development, and Fructifica-
tion of the Higher Cryptogamia, and on the Fructification of the
Conifers. Translated by F, Currey. (Ray Society.) 1862. From
the Ray Society.

Hoyt, J. W. Wisconsin; its natural resources, and industrial pro-
egress. 1862. From the Legislature of Wisconsin.

Liebig, J. F. von. Rede in der 6ffentlichen Sitzung der k. Akademie
der Wissenschaften am 28. November 1861, zur Feier des Aller-
héchsten Geburtsfestes Sr. Majestat des Konigs Maximilian II.
1861. From the Royal Academy of Munich.

Malaise, C. De Vage des phyllades fossiliferes de Grand Manil
prés de Gembloux ; avec un rapport par M. Dewalque. 1862.

—. Note sur quelques ossements humains fossiles et sur quel-
ques silex taillés. 1860.

Marsh, O. C. Description of the Remains of a new Enaliosaurian
(Eosaurus Acadianus) from the Coal-formation of Nova Scotia.
1862.

Martius, C. F. P. von. Zum Gedichtniss an Jean Baptiste Biot.
1862. From the Royal Academy of Munich.

Mortillet, G. de. Note sur le crétacé et le nummulitique des envi-
rons de Pistoia (Toscane). 1862.

Naumann, C. F. Lehrbuch der Geognosie. Zweiter Band ; zweite
Abtheilung. Zweite verbesserte und vermehrte Auflage. 1862.

Owen, R. On the Extent and Aims of a National Museum of Natural
History. 1862.

Paléontologie Francaise. Description des animaux invertébrés
fossiles de la France, continuée par une réunion de paléontolo-
gistes sous la direction d’un comité spécial. Terrain Crétacé.
Tome vii. Livraisons I., II., III., V., VI.: Echinides Irréguliers,
par G. Cotteau. 1861-62.

: Terrain Jurassique. Brachiopodes, par E. E. Des-
longchamps. Livraison I. 1862. From M. Deslongchamps.

Perrey, A. Documents sur les tremblements de terre et les phé-
nomenes volcaniques aux Moluques. Premiére partie. 1857.

——. -——. Supplement 4 la premicre partie. 1858.

——. ——. Troisicme partie. 1859.

£2 DONATIONS,

Perrey, A. Documents sur les tremblements de terre et les phéno-
meénes volcaniques aux Moluques. Quatrieme partie. 1860.

——. Note sur les tremblements de terre en 1858, avec supplé-
ments pour les années antérieures. 1860.

——. Note sur les tremblements de terre en 1859, avec supplé-
ments pour les années antérieures. 1861.

Reeve, L. Conchologia Iconica. Monographs of the Genera Trochus,
Cyclostoma, Leptopoma, Vitrina, Simpulopsis, Phasianella, Orbicula,
Crania, Hippopus, Tridacna, and Cyclophorus. 1862.

Schvarcz, J. On the Failure of Geological Attempts in Greece
prior to the epoch of Alexander. Part 1. 1862.

Schulz, D. G. Descripcion geologica de la provincia de Oviedo,
Asturias. Conun Atlas. 4to. Madrid, 1858.

Sequenza, G. Intorno ad un nuovo genere di foraminiferi fossili
del terreno miocenico di Messina. 1859. From Sir C. Lyell,
V P.GS:

Siebold, C. T. G. Ueber Parthenogenesis, 1862. From the Royal
Academy of Munich.

Sinnett, F. An Account of the Colony of South Australia; together
with a Catalogue of all the Products of South Australia exhibited
in the South Australian Court of the International Exhibition.
1862. From the Commissioners.

Victoria. The Statistical Register of Victoria, from the foundation
of the colony; with an Astronomical Calendar for 1855. Hdited
by W. H. Archer. 1854. rom the University of Melbourne.

——. The Victorian Government Prize Essays, 1860. 1861. Krom
the Uniwersity of Melbourne.

Vignoles, C. Description of the Model of the Passage of the Tudela
and Bilbao Railway, across the Chain of the Cantabrian Pyrenees,
through the Basque Provinces in the North of Spain. 1862.

Yutes, J. On the Excess of Water in the region of the Earth about
New Zealand, its causes and its effects. 1862.

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

December 17, 1862.

Richard Richardson, Licentiate of the Royal College of Physicians
of Edinburgh, Rhayader, Radnorshire, and John Wickham Flower,
Esq., Park Hill, Croydon, were elected Fellows.

The following communications were read :—

1. On the Sxippaw State Serres. By R. Harkness, Esq., F.R.S.,
F.G.8., Professor of Geology in Queen’s College, Cork. With a
Note on the Graptoritss, by J. W. Satter, Esq., F.G.8., A.L.S.

ContTENTS.
1. Introduction. 4. Carrock- and Caldbeck-fells.
2. The Skiddaw Slates of the west side | 5. The Skiddaw Slates of the eastern
~ of Derwentwater, Bassenthwaite, margin of the Lake-district.
and Binsey Crag. 6. The Skiddaw Slates of Black Comb.

3. The Skiddaw Slates east of Derwent- | 7. Conclusion.
water and Bassenthwaite Lakes.

§$ 1. Introduction.

THE several memoirs by Professor Sedgwick on the older Paleozoic

rocks of the north of England, published in the ‘ Transactions’ and

‘Quarterly Journal of the Geological Society,’ have indicated the

nature and the arrangement of the older Palseozoic rocks as they

occur in the Lake-district. Among these rocks, and forming the
VOL. XIX.—PART I. 1

114 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Deerty,

base of the sedimentary series in the north of England, is a mass
of strata designated the Skiddaw Slates by Professor Sedgwick,
from the circumstance that these slates comprise the Skiddaw range
of mountains. They have hitherto been regarded as all but unfos-
siliferous, the described organic remains consisting only of two species
of Graptolites and four forms which have been attributed by Pro-
fessor M‘Coy to Fucoids.

The Skiddaw slates occupy a large area in the northern portion of
the Lake-district. They also occur in the south-western extremity
of Cumberland, where they form the mountain of Black Comb; and
they are seen in Westmoreland on the eastern margin of the Lake-
district, exhibiting themselves in three small patches. The object of
this memoir is to point out in detail the circumstances under which
they occur in their several areas, and to show that they are more
fossiliferous than they have hitherto been regarded, and also to point
out their equivalents elsewhere.

§ 2. The Skiddaw Slates of the West Side of Derwentwater,
Bassenthwaite, and Binsey Crag.

The Skiddaw slates on the west of Derwentwater and Bassenthwaite
Lakes, and Binsey Crag, form a portion of the area where they exhibit
themselves in their greatest development, both geographically and
geologically. The south-eastern boundary of this western part of
the Skiddaw slates of Cumberland runs from the lower end of
Derwentwater, by the Cat Bells, through Newlands to the head of
Crummock-water. From thence it continues westward, and then,
passing by the lower end of Ennerdale Lake, turns south-westward
round the base of Dent Hill.

The western margin of this area is marked by the Carboniferous
rocks of West Cumberland; and these rocks, in their eastern ex-
tension from Cockermouth, run along the northern edges of Binsey
Crag and Caldbeck-fells, forming the northern limit of the older rocks
of Cumberland.

The eastern boundary of the district under consideration is formed
by the lower portion of Derwentwater, the River Derwent, Bassen-
thwaite Lake, and the ridges extending to Binsey Crag.

Commencing at Newlands, on the southern border of the Skiddaw
slate area, we have, in the hills which lie south of Newlands, the
greenish-grey rocks, containing lead-veins, which appertain to the
series Immediately overlying the Skiddaw slates. On crossing the
Newlands valley northwards, the Skiddaw slates make their appear-
ance at the southern base of the ridge of hills which contains Aiken
Knot and Keskadale Knot. The strata here dip 8.8.E., passing under
the greenish-grey rocks, and consist of hard, slaty, grey shales, with
interstratified coarser beds not exhibiting the same amount of cleavage
as the finer deposits. On the north side of Keskadale Knot there are
considerable masses of débris which have fallen from the outcrop of
the Skiddaw slates. This débris is locally called ‘“ Screes,” and among
it fragments containing fossils are found. These “ Screes ” occur also
on the south side of Keskadale Knot, and yield the same fossils as those

1862. | HARKNESS—SKIDDAW SLATE SERIES. 115

g
g 2
S
a=] 3 -
> 5) 2. ey
n — ip) Lol
o
5 = 3 s ice P
=) to nh ray
a ‘ n = a] (cb)
o o =
g = 2 & g S ig
Becton g Birman Shand ing
8 2 > A s re
= ae a ra)
5 a
A iS) ic) wi o i g
~
a7 ve a ce. A
20,
242 NSS S
*, + a lo)
se: soe FAN ie)
a LAY
re 7— cS)
+ + ~<

Pratrettens ae
8.0679. “00°
Ate OO’!
AO OSS 3
Per S 96

a da.s ee
IRENRITH'2
; NS0GiSioss

aye

d. Winandermere.

ui)
i

|

|
!

S | A {I SS
3 Hee =
= | Sed :
. | S = ———— ;
le = |
Z | I ie ——— :
: Hh ——
Ss < ae |
1 ; = :
= Et

i a H Hh HH

“ Me

fi!
Hh

SIE
SU

NH
i UT) ite

|
A

(III
Me

a. Bassenthwaite Lake.

sae)

The number attached to each line of Section refers to the Figure in which that Section is represented.

116 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 17,

of the north side of this hill, viz. Graptolites sagittarius and a branch-
ing Graptolite. Tracks likewise are seen on the surfaces of some of
the more flaggy strata.

On their strike, the rocks of Keskadale and Aiken Knots extend
W.S.W. through Whiteless to the head of Crummock-water. At
Whiteless they have afforded Professor Sedgwick Giraptolites latus
and Chondrites informis*. From their position, and the relation
which they have to the greenish-grey beds, the rocks of Keskadale
Knot and Aiken Knot are among the highest of the Skiddaw slate
series.

Fig. 2.—Section from Newlands to Sunderland (11 miles).

Ss. 3 g = » N.
bd ° »~
S ey A L

i 3 Se) Nate hl ae ee
ad o> Qa S Bo

ms © A ° Ti 3 U = is
n 2 o : gs » 3 =]
oS a a 3 - 0 oe
a Lo} | a & j=) e es
3 3 Be 2 ° ee SS < 5
=e 2 5 a pape te =| Bo

=} oO
Lae 3 = > (Till.) § g BSE
CAM iy eH eS) Boy eee
i i : ; | : ms
1 ' 4 < eee

Fo S .
>

a a e a
a. Skiddaw Slates. 4. Green slates and porphyries.
ce. Syenite. d. Carboniferous Limestone.

Northwards from the ridge just alluded to there occurs another,
of which Causey Pike forms the highest summit, and in which a
great development of slaty rocks is found. A short distance to
the north of Causey Pike, and forming the southern side of the
Coldale valley, is a lower ridge than that of which Causey Pike
forms a part.

A portion of this ridge is known under the name of Outerside, and
in its northern and more precipitous slope, facing Coldale, there is a
considerable development of ‘Screes” under a rocky escarpment.
The lower portion of this escarpment consists of cleaved rocks, the
dip of the cleavage being N.W. Above these cleaved rocks flaggy
strata are seen, dipping 8.8.E. 80°. Among the “ Screes ” derived from
the flaggy rocks fossils occur, and this is one of the localities among
the Skiddaw slate series which, both in quantity and variety, is most
prolific in organic remains. These fossils consist of Crustaceans,
several forms of Graptolites, including the branching form which is
seen at Keskadale, tube-like bodies apparently allied to the modern
Terebella, and tracks.

East from this, at Hodgen-holm, near Portingscale, rocks of a flaggy
character also occur, which, besides dipping 8.8.E. at a high angle
(60°), also contain evidences of animal life, usually in the form of
tracks.

The Coldale valley, which les N. of Outerside, affords no satis-
factory dips among the strata, the rocks being for the most part of a
slaty nature. North of this valley, inclinations are seen among the

* Quart. Journ. Geol. Soc. vol. iv. p. 223.

— s,s

~ ee ee a ee

led

1862. | HARKNESS—SKIDDAW SLATE SERIES. 11%

strata having an opposite direction from those on the south side,
viz. N.N.W.

This valley seems to indicate the position of a well-marked anti-
clinal extending, in a W.S.W. direction, through the Skiddaw slates
which lie to the westward. At Barft, which is situated near the head
of Bassenthwaite, on the west side of the lake, these N.N.W. dips are
very apparent. The south side of this hill, from the base for a con-
siderable extent upwards, is covered with “ Screes” composed of
fragments of slaty rocks mixed with fragments of coarser flags, and
with the outcrops of the Skiddaw slates well seen above them.
These outcrops consist of slaty rocks interstratified with flaggy beds ;
and while the faces of the former are perpendicular, from the rocks
exfoliating along the cleavage-planes, the latter have a regular
N.N.W. dip at an angle of about 30°.

The “Screes’’ of the hill of Barff, like those of Outerside, afford
abundance of fossils of a nature similar to those of the latter locality.
Some of the fossils which occur at Barff were obtained by Professor
Sedgwick at Scawgill, in Whinlatter-fells, which is immediately on
the strike of the Barff strata.

These Scawgill fossils consist of Graptolites sagittarius and G. latus ;
and at Kirkfall, near Scawgill, Palewochorda major is found*.

The position and mode of occurrence of the fossiliferous strata of
Outerside and Barff show that they are the representatives of the
same zone on opposite sides of the anticlinal already alluded to,
and their proximity to this axis leads to the conclusion that their
horizon is low down in the Skiddaw slate series.

Northwards from Barff slaty rocks without very definite bedding
occur. On approaching Wythop-fell from the south, the flaggy
beds, having 8.S.E. dips, again begin to make their appearance
among the more slaty rocks. On the west side of Bassenthwaite
Lake, a short distance south of the landing-place, near the Pheasant
Inn, the flaggy beds with S.S.E. inclinations are seen intercalated
among the slaty rocks; and immediately contiguous to the landing-
place a thick mass of slate makes its appearance, underlying the
flaggy rocks. On the northern escarpment of Wythop-fell, a short
distance west of the Pheasant Inn, the slaty rocks with the inter-
calated flags are well seen, dipping S.S.E. 30°. There is every
reason for inferring that the flaggy rocks seen here are the repre-
sentatives of the fossiliferous strata of Barff and Outerside, and
their opposite inclination to those of Barff shows the occurrence
of a synclinal axis between the latter locality and Wythop-fell.
North of Wythop-fell is the Embleton valley, which is about a
mile wide, extending westward from Bassenthwaite Lake to the
valley of Lorton, and is occupied by till and soil, exhibiting no rock
um situ.

* Barff, being only five miles from Keswick, and close to the high road leading
from thence to Cockermouth, is by far the most accessible locality in the Lake-
district for obtaining Skiddaw slate fossils. In such profusion do they occur
here, that in the course of an hour I obtained a bagful. There is also a comfort-
able small inn, called “ The Swan,’ at the base of Barff.

118 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 17,

Besides the localities alluded to as furnishing Professor Sedgwick
with fossils, there occur, S.W. of the places named, other localities
in the area ‘under consideration which also afforded him organic
remains. At Knockmurton-fell Graptolites latus and G. sagittarius
have been found. Here the dip of the Skiddaw slates, which are
hard and flaggy and of a grey colour, is W.; but this is a local dip.
In this locality the Skiddaw slates yield iron-ore, one vein of which,
about five feet in thickness, striking N. and S., and with an inclina-
tion towards the E., is here wrought.

To the east of this, at Blake-fell, Professor Sedgwick also obtained
Paleochorda minor; and at Lowes-fell, on the north side of Lowes-
water, he mentions Chondrites acutangulus as occurring. Besides
this, I have found here Diplograpsus pristis. The general dip of the
strata in this part of Cumberland is N.N.W., and some of the fossili-
ferous rocks are on the line of strike of the beds of Barff and Whin-
latter-fell. The anticlinal axis, previously mentioned as traversing
the country W.S.W. from Coldale, seems to ran to the southward of
these fossiliferous rocks, and to eross Mellbreak, which is situated onthe
west side of Crummock-water, and is a hill having 8.8.E. dips on its
southern flank. In proceeding northwards from Crummock-water,
down the Vale of Lorton, the mountains on both sides of this valley
are made up of strata which correspond and conform with those on
the west side of Bassenthwaite Lake, and are an extension W.S.W. of
the rocks of that locality. There is an abundance of “ Screes” on
the flanks of the mountains on both sides of the Vale of Lorton, and
also on Mellbreak, which would doubtless afford abundance of fossils
if they were well examined.

On the north side of the Embleton valley are seen ridges of com-
paratively low hills, separating this valley from the vale of the Der-
went. On the south side of these ridges there occurs at Lambfoot-
fell a syenite which, when well exposed in its interior, is seen to be
made up of very distinct crystals, but which near the outer margins
becomes fine-grained and more trappean inits aspect. In this latter
condition it is seen at the farm of Crag, near Bassenthwaite Lake, and
eastward from Lambfoot-fell on its line of strike. Immediately north
of this syenite, at. Lambfoot-fell, are seen hard, flaggy Skiddaw slates,
dipping N.N.W. 20°.: .

This inclination is the reverse of that which occurs on the opposite
or south side of the Embleton valley, and indicates the presence in
this valley of another anticlinal axis, parallel to the one which
manifests itself to the southward. The Skiddaw slates of Lambfoot-
fell incline towards a small ‘valley separating this hill from the Hay,
which forms part of another ridge north of the Lambfoot-fell range.
In the Hay the Skiddaw slates are of a similar nature to those of
Lambfoot-fell, and also have the N.N.W. inclinations. East from
the Hay the ridge becomes higher, and forms Dunthwaite-fell, where,
at Elba Plains, there are the same hard, grey, flaggy rocks, with
intervening slaty beds, as seen at the Hay. Here also the dip is
N.N.W. 35°, and the rocks, as well as the hill, slope away towards
the River Derwent. . i .

1862. | HARKNESS—SKIDDAW SLATE SERIES. 119

The rocks north of the Embleton valley differ somewhat in their
mineral character from the Skiddaw slates which lie south of this
vale, being harder, of a lighter colour, and having a greater affinity
to the greywacke sandstones and shales of the Southern Highlands
of Scotland.

North of the River Derwent, in the district between this and the
margin of the Carboniferous rocks, the country is comparatively flat,
and no good exposures of rock occur. In the course of a stream
called Scalegill, which flows from the west side of Binsey Crag into
the Derwent, there are seen at intervals small exposures of rock
an situ. Several of these occur in the course of this rivulet through
the flat moory country which lies between Binsey Crag and Sunder-
land, and exhibit soft black shales, considerably contorted, resembling
the Skiddaw slates as they occur in the small areas of Westmoreland,
rather than the rocks lying westwards of Bassenthwaite Lake and
Derwentwater. Although considerably contorted, the prevailing
inclination in this most northerly district of Skiddaw slate is N.N.W.,
and on the northern margin of this moory tract the Carboniferous
formation makes its appearance, as seen at Sunderland.

With reference to the section extending from Newlands on the
south to Sunderland on the north (fig. 2), no fossils have been
obtained from that portion of the Skiddaw slates which lies north
of the Embleton valley. There is, however, every reason to believe
that, when the rocks in this portion of the area have been carefully
examined, they too will furnish the same organic remains as occur
in the strata lying on the south side of this valley. In the more
southern portion of the area under consideration, the mode in which
the rocks occur and the localities in which the fossils are found
justify the conclusion that, notwithstanding the cleaved character of
the great mass of the deposits, there are strata in which this structure
is only very imperfectly developed, and which possess a well-marked
flagey nature. These flaggy beds occur at intervals through the
whole of the Skiddaw slate series ; and, wherever they present them-
selves, they yield fossils which are identical throughout the series,
marking these deposits as paleontologically the same through the
whole of the group.

§ 3. The Skiddaw Slates of Cumberland, east of Derwentwater and
Bassenthwarte Lakes.

The north-eastern portion of the Lake-district is occupied by an
extension eastwards of the Skiddaw slates which occur in the area
already described. This portion has for its western boundary the
eastern limits of the district just alluded to, being flanked on this
side by the northern end of Derwentwater, the River Derwent, and
Bassenthwaite Lake. Its northern boundary is the porphyritic rocks
of Caldbeck-fells. On the east it is margined by Carboniferous
rocks which skirt Carrock-, Bowscale-, and Mungrisdale-fells; and
on the south the greenish-grey rocks which occur north and west of
Matterdale, forming the northern flanks of Great Dod, White Pike,
and Wanthwaite Crag, and, extending from the entrance into the

120 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec..17,

Vale of St. John westward to Keswick, bound the Skiddaw slates of
this portion of Cumberland.

The southern portion of this area rarely exhibits the rocks in situ.
The Skiddaw slates in this district occupy Flascow Moor, a large
tract of barren country lying between the Keswick and Penrith Road
on the north, and the base of the hills just referred to on the south.
Two streams, having their origin among the greenish-grey rocks on
the south, intersect this moory district in their course to the Glen-
dermaken River, which flows into the Greta near Threlkeld. The
most easterly of these streams, called Troutbeck, after passing over
the greenish-grey rocks, reaches the moory country, and begins to
exhibit in its course the Skiddaw slates. In a small brook which
flows into Troutbeck from the west, these slates are considerably
contorted, but have predominant 8.S.E. dips. A short distance
above the hamlet of Troutbeck this inclination is well seen, the
angle being 40°; and a gritty quartz-rock, strongly impregnated
with iron-pyrites, is here seen associated with the Skiddaw slates.
For a considerable distance below this hamlet, through the moor,
no exposures of rock occur; but when the stream reaches near to
the Keswick Road, parallel to which it flows for some distance, we
have good sections of the Skiddaw slates, principally on the line of
strike. The stream in this portion of its course is called Gills-beck,
and here the Skiddaw slates, which are thin-bedded and of a dark
colour, have prevailing N.N.W. dips. Intercalated with the strata
are masses possessing the structure known as cone-in-cone, a feature
which accompanies the Skiddaw slates im some other localities. In
some portions of this section there are great contortions in the bed-
ding, and quartz-veins are abundant, running along the lines of the
contortions.

Fig. 3.—Section from Matterdale to Uldale (12 miles).

‘
‘
S

a. Skiddaw Slates. 6. Granite. ¢. Green slate and porphyry.
d. Felspathic Traps. e. Carboniferous rocks.

N.N.W. S.S.E.
1) > 2 .
.. > Gare B u
= o = os 2 oo =
7 ~~ . a QQ = no 2)
oa ame as) > sy or as =
: to 6OU a 2 a = Ee Ss
See Sede ete ris g «5 eee 5
3 “ -_ Uh =| — Ye ~~ : ~
os — ES S & i 2H 3 (Till.) =
= 3 ° Gq 3 3 S iS)
» | =) 9 S) <3) Rae =
: i : A i -

Westward from this stream we have the Skiddaw slates exhibited
in the course of another brook, which also traverses Flaseow Moor
from the south. This, which is known as Mosedale-beck, rises from
the northern flank of Great Dod, and its upper portion is likewise
over the greenish-grey rocks. The junction of these with the Skid-
daw slates in the course of this brook is not seen, in consequence of

1862. | HARKNESS—SKIDDAW SLATE SERIES. 121

the peaty nature of the country at the base of the crags of the green-
ish-grey rocks. Below this peaty interval the Skiddaw slates occur,
and are seen in Mosedale-beck, consisting of contorted black shales,
like those of Gills-beck, having the cone-in-cone masses imbedded
among them.

The Skiddaw slates in the course of this stream have a prevailing
N.N.W. inclination. They yield Graptolites sagittarius *.

The interval of country between the Keswick Road on the south
and the Glendermaken River on the north affords no exposures of
rock. In the Glendermaken, as it flows along the eastern base of
Souter-fell and south from Mungrisdale, the Skiddaw slates, of a
dark colour, are seen at intervals dipping 8.8.E. At Mungrisdale
these Skiddaw slates are worked, and have a well-marked cleavage ;
but the surfaces of some of the strata very frequently show distinct
tracks. Tracks similar to those of Mungrisdale also occur at Two-
seats, near Threlkeld, on the south base of Saddle-back, which is on
. the line of strike of the Mungrisdale beds. The strata at Mungris-
dale, some of which are flaggy, dip towards the 8.8.H. at 55°.

With reference to the Souter-fell ridge, which hes between Mun-
erisdale and Saddle-back, on its south side it has a very regular slope,
while on the north side it is more abrupt and marked by escarpments,
from which results a considerable development of “ Screes.’’

Among these ‘“‘Screes,” tracks are found resembling those of
Mungrisdale, and the rocks which produce the “ Serees” dip 8.8.E.
about 30°. On the opposite side of the valley of the Glendermaken, »
north of Souter-fell, the ridge known as Bannerdale-fell is seen.
In the south spur of this ridge a considerable mass of chiastolite-
slate makes its appearance, and has been extensively wrought here.

The first appearance of this mineral in the Skiddaw slates is
marked by the occurrence of chiastolite in the form of very small
dots, and some of the rocks so marked contain tracks. Following
the southern spur of Bannerdale-fell northwards, the chiastolite is
seen to become more abundant, and, on the higher portions of the
hill, obtains to such an extent as to constitute chiastolite-rock ; and
rocks of this nature form the ridges which occupy the southern side
of the Caldew valley. A southern spur from Bowscale-fell, called
Tongue, parallel to the southern spur of Bannerdale-fell, exhibits
similar rocks to those just described.

Following the Glendermaken, between Souter-fell and Banner-
dale-fell, to its source, tracks occur, on the south-west flank of
Bannerdale-fell, in the unchanged Skiddaw slates which dip S.S.E.
Towards the north these slates become more black and glossy, and
have spots of chiastolite in them. A short distance brings on the
chiastolite-slates, and at the summit of the low ridge connecting
Bannerdale-fell and Saddle-back the chiastolite-rock occurs.

* The streams which intersect Flascow Moor cut through a fine mass of glacial
débris, consisting of sandy clays containing imbedded boulders of the several
rocks which occur in the northern portion of the Lake-area. These boulders are
often very beautifully striated; and on the surface of the moor large erratic
blocks are very common.

122 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Deewars,

From this ridge northwards, in passing into the Caldew valley, a
still greater exhibition of the metamorphic changes produced on the
Skiddaw slates by the influence of the granite of the Caldew valley
is seen. In Black Hazel-gill, a stream which flows from the north
side of Saddle-back into the River Caldew, the following changes in
the metamorphic rocks occur. In the higher portion of the stream
chiastolite-rocks are found; below these there comes on dark-
coloured hornblendic rock, which passes downwards into horn-
blendic gneiss, and in some cases into mica-schist, the whole dipping
S.S.E.; and, in the bed of the Caldew, granite appears. A similar
sequence of metamorphic rocks is seen in the course of other streams
which flow from the southern ridges of the Caldew valley.

Professor Sedgwick has described a nearly similar sequence of
metamorphic rocks as occurring on the south side of the Caldew
valley.

On crossing the area occupied by the granite of the Caldew valley,
and following the course of the streams which flow from its northern
slope, we have the metamorphic series of the Skiddaw slates, but not
so well developed on the north side of the River Caldew as on the
south.

Wiley-gill is one of the tributaries of the Caldew from the north,
and enters this river a short distance above the junction of Black
Hazel-gill, flowing from the south. The lower portion of Wiley-gill
is over granite, which forms the south base of the hill on its eastern
side.

This granite is not seen in the stream, the lowest rocks shown in
situ having a gneissose character; but the exposures of rock in this
brook are by no means good. At the junction of a small stream
which joins Wiley-gill from the east, slates having a chloritic nature
are seen dipping 8.8.E. at a high angle; and at the head of Wiley-
gill rocks of nearly the same nature occur, haying a glossy aspect
and a light-grey colour. Here they are almost vertical, but still the
prevalent dip is 8.8.E.

On crossing over the watershed at the head of Wiley-gill, north-
wards, there is the head of astream called Whitehouse-gill ; ordinary
Skiddaw slates of a grey colour, having a vertical cleavage and a
well-shown 8.8.E. inchnation of 30°, here present themselves. The
south side of the hill called Burn Dod, forming the northern side of
the valley drained by Whitehouse-gill, is covered with small blocks
of a coarse, gritty character, containing occasionally fragments re-
sembling Skiddaw slate. Similar coarse rocks are alluded to by Pro-
fessor Sedgwick as occurring in the mass of Skiddaw. At the south-
west base of Burn Dod, Whitehouse-gill is joined by Frozzen-gill,
flowing from the north-east ; and the hill called Cockup-fell, lying on
the north side of this stream below the junction, exhibits the mode
of association of the grits, which are seen covering the south side of
Burn Dod, with the Skiddaw slates. On the south-west side of
Cockup-fell, where these gritty beds have been wrought, they are
seen interstratified with the Skiddaw slates, and dipping at a high
angle towards the 8.S.W. On the east side of Cockup-fell and in

1862. | HARKNESS—SKIDDAW SLATE SERIES. 123

the lower portion of Frozzen-gill, these grits also occur under like
circumstances. |

In following up Frozzen-gill to its source, the Skiddaw slates are
well seen; they consist of grey beds considerably contorted, but with
prevailing S.8.E. dips; and on both sides of the stream abundance
of “ Screes”’ occur, from which Graptolites were procured, including
the branching form before alluded to, and also tracks.

North of the head of Frozzen-gill, on the opposite side of the water-
shed, is the source of the Ellen, the river which enters the sea at
Maryport. The banks of the stream, at its highest part known as
Ellen-gill, afford exposures of rocks in situ, consisting of grey Skiddaw
slates also dipping 8.8.E. ; and on following down its course, as it flows
between Lowthwaite-fell and Mell-fell, the Skiddaw slate is again
seen, dipping 8.8.E. 35°.

There are numerous “Screes” on the sides of this stream yield-

ing ordinary Graptolites and the branching form, the latter in con-
siderable abundance *. The Skiddaw slates prevail down Ellen-gill
for a considerable distance, when they are succeeded by rocks of a
trappean nature, as these are exhibited in the enclosed ground on
the north side of Lowthwaite-fell. East from this, at the head of
Red-gill, and partially also at the head of Silver-gill, the Skiddaw
slates make their appearance f.
_ The western side of the district of the Skiddaw slates under con-
sideration is well seen among the rocks forming the western skirts
of Skiddaw. In this portion of the district, to the north of a thick
mass of quartz-veins known as ‘“‘ White Stones,” above a plantation
on the south-west side of Skiddaw, there is an escarpment of flaggy
rocks; they dip 8.S.E. 30°, and are associated with cleaved strata.
Beneath this escarpment ‘“ Screes” are found which furnish Grap-
tolites sagittarius, G. tenuis, Diplograpsus pristis, Tetragrapsus (the
branching Graptolite before referred to), Crustaceans, Annelid-tubes,
and tracks.

The whole of the fossils here have a great resemblance to those of
Outerside, on the opposite side of Bassenthwaite Lake, and the posi-
tion of the rocks here shows that they are an extension E.N.E. of
the strata of that locality. Northwards from the escarpment of the
south-west of Skiddaw, along the eastern skirts of the Dod-fell, al-
though cleavage with a north-west inclination greatly prevails, the
direction of the dip of the strata is on the whole 8.8.E.; and the
same dip may be seen on the road along the western base of Dod-
fell, between Bassenthwaite and Keswick.

North of Dod-fell, which is the western spur of Skiddaw, on the
side of the hill immediately north-east of Mirehouse, another escarp-

* On merely passing over the “ Screes ” of Frozzen-gill and Ellen-gill, I found
the fossils alluded to in considerable quantities, especially in the latter locality.
There is every reason to infer that if these “ Screes” were well examined, they
would afford numerous fossils, some of which might probably prove to be new.

+ Red-gill is the only locality in England which affords the rare mineral ca-
ledonite—the cupreous sulphato-carbonate of lead. This, however, is not ob-
tained from the Skiddaw slates, but in igneous rocks occurring here which will
subsequently be alluded to.

124 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 17,

ment is seen, from which “Screes” have originated. The strata
here are contorted, but on the whole the dip is S.S.K. They have
a mineral nature like the rocks north of White Stones, and like them
they also afford Graptolites, among which Giraptolites sagittarius is
most abundant *.

In the Skiddaw slate district lying east of Keswick Lake and Bass-
enthwaite Lake there is no axis distinctly shown. Sections along
the western side of this area and along its eastern margin alike
manifest a succession of §.8.E. dips from the northern portion of the
Skiddaw slates almost to their southern limits. In this area also,
wherever the Skiddaw slates occur, if they do not exhibit a highly
metamorphic condition, nor a great development of cleavage, they
yield the same fossils throughout the series.

§ 4. Carrock- and Caldbeck-fells.

Allusion has already been made to the granite of the Caldew val-
ley, the Skiddaw Forest granite of Professor Sedgwick. ‘This rock
is seen extending down the course of the Caldew at intervals to near
the junction of the stream flowing from the north, called Brandy-gill.
It forms the south-east flank of the hill lying west of Brandy-gill,
the surface of this flank being strewed over with granite-blocks.

From this hill it is well seen in the lower portion of the Brandy-
gill rivulet, where it occurs in the condition of a fine-grained granite,
much intersected with quartz-veins.

On the east side of Brandy-gill the same fine-grained granite is
seen, forming the western spur of Carrock-fell, also much intersected
by quartz-veins. From this spur eastwards, the crest of Carrock is
flat, and covered with peat and vegetation, exhibiting very few traces
of rock; but when the east side of the north spur of Carrock is
reached, a very felspathic granite, approaching somewhat to porphyry,
makes its appearance, and this forms also the summit of Carrock-
fell, Although differing in its texture somewhat from the granite
seen in Brandy-gill, I have little doubt of its being a continuation
of the same mass, which, following the strike of the stratified
rocks, extends W.S.W. into the valley of the Caldew, and E.N.E.
through the northern half of Carrock-fell. On the south side of the
granitic area there is seen, forming the southern mass of Carrock, and
in close contact with the fine-grained granite of the western spur
of Carrock-fell, a rather singular felspathic rock, consisting of two
felspars, orthoclase and labradorite, and having an aspect greatly
resembling that of a greenish-coloured syenite. This rock is not
however confined to Carrock, but occurs also among the Caldbeck-
fellst.

* The localities in the neighbourhood of Keswick which afford fossils, viz.
Outerside, Barff, Skiddaw, Longside, and Mirehouse, were, I believe, first re-
cognized as fossiliferous by Mr. Joseph Graham, mineral-dealer, Keswick.

ft The quartz-veins of Carrock-fell are famous for the rare minerals which
they afford. Besides wolfram, which is found in considerable abundance,
they yield scheelite (tungstate of lime), apatite, telluric bismuth, molybdenum-
glance, and also, to the north-west of Carrock, in Caldbeck-fells, fine specimens

ee ee

hana a tet

1862. | HARKNESS—-SKIDDAW SLATE SERIES. 25

On the north side of the granite of Brandy-gill, in the course of
the stream, hard, grey, crystalline rocks devoid of bedding occur ; and
rocks of this character are seen likewise in the courses of Thief-gill,
which flows from the north side of the western spur of Carrock-fell
into Brandy-gill. Although devoid of bedding, these rocks often
show traces of lamination, and they appear to be the representatives
here of those gneissic rocks which are so well developed on the
south side of the plutonic area. What they pass into northwards is
not seen, the flat summits of the Caldbeck-fells being extremely

eaty.

: The interval between the north end of Carrock-fell and the south
side of High Pike, the adjoining mountain, does not exhibit the rocks
in situ, so that the relation between the plutonic masses of Carrock-
fell and the igneous rocks of the Caldbeck range is not apparent.
The brook-courses in the interval also afford no Skiddaw slate, and
there is strong reason for concluding that no sedimentary rocks in-
tervene between these plutonic and igneous masses.

High Pike itself is composed, for the most part, of claystone-por-
phyry, which is well seen in the course of the Pottsgill-beck, a
stream flowing from the north side of this mountain by Caldbeck
into the Caldew. This claystone-porphyry has a greyish-drab colour,
and contains yellow crystals of felspar, which are generally partially
decomposed. ‘The stream which flows to the west of Pottsgill passes
over rocks which have a similar nature.

In the upper portion of Roughten-gill, a stream which rises among
the flat summits of Caldbeck-fells and flows northwards through
these mountains, there is a more varied series of igneous rocks. On
the moors at the head of this stream claystone-porphyry, similar to
that just alluded to, occurs; on passing down the stream, a mass of
compact felspar makes its appearance; and this is succeeded by a
considerable development of a rock composed of orthoclase and la-
bradorite, like that forming the south side of Carrock-fell, and in
which the lead-veins at Roughten-gill principally occur.

One of the best exposures of the porphyritic rocks of Caldbeck-
fells is seen in the course of a stream called Charlton-wath, flowing
between Brae-fell and Langlands-fell. The upper portion of this
stream is over claystone-porphyry, being an extension westwards
of that at the head of Roughten-gill. Lower down the stream, and
near the junction of a rivulet flowing from the south-west, a grey
trap makes its appearance. For some distance below this junction
no rock is seen ; but after the barren interval is passed over, we come
upon a fine-grained, greenish-grey, felspathic rock, beyond which is
a small development of claystone-porphyry. Still lower down the
stream we meet with a rock having a singular aspect. This rock is
much broken wp in structure, has a mottled appearance, and seems to
be composed of white and green felspars. It is usually partially
decomposed, and its mottled character is well seen on its weathered
of phosphate of lead. There occur also arsenio-phosphates, sulphates, cupreous

sulphates, and cupreous sulphato-carbonate of lead; and along with these are
seen radiated malachite, brochantite, and other minerals.

126 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Decra7}

surfaces. This mass of rock is probably the same as the double-
felspar rock of Roughten-gill, with larger crystals, which appear to
have undergone changes from chemical action. Below this mottled
rock, in the course of the stream, we come upon a grey felstone, well
developed, and succeeded by a purplish claystone which, on passing
downwards, assumes a porphyritic nature, containing small white
crystals of felspar. This last-named rock is seen immediately above
the moor-road to Caldbeck, and a short distance below this road the
Carboniferous rocks occur *.

The felspathic rocks extend still further to the north-west. The
mottled rock is seen on the west side of Langlands-fell, and in it
copper has been partially worked. The grey felspathic traps occur.
in Lowthwaite-fell, and from thence they extend to the north side
of Overwater, being well seen at Latrig-fell, which lies immediately
north of this small lake ; they are also well exhibited in Binsey Crag,
where they are principally of a porphyritic nature. Here some-
times they occur in the form of strata, and seem to be composed
of masses of felspathic ash, containing fragments of felspar-por-
phyry. When presenting this aspect, they have a conglomeratic
nature, and are excessively hard. On the north side of Binsey a
fine purple porphyry, with greenish crystals, is seen ; to the north of
this, on the ridge called Whitehouse Hill, hard grey rocks make their
appearance, being succeeded northwards by the Carboniferous series.
To the west of Binsey Crag and Whitehouse Hill there again occurs
a flat moory country like that before described in connexion with
the Skiddaw slates.

I believe that Professor Sedgwick 1s disposed to regard the felspathic
traps of the Caldbeck-fells Range as the northern equivalents of the
greenish-grey rocks which, to the south, succeed the Skiddaw slates.

5. The Skiddaw Slates of the Eastern Margin of the Lake-district.

At the lower end of Ullswater, a small stream called “ Ellerbeck ”
enters the lake from the south; it crosses the road leading from
Pooley to Howtown, and, at a short distance above, divides into two
branches. The more southerly branch is known as Egebeck ; the
lower portion of its course is over gravel and large blocks of stone
derived from the boulder-clays of Doveack Moor. On ascending the
stream, after passing through the enclosed ground, a plantation is
reached which marks the boundary of the cultivated land, and above
which rocks are seen, in situ, in the bed of the brook.

These rocks consist of contorted shales, dark in colour, thin-
bedded, and having a great resemblance to the graptolitiferous shales
of Dumfriesshire, but they do not present beds so highly anthracitic
as those of the south of Scotland ; as they are much broken up by
closely approximated joints, they have a very shivery character.

On ascending the stream, above the dark shales others are seen

* IT am indebted to Mr. Joseph Peat, of Caldbeck, for directing me to the
several streams in this district where good sections occur, and also for informa-
tion concerning the igneous rocks and mineralogy of Caldbeck-fells.

~

1862. | HARKNESS—SKIDDAW SLATE SERIES. 127

of a lighter colour, which are again succeeded by dark shales resem-
bling those below, and containing Graptolites. Drab shales are seen
above these in the course of the brook, having intercalated grey
beds, the whole presenting a shivery aspect.

Above the foregoing shaly strata, for a short distance no rocks
are seen in the bed of the stream ; but a little above where the main
road from Barton to Martindale crosses Eggbeck, a greenish-grey
porphyry, with orange-coloured crystals of felspar, makes its ap-
pearance, and continues to occupy the bed of the stream to near its
source, having occasionally ashy masses intermixed with it.

The Graptolites which occur in the dark shales of Eggbeck con-
sist of Graptolites sagittarius and Didymograpsus geminus, together
with the branching form previously referred to. These fossils are
by no means abundant here, and, owing to the shivery nature of the
strata, they are usually in a fragmentary condition.

Fig. 4.—Section from Ullswater to Wastdale Crag (11 miles).

N.N.W. S.S.E.
“= 3 = of
3 & 2 ® a
2 : 5 : -Q = -
; rt Ale Ne ie. See Ss wd = shite
So ue RC: ice a a on So ae
A jen] ? eS (a) 3 . oG o oO 3
ea eS a en)! a aE n ‘ina
Sy GR 88) OR Wad wg Seuulie g 2
ae es, Ga ee “Ea #8 a
i i : Cee 3 I ; : PE 3 as a
auth b i eae
VF A
YS LIN
S S > MH, MY SAAR ES
Skiddaw Slates. Green slates, Skiddaw Green a b
porphyries, &c, Slates. slates, &c.

a. Trap. 6. Syenite.

Lying west from Eggbeck is Barton-fell. At the top of this hill
is a greenish, ashy-looking grit; and in the stream which separates
Barton-fell from Swarth-fell, the hill still further westwards, the
porphyries of Egebeck are well seen, together with greenish rocks,
which are not porphyritic, intercalated among them, but having no
distinct bedding. The rocks here are rudely prismatic, and to the
S.S.E. they seem to pass upwards into the greenish-grey rock above
alluded to.

Egegbeck is the only spot in this neighbourhood where the Skid-
daw slates are seen. To the north of Barton-fell and Swarth-fell,
both of which rise boldly above Ullswater, exhibiting escarpments
on their north sides, there is a comparatively low tract of country ;
but there no rocks in situ appear, the interspace from the south side
of Ullswater to the adjoining hills being covered by soil and débris.
The contour of the country, however, justifies the conclusion that
the Skiddaw slates extend some distance along the northern base
of Barton-fell and Swarth-fell, but that they soon become covered
up by the porphyries, ash-beds, and green slates, which are so ex-
tensively developed along the margin of Ullswater, from Howtown to
Patterdale, and also in the mountainous district lying southwards.

128 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee t7,

There are strong reasons for inferring that the presence of the
Skiddaw slates at Eggbeck is the result of an anticlinal axis crossing
this portion of the Lake-district and extending in a W.S.W. direc-
tion. Proofs of the existence of this axis can be seen in the neigh-
bourhood of Patterdale. On the east side of this portion of Ulls-
water several slate-quarries have been wrought, at Blowick, along
the western base of Place-fell.

These slates usually show very imperfect stratification, and the
cleavage commonly intersects the bedding. In some localities, how-
ever, the dips are apparent, being 8.8.E., generally at an angle of
30°, which is also the prevailing dip of the Skiddaw slates at Egg-
beck. On examining the arrangements of the lines of lamination
among the slates here, they also are found to conform to the dips
of the strata. Among the more regularly stratified beds east of
Patterdale, there is often a rapid thinning-out of the strata.

On the opposite side of the lake, in the face of the cliff looking
towards Ullswater, immediately north of Patterdale Hall, the strata,
which consist of a dark greenish-grey grit, spotted with red, so as
to have almost a porphyritic appearance, dip towards the N.N.W.
about 35°, an inclination directly opposed to that on the east side of
the lake.

These features support the inference that the axis before referred
to extends through Place-fell, and, crossing the upper reach of
Ullswater, passes through Grisedale, from whence it runs in the
direction of the granite-area in the lower part of Eskdale, in West
Cumberland.

To return to the section along the eastern margin of the Lake-
district. To the south of the porphyries and greenish-grey rocks
associated with them in the higher portion of Eggbeck, we have in
Heltondale a development of the greenish-grey grits with indistinct
dips, but apparently inclining 8.8.E. These also occur further south
at Butterwick, where they are intersected by north and south joints ;
and here likewise the stratification is imperfect. Southward from
this, at Bampton, the greenish-grey rocks are also seen, being worked
here for building-purposes.

In this locality, besides the ordinary greenish-grey rocks, there
occur others which contain angular fragments of a hard, grey rock,
not unlike some of the harder varieties of the Skiddaw slates, im-
bedded in a greenish-grey matrix. A similar rock is seen on the
road from Ullswater, leading over Karkstone Pass, and is also worked
for a building-stone in Borrowdale.

The rocks at Bampton dip N.N.W. about 40°, and in the interval
between this and Butterwick a synclinal axis occurs. Southward
from Bampton, in the neighbourhood of Thornthwaite Hall, situated
on the stream which flows out of Haws-water, there is a large mass
of the greenish-grey rocks; they continue southwards, forming the
ridge called Scaleborrow, that separates the Haws-water valley from
Swinedale. Here too the rocks are equally devoid of stratification,
but are much intersected by joints, which often assume so regular an
aspect as to look like bedding.

a

1862. ] HARKNESS—SKIDDAW SLATE SERIES. 129

On the south side of Scaleborrow, in Rossgill-beck, which flows
into the stream draining Swinedale, the Skiddaw slates are again
seen; and here they were formerly worked for slate-pencils. In
this locality the slates, which are somewhat shaly, are, by cleavage
and fine jointing, cut up into long thin pieces. Intercalated with
them are masses possessing the cone-in-cone structure, and which on
decomposing produce abundance of hydrated peroxide of iron, show-
ing their affinity in composition to iron-stone. The strata here are
much contorted, but on the whole dip 8.8S.E.

Higher up Swinedale than the junction of Rossgill-beck, where
the rocks become prominent on both sides of the dale, they consist
of the hard greenish-grey grits, equally without distinct bedding
with those lying northwards, and to such an extent cut by vertical
joints that they have a columnar aspect. This exposure of the Skiddaw
slates in Rossgill-beck is doubtless the result of another anticlinal,
which, like that before alluded to, has a W.S.W. strike.

In the course of the River Lowther, southwards from the junction
of Swinedale-beck, no rock is seen for a considerable distance. On
the east side of the river occurs the Carboniferous series, which
bounds the Silurians on the east. The lower part of the Carboni-
ferous rocks is well seen in the escarpment on the east side of the
Lowther, immediately above the ruins of Shap Abbey; here also the
equivalents of the green slates and porphyries are seen in the
stream, and, in consequence of having been stained by the beds of
the Carboniferous series, they present a purple colour.

Above Shap Abbey, a small stream enters the Lowther opposite
to the hamlet of Keld, and is called Keld-gill. Between this and
the Abbey there are abundant exhibitions of rock in the course of
the Lowther, all of which possess the greenish-grey colour and an
imperfectly bedded character.

Southwards from Keld-gill, over that portion of Rafland Moor
which lies between this and another small stream, called Thornship-
gill, no good exposures of rock occur; and this remark applies also
to the River Lowther in the interval between the junctions of these
streams.

The lower part of the course of Thornship-gill is over gravel
composed of small rounded fragments of Skiddaw slates; and on
following up the stream for a short distance, these rocks are seen in
situ. They consist of dark-coloured, shaly beds, like those of Ross-
gill and Eggbeck, enclosing masses which have also the cone-in-cone
structure. The strata here are much contorted, but the prevailing
dip is N.N.W. Quartz-veins intersect the beds, and have a N.W.
and §.E. strike. The slates here, like those of Rossgill, are much
broken up by cleavage and jointing; and they have also been exten-
sively wrought for slate-pencils. This locality also affords fossils,
among which we have Graptolites sagittarius, the branching forms, and
others too imperfect to determine. In one locality on the N.E. side of
Thornship-gill, porphyry is seen, which, from the dip of the slates,
must overlie the latter, and here consequently we have the same
sequence of strata that occurs at Eggbeck.

VOL, XIX.—PART I. K

130 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ DéGaigs

The appearance of the Skiddaw slates in this locality must be
referred to the same cause to which those of Rossgill and Eggbeck
have been assigned, namely, the occurrence of another anticlinal
parallel to those already mentioned.

In following up the Lowther from the junction of Thornship-beck,
we have at intervals many exposures of the imperfectly bedded,
greenish-grey rocks. These are well seen at Cragg Mill on the
north side of Shap Moor, and among the rocks here are found the
masses which have the imbedded angular fragments already men-
tioned as occurring at Bampton and elsewhere. Like the same rocks
at Bampton, it is probable that they mark the position of a syncli-
nal, the rocks on their N.N.W. side having a 8.8.E. dip, while in
Wet Sleddale, on the south side of the Lowther, an opposite dip
obtains. In the streams flowing from Wastdale Pike and Harrup
Pike, which are tributaries to the Lowther from the south side of Wet
Sleddale, the prevailing dips are also N.N.W.

On the high road leading from Shap to Kendal, owing to the moory
nature of the ground, the greenish-grey rocks are not well seen in
the interval between Shap Common and Wastdale Crag.

In this interval we have, however, at Blea-beck, a mass of basalt
crossing the road, and extending north-eastwards to the Lancaster
and Carlisle Railway, where, at the summit-cutting, this basalt and
its relations to the Silurian and Carboniferous rocks can be distinctly
made out (fig. 5).

Fig. 5.—Section at the Summit-cutting on the Lancaster and

Carlisle Railway.
N. Ss.
Carboniferous beds. Conglomerate.

/}
ae ph ly yf
Mu a VEZ,

ed

Basaltic trap-rocks.

The principal mass of this cutting is the basaltic trap, which on
its north side has greenish Silurian shales dipping N.N.W. at a high
angle (above 50°). Upon them, and also upon a portion of the trap,
conglomerates occur, made up of fragments of Silurian shales, quartz,
chert, and trap, and dipping N.E. 10°. The conglomerates have
purple grits above them, the total thickness of both being about
20 feet; and an irregular, nodular limestone, averaging a foot in
thickness, lies upon the latter. On this irregular limestone, 8 feet of
purple shales with limestone-nodules are seen, being succeeded by
grey shales about 5 feet thick, having upon them another nodular
limestone 18 inches in thickness, above which is a white grit, sup-
porting the hard limestone which is wrought on Shap Moor.

The junction between the greenish-grey rocks and the porphyritic
syenite of Wastdale Crag is nowhere very apparent. There is seen,

1862. | HARKNESS—SKIDDAW SLATE SERIES. 131

however, on the east side of the high road, a small quarry in which.a
felstone occurs, intermediate in character between a syenite and the
greenish rocks ; and a similar rock is also seen south-west from Wast-
dale Crag in the direction of Long Sleddale, where it is known under
the name of “flint.” It is probably a mass of plutonic rock having
the same origin as the Wastdale Crag syenite, but possessing a less
crystalline nature in consequence of more rapid cooling from having
been in immediate contact with the greenish-grey rocks.

§ 6. The Skiddaw Slates of Black Comb.

The most southerly position occupied by the Skiddaw slates in
Cumberland or in Westmoreland is Black Comb, a mountain rising
abruptly to the height of 1919 feet, in the south-west of Cumber-
land; it is surrounded on all sides, except the west, by the greenish-
grey rocks which succeed the Skiddaw slate series in the north of
England. On the west side, Black Comb is margined by a compa-
ratively low and flat tract of country, composed of the Trias sand-
stones extending southward from St. Bee’s Head, and flanking on the
west side the Silurian rocks and their accompanying granites and
syenites.

To the south of Black Comb there is a flat tract of country which
separates this mountain from the greenish-grey craggy rocks of Mil-
lom, and in which no rocks are seen, the area being covered with till
and soil. Still further south, greenish-grey rocks occur, exhibiting
their usual broken outline, and presenting bold escarpments towards
the north—a feature generally accompanying their line of outcrop,
while on their dip they present commonly a less rugged aspect. To
the S.S.E., at Millom, these greenish-grey rocks pass under the
Coniston limestone and Coniston flags, which also dip S.8.E.

Fig. 6.—Section across Black Comb (5 miles).

Whicham.
Stoneside-fell. Black Comb. (Till and soil.) Millom.

a
a. Skiddaw Slate. 4. Green slate, porphyries, &c.

On the north side of the Whicham valley (the flat interspace just
alluded to, where the southern flanks of Black Comb exhibit the
Skiddaw slates) the beds dip N.N.W.

Portions of the southern escarpments of this mountain have been
wrought for slate ; and among the débris of the quarries Graptolites
may be found, though from the Black Comb beds I have obtained
only one species, namely, Graptolites sagittarvus. The position of the
strata here shows that they are very low down in the Skiddaw slate
series.

K 2

132 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 17,

The rocks on the southern flank of Black Comb consist of strata
with slaty cleavage, interstratified with flaggy beds, the latter yield-
ing fossils and dipping N.N.W. Along the course of the stream flow-
ing from near the summit of Black Comb southwards, and which
is known as Black Comb Beck, a coarse slaty cleavage prevails
among the rocks, which also dip N.N.W. These rocks abound in
quartz-veins, in which cobalt has been sought, but without profit-
able success.

Towards the south-west side of Black Comb, a little above Whicham
Church, the Skiddaw slates are also seen. Here they are hard, and
possess somewhat the nature of flinty slate. In this locality also
cobalt has been attempted to be worked. Continuing along the west
side of the range, the Skiddaw slates still have the N.N.W. in-
clination, but at varying angles; they are well seen at Whitebeck
and also at Foss-beck *.

North of Foss-beck, near Hole-beck, and on the south side of the
latter stream, a fine-grained grey granite occurs, which has been
worked ; but it seems in no way to affect the general arrangement of
the Skiddaw slates. This granite was described as occurring here by
Mr. J.G. Marshall at the Manchester Meeting of the British Associ-
ation, 1861. The Skiddaw slates of Black Comb continue northward
to near Bootle, where the porphyries associated with the greenish-
grey rocks begin to make their appearance.

The Skiddaw slates of the Black Comb range do not extend north-
wards beyond the parallel of Bootle, the road from this place over
the hills to Broughton exhibiting no Skiddaw slate. At Fell Green,
a mile east of Bootle, on this road, the greenish-grey series and
the accompanying porphyries are seen, and the country between
this and Stoneside-fell is composed of rocks of a similar character.
At Stoneside-fell, on the south side of the road, a dark porphyry
with light-grey crystals appears in this greenish-grey series; and
the outline of Corney-fell, a hill on the north side of this road, in-
dicates that the rocks which compose it also belong to the same
greenish-grey series. At the Druids’ Temple, about a mile south-
east of Stoneside-fell, they also occur, while at Swineside, a short
distance to the west, the Skiddaw slates make their appearance,
dipping N.N.W. 40°, and having a greyish-drab colour.

The section of the Skiddaw slates of Black Comb shows an almost
continuous N.N.W. inclination, from their appearance on the south-
ern flanks of this range until they are succeeded by the greenish-grey
rocks of Stoneside-fell. Their relation to the greenish-grey series on
the south, at Millom, is seen in Professor Sedgwick’s section f.

In the Whicham portion of the section there is a great fault, from
which the rocks dip in opposite directions. The continuous exposures
of N.N.W. dips in the Skiddaw slates of the Black Comb range,
from the southern flank for about three miles N.N.W., lead to the
conclusion that on the south side of this range ‘some of the lowest

* There are abundant ‘‘Screes” on the west side of the Black Comb range ;

and, if well examined, they would no doubt afford fossils. °
+ Quart. Journ. Geol. Soc. vol. ii. p. 111.

1862. ] HARKNESS—SKIDDAW SLATE SERIES. 133

beds of the series are exposed. This conclusion shows that Grapto-
lites occur very low down in the series,—an inference which is justi-
fied by the sections of these rocks as seen in other localities.

§ 7. Conclusion.

The lithology of the Skiddaw slates varies considerably in the
several areas where they occur, and, with reference to geological
position, there is in some cases a difference in their mineral nature.
This, however, is not of so uniform a character as to admit of this
series being divided into subgroups marked by mineral aspects. The
fossil contents are even less applicable for subdivisions than mineral
nature, since, as already stated, the same organisms are disseminated
through the whole of this portion of the Lower Silurians as they
occur in Cumberland and Westmoreland. Under these circumstances,
I am induced to look to other evidence for relative position among
the strata forming the Skiddaw slates.

The physical geology of the various areas under consideration
shows that in all of them, except that which lies west from Derwent-
water and Bassenthwaite Lake, axes are by no means well exhi-
bited. Even in that large area south of Caldbeck-fells there is no
well-defined axis, but a continuous 8.8.E. dip from the northern
limits of the Skiddaw slates almost to their southern margin. The
area west of Derwentwater and Bassenthwaite affords two well-
marked axes; and the nature of the rocks between them shows that
the Skiddaw slate series is made up of fine indurated shaly beds
with well-developed slaty cleavage, having intercalated through them
coarser strata almost devoid of cleavage, possessing a flaggy nature,
and affording fossils.

-From Newlands, where the upper members of the Skiddaw slates
are seen with the superposed greenish-grey rocks, to Coldale, where
the most southern of the axes just alluded to occurs, the distance is
less than three miles measured along the dip, which averages 30°.
This portion of the section (see fig. 2, p. 116) would give a thickness
of Skiddaw slates, from the greenish-grey rocks above to the lowest
beds exposed at Coldale, of about 7000 feet; and this is probably
their average thickness where best seen in the north of England.

The thickness of the succeeding greenish-grey rocks is not so
easily made out. There are, however, circumstances which render
it probable that these latter rocks do not exceed in thickness those
of the Skiddaw slate series; so that between the base of these latter
and the Coniston limestone, the equivalent of the Bala limestone,
there is a varied mass of rocks of 14,000 feet in thickness, the lower
half consisting of rocks of a sedimentary nature, while the upper
half is composed of rocks which had an igneous origin, and which
consist principally of porphyries and ashes. This thickness of rocks,
which in Cumberland and Westmoreland lies below the Coniston
limestone, corresponds with the thickness of the Llandeilo flags*.

The Skiddaw slates yield some forms of Graptolites which occur in
the southern Highlands of Scotland, indicating some paleontological

* ‘Siluria,’ 2nd edit. p. 194.

134 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 17>

affinity between the rocks of these areas. There is, however, in the
former, so far as we yet know, an absence of the genus Rastrites,
which is well represented in the south of Scotland; but we miss in
the Scotch deposits the genera Dichograpsus and Tetragrapsus, which
make their appearance in the Skiddaw slates. But with reference to
the fossils from this series, their nature and the evidence they afford
as to age are discussed in a note which Mr. Salter has kindly added
to this memoir.

If we take into consideration the direction of the strike of the
strata in the north of England and in the south of Scotland, we
find in this a great conformity, the prevalent strike in both countries
being W.S.W. and E.N.E.; and, with reference to the dips, the di-
rection generally obtaining north of the Border is N.N.W., while to
the south thereof the most common inclinations are S.S8.E. The
physical geology of the older rocks of the north of England and
south of Scotland supports the conclusion that the disturbing forces
which acted upon them operated in both areas at the same geolo-
gical epoch; and also, judging from the arrangement of the meta-
morphic rocks of the Highlands proper, that the strata of the north
of Scotland owe their elevation to the same period.

The general arrangement of the older rocks of the north-west of
England shows that not only have the Lower Silurians been sub-
jected to elevations producing a W.S.W. and E.N.E. strike, but also
that the succeeding Coniston limestone, Coniston flags, Coniston grits,
Treleth flags, and Kendal group of Professor Sedgwick—deposits occu-
pying the horizons of the Caradoc, the Llandovery, the Wenlock, and
the Ludlow series of Sir R. I. Murchison—were elevated at the same
time as the older Silurian deposits.

In Cumberland and Westmoreland, the older palozoic rocks are
succeeded unconformably either by the Upper Old Red Sandstones or
by the Carboniferous strata, both of which have strikes totally at
variance with the older rocks ; and consequently we are led to infer
from this evidence that the elevations of the Silurian series, both in
the northern and southern Highlands of Scotland and in the north
of England, took place during the earlier portion of the Old Red
Sandstone epoch.

Denudation has removed from the northern Highlands probably
all the Upper Silurians (the metamorphic character of most of these
rocks does not allow of their being assigned to very definite Silurian
zones), and in the southern Highlands nothing remains of the older
paleeozoic rocks except the Lower Silurian series. In that portion
of the north of England which most nearly approximates to the
Silurian area of the south of Scotland, we have also only the lower
members of this series represented, while further to the south, denu-
dation not being so powerful, the whole of the Upper Silurian rocks
occur.

The eastern edge of the older paleeozoic rocks of Cumberland and
Westmoreland had suffered a considerable amount of denudation
antecedent to the deposition of the Upper Old Red series, for, in these
latter, fragments of Skiddaw slates are, in some localities, very abun-

1862. ] HARKNESS—SKIDDAW SLATE SERIES. 135

dant. The exposure of the Skiddaw slates at Black Comb also shows
that the south-west margin of the area of the older paleozoic rocks
has likewise been subjected to great denudation.

As concerns the age of the Skiddaw slate series, the sequence of
the strata above it, its position, and also its depth below the Coniston
limestone would lead to the inference that it occupies the horizon of
the Llandeilo flags; and the fossils corroborate this conclusion.
Mr. Salter has already pointed out the affinity of these fossils to
those of the lower portion of the Llandeilo series* ; and in a note he
informs me that the Skiddaw slates are referable to “that group
which is best represented in the rocks of Shelve, and which occurs in
North Wales overlying the Tremadoc group, and underlying the mass
of the Llandeilo,—a series containing the earliest and most varied
forms of Graptolites, and which is at once the birth-place and metro-
polis of the family, as nowhere else are there so many gcnera or such
complex forms.” This evidence, combined with the sequence of the
rocks in the Lake-district, distinctly places the Skiddaw slate series
on the horizon of the Lower Llandeilo, and also places the Quebec
group of Sir William Logan, as suggested by Mr. Salter, in the same
position.

Note on the Sxippaw Stare Fosstrs. By J. W. Satter, Esq., F.G.S.,
A.L.S., of the Geological Survey of Great Britain.

Tue persevering labours of Prof. Harkness have been again rewarded.

But little was known, notwithstanding the old explorations by Prof.
Sedgwick, of the fauna of the Skiddaw slates till within the last
three years, when, at my request, Mr. Bryce Wright took advantage
of a short residence each year near Skiddaw to search for organic
remains in what proves to be a rich formation. The Museum in
Jermyn Street and the Cambridge Museum have received, since
that time, many accessions through Mr. Wright’s labours. The
fauna proved to be of a newer date than had been assigned to it in
Prof. Sedgwick’s table of classification : not, indeed, relatively to the
other rocks of the Lake-district, for the Professor has put it in its
right place with respect to them; but instead of being, as suggested,
an equivalent of the great formation of the Lingula-flags, its fossils
indicate it to be of the age of some part of the Llandeilo-flags; and
I shall endeavour to show that it must be the lower portion of that
formation.

Two species of Graptolites and some imperfect remains (considered
as sea-weeds by Prof. M‘Coy) were the fossils known to Prof.Sedgwick
at the time of the publication of his great work in 18517.

Mr. Wright fortunately discovered at least six more Graptolites,
and a Crustacean with a curious, elongated carapace of two valves,
which I shall here term Caryocaris (fig. 15), as it has long wanted
a name. An obscure figure of it appeared in the ‘ Geologist’ of
February 1861, together with a figure of the most remarkable of the

* ‘Geologist,’ vol. iv. p. 74.
att : Synopsis of the Classification of the Paleozoic Fossils in the Woodwardian
aLuseun..

136 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Deesky,

new Graptolites—a doubly and triply branched form which I termed
Dichograpsus, after ascertaining its identity with those remarkable
fossils discovered by Sir W. Logan near Quebec, of which he sent
drawings to England many years back, and which, admirably en-
graved, were to be seen in the Canadian Department of the Great
Exhibition.

There were also with these forms some foliaceous Graptolites,
which I have referred to Phyllograptus, Hall, together with the now
well-known species Graptolites sagittarius and G'. tenuis, the latter
very abundant. Mr. W. West, of Wimpole Street, has since made
some notable additions to this list, and some of his specimens are
figured on p. 137.

Prof. Harkness has not only added to our correct knowledge of the
beds from which these are obtained, but has also furnished a few new
forms to the British list; among them, especially, the beautiful
Didymograpsus caduceus, a swallow-tailed form, formerly described
by myself, from Canada.

Indeed, the most interesting point about these collections is the
positive identity that appears to obtain between the fossils of the
Skiddaw slates and those of the Quebec group of Canada. In both
we have the ordinary genera of Lower Silurian Graptolites—
Graptolites, Diplograpsus, and Didymograpsus ; but mixed up with
these are some others peculiar to this horizon, viz. Phyllograptus,
the Dichograpsus mentioned above, and a kind of double Didymo-
grapsus, for which it is perhaps admissible to form a new genus—
Tetragrapsus.

The series of forms in the Graptolite group is now so perfect, that
it may well be surmised that we have pretty nearly exhausted the
variations.

There are simple Graptolites with a single row of cells, unbranched
or only irregularly proliferous—Graptolites. Straight Graptolites
with a double row of cells—Diplograpsus. Twin Graptolites, having
a single row of cells only on each branch, the bifurcation taking place
from the root—Didymograpsus (figs. 13 a to 13 f); again, a form in
which this bifurcation takes place twice, the branches patent or
nearly close—Tetragrapsus (figs. 8.a,86); Phyllograptus (Hall), also
composed of four stems, z.¢. doubly branched, but the stems close
together, and giving the appearance of a cruciform Diplograpsus
(figs.7a,7b). Tetragrapsus comes near to the Canadian genus Dicho-
grapsus, Which is doubly branched, and again dichotomous more than
once, in most of the species. But the main character which distin-
guishes Dichograpsus is the presence of a corneous plate which en-
velopes all the lower part of the branches (fig. 10), and which is not
known in any other genus of the group; it has not, indeed, been seen
in more than two or three species of Dichograpsus, but it may not
have been preserved in all cases. I still believe that the best ana-
logy for this plate is in the basal plate of Defrancia, a Bryozoon com-
pared with it several years back by Huxley. Lastly, we have the
extremely branched form Dendrograpsus (Hall), the name of which
sufficiently expresses its ramose character. The branches in this

a

Figs. 7-15. Sketches of Graptolites from the Skiddaw Slates. (Natural size.)

i. Phyllograptus, Hall. 8. Tetragrapsus, gen. nov. (a. is the typical form; 6. may possibly
be a form of Dichograpsus). 9. Dichograpsus araunea, Salter. 10. Dichograpsus, Salter,
with its corneous cup (from Logan). 11. Dichograpsus Sedqwickii, Salter. 12. Branchlet
of Dichograpsus. 13. Several forms of Didymograpsus. 14. Branching Bryozoon? 15.
Caryocaris Wrightii, Salter.

138 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 1%,

genus have no connecting bars; but in Dictyonema, which is the
oldest form of the Graptolite group, the rods are held together by
very regular processes, that give the whole frond, which is tubular,
exactly the aspect of a Fenestella. The presence of the projecting
Graptolitoid cells and the horny texture, however, prevent its being
confounded with that genus; but the resemblance is very close, and

the general agreement of the long-celled Graptolites with recent
genera of the Tubuliporide.

I herewith give figures of the new species of Dichograpsus, Tetra-
grapsus, &¢. ; ‘and it subjoin a list of all the known Skiddaw slate
fossils. Those marked W. were collected by Mr. Bryce Wright;
those marked H. are due to the researches of Prof. Harkness ; and
those marked ‘ West’ are from that gentleman’s collection.

Fosst1s. LocaLitres NEAR SKIDDAW.
Radiating Worm-burrows...............0+ Skiddaw, Longside (H., West).
Annelid-bunrowal pense a. -: snes. oc eoeere Hodgson, Holm (W.), Keswick, &e.
Nereities 2 i.) -iscanggcees anne tease eee: Skiddaw, Longside (H.).
New Crustacean—Caryocaris ee Outerside, Barff, Skiddaw, Longside
n.s., fig. 15. (W., H., West).
Graptolites sagittarius, His. ............... Scawgill, Hakengill, Mirehouse, Brai-
thwaite Brow (W.., H.).
tenuis; POred. sxc sweet sttee sande c sages Keswick (W., H.).
—=— Nilsson, Bart.,.n20) scales cnaceees Braithwaite Brow (W.).
lotus, ME Cowen. sesaccnics acoso Braithwaite Brow, Whiteless, Scawgill
(Sedgw.).
ADE niseciecyacinniod sapadn Oona d deladaedaciiat Keswick.
Diplosrapsus pristis7, 210s. ....Fe..2.c6o0 Braithwaite Brow (W.).
Didymograpsus sextans, TON i. siass'- A Braithwaite Brow (W.).
hirundo (MS.), fe 1S fh ost. c cea Ellengill (W., H.).
geminus~2zs., fig. 13.65. 3in.saccene Eggbeck, Ullswater (H.).
caduceus, Salter, fig. 13a,b.. Keswick (H.).
sp. like G. Pantoni, “Mt Coy, fic. 13e
(DV siraetus:2MS.) dacccccmesaeansaeee Keswick (West).
Phyllograptus angustifolium, Hall, fig.
Tg (CO penonSae tte tee ae areas Barff, Keswick (W., H.).
Dichograpsus Sedgwicki, fig. 11 ......... Braithwaite (W.).
sp., small branches, fig. 12 ......... Keswick (H.).
Tetragrapsus bryonoides, Hall, fig. 8a... Frozzengill (H.).
Crucialis) Nsjs5 MELO Owe esteecucteee Keswick.
Dichotomous Bryozoon ?, fig. 14......... _ Barff, Keswick.

A few words will suffice to show the relations of this fauna with
that of the corresponding beds in other countries. In the grouping of
the Graptolites of the Skiddaw slates there is the closest resemblance
to that group discovered by Logan near Quebec, and which is known to
some authors under the name of the Taconic system. All the forms
are representatives in the two cases, and several of the species are, I
believe, identical; but as the Canadian figures have not yet received
their long-desired publication, we cannot identify the names except
in a few instances.

Moreover, there is a remarkable coincidence, even to minutie of
character, between the Skiddaw slates and the Graptolite-bearing
rocks of Melbourne, Australia. In the collections sent over by

1862. | HARKNESS—SKIDDAW SLATE SERIES. 139

Prof. M‘Coy and Mr. Selwyn to the International Exhibition, a
large series of Graptolites appeared; and these agreed, genus for
genus, and almost specifically, with our North-of-England forms. I
cannot think this accidental, and believe, therefore, that there is a
peculiar zone or horizon of the Llandeilo rocks of which these genera
of Graptolites are characteristic*.

The mass of the Llandeilo strata is not tenanted by such compound
forms. The species of Didymograpsus known in the Upper Llandeilo
have the branches diverging at a moderate angle, while the strata
known as Lower Llandeilo in England have the widely diverging
forms of this genus, and such are found in the Skiddaw slates.

In Canada the age of the Quebec series is still under discussion ;
but all agree in placing it low down in the Silurian seriest. Here the
association of these Graptolites with Trilobites is such that we must
either refer them to the Primordial group itself, which is unlikely, or
allow that they represent the lowest beds of Lower Silurian rocks,
the passage-beds from the Primordial zone to the Llandeilo flags,—
the age, in fact, of the Tremadoc slates and Lower Llandeilo.

With regard to the so-called sea-weeds, fucoids, &c., I have shown
elsewhere reason for believing that nine-tenths of these are due to
the action of marine worms. In the Skiddaw slate series there are
found abundant traces of these markings.

CaryocaRis, gen. nov. C. Wrieutii, sp. nov. Fig. 15.

A long, pod-shaped, bivalved carapace (with distinct hinge-pits),
rounded anteriorly, subtruncate behind, and with the back and front
subparallel. The surface is smooth, or with only oblique wrinkles
near the margins, but with no parallel lines of sculpture. Body?
Telson and appendages ?

All I know of this pretty little Crustacean, an inch long, and
rather more than one-third of an inch wide, is contained in the above
note. I was fortunate enough to find the tubercles (Huxley found
them also in Ceratiocaris), which I suppose indicate teeth (and cor-
responding pits) at each end of a short hinge-fulerum. They are
marked a.

The shelly carapace is solid for its size: it appears to have a good
deal of lime in its composition. The genus is evidently distinct,
though so little is known of the entire form.

- Loc. Everywhere in the Skiddaw Slate district. I have named it
after Mr. Bryce M. Wright, of Great Russell Street.

Dicnoerapsts, gen.noy. Figs. 9 to 12.
Frond repeatedly dichotomous from a short basal stipes into 8, 16,

* There is even a Crustacean, apparently of the genus Caryocaris, which
M‘Coy has done me the favour to name Hymenocaris Salteri.

+ Hall has definitely added (see Proc. Amer. Phil. Soc. 1862) his opinion to
give weight to the idea that the Quebec Graptolite-group (including the Hudson
slates west of the river, as decided by Logan’s discovery of the great fault) implies
simply a different condition of the Calciferous Sandstone. ‘Quebec group ”
would surely be a better term; or why not “Skiddaw group”? It is the
oldest.

140 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Deer 17,

24, or more branches, each with a single row of cells—not a double
row as supposed by Prof. Hall, who must have seen the ends of the
cells crushed vertically upon the narrow stipes.

TETRAGRAPSUS, gen. nov. Figs. 8a, 8 b.

Fronds twice dichotomous near the base, of simple, long-celled
stipes ; the base of the branches not connected by a corneous plate
(the branches sometimes patent, sometimes closely reflected: M‘Coy,
in literis).

Puytioerartvs, Hall. Figs. 7a, 76.

There are two species of this beautiful genus in the slates ; but I
prefer to leave the description of them open for the present. Prof.
Wyville Thomson is hard at work on this group, and it is a pleasure
to put good materials in the hands of so good a naturalist.

Two of the most remarkable of these Graptolites (see figures 8
and 13) were drawn from specimens in the collection of Mr. W.
West, of Wimpole Street. I refer specially to the rare Tetragrapsus
erucialis, and the Didymograpsus marked e, fig. 13, which is exceed-
ingly like D. Pantoni, M‘Coy, from Victoria. I have called it D.
V-fractus. In truth, no one can collect in this region without
doing some good; for the Skiddaw slate is the metropolis of the
Graptolites.

2. On Fossin EstHEerta and their Distrisution. By T. Rupert Jonsgs,
Esq., F.G.S., Professor of Geology and Mineralogy at the Royal
Military College, Sandhurst.

Introduction.—In 1856* I offered to the Society some remarks on the
probably Crustacean character of the little fossil that used to be termed
Posidonomya minuta, on its Estherian relationship, and on some points
in the geological distribution of Estheria+. Much of the material that
I have used for my ‘ Monograph of Fossil Estherie,’ published by the
Paleeontographical Society, was then in my hands, but much informa-
tion and very many specimens have been contributed since by friends,
abroad and at home, so that I am now enabled to recognize fourteen
fossil species, with several varieties. These are from the freshwater
or brackish-water deposits of the Devonian, Lower and Upper Car-
boniferous, Permian, Triassic, Rheetic, Oolitic, Wealden, and Tertiary
formations.

Though often imbedded in shales or marls in close proximity to
other beds containing truly marine organisms, and even near beds
impressed with casts of salt-crystals, yet the fossil Hstherie have

* Quart. Journ. Geol. Soc. vol. xii. p. 376.

t In this paper Hstheria was erroneously referred to as a marine Crustacean ;
and a mistake was made in the allusion to a Silurian Nummulite. The lime-
stone containing this Nummulite is Carboniferous; but, coming from a Silurian
district in Shropshire, it was at first mistaken for Aymestry limestone.

1862. ] JONES—FOSSIL ESTHERIZ. 141

rarely any unmistakeable sea-shells associated with them in the
same bed; and, when such do occur (as in the case of Lingula tenws-
sima), the marine mollusk sometimes appears to have been dwarfed
by deteriorating influences. From what we know of the habits of
existing bivalved Entomostraca, it is probable that some degree of
saltness could be borne by Estheriv, temporarily or continuously ; but
the recent Estherie (of which 22 species are known) have been mostly
found in rain-water pools and other fresh waters, and a few only
have been met with in brackish marshes, and none in the sea. So
also, of the allied Limnadia and Limnetis, their six or seven species
have all freshwater habitats.

If living in lagoons communicating with the sea, the old Estherve
would have occasional marine companions; and those associated
shells that seem to have belonged to the sea from their supposed
relationship to existing marine mollusks may really have been in-
habitants of brackish water, or of more or less saline lakes. Where,
therefore, Hstheriw occur by themselves, or in the company only of
Fishes and Plants (as is often the case), it appears to me that they
may be regarded as having lived and died in fresh (or possibly
brackish) water. Where they are mixed with shells of presumed
marine habitat, they probably indicate either that they inhabited
brackish lakes having a quasi-marine fauna (such as the Caspian
Sea), or that fresh water was in close proximity to the place of
deposit ; or that they had lived in fresh water that had been perhaps
frequently replaced by the sea.

The fossil Hstherice will serve the geologist as useful indicators of
even transient changes of fresh- and salt-water conditions, either in
shallow water on coasts, or in inland lakes, where evaporation and
influx of rain-water, each varying in amount periodically, may have
produced freshwater, brackish, and saline deposits alternately.

I refer to the ‘ Monograph’ for full descriptions and illustrations,
and for copious references to the works of others on the subject.

Table of the Fossil Estherize and Leaiz*.

Genus and Species. Locality. Geological Stage.

Estheria membranacea, Livonia; Caithness; Ork-|Old Red Sandstone.
Pacht, sp.| ney.

striata, Miinster, sp. |Bavaria; Belgium ......... Lower Carboniferous.
— , var. Tateana ...|Berwickshire ............... Lower Carboniferous.
—— ——, var. Beinertiana Silesia; Lancashire; La-|Lower Coal-measures.
narkshire.
—— ——, var. Binneyana |Derbyshire .................. Lower Coal-measures.
— , var. Beinertiana|Lancashire .................. Middle Coal-measures.

—— tenella, Jordan, sp. .../Lancashire; Lanarkshire ;|Upper Coal-measures,
France (Autun); Sch-| or Permian.

warzwald (Murgthal).
Sele Segaddenbedte ls Saxony (Salhausen) ...... Lower Permian.
—— exigua, Hichwald, sp. |Russia (Orenburg and{Permian.
Kazan).
—— Portlockii, Jones ...... ‘Tyrone, Prelate’. 22 c33. 2 Permian.

* Leaia is a problematical ally of Estheria.

142 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 17,

Table (continued).

Genus and Species. Locality. Geological Stage.
Estheria minuta, Alberti, sp.|Alsace; Hanover ......... Bunter.
SE cc teat ce tates Germany (Wiurtemberg,/Lettenkohle.
&e.).
Sean clan ud crooner sss Worcestershire ; Keuper.
Warwickshire; Somer-
setshire.
—— ——, var. Brodieana |Gloucestershire; Somer-|Rheetic. |
setshire; | Morayshire
(Linksfie!d).
—— Mangaliensis, Jones ...!Mangali, India ............ Triassic or Rhetic.
| —— ovata, Lea, sp.......... N.America (Pa. Va.Ca. &e.)/Triassic or Rheetic.
Kotahensis, Jones...... otal inctas sieaccs cece: Jurassic or Rheetic.
concentrica, Bean, sp./Yorkshire .................. Oolite (Lower).
— Murchisoniz, Jones...|\Skye..........2...:0ceeeceeeees Oolite (Oxfordian).
elliptica, Dunker ...... FISMOMER con tence ee oc eceere Wealden. |
aaa , var. subquadrata Hanover; Sussex ......... Wealden. |
Forbesii, Jones......... Cacheuta, South America |Mesozoic ?
Middendorfii, Jones.../Tourga, Siberia ............ Tertiary ? |
Leaia Leidyi*, Lea, sp. ...|Pennsylvania ............... Lower Carboniferous.
, var: Salteriana, |iMifeshine*s/se..sscca-s. soaeee Lower Carboniferous.
— , var. Williamson-'Lancashire .................- Upper Coal-measures.
jana.

1. Estheria membranacea, Pacht, sp., was described by me in 1859 ¢
under the name of Estheria Murchisonianat. It is found abundantly
in the fish-bearing flagstones of the Old Red Sandstone of Caithness§$
and Orkney; and in a marl at Kokenhusen, Livonia, which belongs
also to the Old Red or Devonian group. This species has more nearly
equilateral and orbicular valves than most of the known Estheria,
and the umbones are more nearly centrade than in any except
E. concentrica; the valves resembling in outline those of a minute
Posidonomya or Aviculopecten||. Owing to its suborbicular shape,
Dr. Pander, to whom I am indebted (through Von Helmersen) for
a valuable bibliographical note on this species, retains Pacht’s generic
term “ Asmusia” for this fossil; but I do not see any necessity for
it, as the difference in outline between this and other Hstherice is one
of degree only, and not essential.

The only fossils that are associated with EZ. membranacea are Fishes
in Caithness and Orkney, and Fishes and Lingula bicarinata in

* Cypricardia Leidyt, Lea. t Quart. Journ. Geol. Soc. vol. xv. p. 404.

t I thought that the name “‘ membranacea”’ was preoccupied for a fossil Estheria
(of the Wealden); but, although used in collections, it had not been applied in
books; and if it had, the ground of its application, namely the supposition that
Cyclas membranacea, Sow., is an Estheria, is baseless. Cyclas subquadrata, Sow..,
is a Wealden Estheria.

§ Banniskirk,Caithness, is another locality, in addition to those mentioned in my
‘Monograph,’ judging from a specimen that I lately saw in the Newcastle Museum.

|| Mr. S. P. Woodward suggested its crustacean character in 1854; and Dr.
Pander also regarded it in that light not long afterwards. Sir R. Murchison,
Mr. C. Peach, Mr. J. Miller, and others (including Dr. Pander and M. d’Eich-
wald in Russia) have helped me in working out the history and nature of this
Estheria.

1862. ] JONES—FOSSIL ESTHERLE. 143

Russia. Lingule occur also with Estherie in the Triassic beds of
Germany, and certainly must be accepted as evidence of marine
conditions, according to paleontological rules; but the Triassic
LTingula tenuissema, in successive beds, appears smaller and smaller
in size, until it is dwarfed and disappearing, when Estheria minuta
comes in; as if more and more fresh water invaded the area, un-
favourably to the Lingule, and ultimately bringing in the Estherie.
The Lingula bicarinata has been referred to as presenting “ traces ””
only, in some instances, in the Estherian marl of Kokenhusen ; hence
these Lingule may have been “ derived” fossils; or more probably
they may have been truly of marine and local origin, but destroyed
by the invasion of the fresh water which favoured the Estherie. The
fossil Fishes of Scotland and Russia, associated with the Estheria,
do not bear any exact testimony of marine conditions (although
occurring in some places with truly marine fossils); their recent
allies are the Polypteride and Siluride, inhabitants of rivers and
lakes; and they may have been at home in both fresh and salt water.

2. Estheria striata, Minster, sp., does not bear the true Estherian
characteristics so clearly as HL. membranacea. The brown, horny, wide-
ridged, neatly sculptured valves of the latter are here replaced by
black, filmy, closely striated valves, which, however, by their tenuity,
their ovato-oblong shape (similar to that usual among Estherie), and
even by their close striation, different from that of Aviculide and
Anthracomye, and not unlike what occurs in some Hstheriw under
certain conditions of growth, appear to me to belong to this genus.
Their gregariousness and their associating with Fishes and Plant-
remains are also habits common to them and Estheriw. In one in-
stance (Lammerton) I have seen reticulate texture in the valves, and
that helps to place them aright. Further, they present subquadrate
or rather suborbicular individuals (Lammerton), a peculiarity found
- also with two or three known species of Estheriw,—the difference of
form being probably of sexual significance. Lastly, in the Coal-
measures there are smaller Estherie, with distinct ridges, interspaces,
and sculpturing ; and, were the large and the small found together (as
the large and small of #. ovata and E. elliptica are found together
presenting similar differences to those under notice), I should be in-
clined to regard them as presenting stages of growth; for we find
not unfrequently that the older individuals of Hstheria cease to de-
velope evenly separated concentric ridges and neat uniform inter-
spaces, and produce layer after layer at the edge of the valve so
rapidly that nothing but a series of close concentric striew is to be
seen; and this growth seems also to occur sometimes in small speci-
mens that have not had favourable conditions of growth.

E. striata has passed about from name to name* in paleontological
works ; in collections too the specimens have been doubtfully placed ;
and such good geologists as Mr. G. Tate and Mr. E. W. Binney
refused to give them a place among the Mollusca; they indepen-
dently suggested an Estherian relationship for specimens which they

* Sanguinolaria striata, Minster and Goldfuss; Cardiomorpha striata, De
Koninck.

144 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Deter,

each confided to me some years since. So also Geinitz and Beinert
eliminated F. striata of Silesia from amongst the mollusks.

Count Miinster’s specimens came from the Lower Carboniferous
shales near Hof, Bavaria; De Koninck’s from the same horizon at
Visé, Belgium. The many specimens that have come under my
notice differ, for the most part, in some slight degree as to their
outline ; and, as they belong to several different localities, and to
different horizons in the Lower and Upper Carboniferous formations,
I have regarded these slightly different features as of varietal im-
portance. Thus, £. striata, as recorded by Goldfuss and De Koninck,
serving as the type, we have a very similar form from Silesia (Lower
Coal-measures, Beinert), from Lancashire (Middle Coal-measures and
upper part of the Lower Coals, Binney), and from Lanarkshire (Lower
Coal-measures, Binney). ‘This is distinguished as £. striata, var.
Beinertiana, after Dr. Beinert of Charlottenbrunn, who collected the
Silesian specimens in the Lower Coal-measures at Volpersdorf, in the
Duchy of Glatz. Z£. striata, var. Tateana, less oblique in shape, is
from the Lower Carboniferous shale at Lammerton on the Berwick-
shire coast, where Mr. G. Tate, F.G.S., found it abundantly in one
bed, with remains of Plants, Fishes, and Cypride*. Occasional
evidence of reticulate structure accompanies these EHstherie, and
among them are individuals with the subquadrate or suborbicular
valves above referred to.

Estheria striata, var. Binneyana, has a fine large carapace with ob-
long valves, and occupies a shale found (by Mr. Binney, F.R.S., F.G.S.)
near Chesterfield, Derbyshire, and lying between the Winnmoor Coal,
below, and the Black Shale or Silkstone bed, above (distant about
70 yards).

With regard to the possibly freshwater or marine character of
Estheria striata, as indicated by its associates, leaving out the Fishes
as altogether doubtful witnesses, I can only say that, excepting the
occasional proximity of those dubiously marine forms, the Anthracosie
and Anthracomye, and the presence of Spirorbis at Lammerton, sea-
shells are wanting in the shales and cannel-coal in which this
Estheria has been found. As for the presence of Spirorbis, Sir C. Lyell
has before now pointed out that the occasional influx of salt water
into a marshy jungle can destroy terrestrial vegetation. and leave, on
retiring, Serpule and Cirripedia attached to the stems.

3. Estheria tenella, Jordan, sp., is the true Estherian species to
which I have alluded above as occurring in the Carboniferous strata,
and fit to stand as the young of #. striata, had we the evidence of
collocation and gradational conditions of growth to support the
supposition. .

I have not, however, seen them in the same bed, and the largest

* One specimen only of these Cyprids is sufficiently preserved even for partial
examination. ‘To indicate its seeming alliance, and the circumstance of its dis-
covery, I have named it (in the Appendix to my Monograph on Fossil Estherie)

Candona? Tateana.
t Some of the so-called Spirorbes and Microconchi found in the Coal-measures

have of late been looked upon by Continental paleontologists as being possibly
due to minute parasitic plants.

1862. ] JONES—FOSSIL ESTHERIE. 145

individuals of Z. tenella yet met with (from Bradford Pit, Manchester)
‘have not taken on the thickly striated valve-surface, such as is seen
in the other form.

This Estheria was first noticed in the Autun shales*, regarded as
of Permian age by some (Geinitz), and as Upper Carboniferous by
others ; it was thought to be a small Posidonia (with some doubt) by
Michelin; A. d’Orbigny, Landriot, and Naumann, however, regarded
it as being probably a bivalved Crustacean. Jordan found it again
in the Upper Carboniferous strata of the Murgthal, near Sulzbach, in
the Schwarzwald, and, with Bronn, named it Posidonomya tenellay.
This is also the species that occurs in the Brandschiefer of the Roth-
liegendes at Salhausen, near Oschatz, in Saxonyt. I have it also
from the Upper Coal-measures at Astley and Bradford in Lancashire
(Binney and Salter), and from the Upper Coal-measures of Lanark-
shire (Mr. Grossart). Lastly, I am inclined to think that EF. exigua,
d’Eichwald, from a Permian marl at Burakova, Russia, may possibly
prove to be the same §.

E. tenella is a relatively small form, and often occurs in immense
numbers. In one instance (Astley, Lancashire) it is associated with
Beyrichice (B. subarcuata), of a form not far removed from the common
B. arcuata of the Coal-measures, but differing, in the less distinct
lobation of the valves, from the Lower Paleozoic species. If this
Beyrichia were as truly marine as the Silurian Beyrichiw proper,
E. tenella must have lived in salt water ; perhaps, on the other hand,
these associates were brought together, to the hurt of one or the
other, by the inroad either of salt or fresh water, respectively. Sp7-
rorbis again appears in company with Hstheria (in Lanarkshire), and
may possibly indicate permanent sea-conditions, as must also Avicula
in the same locality, since it occurs as a participator of the same bed,
unless sudden changes of fresh and salt waters have left their effects
in one and the same deposit, or unless we are looking at the quasi-
marine fauna of an old brackish lake. Anthracomye (Lancashire) and
Anthracosie (Lanarkshire) are also associated with £. tenella.

4, Estheria exigua, Kichwald, sp., is known to me by a few very
small specimens on a little piece of Permian marl from Burakova,
Kazan, Russia, where it is found, with Plant-remains, in some
abundance. These specimens (sent by M. d’Eichwald) are not equal
to those described by Kutorga and d’Eichwald; but they constitute
the only basis on which I can at present form an opinion. My
materials being limited, I keep this form distinct from H. tenella, to
which the Russian specimens (small as they are) present much
resemblance. If they belong to the same species, the name Z. exigua
will have priority ; and, further, we have one more instance of com-
munity of specific forms in the Carboniferous and Permian deposits ;
indeed £, tenella itself proves as much, if the Permian character of

* T have not seen specimens from this locality.

+ Dr. Sandberger has sent me specimens.

¢ Professors Naumann and Geinitz have aided me with specimens.

§ In which case the name given by d’Eichwald in 1846 would have priority,
T have not yet seen enough specimens from Russia to decide by. 5

VOL. XIX.—PART I. L

146 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 17,

the Brandschiefer of Oschatz is unmistakeable, and if the carbonaceous
shales of Autun and the Murgthal should prove to be really Permian,
as some suppose.

EH. exigua is accompanied by a feebly developed Beyrichia (B.
Pyrrhe), to which the remarks made above on B. subarcuata equally
apply.

5. Estheria Portlockii, Jones.—A unique specimen, and that a cast,
in an isolated deposit, is the basis for the determination of this species.
Yet it bears such evident proofs, in shape, surface, and relative size,
of its Estherian relationship, that I do not hesitate to dedicate it to
the eminent geologist who first noticed it (under the name of ‘ Posi-
doma minuta”’) as occurring at Rhone Hill, near Dungannon, Tyrone,
where he found it in the shale-seams between beds of the red sand-
stone containing Palwoniscus catopterus.

The Geological Survey will ultimately clear up all doubt as to the
geological place of this sandstone; in the meantime I follow Sir P.
Egerton and Professor Morris in alluding to it as of Permian age ;
and its position on the map does not seem inimical to this view.

Paleoniscus may or may not have had both marine and freshwater
species, like many recent genera of fishes ; and therefore no collateral
evidence at present exists as to the habitat of E. Portlockii.

6. Estheria minuta, Alberti, sp.—This little Cyclas-like Crustacean
has long been a type-fossil for the Keuper, and more especially for
the lignitic deposits (Lettenkohle) at the base of the Keuper, which
have been sometimes grouped as Lower Keuper and sometimes as
Upper Muschelkalk. ££. minuta occurs in the Lower Bunter of
Eastern France (Soultz-les-bains, Bas Rhin); in the Upper Bunter
at Gersfeld in the West Rhon (Hassencamp), and near Dassel in
Hanover (Volger) ; in the Muschelkalk? at Durlach in Baden (Sand-
berger), and at Weimar in Thuringia (Seebach) ; in the Lettenkohle
of Haute Saéne and Bas Rhin, Baden, Wiirtemberg, Bavariat, Ha-
nover, and Thuringia; in the Lower Keuper at Hall in Swabia (Von
Dechen) ; in the Upper Keuper of Tubingen in Wirtemberg (Bronn).

Table of the Distribution of Estheria minuta in the Huropean Trias.

Baden, Wir- :
ee of the England.| Eastern temberg, and |Hanover. Thurin-

rias. Fra Bavaria, gia.
Upper Keuper ...... * * * *
Dower Metper ost! ells: 1 *
Lettenkohle ai-scsss.| saacey * * * *
Mishel: ccdscuel sesenee «|p yeBeane A Pate WOE at x?
ip pee UNPeE Vie cuend). Mecuuecsuatane dea. x *
Lower Bunter’ ° 2.20.) rsi2 2: * x?

+ The “ Lower Keuper” and the “ Muschelkalk” in this list may both really
have reference to the Lettenkohle group.

t In his ‘Geognostische Beschreibung des bayerischen Alpengebirges,’ &c.,
1861, Gumbel states that ‘“‘Posidonomya minuta” (Estheria minuta) occurs in
each of the three divisions of the “ Lettenkohlengruppe,” the lowest division of the
Keuper in the Bavarian Alps,—the “ Hauptdolomit-Gruppe” being the middle,

ee

eS eo ee

1862. | JONES——FOSSIL ESTHERI A, 147

- In England Z. minuta is abundant in the upper portion of the
Keuper of Somersetshire (C. Moore), Worcestershire (Symonds),
Warwickshire (Strickland, Murchison, Brodie), Leicestershire (Plant),
and Cheshire (Hull); and does not appear to have been met with in
any other division of the English New Red Sandstone.

The sources of information and material that have aided me during
the last ten years in working up the history of H. muta are very
numerous, and I have gratefully acknowledged the help of my
Foreign and English friends—including the veteran Von Alberti, the
late lamented Bronn, and many others, in the ‘ Monograph’ before
referred to.

Habitat of Estheria minuta.—In Alsace, Baden, Wirtemberg,
Bavaria, Thuringia, and Hanover, Estheria minuta is associated with
LIingula tenwissima, a marine shell, which has been subjected appa-
rently to the deteriorating influence of fresh water. (See Mono-
graph, p.48.) Other marine mollusks also, such as Myacites, Ger-
villia, Trigoma or Myophoria, Pecten, and Plewrophorus, accompany
E. minuta at various localities over this wide district, occurring for
the most part, however, in beds amongst which the Estherian shales
are occasionally intercalated. The general occurrence of the Estherie
in interlaminated shaly beds strengthens the opinion that they ex-
isted chiefly at the intermediate periods when fresh water had gained
some predominance in the shallow seas, lakes, or lagoons. In the
Bunter-sandstone of Alsace, land-plants occur in the Estherian clays ;
and here, whilst the freshwater Apus is one of the associates of
Estheria, a Limulus (?) intrudes itself in accompanying strata of the
same age.

In some of the beds of the Keuper, crystals of salt have left their
casts abundantly, showing both the saltness and the shallowness of
the seas or lakes in which the Upper Keuper beds were deposited,
But however near to these salt-bearing beds the Kstheriw occur,
they are never found in them. Such pseudomorphic salt-crystals
occur near Luneberg, in the shales with Lingula tenuissima, alter-
nating with limestones, just above the Lettenkohle group, in the
dolomitic beds of which latter Estheria minuta occurs (sparingly)
with Myophorie, &c.

In England there are no marine organisms (fishes being excluded
as doubtful witnesses) accompanying the Hstherie of the Keuper;
and these might have been at once regarded as of equally freshwater
habits with their recent congeners, were it not that the salt condi-=
tion of the waters depositing much of the Keuper sandstones and
shales is proved by the masses of rock-salt and by the casts of the
cubical crystals of salt occurring abundantly in some beds all over
the country of the Keuper. Still Hstheriw have not been found (to
my knowledge) in these salt-bearing beds. They appear to keep a
definite line above the horizon of the rock-salt and beneath that
of the salt-pseudomorphs, and may represent a nearly, if not quite,

and the Avicula contorta (Bone-bed) series and the Dachsteinkalk constituting
the Upper Keuper, according to Gimbel. He states also that it occurs in the
‘Buntsandstein ” on both sides of the Alps.—March 28, 1863.

L2

148 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 17,

freshwater condition of the waters of the Upper Triassic period for
the horizon and localities in which they occur.

E. minuta, var. Brodieana, is closely related to its type, but is
unfformly of less size, has a relatively smaller reticulation, and is
only found in the next succeeding group of strata above the Keuper,
namely the Rhetic*, formerly known as the Lower Lias shales,
including the Bone-bed. Sections of these beds at Aust Passage,
Wainlode, and Westbury, on the Severn, have been published by
Strickland, Brodie, and Wright; and Mr. Etheridge, F.G.S., has
supplied me with an accurately measured section of the Garden Cliff,
Westbury, in which the exact position of the Estheria-bed and its
relation to the immediately underlying marine limestone are care-
fully attended to (see Monograph, p. 70).. Sections of the same
series in Warwickshire (Binton and Wilmcote) have been made and
published by Mr. Kirkshaw, F.G.8., and Dr. Wright, F.G.S. Near
Frome in Somersetshire, Mr. Charles Moore, F.G.S., has recognized
the Rheetic group containing this Hstheria; and he has found these
strata near Ilminster and elsewhere.

In the north, the Rheetic beds are represented by the fossiliferous
shales of Linksfield, near Elgin, long ago referred by the late Dr.
Malcolmson and Mr. Patrick Duff+ to the Purbeck or Wealden
series; afterwards to the Lower Oolite by Professor Morris; and
lastly to the Rheetic group by Mr. Charles Moore.

At Linksfield E. minuta, var. Brodieana, is of somewhat larger
growth than is usual with the Rhetic specimens of Somerset and
Gloucestershire; and its reticulation is slightly modified, having
sometimes a more linear arrangement of the meshes. It occurs here
in company with hosts of Cypride, that are referable to one species
only, as far as I can see, and that is very close to some of the fossil
and recent freshwater Candone. As Mr. P. Duff referred to it some
years since as Cypris globosa, I retain the trivial name for this
Candona. The so-called Mytilus and other shells of the Linksfield
shales do not occur in the Hstherian marls.

Habitat of KE. minuta, var. Brodieana.—In Gloucestershire, Wor-
cestershire, and Warwickshire, the Rhetic Estheria occurs along a
certain zone immediately above a stratum full of marine shells,
which, like others belonging to this Rhetic stage, appear to be
dwarfed, as if they had been the inhabitants of an unfavourable
locality, or lived in sea-water under the influence of large freshwater
affuents. In the Estheria-bed itself no marine shells are found.
Fragments of terrestrial Plants and of Insects in the associated beds
indicate the near proximity of the land to the waters in which these
deposits were formed. Here, as in the Keuper, we may suppose
that the Hstherie flourished in brackish, if not in fresh, water, at
intervals when the saltness of the sea (or lakes) was more or less
reduced by the land-waters.

* Grouped by Herr Gitmbel in the Upper Keuper, in his ‘ Geogn. Beschreib.
bayer. Alpengeb.,’ a work which I have only lately seen— March 28, 1863, T.R.J.

+ The death of this esteemed geologist, who worked so long and so well at
the geology of Moray, took place during the printing of my ‘ Monograph,’ after
T had received his friendly assistance both by specimens and letters.

Uy) JONES—FOSSIL ESTHERLE. 149

The absence of Estheriw in the Rheetic beds (or Avicula contorta
zone) of Germany is coincident, apparently, with their more decidedly
marine character; more constant marine conditions, perhaps, having
obtained during the Upper Triassic period in that area than in the
Western European region.

7. Estheria Mangaliensis, Jones.—At Mangali in Central India,
about sixty miles south of Nagpur, the Rey. Messrs. 8S. Hislop and
R. Hunter discovered in 1853 a fossiliferous, brick-red, laminated
sandstone*, which contains remains of Plants, of Ganoid Fishes, and
of Labyrinthodont Reptiles (Brachyops laticeps, Owen), and wide-
spread thin layers of Hstheriw. These, though of various sizes and
somewhat different outlines, are all referable to one species, condi-
tions of growth being sufficient, in my opinion, to account for all the
seeming varieties. This Estheria (E. Mangaliensis) is not without
close alliances (as far as the carapace is concerned) to other species,
fossil and recent, as is generally the case; but it gives no direct
evidence as to its geological horizon. The Geological Surveyors of
India seem inclined to regard the Mangali beds as of Upper Palzxo-
zoic age,—with doubts in favour of its Triassic relationship. Mr.
Hislop used to think that it was Lower Jurassic, but now believes
it to be Upper Triassic ; and I am much inclined to this opinion.

The absence of marine remains in the Plant-bearing and Reptili-
ferous sandstone of Mangali goes far to indicate the freshwater
habitat of the Estheriw, which it so abundantly contains. Another
locality for Estherie in Indian strata of approximately the same age
has been found by Mr. W. T. Blanford near Pa‘cheet in Bengal.
Dr. T. Oldham kindly sent me a sample of this Estherian shale; but
I cannot say more than that this Hstheria seems to be the same as
the smaller specimens from Mangali.

8. Estheria Kotahensis, Jones, is from Kotah (or Kota) on the
River Pranhita, Central India, and was found by Mr. Hislop in a
shale occupying a relatively higher geological place than HL. Manga-
hensis, and regarded by him, probably with reason, as of Lower
Jurassic age. It is more nearly allied in some respects to the
Wealden EHstherie than to that from Mangali. Ganoid Fishes
(Lepidotus Deccanensis), Cypride (Candona Kotahensis, Jones), In-
sects, an obscure Unio-like shell, and some Plant-remains accom-
pany this Estheria; and other remains of Plants (Ferns), Fishes
(Lepidotus and dichmodus), and Reptiles (Teleosawrus) are found in
the associated limestone and bituminous shales. Similar strata with
Fish-remains and Estheriw have been discovered by Mr. Hislop at
Katanapali, fifteen miles north of Kotz.

None of the organic remains yielded by these Estherian beds have
marine characters, the fishes being excluded as doubtful witnesses.

The accompanying Table shows the probable correlation of the

eal and Plant-bearing strata of Central and North-eastern
ndia :—

* Quart. Journ. Geol. Soc. vol. xvii. p. 347.

[Dec. 17,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

150

‘dnorg mmaveltg

‘snorojIIS | ‘oU0SOUITT
-soyun puv } uweAowty, | ‘sorteg orou
(4) orgd ‘dnoxg { -Ay-qng “487
-LOWB IO] LIuag |
‘dnoag |
‘R09 aLourd Wf
qnoyyrar p ‘dno \ ‘gatreg
‘opeyS pue ) yoaoy (urydputA “pug
auojspueg | ‘dnor
Larepang}

[BOQ JNOyIM ‘om ‘oyvLOWLOT.S
-W0) ‘OMOJspURY ‘SELIG JOOTITV], “pre
‘SoLIog Ivyeaeg
10 (JOOT[|PoPY JO) vpnueq LoMo'T
Csazudogy )
‘dnorg fuvstury oy} wr0F
spoq aoddn oyy, (‘sutreoq
-[BoQ) ‘solzeg vpnueg ondy,
(Conlayisy) “SoLtog JpyoUe_ |
"SOLIOQ
eyemley pue epnueg soddg ‘We J
[ dojstyy ‘(g) snosovyer¢ |

> “UIP

‘SOLIOG BjJoTIeT puev BMOPLYCTT “19

"erpuy jo Aoaang [eotsopoon

‘DIPUT UkIpSDA-YILOKT PUY Jouquag fo suoYMULLOT NLoZOMINY 42 pun oozosapy ey fo 21qQn], jwoudouliy

|

‘punojopung pure AyrepPopooy_y

Se ee
OL ‘Apepepooy Uy
-yoTU} “IE OOT ouojsoury “qq dnorp)
qnoqe ‘mdse yy 180 Ny |
‘TpoTRyy Jo Avpo-snpoyery ) |
‘poyreur-yovry (
‘Ipeyloy, Jo soyeys snosoey[wry 7
‘sJUDI_ pus ‘saysyy ‘ajudoay WYTAK |
‘TTesury, jo suoyspuns-nrwoysy | ‘go pus |
‘Indsv Ny Jo souojspuvs-yuepy J sdnorg )
‘JOIUL A JO SoTBYS-[VO0A }

‘ROY JO saypys-wrway?
-sq pue ‘ouojsotmy ‘sopeys-ystyy )
‘0006 “SITH @opeqeyy 94}

Joyun Fy “ye pue doystzT “Gg ‘sassoyy

"SOLIOG OUOJSPUBY TOALOTT

‘oOJSpUBY
Pau = le

‘seTeUS

‘SOLLOG poJeUIMIe’T | BIIAVY “TT

‘QUO}SpUBY

ye ¢ sory “43 Gg “mdse rvoy “ydnoxrg ‘sotteg ouoyspuvg reddy | vuureg ‘Ty

*‘AOIV) “AC

1862. ] . JONES—FOSSIL ESTHERIZ. 151

9. Kstheria ovata, Lea, sp., is a8 important in the paleontology
of North America as #. minuta is in Europe; but its exact geolo-
gical place is not defined without difficulty. It has long been re-
cognized as an abundant fossil in some of the shales and flagstones
accompanying the carbonaceous deposits of South and North Caro-
lina, Eastern Virginia, and Pennsylvania; and its importance has
been indicated especially by Prof. W. B. Rogers and Sir C. Lyell.
It has passed under the names Posidonomya and Posidonia; and
Dr. I. Lea and Prof. E. Emmons have given several names to what
at first sight may appear to be distinct forms of this fossil; but,
after a careful comparison of specimens, figures, and descriptions, as
far as the means at my command allow (and I have been liberally
aided by my friends the Brothers Rogers and Mr. C. M. Wheatley,
of Phoenixville, Pennsylvania, as well as by Sir C. Lyell), I have
come to the conclusion that only one form really exists in these
North American Estherian shales, namely, Estheria ovata, Lea, sp.
The rarely perfect condition of the valyes, owing to the crushing
they have usually suffered, and to the imperfect exposure of the
edges of the imbedded valves, render it difficult to find trustworthy
specimens ; and every one of the forms, figured by Dr. Emmons *,
however different from the perfect valve they may appear to be, are,
I am sure, only squeezed and imperfect specimens, more or less badly
drawn.

Throughout the wide area in which these Estherian shales occur
(500 miles from N. to $.), and at two horizons separated by an
estimated thickness of upwards of 2000 feet of strata (on the Deep
River), the same species occurs. The only real difference that I have
detected in the many specimens I have seen being such modifications
of the reticulate sculpture of the interspaces as occurs in other
species, and an occasional crowding-together of the ridges into
numerous striz, such as we see in Estheria striata, E. concentrica,
and others.

As for the geological age of these Estherian and carbonaceous
shales of the Atlantic Slope, we all know that they were formerly
grouped as Lower Jurassic (Liassic) by Rogers, Lyell, Bunbury,
Marcou, and others; that Marcou has since argued in favour of
their Triassic relationship; ; and that Prof. Emmons makes them
Triassic in the upper part, and Permian in the lowert;—partly on

* American Geology, &e.

+ Both on account of certain geognostic features, and Prof. O. Heer’s opinion
of the Triassic character of some of the fossil plants of Virginia. See Bullet.
Soc. Géol. France, 2° sér. xii. p. 870, &c., and especially ‘Geology of North
America,’ 4to, Zurich, 1858, p. 13 & note, where M. Marcou, after giving an
account of various opinions held of the age of the Coal-formation of Eastern
Virginia and Carolina, adopts Prof. Emmons’s classification of the carbonaceous
and Estherian shales of N. and 8. Carolina, as being partly Permian and partly
Triassic ; both, according to M. Marcou, belonging to one great system, more
nearly related to the Secondary than the Primary formations.

¢ The occurrence of a Bird’s bone in the upper part of the series, and mam-
malian jaws (Dromatherium sylvestre) in the lower, as figured and described by
Prof. Emmons, and of the tracks of bipeds and quadrupeds in the northern equiva-
lents of these deposits, makes this series very interesting to the palxontologist.

152 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dees 17,

account of his finding Reptilian remains supposed to be allied to the
Thecodontosaurus of the dolomitic conglomerate of the West of Eng-
land (formerly referred to the Permian group), and partly because of
the great aggregate thickness of the Carolina series (upwards of 6000
feet), and the probable unconformity between the lower and upper
portions.

Lable* showing the occurrence of Estheria (KE. ovata) in the Lower
Mesozore Strata in North and South Carolina (from Orange to
Anson, ‘on the Deep River).

feet.

? ( I, Red and mottled sandstones, shales, and marls.
Estherie and Cypride; also a Fish-scale (in a
Coprolite), Saurian bones, anda Bird’s bone.... 1000

. Grey sandstone. Plants; Saurian bones.... 300 to 500

. Blue shale. Cycads and other Plants .. \ 40

’. Conglomerate, including beds of sandstone f *"*°*”

Triassic, accord-
ing to Emmons.

Sot
Ry RQ ss

There is probably an unconformity of the beds here.

E. Grey, thin-bedded sandstone, often rippled. Fucoids. 1200
D, Bituminous shales (Estherie and Cypride), with cal-
careous shale in their upper part, and comprising
coal-seams and iron-stones. Plants, Entomostraca,
Astarte (?), Mytilus (?), Fishes, Reptiles, and
Mammal (Dromathervamy 9 ond inte eee 700
C. Bituminous shale alternating with grey sandstone,
and passing downwards into red and brown sand-
stone (Coniferous Trees and Fucoids) .. 1000 to 3000
Be -Conslomeratete, 21: oiccie cia cteletite gue Moet sen ee 50 to 60
| A. Taconic slates. :

ee

mian, according to Emmons.
Ne

“Chatham group” (Emm.). Per-

The measured thickness of these strata is not necessarily a vertical
thickness, indicative of continued slow subsidence and vast lapse of
time. In Prof. H. D. Rogers’s ‘« Essay on the Geology of the United
States,” in the last edition of A. Keith Johnston’s ‘ Physical Atlas,’
are some pertinent remarks on the stratigraphical conditions of the
Mesozoic sandstones and shales under notice. Whatever may be the
thickness of the several strata, measured perpendicularly and added
together, yet, as these deposits have been formed in confined areas
and on sloping shores, it appears to me that Prof. Rogers’s observa-
tions must satisfy any dynamic geologist that no great vertical dis-
placement of the area has been required for the accumulation of this
sedimentary mass in the shallow waters of the old sub-Appalachian
water-belts.

The Reptilian remains and Fishes are not of paleozoic genera ;
and the Plants, according to Prof. O. Heer, are such as are ene
in Europe. The unconformity of the beds is no more than may be
seen between the Bunter and the Keuper in England; nor is the
estimated thickness of the whole of the series on the Deep River
(North and South Carolina) very much greater than that of the New

* Compiled from Dr. Emmons’s ‘ American Geology,’ part 6, 1857.

1862. | JONES—FOSSIL ESTHERLE. 153

Red Sandstone of Cheshire, estimated by Mr. E. Hull at about 5350
feet.

Isolated as these Lower Mesozoic shales of North America are, it is
difficult to co-ordinate them with the European scale of strata. They
are decidedly almost, if not quite, destitute of every trace of truly
marine agency, and must have been formed in long lagoons, or
brackish lakes, parallel with the Alleghany ridges (Rogers), under
somewhat similar condition to those which led to the formation of the
Lower Bunter of Alsace, the Lettenkohle of the Trias in Wiirtemberg,
&c., the lignitiferous and Estherian Upper Keuper of Worcester-
shire and Warwickshire, the Rheetic Estherian shales of Gloucester-
shire and Morayshire, the coal-bearing beds of the Lower Lias of
the Banat, and the plant-beds and coal of the Lower Oolite of
Yorkshire and the Venetian Alps. The plant-beds with Estheria
in Bengal and Central India are similarly circumstanced. From the
time, then, of the Lower Trias to that of the Lower Oolite *, we see
that shallow lagoons, if not inland seas, of brackish water, largely pre-
vailed over some regions, and received the debris of a very similar flora;
or we have before us the deposits of such waters, not truly contem-
poraneous, but presenting similar phenomena at different, but perhaps
not far distant, periods. To class all these as “‘ Lower Mesozoic ”’ will
be correct enough; but it is hazardous to adjudicate definite geolo-
gical periods for all these several groups of strata. ‘‘ Triassic” may
be the right term for the Indian and North American Estherian shales
and sandstones ; but the Rhetic group may also claim them, as ex-
hibiting both Triassic and Jurassic belongings. Nor may we forget
that in all these instances we have to do with the freshwater fringes
or the lacustrine equivalents of the great marine formations ; which
latter alone, as Godwin-Austen has so cautiously insisted upon +,
should be strictly taken as the stratigraphical types, if, according to
the accepted rule, the geologic scale be based on the sea-conditions of
past periods. Thus the Old Red Sandstone and the Coal-measures
will take rank, as transitional and terrestrial formations, with the
Lettenkohle, the Jurassic and Cretaceous ‘‘ Wealdens,” and other
more or less freshwater deposits of marginal lagoons and deltas, or
of inland lakes, of the Primary, Secondary, and Tertiary periods, and
not stand as independent groups or systems.

10. Estheria concentrica, Bean, sp., from the Plant-beds near Scar-
borough, is beautifully preserved in some instances, and at its first
discovery was recognized (by Mr. W. Bean, in 1836) as belonging to

* Not that we are limited at this stage, except as regards the facies of the flora
reierred to. Freshwater and estuary conditions, however prevalent in the Lower
Mesozoic period, were of equal importance in later Mesozoic times: not only in
the Middle Oolitic (Oxfordian), but in the Upper Oolitic and Cretaceous periods,
more or less known freshwater and terrestrial equivalents of the great marine
deposits spread far and wide in Europe and America (north and south); and in
the Tertiary formations, the freshwater and estuarine deposits have been fertile
sources of discussion with geologists and paleontologists, who have often pre-
ferred a rich lake-deposit as a guide (however eccentric), in the puzzle-work of
correlation, to the more uniform sea-beds.

t+ Quart. Journ. Geol. Soc. vol. xii. p. 54.

154 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec, 17,

the Crustacea. Its place in the strata is indicated by Dr. Wright’s
section of the Lower Oolite of the Yorkshire coast *. It is rare, but
is found in most, if not all, of the plant-beds of the series, and bears
witness of their freshwater origin.

11. Estheria Murchisome, Jones, found by Sir R. I. Murchison
thirty-five years ago in the Isle of Skye, and then regarded as being
possibly a Tellinay. This is a delicate and beautiful Hstheria, well
preserved, and probably a witness of freshwater conditions that ob-
tained during the Oxfordian period. The estuarine Jurassic fossils
from the Isle of Skye, described by Prof. E. Forbes t, belonging to
the same area, were found by him to underlie the Oxford Clay §.

Since completing the ‘ Monograph of Fossil Estherie’ for the
Paleontographical Society, [have seen Dr. Baird’s figures and de-
scription || of the recent Hstheria Jonesi, from Cuba, and in G. West’s
beautiful illustrations of the ornamentation of this species we may
see a near approach to that of H. Murchisonie, and in the shape of
the carapace a close resemblance to that of H. concentrica.

12. Estherra elliptica, Dunker, was the first fossil rightly and clearly
referred to Hstheria. Of some it had been suggested that they might
be bivalved crustaceans; and Mr. Bean and others had definitely
given to some that have since proved to be Hstherie the term
“Cypris;” but Dr. W. Dunker (in 1843) was the first paleontologist
who recognized and described a fossil Kstherva.

E, elliptica is abundant in the Cyrena-shales of the Wealden of
Hanover, where it presents two forms, the larger one elliptical or sub-
ovate in outline, the other nearly oblong or subquadrate ; the latter
variety Dr. Dunker described as EL. subquadrata in 1843. Mr. J.de
C. Sowerby in 1836 had given the name Cyclas subquadrata to a little
Estheria found near St. Leonard’s by Dr. Fitton 4]. This was found in
abundance at Bulverhithe (the same locality) by Prof. Morris and
myself afew years since (without our having recognized Dr. Fitton’s
locality, and Sowerby’s notice and figures), and I have no doubt of its
being the same as Dunker’s C. subquadrata. This has also been found
by Fitton, Binfield, Beckles, Baily, and ourselves in the East Cliff,
Hastings, and near Tunbridge Wells by Dr. Mantell; but the large
and typical Z. elliptica has not yet been recognized in England.

Cypride (Cypridea Valdensis, &e.), Cyrena, Paludina, and Plant-
remains are the associates of the Wealden Estheriw, both in Sussex
and Hanover; and these indicate only fresh, or, at the most, brack-
ish water as the habitat of Z. elliptica and its variety.

Obscure remains of Estheria have also been observed by Dunker

* Quart. Journ. Geol. Soc. vol. xvi.p.3l. + Geol. Trans. 2 ser. vol. ii. p. 311.

+ Quart. Journ. Geol. Soe. vol. vii. p. 104.

§ Some years since, the late Dr. Mantell gave me a hand-specimen of Oxford
Clay, from Wilts (probably from the railway-cutting near Trowbridge, Quart.
Journ. Geol. Soe. vol. vi. p. 312), in which a Cyprid, extremely like Cyprideis
unicornis of the Upper Eocene freshwater beds of Hempstead Cliff, Isle of
Wight, occurs in abundance. This may indicate lacustrine or estuarine con-
ditions of some portion of the Oxfordian group in the South of England.

| Proc. Zool. Soc. 1862, p. 147, pl. 15. figs. 1-1d.

€| Geol. Trans. 2nd ser. vol. iv. part 2. p. 177, and p, 345, pl. 21. fig. 8,

EEE

1862.) — JONES-—FOSSIL ESTHERLE, : 155

in the Lower Wealden of Hanover*. £. elliptica necessarily ranks as
a Cretaceous fossil in geological relation to its Jurassic, Triassic, and
Rheetic allies; for the freshwater Wealden group merges in its typical
marine system of the stratigraphical series.

13. Estheria Forbesii, Jones——David Forbes, F.R.S., F.G.S.,
brought many specimens of this elegant species home with him from
South America in 1859 or 1860. He found it in abundance with
plant-remains in a shale near Cacheuta, about 3500 feet above the
sea, on the eastern slope of the Andes, south of Mendoza; and he
thinks that possibly these beds may be related to those containing
fossil trees that Mr. Darwin saw in the Uspallata Pass. This
Estheria, however, gives no clear evidence of its paleontological age.
It is somewhat allied to H. ovata of North America, and still less
closely to H. minuta of Europe. It is probably of Mesozoic age ; but it
may be Tertiary. There is nothing to gainsay its freshwater origin.

14. Estheria Middendorfir, Jones.—This is from Siberia, and
was recognized as Crustacean by J. Muller, who regarded it as a
Inmnadia. It is one of the largest and most elegant of Estherie,
and is probably of Tertiary age. Mr. C. E. Austin’s paper { on the
locality where it was found, and Von Middendorf’s note on it in his
‘ Sibirische Reise,’ give all that is known of its geological relations.

Remains of Plants, Insects, and Shells (Limneus?), all obscure,
add little to our knowledge of its habitat; but what they do show
is strengthened by the fact of the Aspius, which accompanies the
Estherva in great numbers, being a Cyprinoid fish, such as is found
in fresh water, and being also found in some of the Miocene fresh-
water deposits of Europe.

Leava.—Together with the fossil Hstherie, I have described and
figured in my ‘ Monograph’ some small enigmatical fossils that occur
in the Carboniferous strata. Some of these were noticed twenty-six
years ago by Prof. W. C. Williamson and Prof. J. Phillips$; but no
conclusions were arrived at as to their probable relationship. They
are dark-coloured, horny, thin, quadrangular valves, either lying
separate, or with the dorsal edges approximate, and are marked with
concentric furrows, running parallel with three sides of the valves,
and by two oblique transverse ridges crossing the valve, from the
umbo to the ventral angles. I know no recent Crustacean haying
such valves ; but the horn-like appearance of the fossils, their small
size, and their dissimilarity to any mollusk have brought them under
my notice. I find that Dr. I. Lea has described and figured a cast
of a similar little fossil as Cypricardia Leidyi, from the red sand-
stone at the base of the Carboniferous series in Pennsylvania; and
there are but slight differences between this form and that of the
specimens found by Williamson in the Upper Coal-measures at Ard-

* Mr. Harry Seeley, F.G.S., assures me that he has detected the cast of an
Estheria, very like that found at Bulverhithe, in a specimen of Cyclas-bearing
marl from the Lower Purbeck beds of Durleston Bay, near Swanage.

t A. Th. von Middendorf’s ‘ Sibirische Reise,’ vol. i. part 1.

{ Quart. Journ. Geol. Soc. No. 73. p. 71.

§ Prof. Phillips suggested that they might be Trigonellites; but this suppo-
sition does not appear. to me to be well founded.

156 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 17,

wick, near Manchester, and of others found lately a Mr. Salter in
the Lower Carboniferous strata of Fifeshire.

For convenience I have made the most of these. differences of
contour, and have termed the Ardwick specimen Leaia Leidyi, var.
Williamsoniana ; and those from Fife, var. Salteriana ; keeping Leaia
Leidy? as the name for the Pottsville specimen, instead of Cypricardia
Leidyt.

hey are found without any immediate associates, except Plant-
remains and, at Ardwick, Anthracosia (Unio) Phillipsii.

Conclusion. Having nothing but the carapace-valves of these
little Crustaceans to guide us in working out their geological history,
we certainly cannot pretend to know everything about them. Among
the living Bivalved Entomostraca, different specific forms are found
to have carapaces much lke each other; and, again, nearly allied
species have markedly different carapaces; and Hstherie are not
without their peculiarities in this respect. Still I think we may
fairly believe that the marked differences of the Estherian carapaces
found in the several deposits really indicate distinct species; and
possibly some of the forms that I have kept apart as varieties may
have been independent species characterized by stronger differences
in limbs and other organs than their carapaces show.

That this genus should have clearly preserved its peculiarities
during so large a portion of geologic time will not be disregarded by
those interested in the study of “‘ persistent types”; nor is it with-
out Entomostracan allies equally tenacious of generic independence
throughout the lapse of geologic time. Where freshwater conditions
existed Estheria seems to have been often aready comer. Probably
we shall have many other localities and horizons for it in the fossil
state as the little valves become better known to collectors *.
Of the wide distribution of the species, both in Palwozoic and
Mesozoic times, we have clear evidence (judging from the carapaces,
and they appear to be distinct enough) in the occurrence of HL. mem-
branacea in the Old Red Sandstone of North Britain and of Livonia
(900 miles apart); of H. striata ranging in the Carboniferous deposits,
from western Scotland to Silesia (900 miles); and of E. tenella,
with almost as wide a range 7, and passing upwards from the Coal-
measures into the Permian group. The apparently co-ordinal Leaia
presents almost indistinguishable carapaces in Pennsylvania, Fife-
shire, and Lancashire (through nearly 70 degrees of longitude), in the
lowermost and the uppermost Carboniferous deposits. Hstheria minuta
is widely spread in certain strata of western Europe over a tract
measuring at least 600 miles from N.E. to S.W.; but its variety
Brodieana is not known, it seems, out of Britain, where its southern
and northern localities are 400 miles apartt. #. Mangaliensis and
its representative in Bengal are upwards of 400 miles apart. Z. ovata

* They have hitherto been mistaken for various shells and for fish-scales.
+ Much wider if EZ. tenella and E. exigua prove to be the same.
+ E. minuta, var. Brodieana, has to be looked for in the Rheetic beds at the
base of the Lias in the north-eastern counties of England.

Jan. 7.] SPECIAL GENERAL MEETING, 157

occurs at isolated spots in a tract of 500 miles. The English £.
elliptica is about 400 miles away from its Hanoverian type. These
species were probably represented at their several epochs by isolated
communities in distinct lakes, lagoons, and deltas; just as some of
the recent species are recognized at different localities, occasionally
far apart: thus £. gigas has been found in pools at Strasbourg, at
Toulouse, and in Tunis (the first and last upwards of 800 miles
apart); E. Dahalacensis is known to live in both Abyssinia and
Mesopotamia (1600 miles apart) ; and EH. Melitensis at Malta and in
Sicily (at least 50 miles apart). There are, however, very many more
species recorded as existing at the present period (22) than we have
found fossil in the deposits of any one past period, only two at
most being the number of known species for any one of the recognized
ereat formations. This, however, is partly due to zoological distine-
tions founded on the limbs and other parts of the body in some of
the existing species, but not recognizable in the fossil state; partly,
perhaps, to imperfect search in the strata; and possibly, in some
degree, to a greater differentiation of the more modern forms, if their
specific distinctness is accurately determined *.

Further search for, and strict examination of, fossil and recent
specimens, with careful records of the exact conditions of the strata
imbedding the former, and of the habitats of the latter, are necessary
before we can be satisfied on many of the points, referred to above,
in the geological history of Hstheria and its Phyllopodous allies.

3. On the Fuora of the Davyontan Prrtop in Norra-Eastern
America. Appendix. By J. W. Dawson, LL.D., F.RS., F.G.S.

[Published in the February Number of the Journal, by permission of the
Council. See vol. xvii. p. 329. |

JANuARY 7, 1863.

SPECIAL GENERAL MEETING.

It was Resolved :— ;
I. That the number of Foreign Members be in future limited
to Forty, instead of Fifty as heretofore.
II. That a Class of Foreign Correspondents be instituted, not
exceeding Forty in number. '
Ill. That the Foreign Members shall be elected out of the list
of Foreign Correspondents.
It was also Resolved that the Meetings of the Society shall be held

in the Society’s Rooms at Somerset House, on and after the Anni-
versary Meeting next ensuing.

_ * Some of the recent species are known only by their carapaces; and, if
fossilized, would be with difficulty discriminated one from the other. The deter-
mination by the valve-characters alone is as likely to lead to an over-estimate of

the number of recent species, as to a too cautious consideration of the fossil
species.

158 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

ORDINARY GENERAL MEETING.

John Daglish, Esq., Hetton, Durham; Griffith Davies, Esq., 17
Cloudesley Street, Islington; John Walter Lea, Esq., B.A., The
Grange, Shepperton Green, Chertsey ; and Henry Michael Jenkins,
Esq., Assistant-Secretary of the Geological Society, 22 St. George’s
Road, London, were elected Fellows.

The following communications were read :—

1. On the Lowrr Carponirerovs Bracutopopa of Nova Scorta.
By THomas Davinson, Esq., F.R.S., F.G.S., &e.

[Puate IX. ]

At the request of Dr. J. W. Dawson, F.R.S., F.G.S., Principal of
M°Gill University, Montreal, I have examined the Brachiopoda col-
lected by him from the Lower Carboniferous formation of Nova
Scotia, as well as those obtained by Sir C. Lyell during his first
journey in America, and I now submit the result of this examination
to the Geological Society.

The geology of Nova Scotia has already received the attention of
several distinguished observers; and I may mention that, although
prior to Sir C. Lyell’s visit to the country in question Mr. R. Brown
had described the limestone of East River and Cumberland as Lower
Carboniferous, the limestones of Windsor and Shubenacadie were at
that time regarded as “ New Red Sandstone” or “ Permian.” Sir
C. Lyell was ‘the first to maintain that the whole was of Carboni-
ferous age; and, by so doing, he unravelled a complication which
might for a time have involved the geology of the country in much
confusion. He may therefore justly claim to have been the first
geologist who was able to determine the geological age of the Gypsi-
ferous strata of Nova Scotia, which he considered to be a member of
the Carboniferous group instead of the Triassic or the Permian, or
both of them, as previously conjectured*. Dr. Dawson informs me
that his first papers on the subject were the results of investigations
which he made to test Sir C. Lyell’s views, and that Mr. Brown and
he followed up these observations, and accumulated a vast number
of facts subsequently published in his ‘ Acadian Geology,’ and from
which I extract the following synopsis of the Carboniferous rocks of
Nova Scotia; in order to point out the horizons at which the Bra-
chiopoda have been obtained.

Upper or Newer Coal-formation.

Greyish and reddish sandstones and shales, with beds of conglo-
merate, and a few thin beds of limestone and coal; the latter not of
economic importance. Thickness, 3000 feet or more.

Fossils :—Coniferous wood, Calamites, Ferns, ce.

* See Sir C. Lyell’s ‘Travels in North America, with Geological Observa-
tions on the United States, Canada, and Nova Scotia,’ vol. ii. p. 204, 1845.

+ “An Account of the Geological Structure and Mineral Resources of Nova
Scotia,” &e. 1855.

——

1863. ] DAVIDSON—NOVA-SCOTIAN BRACHIOPODA. 159

Localities: —Cumberland, north of the Cobequid Mountains ;
Northern Colchester, Pictou ; well exposed on the Joggins coast, and
on the coast of Northumberland Straits, west of Pictou Harbour.

Lower or Older Coal-formation.

Grey and dark-coloured sandstones and shales, with a few reddish
and brown beds; valuable beds of coal and ironstone; beds of bitu-
minous limestone, and numerous under-clays with Stigmaria. Thick-
ness, 4000 feet or more.

Fossils :—Stigmaria, Sigillaria, Lepidodendron, Poacites, Calamites,
Ferns, &c., erect Trees in situ, remains of Ganoid Fishes, Cypris,
Modiola, and three species of Reptiles.

Localities :—Cumberland, north of Cobequid Mountains, Pictou,
especially East River, Port Hood, Inhabitants’ Basin, and other
places in Inverness and Richmond; eastern part of Cape Breton ;
parts of Colchester, south of Cobequid Mountains. The finest ex-
posures are in the South Joggins, and near Sidney, Cape Breton.

Lower Carboniferous br Gypsiferous Formation.

Great thickness of reddish and grey sandstones and shales, espe
cially in the upper part; conglomerates, especially in the lower part ;
thick beds of limestone (with marine shells) and of gypsum. Thick-
ness, 6000 feet or more.

Fossils :—Productus, Terebratula, Encrinites, Madrepores, and
other marine remains in the limestone. Coniferous wood, Lepido-
dendron, Poacites, &c., in the shales and sandstone. Scales of Ganoid
Fishes very abundant in the shales associated with the lowest beds,
in which are also coaly seams and bituminous beds.

Localities :—Northern Cumberland, Pictou, Colchester, and Hants;
Musquodoboit, in Halifax county; Guysboro (in part), parts of Inver-
ness, Richmond, Cape Breton, and Victoria.

All the Brachiopoda, with one exception, are stated to have been
derived from the Lower Carboniferous or Gypsiferous formation ;
and, although the fossiliferous rocks submitted to my examination
vary considerably in composition and texture, it is evident that the
larger number of the species continued to live together for a con-
siderable period of time. There is a compact, light-yellowish-grey
limestone, full of Spirifera glabra, Terebratula sacculus, Productus
Cora, &c.; while some limestones, with the same fossils, are almost
black in colour; others are arenaceous, yellow, and full of small
cavities, the interior of the shells being often hollow; and, again,
other limestones, as that of Brookfield, are formed almost entirely of
shells, Bryozoa, &c., so closely packed that there appears in some
cases to be hardly any cementing material or intervening matrix.
Some shales also contain flattened valves of Streptorhynchus crenistria.
Dr. Dawson believes that this remarkable lithological difference in
the Lower Carboniferous rocks of Nova Scotia may have been caused
through the limestones having been deposited in limited basins or
narrow straits, and probably at a time of much volcanic disturbance ;

160 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

hence the great local diversity. He is, moreover, inclined to con-
sider that in each locality the ‘‘ Lower Limestones” are darker in
colour, more laminated, and less fossiliferous than the upper; also
that the individual beds become darker, more impure, and less fossili-
ferous as they approach the high lands which formed the old shore-
lines; but that there are, of course, exceptions to these statements.

The very remarkable shell-rock above described occurs at Brook-
field, a little east of the Shubenacadie River; it was first discovered
by the late Mr. G. Dunkin, and by him made known to Dr. Dawson.
It is in the line of strike of the Shubenacadie beds, and is doubtless
a continuation of them. ‘This rock has such a great general resem-
blance to certain Permian shelly limestones, with which I am ac-
quainted, that, had the specimens heen submitted to me without any
indication as to their geological age, I should certainly have felt
somewhat puzzled to determine whether I had to deal with a Per-
mian or a Carboniferous rock and its fossils; and, indeed, when M.
de Verneuil determined these fossils: for Sir C. Lyell in 1845, he
enumerated, among others, Terebratula elongata and T. sufflata,
Schl., Spirfera cristata, Schl., Avicila antiqua, Munster, a Modiola,
a Littorina, and one or two other fossils which he considered to be
common to both the Permian and the Carboniferous strata. Although
I may modify to some extent the lists of species published by Sir C.
Lyell and Dr. Dawson, I quite coincide with what is stated by the
former author, at p. 205 of his ‘Travels,’ viz., “That geologists
should at first arrive at this result (of considering the rocks in ques-
tion as the equivalents in age of the Permian of Russia) will sur-
prise no one who is aware how many of the fossils of our Magnesian
Limestone and Coal resemble each other, or who studies the lists
given at p. 218, in which several species both of shells and corals
from Nova Scotia, identical or closely allied to well-known Per-
mian or Magnesian Limestone forms, are enumerated.”

This is important to note: for it was written in 1845, just at the
time the celebrated authors of the great work on Russia in Europe
and the Ural Mountains (published in 1845) arrived from that
country ; and it denotes how strongly impressed they were that a
certain number of Carboniferous species had continued to exist
during the Permian period. Subsequent researches have confirmed
this view, and considerably multiplied the number of species common
to the two epochs; and it has been proved in the most satisfactory
manner that the Permian formation is the natural continuation of
the great Carboniferous system, of which it composes the upper
portion, although it is desirable to distinguish the group by the
separate designation of “Permian.” It is not the Mollusca and
Plants of the Permian period alone which, as M. Marcou supposes,
have a Paleozoic aspect, but, as M. de Verneuil *, Mr. Kirkby f, and
others have already shown, the whole bulk of the animal and
vegetable remains found in the Permian rocks bear the most unmis-
takeable Paleeozoic stamp. But, again, it would be fallacious to

* Bulletin de la Soc. Géol. de France, 2° sér. vol. xix. pp. 599, 627 (1862),
+ Annals and Mag. Nat, Hist. 3rd Series, vol. x. Sept. 1862,

ae he =

1863. ] DAVIDSON—NOVA-SCOTIAN BRACHIOPODA. 161

suppose, as many have done, that at the expiration of each of the
supposed great divisions of the sedimentary crust of the earth,
namely, the Paleozoic, Mesozoic, and Cainozoic, there was a com-
plete extinction and renewal of life. Such an idea in 1863 would
be completely out of place ; for it has been shown over and over again
that many Paleozoic genera have not only continued to be repre-
sented during a greater or less portion of the Mesozoic time, but
also throughout the entire geological sequence of sedimentary strata.
It is also quite evident that the admirable science of paleontology,
notwithstanding its rapid strides and great discoveries, is far from
haying revealed all its secrets, and is still in its youth. It cannot,
therefore, be expected that those who are now endeavouring to de-
cipher its difficult language can yet be in a position to furnish the
key to the genealogy of the numerous forms they daily meet with in
almost every rock and latitude, or that they can link together the
multitudinous and varied forms composing any class, and far less the
whole animal kingdom.

It is quite true that, in the present state of our knowledge, there

appears to exist between the Paleozoic and Mesozoic divisions or
periods a much wider break or difference in the life-groups than
between the individual systems of which these divisions are com-
posed. It is, however, highly probable that, when our science is
more advanced, a closer agreement will be obtained. Experience has
taught us that no genus or species, once become extinct, is ever re-
created ; and it is to my mind quite certain that, as long as the same
genus is represented in any successive geological formations, this alone
is a positive proof that life was not interrupted during that period.
We are all aware that a certain number of genera of different classes
passed from the Paleozoic into the Mesozoic period; but I will not at
present enter into the discussion of this subject further than to men-
tion that, among the Bracutopopa, Terebratula, Spirifera, Spiriferina,
Cyrtia, Athyris, Rhynchonella, Leptena, Crania, Discona, and Lingula
passed from the Palseozoic into the Mesozoic division. The Triassic
species have not yet been sufficiently compared with those from our
Paleozoic deposits; but a glance at some of the St. Cassian forms, or
even at Klipstein’s and Minster’s figures, will suffice to remove the
idea that there was a complete extinction of life at the close of the
Paleozoic period and an entire renewal of species at the commence-
ment of the Mesozoic epoch.
- Geologists and paleontologists are fully aware that the Permian
fauna is not nearlyso rich in species as that of the Carboniferous period.
When we, therefore, compute the percentage of species common to
the two, the Permian fauna must be taken as the standard, not the
Carboniferous. The subject of the recurrence of Carboniferous species
in the Permian period is far from having been completely worked
out; but, since 1845, it has attracted the attention of several com-
petent observers, amongst whom I may mention Messrs. de Verneuil,
Brongniart, Geeppert, Gutbier, Geinitz, Kirkby, King, Howse, Rupert
Jones, and myself, in Europe; Messrs. Meek and Hayden, Swallow
and Hawn, Dr. Shumard and Mr. Newbury, in America.

VOL, XIX,—PART I, M

162 ‘PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

M. de Verneuil informs us* that Dr. Geeppert is of opinion that, in
general, the Permian flora offers in its composition a great resem-
blance to that of the Coal-formation, fourteen or sixteen species being
common to the two. I shall not pretend to offer a complete list of
those hitherto recognized, but shall merely quote the following :—

. Calamites approximatus, Schloth. Tynemouth ; Manchester.
Cistii, Schloth. 'Tynemouth.

nodosus?, Schloth. Tynemouth.

— Suckovii, "Brong. Tynemouth; Manchester.
Sigillaria reniformis, Brong. Tynemouth.
Odontopteris Schlotheimi, Brong. Tynemouth.
Neuropteris Soretii ?, Brong. Tynemouth.
angustifolia, Brong. Tynemouth.

. Cyatheites arborescens, Schloth.

villosus, Brong. Manchester.
Oreopteridis, Gepp. Manchester.

12. Alethopteris Mertensioides, Guz.

Lonchitidis, Sternb. Manchester.

14. Sphenopteris latifolia, Brong. Tynemouth.
irregularis, Sternb. Manchester.
coralloides, Guth. Manchester.

17. Walchia piniformis, Schloth.

18. Guglielmites umbonatus, Sternd.

19. Trigonocarpum postcarbonicum, Giimbel.
Neggerathi, Lindl. & Hutt. ‘Tynemouth.
oblongum, Lindl. & Hutt. Tynemouth,
22. Cyclocarpon marginatum, Ar‘zis, sp.

: tuberosum, Gezn. T

24. Neggerathia palmeformis, Gepp. ‘Tynemouth.
25. Araucarites Schrollianus, Gepp.

3 Brandlingi, Lindl. & Hutt. Tynemouth.
27. Sagenaria dichotoma, Sternb. Manchester.

28. Dictyopteris neuropteroides, Guth. Manchester.

The thirteen species to which the locality “ Tynemouth” is attached
were identified by Mr. R. Howse as common to the Lower New Red,
or Rothliegende, and the Coal-measures of the north of England,
the former of which he thinks should more properly be considered as
the upper portion of the true coal-measures. Seven, namely Nos. 13,
14, 16, 17, 18, 21, and 23, are mentioned by Dr. Geinitz as common
to the German Rothliegende and Steinkohlen-formation. Mr. Binney
has also recorded the occurrence of common coal-plants of the genera
Sigillaria, Lepdodendron, and Calamates in the Lower Permian
strata of the north-west of England. Those to which I have ap-
pended the word ‘“ Manchester” are taken from.p. 313 of Dr. Gei-
nitz’s valuable work ‘ Dyas.’

_ Among the Entomostraca, Messrs. Rupert Jones and J. Kirkby have
identified the following species as being common to both periods in
Britain :—

1. Cythere elongata, Miinster, 1830. pamdiaty (Bairdia) plebeia, Reuss.

2. —— inornata, M‘Coy, 1844. (Bairdia) Schaurothiana,
3. —— (Bairdia) gracilis, M‘Coy, 1844. Kirkby.

Among the Annelida, Mr. R. Howse informs me that Microcon-

* Bull. Soc. Géol. Fr. 2™° sér. vol. xix. p. 600.
+ Mr. Howse considers these so-called fruits to be“fish-scales (Holoptychius ?

sp.).

$00 VSD STH Go bo

ae ee a.

1863. | DAVIDSON—NOVA-SCOTIAN BRACHIOPODA,. 168

chus carbonarius, Murch., has been found in the “ New Red” of
Tynemouth, as well as in the Coal-formation.

Mr. J. Kirkby has also recognized the Bryozoon, Fenestella plebeia,
M‘Coy, as common to both periods in England; and, although Mr.
Salter seems to doubt the identification of the Carboniferous form
above named, it is quite evident that the Fenestella discovered by
Mr. Kirkby in our Permian deposits is also represented by the same
species in the Carboniferous strata of this country.

Among the Pisces, Gyracanthus tuberculatus, Ag. (G. formosus,
Howse, Cat. Perm. Foss., non Ag.), has been stated by Mr. R. Howse
to be common to the Lower New Red and the Coal-measures of Eng-
land, and he considers that a species of Holoptychius? has been found
in the Rothliegende and the Coal-measures of Germany.

It has been very justly observed that, with the Plants, the Brachio-
poda have, up to the present time, received the greatest attention ; and
it has appeared to Mr. Kirkby and myself, after a minute and length-
ened examination, that, out of the eighteen or nineteen species of
British Permian Brachiopoda hitherto discovered, half at least, or
50 per cent., are common to the Permian and Carboniferous periods ;
and in support of this statement I must refer the reader to pages
266-270 and 279-280, and Plates 54 and 55 of my Monograph of
Carboniferous Brachiopoda, in addition to Mr. Kirkby’s paper already
mentioned.

To the following list I have added, between brackets, the names of
those palzontologists who have acknowledged the recurrence :—

1. Terebratula sacculus, Martin, 1809, C. =T. ‘sufflata, Schloth., 1816, P.
(King, De Verneuil, Kirkby, Davidson, Salter.)

2. Athyris Royssii, L’ Eveillé, 1835, C. = A. pectinifera, Sow., 1840, P. (De Ver-
neuil, Kirkby, Davidson.)

3. Spirifera Urii, Flem., 1828, C. = Martinia Clannyana, King, 1848, P. (David-
son, Kirkby, De Verneuil, Salter.)

4, Spiriferina octoplicata, Sow., 1827, C. = Sp. cristata, Schloth., 1816, P. (De
Verneuil, Davidson, Kirkby, Salter.)

5. Camarophoria crumena, Martin, 1809, C. = T. Schlotheimi, Buch, 1834, P.
(Morris, Davidson, Kirkby, King, De Verneuil, Salter.)

6. Camarophoria globulina, Phil., 1834, P. =. rhomboidea, Phii., 1836, C.
(Davidson, Kirkby.)

7. Discina nitida, Sow., 1812, C.=D. Koninckii, Geinitz, 1848, P. (Davidson,
Kirkby.)

8. Lingula mytiloides, Sow., 1812, C. = L. Credneri, Geinitz, 1848, P. (Kirkby,
Davidson. )

It may be further observed, that it is hardly possible to distin-
guish the Permian Crania Kirkbyi, Day., from the Carboniferous
Crania quadrata, M‘Coy ; and it is almost certain that Spiriferina
multiplicata, King, occurs likewise in our Carboniferous strata.
Strophalosia Morrisiana, so characteristic of the Permian period in
Europe, has been found by Mr. Purdon (and described by myself in
this Journal *) in the Carboniferous limestone of the Punjaub, as
well as another larger species, which closely resembles the Russian
Aulosteges Wangenheimi, Vern. (A. variabilis, Helmersen), Mr,

* Quart. Journ. Geol. Soc. vol. xviii. p. 32.

M2

164 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

Kirkby has also recently found, in the Lower Permian limestone of
Hartley Quarry, Sunderland, a species of Chonetes, which I believe
will turn out to be identical with the Carboniferous C. Hardrensis.
It must also be remembered that M. de Verneuil has stated, in the
work on Russia, that Chonetes sarcinulata has been found to range
throughout the whole Silurian, Devonian, Carboniferous, and Per-
mian periods; but it is probable that the Carboniferous and Permian
form is more properly referable to C. Hardrensis than to the Silurian
species (?); so that we may further estimate that out of the eighteen
or nineteen British Permian species, eleven are common to the two
periods. Now of the remaining seven.

Terebratula elongata has often been considered to be Carboniferous
as well as Permian, but of the absolute identity of the two forms I
do not profess to feel quite certain.

Spirifera alata has not hitherto been positively recognized in rocks
older than the Permian; but there are certain Devonian and Car-
boniferous Spirifers to which it is somewhat related.

Camarophoria Hambletonensis, Howse, has not hitherto been found
except in Permian rocks.

Streptorhynchus pelargonatus, Schloth., bears much resemblance
to certain varieties of Strept. crenistria, although probably specifically
distinct.

Productus horridus and P. latirostratus are not known up to the
present time, except in Permian rocks; but in their shape and cha-
racter they are not extremely distant from certain Carboniferous
forms.

Strophalosia Goldfussi is still characteristic of the Permian period.

This rapid examination of British Permian Brachiopoda will, I
trust, suffice to show that there exists not only a general close affinity
between the Permian and Carboniferous Brachiopoda, but also that
the majority of the species of the former period are identical with
some of the latter: and I may likewise mention, that although the
Permian rocks of Russia, Germany, Spitzbergen, and other places
present us with a few distinct forms, even some of these recall to
mind certain Carboniferous species; nevertheless I dare not pro-
nounce them identical; and it will require much further examina-
tion before they can be considered entirely distinct.

The Gasteropoda and Conchifera that occur in the Permian
rocks are few in number, and have not yet been carefully compared
with those of the Carboniferous period. Mr. Howse has informed
me that the Anthracosia aquilina, Sow., sp., found by him in the
Lower New Red of Tynemouth, is the same as that which occurs in
the Coal-formation of England. Mr. Rupert Jones has also recently
been able to add another lnk between the two formations in Estheria
tenella, which is common to the Permian and Carboniferous rocks of
Germany. M. de Verneuil observes, in his excellent paper pub-
lished in the ‘ Bulletin de la Soc. Géol. de France,’ 2™ sér. vol. xix.,
that, among the Pteropoda, there exist a species of Theca and one of
Oonularia so nearly related to certain Devonian (Carboniferous ?)
forms of the same genera, that it requires great attention to be able

1863.] DAVIDSON——NOVA-SCOTIAN BRACHIOPODA. 165

to distinguish them; and that, in addition to these, a species of
Bellerophon and a Trilobite of the genus Phillipsia have been found
by Messrs. Meek and Hayden in the Permian rocks of New
Mexico, &e.

Although paleontological research is not in so advanced a state in
America as in Europe, and though the species of that contment will
require to be very carefully studied and compared with those of
Europe before being definitely recognized, still it is probable that the
relations between the Carboniferous and Permian deposits of the
States of Kansas and New Mexico are very close, and that there ex-
ists no marked line of break between them. A single investigator
might be mistaken; but it is hardly likely that Messrs. Meek and
Hayden, Swallow and Hawn, and Shumard and Newbury, who have
examined for themselves, should all be in error!

The species recorded by these American geologists and palzeontolo-
gists as being common to the Carboniferous and Permian periods are
the following; but I append their list with the greatest possible
reserve on my part, and solely on their authority, as it is certain
that several of their identifications will require revision prior to
being definitely admitted :—

1. Productus semireticulatus, Martin. 9. Orthisina Missouriana, Swallow.
2. Rogersii, Norwood & Pratten. 10. Rhynchonella Osagensis, Swallow.
3. —— equicostatus, Shumard. 11. Terebratula (?) subtilita, Had/.

4. Spirifera camerata, Morton. 12. Myalina recta, Shumard.

o. plano-convexa, Shumard. 13. subquadrata, Shumard.

6. pectinifera, Sow. 14, ——- Kansasensis, Shumard.

7. Chonetes Flemingii, Norwood § Pr. 15, Allorisma Minnahaha, Swallow.
8. Orthisina umbraculum, Buch. 16. Naticopsis Pricei, Shumard.

Dr. Shumard mentions also that Productus Calhounianus, Swallow,
has been found in both formations.

However imperfect may be the lists I have given of the recurrent
species, it cannot be denied that, both by their genera and species, the
life-groups of the Carboniferous and Permian periods are closely re-
lated, and that although the Permian epoch possesses a large propor-
tion of species peculiar to itself, yet the general aspect of its fauna
greatly resembles that of the Carboniferous period.

The immense material now in hand is piled up and carefully
stored, but we have not yet had time to sort our treasures. The time
and research hitherto required in the preparation and illustration of
the Monograph entrusted to my care by the Palzontographical
Society, and the necessity of keeping my collections for that purpose
geologically and geographically arranged, have retarded the special
investigation of the class I am desirous of attempting in order to re-
spond to the request made me some time ago by Mr. Darwin, namely,
“that I should endeavour to exemplify and work out in some detail,
and with some single group, the theory of descent with modification,
so as to test the value of his theory.” It appears to me, however,
preferable, and more advantageous to the point in view, that I should
continue and complete my Monograph prior to rearranging my whole
collection in a purely zoological order, and irrespective of all geolo-
gical divisions. By this last operation, all the forms that most re-

166 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

semble each other, as well as those which gradually diverge, will
be placed in regular order; and it will then be in my power to show,
to a certain extent, what the Brachiopoda may do for the theory of
descent with modification. The difficulties to contend with in such
an investigation are, however, far greater than they are generally
supposed to be; but it is quite evident, and my daily experience
(which, as far as the Brachiopoda are concerned, exceeds twenty
years) teaches me, that the number of supposed distinct species has
been wonderfully exaggerated, and that a vast number of them are
in all probability, and in many cases certainly, mere modifications
in shape, or varieties in the Darwinian sense, which palontologists
will sooner or later be able to link together. Indeed, are we not con-
tinually puzzled to know how to find words or characters to distin-
guish our nearly related species? Are not our supposed distinctions
often exceedingly uncertain? and are we not generally far more pre-
occupied with the desire to find out trifling differences than to ex-
amine whether a closely related form might not be due to descent
with modification? To what extent variation has extended, our
knowledge will not enable us to determine; and, therefore, we can-
not pretend to know whether a supposed new form is in reality the
result of a distinct and original creation. We may suppose it so,
with more or less reason, founding the supposition on the imperfect
state of the science, which leaves us no other alternative than to
consider new that which we cannot connect or identify with what is
already known. What, again, adds to the difficulty is the imperfect
knowledge we possess as to what is really the value of the term
““ species, ’—for on that primary question naturalists are far from
unanimous*. JI am of opinion that there has never been a total
extinction of life since its first appearance, and consequently no
sudden renewal of the entire fauna at any geological period. It is
likewise quite certain that species have gradually and continually
become extinct from the date when the first form was created, and
that perhaps new species have appeared in the same ratio, to suit the
different conditions of sea and land in which they had to existt. It
is also highly probable, if not quite certain, that there never has

* In 1860, Prof. Suess registered 1954 species of Brachiopoda; and this is
far short of the total number that have been described ; but it would be most
erroneous to suppose that these 2000 or more names represent as many inde-
pendently created species, a large proportion being either synonyms, varieties, or
modifications in shape, of a limited number of original types.

t+ M. Deshayes states that “it is an absolute palzxontological demarcation
which serves to clearly separate the geological formations; that at St. Cassian
not a single species has been known to pass from the Triassic into the Jurassic
formation ; and that the same thing takes place between the five great series of
formations which he admits.” (Bull. Soc. Géol. France, 2™* sér. vol. xix.
p. 397, 1862.) I am sorry to be obliged to dissent from this view, which is
entirely in opposition to my experience; I neither believe in the existence of
five absolute series of formations, or in any absolute paleontological demarcation
between any geological systems that have been hitherto proposed, and for the
reasons above specified. On the contrary, I entirely concur with M. de Verneuil
while stating that he attaches less importance than do many geologists to those
geological and palzontological divisions of the crust of the globe, which are

i ee a

1863.) _DAVIDSON—-NOVA-SCOTIAN BRACHIOPODA. 167

been a complete discontinuance of sedimentary deposition over the
whole surface of the globe since the time when the first sediment
was formed,—that there has always existed a sea somewhere or
other upon the surface of the world, and that this sea has always
been inhabited. It is also certain that a number of favoured species
did escape for a time those local geological convulsions which have
taken place at numerous intervals; for the idea that universal
geological revolutions have ever taken place is now an all but ex-
ploded theory. Those hardy and favoured species have migrated
(as M. Barrande and others have so clearly shown), and continued to
exist, if not in their original home, in some other more distant place,
for a greater or less lapse of time, while the larger number of the
others may have been suddenly or gradually destroyed by those great
changes in the configuration of land and sea which have no doubt
taken place gradually or periodically.

It is not, therefore, surprising to find certain forms of an older
period in newer strata, or to find certain species striving to exist for
a greater or less extent of geological time, irrespective of the geolo-
gical system in the strata of which they are imbedded.

Time and assiduous research will show how far we may speculate
upon the origin of species; but, in the present state of paleontolo-
gical science, all theories built upon such subjects, however ad-
mirably handled, as is that by Darwin, must, before admission, be
tested by more unmistakeable evidence than science is at present in
a condition to offer.

We cannot tell, in the present state of our knowledge, whether the
species of any class, be it Hchinodermata, Brachiopoda, Crustacea, Pisces,
or any other, have been derived from a single or a hundred original
progenitors. I will not say that future researches may not simplify
the question, but in the present state of our experience we are very far
from haying arrived at any such conclusion. A similarity of original
type has sometimes, by exception, occurred during a very prolonged
period: thus, for instance, we have certain forms of Lingula, Crama,
Disema, Rhynchonella, &e., which, to all outward appearance, appear
to have varied but little during all the sequence of geological time;
there is one form of Crania, for example, which occurs in the Silu-
rian, Devonian, Carboniferous, Permian, Jurassic, Cretaceous, and
Tertiary strata, and in the recent state, which, although possessing
as many distinct denominations, is hardly specifically distinguishable,
while other species of that genus varied considerably in the different
geological periods.

But to return to the more immediate subject of this communica-
tion, I may observe that, although I quite agree with M. Marcou
that there exist in the Permian formation some few forms which
may recall to mind some which existed in the Mesozoic period, it
must be allowed that that number forms the minority, and that, on
the contrary, the great bulk of the Permian species, to whatever class
perhaps more in our idea than in nature, and conforming more to the actual

state of science than to its complete development. (Bull. Soc. Géol. France,
-Qme sér. vol. xix. p. 612, 1862.) ;

168 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7;

they may belong, bears the most positive Paleozoic stamp, and that
the species are in many cases the same that lived in the Carboniferous
era, and some even in the Devonian.

Haying sent my plate of Nova-Scotian species to Prof. de Koninck,
he wrote back:—‘It is to be remarked that all this little fauna
completely recalls that of the Carboniferous limestone of Visé in
Belgium ;” and this urges me to remind the Society that it has
been already shown by several paleontologists that there exists a
great general similarity in the Carboniferous fauna in almost every
portion of the globe where the rocks of that period haye been dis-
covered; and I have myself been able to confirm and extend this
fact by the lengthened examination I have made of the Brachiopoda
of that period from Europe and from many distant regions. It
would, however, be hazardous in the extreme to affirm that the
species found in one particular bed or at one horizon of the Carbo-
niferous period of Nova Scotia were strictly contemporaneous with
the same rock or forms found, for instance, at Visé in Belgium or
elsewhere. They may, perhaps, have been so, but we have no direct
means of arriving at so positive a conclusion; but, from the differ-
ence in the size of the specimens, we may say, for example, that the
Carboniferous sea of the Punjaub, where many of the same species
are found, was much more favourable to the development of the
species than was that of Nova Scotia, where, as a general rule, the
shells were all very much smaller; and I quite coincide with Prof.
Huxley when he asserts that the term ‘‘ contemporaneous” cannot
always be made use of in its absolute or literal meaning. For in-
stance, it 1s highly probable that in some portion of the world the
Lower Carboniferous animals may have continued to exist unmo-
lested, and to have been gradually imbedded, up to the time when
the Permian era commenced; and by this means some of the species
of the older formation may have been transferred to the newer ; and
all this whilst in other parts of the world the Middle and Upper
Carboniferous sediment was being deposited. ‘Two series of Carbo-
niferous strata containing the same animals may, therefore, not be
strictly contemporaneous, although they may both belong to the
Lower Carboniferous series: the term should therefore be made use
of in its widest and most general acceptation.

At pages 220-222 of his ‘ Travels,’ Sir C. Lyell gives a list, with
and without names, of sixteen species of Lower Carboniferous Bra-
chiopods as having been found in Nova Scotia, namely, Terebratula
elongata, T'. sufflata, Spirifer glaber, Sp. cristatus ?, Sp. minimus, Sp.
ocloplicatus, Producta Martini, P. concinna, P. Lyelli, P. Scotica, P.
spinosa, P. antiquata, and four undetermined, But as several of the
designations enumerated are synonyms, the number of determined
species would be reduced to five; and, even of these, three names
will require to be altered.

The study I have made of Dr. Dawson’s and Sir C. Lyell’s specimens
has, however, enabled me to determine fourteen species, or in reality
nine more than had been recorded by M, de Verneuil, and it is pro-

————————

1863.]. - DAVIDSON—NOVA-SO0TIAN BRACHIOPODA. 169

bable that a further search among the Lower Carboniferous rocks of
that country may bring to light a larger number ; and, indeed, there
existed in the collections above named specimens of one or two more
species, which I could not venture to determine on account of their
imperfect preservation.

As a rule, the Brachiopoda of Nova Scotia are small when com-
pared with the same species from some other countries—a result
perhaps of the conditions, already described, under which the beds
were deposited. I must not omit to mention that there occurs no
marine limestone, with which Dr. Dawson is acquainted, over the
productive coal-measures, except at one place, Wallace, where there
is a thin band of limestone in the upper coal-strata, which contains a
Productus ; but this was found in too incomplete a condition to admit
of determination.

1. TeREBRATULA saccuLvs, Martin, sp., 1809, and varieties. Pl. IX.
figs. 1, 2, 3.

Terebratula elongata and T’. sufflata, De Verneuil, in Sir C. Lyell’s
Travels in North America, vol. ii. p. 220, 1845, and in Dawson’s
Acadian Geology, p. 219, fig. 27, 1855.

All the Terebratule from the Lower Carboniferous strata of Nova
Scotia that have been forwarded to me by Dr. Dawson, as well as
those brought from that country by Sir C. Lyell, are variable in shape,
but are evidently referable to a single species. M. de Verneuil has
identified this shell with Schlotheim’s 7’. elongata, and mentions that
a ‘‘ gibbous variety of the preceding one”’ is referable to 7. sufflata
of the same author.

During a lengthened examination of 7. hastata and T. sacculus
from the Carboniferous rocks of Great Britain, as well as of 7’. elon-
gata and T. sufflata from the Permian strata of the same kingdom, I
was led to the conclusion that the specific identity of 7. sacculus and
T. sufflata was clearly established; and, when treating of the Car-
boniferous 7’. hastata and of the Permian 7’. elongata, I observed that,
although it was an unquestionable fact that some specimens of these
two so-called species could not be distinguished, more difference is
shown between the greater number of 7. hastata and T. elongata,
and that the strong resemblance appeared to be the exception. It
must also be allowed that it is often impossible to distinguish certain
examples of 7’. sacculus and of 7’. hastata, which forms appear to merge
the one into the other, and that the same may be said sometimes with
reference to 7’. sufflata and 7. elongata. All this proves how inti-
mately connected are the British forms of Carboniferous and Permian
Terebratule.

But to return to the Nova-Scotian specimens, I could not perceive
in any of them the wide and gradually depressed or shallow sinus,
which, in the larger valve of all well-shaped examples of 7. elongata,
commences towards the middle of the valve and extends to the front,
and which produces in the frontal margin a convex curve. In nearly
every specimen the ventral valve is uniformly convex or but very
slightly depressed near the front, as is the case with the larger num-

170 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

ber of 7’. sacculus and of its synonym 7’ sufflata. I think, therefore,
that it will be perhaps preferable to refer the Nova-Scotian Terebra-
tule to Martin’s 7’. sacculus ; and in this view I am supported by Prof.
de Koninck, notwithstanding some examples may resemble certain
specimens of 7’. elongata, 7’. fusiformis (Vern.), or 7’. hastata. The
largest specimen I have seen was not quite an inch in length, and the
greater number were much smaller. The interior, with its perfect,
short, simple loop, is often found, and is exactly similar to the one
we find in Martin’s species. Sir C. Lyell mentions that he obtained
this shell at Windsor, Brookfield, Shubenacadie, Gay’s River, Debert
River, Middle River, and Cape Breton. Dr. Dawson obtained it in
the same localities, to which he has added Pugwash, East River of
Pictou, Lennox Passage, &c.

2. ArHyris suptinitTa, Hall, 1852. PI. IX. figs. 4; 5.

Athyris subtilita, in Howard Stansbury’s Exploration of the Valley
of the Salt Lake of Utah, p. 409, pl. 2. figs. 1, 2.

The Nova-Scotian specimens all appear to be small in size, but are
exactly similar (except in dimensions) to those found in other parts
of America and Europe. ‘The spiral processes are often preserved.

This shell occurs by millions in the Lower Carboniferous limestone
of Shubenacadie, Brookfield, &c.

SPIRIFERZ,

The four so-termed species referred to in the lists given by Sir C.
Lyell and Dr. Dawson appear to belong to two, or at most three (?),
species.

3. SPIRIFERA GLABRA, Martin, sp. Pl. IX. figs. 9, 10,

Conchyliolithus Anomites glaber, Martin, Petrif. Derb. pl. 48.
figs. 9, 10, 1809.

Spirifer glaber, De Verneuil, in Sir C. Lyell’s Travels in North
America, vol. 1. p. 221, 1845, and in Dawson’s Acadian Geology,
p. 376, 1855.

This appears to be a common fossil in the Lower Carboniferous
limestone of Nova Scotia. It is identical in character with those
found in Great Britain; one example brought home by Sir C. Lyell
measured 13 lines in length by about 17 in breadth.

It occurs at East River of Pictou, Mabou, Cape Breton, Windsor,
Brookfield, Merigomish, &c.

4, SprrIFERINA cristata, Schlotheim. PI. IX. fig. 6.

Spirifer octoplicatus, Sow., Min. Conch. pl. 562. figs. 2, 3,4; Dav.
Mon. Carb. Brach. p. 38, pl. 7. figs. 37, 47.

At p. 221 of his ‘ Travels,’ Sir C. Lyell mentions Spirifer cristatus,
Schl., Sp. minimus, Sow., and Sp. octoplicatus, Sow., as having been
found in the Lower Carboniferous limestone of Nova Scotia; but it
is probable that at least two of the shells so termed, namely Sp,
cristatus and Sp. octoplicatus, are referable to a single species. The

1863. ] _ DAVIDSON—-NOVA-SCOTIAN BRACHIOPODA. 171

Nova-Scotian specimens of the shell under notice are all very small,
none of those that have come under my notice exceeding 4 lines in
length by 5 in width; they exactly resemble some specimens of the
same species found in the Carboniferous shales of Capel Rig, East
Kilbride, Scotland.

Sir C. Lyell mentions having found this shell at Windsor, Brook-
field, Shubenacadie, and Debert River, in Nova Scotia; and Dr.
Dawson adds East River, but that it is nowhere so plentiful as in the
shell-conglomerate of Brookfield.

5. Sprrirera acuticostata, De Koninck. Pl. IX. figs. 7, 8.

Spirifer acuticostatus, De Koninck, Description des Animaux Fos-
siles qui se trouvent dans le Terrain Carbonifere de la Belgique, p. 265,
mi 17, fig. 6,

Shell small and transversely oval; valves convex and ornamented
with from twelve to fourteen small angular ribs. The mesial fold is
comparatively wide, flattened, and longitudinally grooved along the
middle. ‘The sinus in the ventral valve has a small median angular
rib, which commences at about the middle of the valve and extends
to the front. Beak small, incurved; area triangular and of moderate
dimensions. Length 4 lines, width 5 lines, depth 3 lines.

Upon sending a proof of the plate illustrating this paper to Prof. de
Koninck, he wrote back that figures 7 and 8 were referable to his Sp,
acuticostatus ; and, except in size, they certainly resemble those given
by the distinguished Belgian Professor. It must, however, be re-
membered that in some specimens of Sp. cristatus, or of its Carboni-
ferous representative, Sp.octoplicatus, the mesial fold is flattened along
its middle, and even possesses in some cases a shallow groove along
its centre, as seen in De Koninck’s Sp. acuticostatus. All these modi-
fications in British specimens have been described and illustrated at
pages 38 and 226 of my Monograph of British Carboniferous Bra-
chiopoda. :

This small shell is very abundant in the shell-limestone of Brook-
field, Shubenacadie, and in some other localities in Nova Scotia, where
it is always associated with Sp. cristatus, of which it may perhaps
after all be no more than a modification.

CAMAROPHORIA and RHYNCHONELLA.

The specimens referable to these genera sent me by Dr. Dawson,
as well as those brought to England by Sir C. Lyell, are generally
very small, and not in all cases sufficiently complete to warrant a
satisfactory determination. I have, however, carefully represented
the principal forms.

6. CAMAROPHORIA ? GLOBULINA?, Phillips. Pl. IX. figs. 11, 12.

Terebratula globulina, Phillips, Encycl. Metr., vol. iv., Article
“Geology,” pl. 3. fig. 3, 1834.
_ Terebratula rhomboidea, Phillips, Geol. Yorksh. vol, ii. p.222,pl.12,
figs, 18-20, 1836.

172 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

Hemithyris longa, M‘Coy, British Pal. Foss. p. 440, pl. 3. D. fig. 24,
1855.

_ Of this very small shell I have been able to examine only three
specimens; but it is stated to be abundant in a yellow arenaceous
limestone at De Bert River, where, according to Dr. Dawson’s ex-
perience, it is always small. I have also felt somewhat puzzled
in the determination of this fossil; but, after having consulted Prof.
de Koninck, I concluded to refer the specimens represented in figures
11 and 12 to the same species, notwithstanding the apparent difference
they present. Prof. de Koninck referred fig. 12 to 7. rhomboidea,
Phillips, which is a synonym of Camarophoria globulina ; and, after
minutely comparing the Nova-Scotian specimens with the Carboni-
ferous and Permian types, I could perceive no difference sufficient to
warrant the creation of a new species. The three specimens were
exactly of the same size, namely 3 lines in length by 3 in width and
25 in depth. The uncertainty which both Prof. de Koninck and
myself have experienced refers to fig. 11, which much resembles, in
miniature, a form of Rhynchonella acuminata ; but when we remember
that Phillips himself figures a specimen of his Terebratula rhomboidca
with a simple mesial fold, we need not be surprised to find the same
peculiarity in one of those from Noya Scotia. Indeed, after carefully
examining the three examples forwarded by Dr. Dawson, I cannot
bring myself to believe that they should be specifically separated. It
is well known that the same peculiarity occurs with Rhynchonella
acummata ; and any one who examines plates 20 and 21 of my Mono-
graph of British Carboniferous Brachiopoda must feel surprised at the
immense variability of which some species are susceptible.

7. RuyncHonetia Dawsonzana, n. sp.? Pl. IX. figs. 13, 14.

Shell very small, almost circular, a little wider than long; dorsal
valve moderately and uniformly convex to about half its length from
the umbone, at which point a very shghtly elevated and flattened
mesial fold begins to rise, and extends to the front; the surface of the
shell is also either almost entirely smooth or ornamented with from
eight to twelve slightly marked ribs. The ventral valve is gently con-
vex, with a wide sinus; beak small and incurved. Length 3} lines,
width 4 lines, depth 2} lines. |

This small species does not appear to be rare in a black Lower
Carboniferous limestone at Lennox Passage, and is not unlike, ex-
cept in size, certain examples of M. de Verneuil’s Terebratula superstes;
but this last-named Permian shell belongs to the genus Camaro-
phoria, while the one under description belongs to Rhynchonella. I
have compared it with a number of equally small young examples of
Tthynchonella pugnus, from which it appears to differ.

8. RuyNncHoNELLA ACADIENSIS, n. sp.? Pl. IX. fig. 16.

Shell small, obscurely rhomboidal, about as wide as long; dorsal
valve rather more convex than the ventral, and presenting, when
viewed in profile, a regular curve. The mesial fold commences to-
wards the middle of the valve, while the surface is ornamented with

1863. ] DAVIDSON—-NOVA-SCOTIAN BRACHIOPODA. 173

twelve or thirteen small radiating ribs, of which four or five occupy
the surface of the fold. The sinus in the ventral valve is of moderate
depth, and the surface is ornamented as in the dorsal valve. The
beak is gently incurved, and exhibits a small circular foramen under
its angular extremity. Length 5 lines, width 5 lines, depth 3 lines.

Of this shell I have seen but two specimens, which I detached
from a lump of the Brookfield shell-limestone, and of which one ex-
hibited the two curved internal lamelle characteristic of the genus
Rhynchonella. Itis quite distinct from young shells of Rhynchonella
pugnus and L. pleurodon. In the last-named species the ribs that
adorn the lateral portions of the dorsal valve are very much curved,
while those of the ventral are nearly straight, with their extremities
bent upwards; in addition to which, the ribs begin to be longi-
tudinally grooved along their median portion at some distance from
the margin. None of these characters are observable in the small
Rhynchonella under description.

9. Ruyncnonetzia, sp. Pl. IX. fig. 17.

Upon some fragments of Lower Carboniferous limestone brought
from Nova Scotia by Sir C. Lyell are several imperfect, undeter-
minable valves of a Ehynchonella which differs from the preceding
species by its size, as well as by the number of its small radiating
ribs. Of these last I haye counted as many as thirty-five or forty
upon each valve. In size it appears to have measured about 7 or 8
lines in length by 9in width. I abstain from proposing for it a spe-
cific denomination, as the material is so imperfect. The specimen
belongs to the Geological Society.

In fig. 15 is represented another Rhynchonella, also undeterminable.

10. RayncHonELLA PuGNUs?, Martin, sp., Petrif. Derb. tab. 22.
figs. 4, 5, 1809.

Two or three very small specimens, received from Dr. Dawson
after my plate had been completed, much resemble certain young
shells of Martin’s species ; they are derived from the Lower Carbo-
niferous limestone of Windsor and East River.

11. SrropHomens anatocs, Phillips. Pl. IX. fig. 18.

Producta analoga, Phillips, Geol. Yorksh. vol. ii. pl. 7. fig. 10,
1836.

Upon a specimen of dark, impure limestone brought from Nova
Scotia by Sir C. Lyell, and now in the Society’s Museum, I found
a well-characterized example of this species, which, in Sir C. Lyell’s
list, had been confounded with Productus Martini.

12. SrrePToRHYNCHUS CRENISTRIA, Phillips. Pl. IX. fig. 19.

Several crushed valves, referable to this species, occur on a speci-
men of Carboniferous shale from Shubenacadie, for which I am
indebted to Dr. Dawson. These valves exactly resemble certain
small specimens found in several British Carboniferous shales. Their
surfaces are covered with numerous radiating raised strie, with a

age PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

smaller rib between the larger ones, the whole being closely inter-
sected by fine concentric lines, thus giving to the longitudinal ribs a
crenulated appearance. Prof. de Koninck coincides in my identifi-
cation.

PRoDUCTUS.

Although Sir C. Lyell and Dr. Dawson mention seven species of
this genus as having been found in the Lower Carboniferous rocks of
Nova Scotia, all these, as well as the specimens I have been able to
examine, can be referred to two species only, namely P. semireticu-
latus and P. Cora; and I may mention that Prof. de Koninck coin-
cides in this view.

13. Propuctus sEMIRETICULATUS, Martin. PI. IX. figs. 20, 21.

Anomites semireticulatus, Martin, Petrif. Derb. pl. 32. figs. 1, 2,
and pl. 33. fig. 4, 1809.

This species is so well known, that all I shall require to state is,
that the Nova-Scotian specimens are exactly similar to those found in
Europe. Producta Martini, P. concinna, P. antiquata, P. Scotica,
mentioned by Sir C. Lyell at p. 220 (vol. ii.) of his ‘Travels in
America,’ as well as by Dr. Dawson in various pages of his ‘ Aca-
dian Geology,’ belong to a single species, namely Productus semireti-
culatus, Sow. The “ P. spinosa, Sow. ? var. of P. Martini,” of Sir
C. Lyell’s list, belongs likewise to the species under description ; but
P. spinosa, Sow., specimens of which I have not seen from Nova
Scotia, is a distinct species. Sir C. Lyell mentions Windsor, Brook-
field, Shubenacadie, East River, Debert River, and Minudie. Dr.
Dawson states that the shell is found almost everywhere, at Pug-
wash, near Amherst, Boulardarie, Cape Breton, Horton Bluff, Gray’s
River, &c.

The largest specimen measured one inch and a half in length by
about the same in width. The variety Martini is also found in the
same locality.

14. Propucrus Cora, D’Orbigny, 1842. Pl. IX. figs. 22, 23.

Productus Cora, D’Orbigny, Paléont. du Voyage dans Amérique
Meérid. p. 55, pl. 5. figs. 8, 9, 10, 1842.

P. comoides and P. Scoticus, De Kon. 1843 (not of Sow.).

Producta corrugata, M‘Coy, Synopsis of the Carb. Limest. Fossils
of Ireland, pl. 26. fig. 13, 1844.

P. Lyelli, De Verneuil, Sir Charles Lyell’s Travels in North
America, vol. 11. p. 221, 1845.

P. tenuistriata and P. Neffedievi, De Vern., Russia and the Ural
Mountains, 1845.

P. Cora, De Koninck, Mon. du Genre Productus, pl. 4. fig. 1, 1847.

P. pileiformis, M‘Chesney, Descr. of New Species of Fossils from
the Paleozoic Rocks of the Western States of America, p. 40, 1849.

P. Lyelli, Dawson, Acadian Geology, p. 219, fig. 9, 1855.

P. Cora, Dav., Mon. Carb. Brach. pl. 36. fig. 4, pl. 42. fig. 9,
1861.

After a very careful examination of nine or ten specimens of P.

Quart. Journ. Geol. Soc.Vol. XIX. PL. IX.

Se

Poy,
ro,
1 msc mned om weer

avidson del. &

W West imp

ire

Thos

a

ry
ok

rere)

re
y¥

Lower Carboniferous Brachopoda from Nova

1863.] - CURLEY—GRAVEL OF LUDLOW, ETC. 175

Tyelli from the Lower Carboniferous Limestone of Nova Scotia, I have
reluctantly been obliged to place M. de Verneuil’s species among the
synonyms of P. Cora, the latter name (as may be seen by the list
of synonyms above given) claiming three years’ priority. All the
Nova-Scotian specimens I have been able to examine were small, not
exceeding about 11 lines in length by some 12 or 13 in width. But it
must be remembered that, as a general rule, the Nova-Scotian species
and specimens, although adult, are small, and in this respect are
exactly similar to those we find in Scotland. The surface is covered
with numerous longitudinal, straight, or slightly flexuous, narrow,
thread-like, rounded striz, with sulci, or interspaces, of rather less
width ; smaller striz are also here and there intercalated between the
larger ones. The ribs are also regularly and closely crossed by small
concentric lines.

P. Cora is a widely spread Carboniferous species, having been found
in many parts of America, India, Europe, &c.

Sir C. Lyell found this shell at Windsor, Horton Bluff, Shubena-
cadie, Gay’s River, Minudie, and Cape Breton, in Nova Scotia. Dr.
Dawson states that it occurs almost everywhere—at Pugwash, on the
eastern coast of Cumberland, at Lennox Passage, M‘Kenzie’s Mill at
the eastern extremity of Wallace Harbour, &c.

EXPLANATION OF PLATE IX.

Figs. 1,2, 3. Zerebratula sacculus, Martin.

4,5. Athyris subtilita, Hall.
ss Ae Spiriferina cristata, Schlotheim.
» 1,8. Spirifera acuticostata, De Koninck.
» 9,10. Spirifera glabra, Martin.
11, 12. Camarophoria? globulina?, Phillips.
13, 14. Rhynchonella Dawsoniana, n. sp.?
ie |S Rehynchonella (undeterminable).
3 NO: Rhynchonella Acadiensis, n. sp.?
er BE: Rhynchonella (andeterminable).
3 «LS: Strophomena analoga, Phillips.
ay ales Streptorhynchus crenistria, Phillips.
», 20, 21. Productus semireticulatus, Martin.
» 22, 23. Productus Cora, D’Orbigny.

2, On the Gravets and other Surerriciat Deposits of Lupiow,
HeEReEForD, and Sxipton. By T. Curtuy, Esq., C.E., F.G.S.

Tuer plans and geological sections which I have now the honour to
lay before the Geological Society are those of three towns recently
drained by me, namely, Ludlow, Hereford, and Skipton.

_ Inudlow.—The Upper Ludlow rocks are, in my opinion, thrown up
against the Old Red Sandstone by a fault running east and west, and
taking the line of the Old Town ditch, below the Church and the Castle,
as marked on the plan (p. 177). The relations of the intermediate
“ passage-beds,” which connect the Silurian and Old Red systems,
and are so well developed in the immediate neighbourhood of the

176 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 7,

town, have been rendered tolerably clear by the researches of the
Ludlow geologists, and by the discoveries made during the progress
of the drainage-works. Upon these “ passage-beds” and the under-
lying Downton Sandstone the town is mainly situated. The over-
lying Old Red Sandstone is well seen in the line of the section in
the railway-cutting. The Downton Sandstone, about 80 feet thick
at Ludlow, has been generally included in the Silurian rocks: it is
a yellow micaceous sandstone, very similar in composition to the
Caradoc, from the denudation of which it has, most probably, been
derived. But few organic remains occur in it at Ludlow, the prin-
cipal being the Fishes—Pteraspis and Cephalaspis,—with the Crus-
taceans—Lurypterus, Pterygotus, and the small Beyrichia. Above
this rock is a very hard, greenish, micaceous sandstone containing
lime, much resembling an Old Red Cornstone in mineral composi-
tion. The Bull Ring is situated upon this rock, and no doubt owes
its present relative altitude to the hardness of this sandstone and
its capability of resisting denudation. Above it are several thin
beds of sandstone, in which nothing organic has been found. Next
occurs a greenish micaceous sandstone, containing Cephalaspis, Lin-
gula, &e. We then come to the ‘“ Olive Shales,” which are thin
argillaceous beds, easily broken, and containing layers and thick
masses of fossils. Several species of Plerygotus and Eurypterus, and
spines of Onchus have been found. A thin sandstone-band forms a
capping to these olive shales, and underlies a bed of Old Red marl
about 80 feet in thickness. On the top of this marl, N.E. of Ludlow,
is situated the high-level gravel, in a bed about 30 feet in thickness.
The rain-water, falling on this gravel-bed, percolates through it, and
issues forth as a spring. Very nearly the whole of the sand and
gravel here deposited is composed of Old Red Sandstone débris. The
inclination of the sand-belts and their thinning-out towards the east,
in this drift, indicate the direction of the current which brought this
_ gravel to the lake in which it was deposited to have been from the

westward. It is probable, therefore, that, prior to the deposition
of this gravel, the Silurian rocks, which now form the entire area of
the district west of Ludlow, were masked to some extent by Old Red
Sandstone, since removed by denudation.

By subsequent denudation, and an alteration of currents, this
«high-level lake ” became drained, and a lower lake formed about
100 feet below it. Currents from the north deposited sand, gravel,
and other drift in this lower basin, which now forms the site of
Corve Street. This gravel-bed is composed chiefly of Cambrian and
Silurian débris, water-worn fragments of the well-known Cambrian
rocks of Church Stretton being abundant. A very small part of the
present site of Ludlow would, during the deposition of this ‘ low-
level gravel,’ appear above water. The south edge of the lake ap-
pears to be opposite the Feathers Hotel, in Corve Street. A little
lower down that street, opposite the Compasses Inn, large boulders
of Old Red Sandstone were discovered, resting amongst sand,
gravel, and fine clay. These boulders must have been carried to
their present position by floating ice, which became stranded in

Ras

ALE =|
bY psi)
iy ay Vie
“Wy = WZ
: N87, oh
| Y) oath
7 /|

Old Red Sandstone.

Low Level Gravel. Downton Sandstone.

High Level Gravel.

Upper Ludlow Beds.

a. ‘The Compasses’ Inn. ‘ce. The Bull Ring.
6. ‘The Feathers’ Hotel, d. Ludlow Castle.
A, B, C. The line of Section.

water, eight or ten feet deep, near the edge of the shelving lake. The
current which carried down the gravel, &c., passed over the present
site of the River Teme; for a bed of fine blue clay lies at the bottom
of Old Street, and yellow clay below Frog Lane. The dam which
kept back the water of this lower lake was probably opposite to the
tanks at the Old Paper Mill.

The average thickness of this low-level gravel is about 25 feet,
a thickness of 21 feet of which has been exposed by shafts and tun-
nelling for the main sewer. During the existence of this water, the
site of Ludlow appears to have been covered, save a narrow strip,
about 130 yards wide, along the present direction of Castle Street.
The water of this lake would be 70 feet deep at the bottom of
Corve Street, and 90 feet deep at the bottom of Old Street.

In process of time, the rocks which formed its southern dam.
having been worn through, the whole of this lake-water seems to

VOL. XIX.—PART I. N

[Jan. 7,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

178

*QUOJSOWTT snosajiuoqieg °F *Avpo ong a ‘areys 'p JOAvIN) '9 ‘TUNIANITY °9 ‘TlOog ‘7

a
SY S a ay, yy ISI SI SI f> y y L/z S,
S/ SY SIU YA LLL SLIS TAT Epa
Vy” are !
‘ t i to4 ‘
Yi ‘a
YP i ;
Pas 9 g "q2911¢ YSIH ge ne s (stameg ure Jo qe79N0)
; BS 5 2 RB 2, PI 1TH
AVmpeY E09 ae ote
= 2) w ° nu o ot ak
‘TN —-“249BT_ 8, WAI04g a “AL'S
‘OUT Sma1ojyg 04 yoag sani wolf “uordiyg sso1op UoIg—F “SUT
*QUOISPULS PIY PIO *Y ‘Avpo poy °F “hep moTPPA “f ‘yea ‘2 IIIS "Dp "Tlos o[qujoZe,Q ‘9 Aeypa-orppng *9 ‘JOARIQD *D

AAS

"AVM Y 19}S9ONO0]4) *yoinygg yoong *ABmyTey PIOJoIOH 2 D
2p ‘ssoy ‘plojol9H <SJUIBS [LV qsom ‘AuuaarSsoqy ‘“aodmany

"M
"TI
nor wbug on WET hmoong woif “profouayy ssouop W0r02g9—'g ‘SLi Amuoig
‘UIMIANTTY °7/ ‘quoyspurg uojumog *f *saTBYys DATO "Pp *SLIqaP , PPUW PIO , JO pasodurod Jaaviy *¢
*‘spog Morpny teddy +7 *gUO}spURS PIY PIO °2 *]VUl poy PIO °9 *slap[nog eSivy yj1M AvpO pue [earls MOT[AA *D

See tl ban tt ea Teo T St
Ses KL esate
rant

+ Sem ey pr0jor9 }] ag AinqsMaIqS *TOMMYD VUIIMET “45 *aTI8BO

9 “SV ty 0y7 buon ‘MO)pVT ssoLon U0YIIG—'G SLT

1863. ] CURLEY—GRAVEL OF LUDLOW, ETC. 179

have gradually drained away, the rain-water of the catchment-basin
scooping out the beds of the Rivers Teme and Corve,—the courses of
which, however, had then dissimilar directions, as is shown by the
high terraces behind Burway, leading to Broomfield. Similar changes
are now going on, slowly and imperceptibly, though probably not
more so than the former ones.

Hereford.—The city of Hereford is 158 feet above the sea-level,
and stands upon a gravel-deposit 900 acres in extent. The materials
of this bed appear to have been transported from a great distance,
being well rounded and water-worn. In addition to pebbles of Old
Red Sandstone and Cornstone, it contains Silurian pebbles from the
upper part of the Valley of the Wye, and fragments of trap-rocks
from Builth. This gravel is seen to be the lowest of three terraces of
drift, and has an average thickness of 30 feet. At a level of 30 feet
above it we meet with a second deposit, a belt of gravel perfectly
level, and evidently forming the edge of an old lake. Forty-two feet
above this, a gravel-bed of small extent exists as a capping to
Broomy Hill.

I am inclined to consider that the denudation of the Old Red
Sandstone over the area of the Hereford valley was comparatively
rapid; the present River Wye, which flows through it, discharging,
in ordinary dry weather, 1650 million gallons daily. These three
gravel-zones are very similar in their appearance and mineral con-
stituents.. The quantity in the lowest, or City-of-Hereford bed is
25 million cubic yards—sufficient to gravel a walk, 10 feet wide,
round the globe.

Skipton.—The plan and sections of the town of Skipton exhibit a
somewhat similar condition of things. The lower portion of the
town is situated on a lacustrine deposit, lying in a basin of Moun-
tain-limestone, containing gravel composed of the débris of this rock
and the adjacent Millstone-grit.

Under this gravel there occurred, on the south side of the canal,
and in the excavations for the main sewer, a black deposit of silt of
the consistency of tar, which caused great trouble to the contractor ;
for straw had to be introduced behind close boarding to keep out this
treacherous material, which appeared to be composed of pulverized
coal-shale, derived from stratified layers in the neighbourhood. In
the sewer-cutting, opposite Christ Church, a thick bed of dark marl
was cut through, full of the shells of Physa fontinalis. In the
cutting of the sewer north of the canal, opposite Victoria Mills, the
skull, tibia, and other bones of a species of Bos were met with in fine
sand, below 8 feet of peat and gravel-drift. Large boulders, about
37 tons in weight, were found in the gravel opposite the Devonshire
Hotel.

The section along the line of the main sewer has been extended to
include the contorted stratification of the Carboniferous Limestone on
which the Castle stands, and the anticlinal axis of Storem’s Lathe.

n 2

180

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

POSTPONED PAPER.

On the Guonoctcat Srrucrure of the SourneRN GRAMPIANS. By
James Nicon, F.R.S.E., F.G.S., Professor of Natural History in the
University of Aberdeen.

[Read June 18, 1862*.]

ConrTENTS.

1. Introduction. 13. Dunkeld and Blairgowrie.

2. Object of the Paper. 14. Relation ofthe Old Red Sandstone.

3. Clay-slate Formation of Bute. 15. Clay-slate and Mica-slate.

4. Loch Long and Gareloch. 16. Central Gneiss and Quartzite.

5. Loch Lomond. 17. Tyndrum and Black Mount.

6. Callander and Pass of Leny. 18. Glen Shee and Braemar.

7. Leny Limestones. 19. Clay-slate of Loch Creran.

8. Ben Ledi. 20. Loch Leven and Glencoe.

9. General remarks on the foregoing 21. Fort William and Ben Nevis.

Sections. 2. Glen Spean.

10. Comrie and Strath Earn. 23. Geological connexion of the.
11. Bedding or Cleavage (?). Grampians with other parts of
12. Mica-slate of Loch Earn. the Highlands.

1. Introduction.—The nature and origin of the crystalline or me-
tamorphic strata have recently formed the subject of various memoirs,
both in this country and abroad. Living in a region in great part
composed of these rocks, and having for many years been engaged
in examining them in various parts of Scotland, I have naturally
taken much interest in these discussions. I now venture to lay
before the Society an account of some sections which I have recently
examined (several of them not for the first time), as they appear to
me to throw light on some points of high importance both in the
history of the earth and the structure of our own country.

Before noticing special sections, it is right to mention that I have
long held the view of the metamorphic origin of these so-called pri-

* For the other communications read at this Evening-meeting, see Quart.
Journ. Geol. Soc. vol. xviii. p. 378.

NICOL—SOUTHERN GRAMPIANS. 181

mary strata. In my ‘Guide to the Geology of Scotland,’ in 1844, I
pointed out the close resemblance of some parts of these formations
to the Silurian strata in the South of Scotland, and indicated that
they were merely the metamorphosed representative of the latter.
In a paper read before the Geological Society in 1849 I again stated
this opinion, and specially noted the “ band of clay-slate from Stone-
haven to Arran as forming the continuation of the Silurian beds in
the south, rising up on the other side of the synclinal valley in which
the Carboniferous strata of Scotland have been deposited”*. The
same views of the identity of the crystalline strata in the North of
Scotland with the Silurian deposits in the South have been expressed
by me on many subsequent occasionst, and may thus have in some
points influenced the statements given in the following paper.

2. Object of the Paper.—My principal object in describing these
sections is to examine the relation to each other of the three great
formations, the Clay-slate, the Mica-slate, and the Gneiss, which,
with some subordinate groups, as the Quartz-rock and Chlorite-series
of Macculloch, have hitherto been regarded as composing the chief
stratified masses in the Scottish Highlands. These formations,
‘< founded on the great relations which rocks bear to each other and
to the general structure of the earth” +t, have been recognized with
nearly identical characters in the most distant regions of the globe,
thus showing that they are not mere capricious distinctions of local
observers, but true constituents of the crust of the earth§. The
order originally assigned to these formations by Werner—of Gneiss
in the lowest position, followed by Mica-slate, and this by the Clay-
slate—has usually been adopted by geologists, though some re-
markable exceptions to this order have been long known. ‘To some
of these I adverted in 1844, and again in a paper read before the
Geological Society in 1855, in which I endeavoured to explain the
phenomena on the supposition of a reversal of the beds. The
following sections will show how far this view can still be main-
tained ||.

* Guide to the Geology of Scotland, pp. 128, 139, 249; Quart. Journ. Geol.
Soe. vol. vi. (1849) p. 60.

t See especially “ On the Geol. of Cantyre,” Quart. Journ. Geol. Soc. vol. viii.
(1852) pp. 422, 423 (the substance of this paper was read at the Meeting of
the British Association at Edinburgh, in August 1850) ; “On Easdale and Oban,”
ad. vol. xv. (1858) pp. 112, 116; Note to Geol. Map of Scotland, Edinb. 1858.

£ Macculloch, Geological Classification of Rocks (1821), p. 3. In that work
the different varieties of rocks composing each formation are fully described, and
perhaps undue importance ascribed to them. See also his ‘ Western Isles,’ vol. 11.

. 803, note.
‘ It is enough to mention Humboldt’s Essai géognostique sur le Gisement de
Roches (Paris, 1826) among the older, and Naumann’s elaborate ‘ Lehrbuch der
Geognosie’ among the newer foreign works, in proof of this universal recogni-
tion of these formations. Dr. Ami Boué, from his knowledge of Scottish rocks, is
an unexceptional witness to their agreement with those of foreign countries.

|| See Guide to Geol. of Scotland, p. 169 ; “Section of the Eastern Grampians,”
Quart. Journ. Geol. Soc. vol. xi. p. 547. Even in 1821, in his ‘ Treatise on Rocks,’
p. 92, Dr. Macculloch had pointed out this fact, like many others which have been
claimed as new discoveries.

182 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

3. Clay-slate Formation of Bute. — The first formation I shall
notice is the clay-slate. This, as shown by Dr. Macculloch and in
my own map, forms a narrow band along the southern flank of the
Grampians, from Arran to Stonehaven, everywhere presenting very
similar and unmistakeable characters. These it 1s unnecessary to
repeat, and some local peculiarities will be noted in the special sec-
tions. I shall also pass over its relations in Arran, only remarking,
that the granite appears to have risen up nearly in the line of junc-
tion between the clay-slate and the mica-slate. In Bute the clay-
slate dips to the S.E. at angles ranging from 20° to 60°, and appears
to rest on the mica-slate, also dipping in the same direction. Some
sections near Rothsay have led me to suspect that in this island
there are two formations of the clay-slate, as intimated by Mr. D.
Sharpe, the upper green or light-grey slates appearing to rest un-
conformably on the lower blue slates.

4. Loch Long and Gareloch._—On the mainland a similar S.E. dip
prevails along the Firth of Clyde, though in some places, as near
Dunoon, the outer range of clay-slate can scarcely be said to occur.
On the Gareloch a better section of the clay-slate in its relation to
the mica-slate is seen, though still in some places concealed by de-
tritus. This section is represented in fig. 1, beginning on the north

Fig. 1.—Section on Gareloch.
N.W. S.E.

Loch Gareloch Rose- Firth of
Long. Head. neath. Clyde.

Mica-slate. Clay-slate.

side of Loch Long, near Castle Carrick, and extending to the Clyde,
near Roseneath.

On the north side of Loch Long the mica-slate, rising up into the
gnarled and rugged mountain-group known as Argyll’s Bowling
Green, forms an anticlinal axis, apparently oblique to the direction
of the loch. On both sides of Loch Long the mica-slate is so twisted
and contorted that the dip is almost undeterminable. Occasionally
the beds are horizontal, then they dip to the north or south at angles
ranging from 15° to 80°, or, again, are, as it were, twisted in both
directions in the most complex manner. The average direction is,
however, N.E. by E. (or N. 55° E.), and thus nearly parallel to the
general range of the strata. Several dykes or veins of greenstone
intersect the strata, but do not produce much change either on their
direction or character.

The strata, generally a distinct lustrous mica-slate, intersected by
quartz-veins, continue to dip 8. 35° E. from Loch Long to Gareloch
Head. Near the latter place the beds become more regular, with
an average dip of 70°. Further down the Gareloch the rocks are

NICOL——-SOUTHERN GRAMPIANS. 183

more arenaceous or less crystalline, and the dip declines to 55°, 45°,
and even to 30°. On the east side of the loch, near Shandon, some
beds of clay-slate appear; and the strata, dipping first north at high
angles, then south, then again north, and finally regularly south-east,
show that in this place there is probably a faulted synclinal. The
same irregularity, as shown in the section, occurs on the west side
of the loch, but beyond this break the beds have a uniform south-
east dip to the clay-slate near Roseneath. These slates dip at 40°
to 8. 35° E., and appear to consist, as in Bute, of*two divisions, the
lower micaceous or talcose, and of a deep blue or purplish tint, the
upper of a lighter blue or green with a more silvery lustre. Some
of the beds resemble a fine-grained greywacke. This section and
that of Bute show what may be considered the regular normal order
of the formations on the south border of the western Grampians.
First, towards the axis of the chain, the more highly crystalline and
contorted mica-slate, covered by less crystalline and more even beds
of the same rock, and these in turn by talcose or chloritic blue and
green clay-slates, with occasional beds of greywacke. The low and
regular dip of the beds, and the conformity of the order to the only
theory of metamorphic action which seems admissible in the present
state of geological science, induce me to regard this as the true nor-
mal order of these formations.

5. Loch Lomond.—The next section I shall notice (fig. 2) is that

Fig. 2.—Section on Loch Lomond.
N.W. SiE
Ben Lomond. Rowardennan. Sallachie. Auchmar,

i
Mp
>

Balmaha.

Mica-slate. a Clay-slate. b c Old Red
Sandstone.
a. Syenite. b. Granite. c. Limestone.

seen on the east side of Loch Lomond, from Ben Lomond to the
Red Sandstone at Balmaha, about ten miles east of the one just
described.

Ben Lomond, at the northern extremity, consists of mica-slate,
often quartzose, much contorted, and dipping at low angles, and inter-
sected by veins of felspar-porphyry. Near Rowardennan the strata
become more regular, dipping at high angles (80° to 85°) to S. 27° E.
The rocks are still chiefly mica-slate, passing occasionally into a light-
grey talc-slate. About a mile below the inn some of the beds dip
north at high angles, and are intersected by a parallel vein of fine-
grained syenite, composed chiefly of red felspar and dark-green horn-
blende. At Sallachie Wood a coarse greywacke, very hard and full
of quartz-veins, appears, dipping at 80° to 8. 27° E., and thus con-
formable to the mica-slates on the north. It contains distinctly
rounded grains of quartz, thus leaving no doubt of its mechanical
origin. Further on, the clay-slate, well exposed in the quarries,

184 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

dips at 70° to 75° to 8. 27° E., or 8. 33° E., and thus still conform-
able to the mica-slate. The lower beds are compact, glossy, blue
slates of uniform texture, and with a few grains of pyrites; the
higher beds are a similar rock, but of a light grey or green colour. In
his section of this place Mr. Sharpe indicates two planes of division in
these slates—one of cleavage or foliation, the other of bedding or
deposition, but both nearly coincident. So far as I could make out,
the bedding and cleavage coincide, though there are other division-
planes dipping about 38° to N. 75° W.

Beyond the clay-slates coarse greywackes again appear, dipping
first at 70° to N. 12° W., and soon at 70° to S. 17° EK... There is
thus in this place probably an anticlinal fold in the beds, and some
thin irregular veins of a white granite also mark it out as an axis
of disturbance. About a mile further down the lake, beds of reddish
greywacke appear to dip at 40° to N. 10° W., but are not very dis-
tinctly seen. The cause of this change in the dip is probably the in-
trusion of a coarse red granite or felspar-rock, which breaks out near
the junction with the Red Sandstone, about half a mile from the Old
Manse. Some hard, jaspery masses associated with this igneous rock
are perhaps altered beds of the Old Red. Near Auchmar an impure
yellow limestone has been wrought, also probably a portion of the
Old Red, though often conjoimed with the Leny limestone in the
clay-slate. At the Pass of Balmaha the conglomerate of the Old Red
Sandstone, dipping at 60° to S. 45° E., forms a bold projecting hill
in front of the primary mountains. The low ground to the south
consists of finer-grained red sandstone lying ata low angle, and near
Drymen dipping at 12° to E. 15° S.

In this section, though the beds dip at much higher angles, the
relation of the formations is still the same as on the Gareloch. The
mica-slates, dipping south, are covered by an upper group of blue and
green clay-slates and greywackes. The two formations also appear
to be conformable, and the direction of the beds varies little from E.
and W. by compass (E. 27° N. true), but near the south margin
of the clay-slate, probably from the intrusion of the granite, ap-
proaches nearer to the true east and west (HE. 16° N., to W. 16° S.)*.

6. Callander and Pass of Leny.—Passing again to the eastward,
over an interval of about fifteen miles, we reach the well-known
vicinity of the Trossachs and Callander. To the north of the latter
the rocks are very well exposed in the Pass of Leny and on the banks
of Loch Lubnaig (fig. 3).

At Callander, the red sandstone and conglomerate, which form the
low undulating plain stretching south to the Ochils, rise up into a range
of low but rugged hills, immediately behind the village. The rocks
are well seen in a fine natural section at Bracklyn Falls, where the
Keltie forces its way through the upturned beds in a series of deep
pools and whirling caldrons. Higher up the stream there is a thick

* My observations agree generally with Mr. D. Sharpe’s section in Quart. Journ.
Geol. Soc. vol. viii. (1852), p. 129. Sir R. I. Murchison and Mr. Geikie, in their
new Sketch-map, also give a section of this locality, but differing in some im-
portant points.

NICOL—SOUTHERN GRAMPIANS. 185

mass of red and reddish-grey sandstone, with a conglomerate-bed
consisting of masses of brown porphyry and white quartz. The
strata dip at 75° to S. 45° E., and at the Falls consist of coarse sand-
stones below, of a quartzose conglomerate in
the centre, and of deep-red, fine shaly beds
above. They are intersected by ‘‘ backs” or
division-planes, nearly vertical to the bedding,
so that the water removing the softer portions
has left great square ledges projecting like
walls into the ravine. The conglomerate is
also well seen near the Railway-station, dipping
at 65° to 8. 42° E., the whole surface being
deeply grooved and smoothed as by glacier-
action. Here also it consists especially of vein-
quartz, with smaller fragments of the clay-
slates on the north, in a reddish-brown basis
of decomposed felspar. Beyond the village the
lower sandstones, dipping at 70°-77° toS. 37°
E., are quarried for building-purposes, and are
in part fine-grained and greyish purple, in part
deeper brown and more shaly.

The next formation is the clay-slate (d), seen
in the deep gorge of the Pass of Leny. The
lowest beds are light-grey greywacke, weather-
ing brown, and composed of distinct grains of
quartz in a basis of decomposed felspar and clay-
slate. These strata dip to N. 37° W., at angles
of 44° to 50°. Above them are red and yellow
slaty beds, some of them almost a pure iron-
ochre, others more arenaceous, dipping at 47°
to N. 17° W., but with some confusion and
uncertainty. Red beds follow, with a distinct
cross cleavage; but their dip is disturbed and
obscure, probably from a dyke of blue columnar
dolerite, 30 to 40 feet wide, which runs N.
25° K. with a slight dip to the south. Beyond
it are fine-grained grey slates, dipping at 66°
to N. 55° W., but with a cross structure or
cleavage inclined at 20° to N. 35° E.

At this point a marked change takes place
in the position of the strata. The dip is first
25° to N. 20° E., but soon rises to 40° to N.
5° W. Further on, it rises to 67°, N. 37° W.,
and then to 75°, N. 45° W., in curved, irregu- =
lar beds of blue slate, with a cross division 4
or cleavage inclined at 12° to N. 12° EK. Grey slates again follow,
dipping at 68° to N. 37° W., and are succeeded by coarse greywackes
in thick beds, dipping at 60° to N. 5°-10° W. This rock is also
intersected by other planes dipping 55° to 8. 25° W., and by well-
marked fissures, lined on the sides by actinolite, running to W. 62° S.

S.E.

Callander.
Red Sandstone.

Greywacke and Clay-slate.

* Trap-dykes.

a

Foot of

Fig. 3.—Section in Pass of Leny.
L. Lubnaig.

A. B. Faults.

Blue talcose Slates.

Mica-slate.

186 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Beyond this point, near the foot of Loch Lubnaig, there is a great
mass of chloritic slate and greywacke, full of quartz-veins reticu-
lating in all directions, but with no determinable dip or direction.
It contains imbedded fragments of a more siliceous nature. The
coarse greywacke also is composed of fragments of quartz and felspar,
from one-tenth to one-fourth of an inch in diameter, in a basis of
grey chlorite or mica in fine scales. Even the coarser varieties have,
however, a distinctly foliated or schistose texture, unlike anything
I have seen in the South of Scotland. The grains of quartz and
felspar are flattened and drawn out in the direction of the foliation,
so that the rock presents, as it were, an incipient tendency to assume
the structure of regular gneiss*. As illustrating the metamorphic
origin of the crystalline strata, this rock is exceedingly interesting,
presenting, as it were, one of the intermediate steps in the process.
It is more crystalline than the greywackes of the south, less so than
the true gneiss of the north, and, though distinctly foliated, still
clearly fragmentary in origin.

Beyond this point the strata become more regular, and less detail
is necessary. ‘The first beds are greenish clay-slate, dipping about
40° or 45° to N. 42° W., and interlaminated with parallel veins or
layers of quartz with undulating surfaces, as if ripple-marked.
Further up Loch Lubnaig the dip rises to 75°, N. 37° W., in blue
talcose slates. Near Ardchullarie another vein of dark greenstone,
about 50 feet wide, runs nearly E. and W. by compass (E. 30° N.).
Soon after the true mica-slate appears, dipping at 73° to N. 15° W.,
in thin undulating beds. It continues along the whole lake; but
further up the strata become more contorted, and dip very irregu-
larly at lower angles. Though not quite conformable to the clay-
slate, the mica-slate clearly overlies that rock, seen further down the
loch.

7. Leny Limestones.—On the hills to the east of the Pass of Leny,
limestone has been quarried for a long period. The excavations
follow the outcrop of the rock across the ridge of the hill, and in
some places are of considerable depth. In one part of the old quarry
there is the section represented in fig. 4.

To the south are black shales (c), mixed with contorted beds and
masses of limestone. Above the shales is the limestone 6, blue and
reticulated by veins of white calespar, and now wrought out above. It
is covered by grey talcose beds (a,),and these by red shales (a,) curved
and twisted. At «is a bed of red compact felspar-porphyry, with
grains of quartz and crystals of mica sparingly distributed through it.
The limestone is better seen in the quarry now being wrought, where
it is 15 feet thick, and divided into several thin, curved, and irre-
gular beds, dipping at 53° to N. 25° W. It rests on and is covered
by black shales, both dipping at 70° to N. 37° W.,—thus, curiously
enough, both unconformable to the limestone between them. The
shales are covered by a red porphyry, identical with that in the

* Professor Hitchcock, of Amherst College, has recently described a similar
anpetene in America. See Silliman’s Am. Journ. of Science, vol. xxxi. (1861)
p. 302, C.

NICOL—-SOUTHERN GRAMPIANS. 187

former quarry. To the south the shales rest on reddish greywacke,
intersected by a great dyke of basalt, from twenty-five to thirty
yards wide. It dips northwards at about 60° under the limestone,
and runs a little north of east by compass (EK. 40°-45° N.), and
thus approximately parallel to other similar dykes in the southern

Fig. 4.—Section at Leny Old Lime-quarry.

N.W. S.E.

c
by “4

x. Felspar-porphyry. 5. Limestone.
a,. Red shales. ~ c. Black shales.
a. Grey talcose shales.

Grampians. It continues east as far as the Keltie, but seems dis-
tinct from the dyke noticed in the Pass. The limestone has also
been sought in vain in the low ground, as the quarries opened high
on the mountains are very inconvenient. Though of considerable
thickness and divided into many beds, this limestone, as is frequently
seen in the primary strata, is a very partial formation. The red
porphyry, hitherto overlooked, has produced considerable disturbance
in the strata, as shown both by the irregular outcrop of the limestone
and its relation to the other strata. Both the texture and colour of
the limestone, and the black carbonaceous-looking shales associated
with it, remind us rather of the Carboniferous formations than of a
primary deposit*.

8. Ben Ledi—The great mountain of Ben Ledi, on the west side
of Loch Lubnaig, also shows an interesting section of these deposits

fig. 5).

At the foot of the hill, immediately north of the road to the Tros-
sachs, a mass of coarse conglomerate rises into a rugged knob. Be-
yond it the slope of the hill is low, and thickly covered with moss and
vegetation concealing the rocks. Where the acclivity becomes steeper,
a fine hard greywacke dips at 50° to N. 4° E., followed on the first
shoulder of the mountain by a light greyish-green clay-slate, contain-
ing grains of quartz and scales of mica, dipping at 40° to N. 2° E. The
next shoulder of the hill consists of hght-grey mica-slate, dipping at
50° to N. 15° W. along the foliation, but with other very distinct

* Prof. Harkness, in his section of this place, omits both the trap and por-
phyry. He also states that the limestone rests on quartz-rock, which I could
not find either in the quarries or the neighbouring ravines. The only rock at all
resembling quartz-rock is the porphyry above the limestone.

188 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

division-planes, which dip at 60° to8. 43° W. These rocks generally
weather to a dark rusty brown, probably from containing the prot-
oxide of iron. Soon after, the same rocks dip at 60° to N. 27° W.,
again on the foliation of the slate, but in a few yards fall to 35°, N.
27° W., from a curve in the beds. The next acclivity is a fine-
grained mica-slate with a veined aspect, from the folia being arranged
in curved layers. The dip here is still low (30° to N. 17° W.), but
. soon rises to 65°, N. 12° W., in a grey mica-slate full of quartz-veins.
This rock continues to the summit of the hill, where the dip is 55°
N. 17° W., and a nearly similar dip appears in the rugged precipice
along the ridge to the north. Other division-planes, dipping 70°, 8.
50° W., are seen in these cliffs ; and a series of ridges and hollows,
like the outcrop of beds, run N. 50° W. across the top of the hill.
The rock there is still a light-grey mica-slate, with small garnets
rarely disseminated through it.

Fig. 5.—WSection of Ben Ledt.

_ a. Red Conglomerate. ec. Mica-slate. e. Felspar-porphyry.
6. Clay-slate. d. Greenstone.

On descending the mountain on the north-east towards the top of
the great corrie that opens up from Loch Lubnaig, the mica-slate
passes into a coarse granular rock, full of rounded grains of quartz,
and almost like a greywacke, but still distinctly foliated. This is
again one of those transition-forms that so clearly illustrate the me-
tamorphic character of these rocks. The dip of these beds is 45° to
N. 18° E.; but other planes dip at 67° to 8. 38° W., and thus ap-
proximately parallel to the second set of division-planes already men-
tioned. Itis, however, curious that these coarse-grained greywacke-
like beds, both here and in other places, do not coincide in dip with
the slates or finer beds near them. Still lower on the mountain,
towards the south, mica-slate again appears, dipping 70° to N. 40° E.
Below it there is an irregular vein or mass of light-grey greenstone
decomposing in globular concretions, and probably the continuation of
the vein near Ardchullarie on the other side of Loch Lubnaig. Still
lower, a very quartzose mica-slate,in thin beds, dips at 70° to N.27°W.
The stream continues to flow over irregular beds of mica-slate, in some
places much bent and contorted, and dipping E. at 10° to 30°, in other
places more regularly at 65° to N. 10° W. Near the foot of the
corrie the stream forms a series of picturesque linns over the ledges
of the fine-grained mica-slates, which dip at 70°—80° to N. 30°-40° W.
At the foot of the hill the dip falls to 60°, and further south to

NICOL—SOUTHERN GRAMPIANS. 189

50° N. 40° W., in fine granular mica-slate. Still lower, I found
a thick bed of clay-slate, reticulated with numerous veins of quartz,
similar to one mentioned in the section on the east bank of the Lub-
naig; and some slate-quarries are wrought high up on the hill, but
probably lower in the series. Further south, and quite within the
gorge of the river, a concretionary red felspar-porphyry appears,
similar to the porphyry at the Leny lime-quarry. Below it there is
a red greywacke, followed to the south by other beds, apparently the
mere continuation of the first beds in the former section, but much
concealed by woods and detritus.

9. General Remarks on the foregoing Sections.—I have given fuller,
perhaps it may be deemed tedious, details of the changes in character
and in dip and direction of these strata than might otherwise have
been necessary, from the great theoretical importance of this section.
A mere casual walk along the road, with its numerous turnings and
windings, and the distraction occasioned by the wild and romantic
scenery, is apt to leave on the mind an impression of greater regu-
larity in the sequence than really exists. And so it is when the
facts are at once generalized, the numerous exceptions ignored and
passed over, and mere averages, deduced or assumed, only stated.
In such a method of procedure both author and reader are deceived,
and a regularity imagined which has no existence. I have felt this
to be the case in reference to these sections, The first general im-
pression is, that there is here a continuous series of beds dipping
regularly to the north, one below the other. In that case the grey-
wacke to the south would be the lowest and oldest deposit, followed
first by clay-slate, and this by mica-slate, as the upper and newest-for-
mation. This is, of course, exactly the opposite order from that noted
in the former sections, and cannot therefore be adopted without some
consideration. To the general question of order I shall subsequently
advert, and would now only direct attention to one or two special
points. The first of these is the marks of disturbance in the sections,
indicated both by igneous intrusion and by changes in the dip and
direction of the beds, This is especially seen in the Leny section,
fig. 3, at the points marked A and B. The beds north and south of
A seem merely the same group repeated. At B a more decided
change takes place, and here Dr. Macculloch has drawn the line of
junction between the clay-slate and mica-slate. Clay-slate indeed
occurs north on Loch Lubnaig, but more talcose and foliated, or cry-
stalline, than the strata south of B. In Ben Ledi, also, beds con-
taining distinct fragments run far into the interior. The two sets of
division-planes seen in Ben Ledi give rise to another important
question,—which of these indicates the true bedding or stratification ?
If the lines of foliation in the slates are not truly lines of bedding or
deposition, and we must look for these in the other set of division-
planes, then the whole order of the formations is reversed. It would
undoubtedly be easier to assume either supposition as true, than to
assign a sufficient reason for the choice made.

10. Comrie and Strath EKarn.—The next locality I have to notice
is Upper Strath Earn, near Comrie, again about twelve miles north-

190 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

east of the last section. Comrie, though remarkable both for its
picturesque beauty and for the frequency of the earthquake-shocks
felt there, has met with less attention from geologists than the in-
teresting nature of the phenomena around it might demand ; and I
am not acquainted with any detailed description of its formations.
The village lies in the bottom of a wide, flat valley, shut in on all
sides by hills, and traversed by the Earn, Ruchill, and Lednock rivers,
which unite at this place. On the north and west the primary
mountains rise high and rugged, whilst the trap and Old Red Sand-
stone form a lower range, separating it from the central plain. Upper
Strath Earn is evidently a great valley of denudation, with rounded
knobs of slate and trap, smoothed and striated by glacier-action, rising
through the level sheet of detritus.

The section, fig. 6, represents the rocks as seen on nearly a north

Fig. 6.—Section at Comrie.

N. S,
Ben Chonzie. Lednock. Comrie.

« Alluvium. 06 Red Sandstone.

Syenite. a a
Clay-slate.

a. Trap-dykes. b. Greenstone.

and south line passing from the granite, or rather syenite, of Ben
Chonzie, through Comrie, to the red sandstone of the central valley.
Where it begins in the south, the strata are chiefly fine-grained red
sandstones intermixed with grey micaceous beds or dark-red sandy
shales covered with bright-green blotches. In the low ground the beds
le at a low angle, but towards the north dip at 70° to 8. 15° E., and
rest on thick masses of coarse conglomerate. In this rock the strata
are nearly vertical, with a direction from E. 28° N. to W. 28°S. It
appears to have been elevated by the greenstone on the north, which
runs in a series of low, rounded, and interrupted knolls from N.E. to
S.W., separating the Red Sandstone from the primary formations.
The changes that the igneous rock has effected on the conglomerate
are very remarkable. In one place, large, distinctly rounded boulders
are imbedded in a basis of porphyritic or amygdaloidal trap, inter-
sected by veins of chalcedony and ealc-spar. It looks almost as if,
in some period of violent convulsion, a bed of molten lava had forced
itself in amidst a heap of water-worn shingle, and kneaded up the
loose boulders into its own mass. Probably, however, it is only a
true conglomerate with a basis of broken-down or decomposed trap,
which has subsequently been semi-fused, thus giving the mass the
aspect of an igneous rock.

The boulders in the conglomerate range in size from fine sand or
gravel to masses of nearly a foot in diameter. Lying close to the
foot of lofty mountains of the primary formations, it might naturally
be expected that the conglomerate should be composed of fragments

NICOL—SOUTHERN GRAMPIANS, 191

derived from these rocks; this, however, is not the case. I ex-
amined a very large number of specimens collected indiscriminately
in several localities, and found them, almost without exception, frag-
ments of igneous rocks, and especially of clove-brown felspar-por-
phyries and claystone-porphyries. They are thus derived from rocks
distinct both from the augitic greenstone on which they rest, and
from the crystalline rocks forming the mountains on the north and
west. This peculiar character of the conglomerates of the Old Red
Sandstone in the central valley of Scotland is by no means confined
to this locality ; it reappears in many other places, both along the
foot of the Grampians and on the south side of the valley near the
Ochil Range. Thus, in the coarse conglomerates near the Bridge of
Allan, similar brown felspar-porphyries and claystones predominate,
in many places to the exclusion of almost every other rock. In
the Ochils, rocks of this nature, from which these conglomerates
may have been derived, are not uncommon; but near Comrie they
either do not occur, or are probably concealed by newer deposits.
The whole phenomena of these red-sandstone-conglomerates lead to
the conclusion that they have been formed along lines of fissure,
through which outbursts of igneous matter were taking place,—one
of these lines running along the foot of the Grampians, and another
marked by the present Sidlaw, Ochil, and Campsie Hills. Along
these lines the materials of the conglomerates are chiefly trappean.
In some localities, however, as near Callander, fragments of quartz
or primary strata predominate, the rocks in these places having pro-
bably been formed near the outlet of some ancient river, or where
projecting points of the old strata rose high above the waters and
were thus exposed to atmospheric and oceanic influences. It is alsoa
curious fact that, mixed with these trappean conglomerates, there are
other beds of finer materials, undoubtedly derived from the older cry-
stalline rocks. Thus, some of the Pteraspis-sandstones at the Bridge
of Allan consist of angular fragments of quartz, felspar, and mica, and
hence like a true granite or gneiss, only with a fragmentary or
clastic, not a crystalline structure. The prevailing red colour of the
sandstones also seems owing to the ejection of ferruginous matter
during these long-continued eruptions*.

The next formation is the clay-slate and greywacke, which pro-
bably underlie the flat plain south of Comrie, though concealed by
the covering of detritus. They are, however, well seen on the north
side of the Earn, especially in the deep gorge of the Lednock, which
has cut through them in a series of romantic rapids and cascades.
The rocks vary from a moderately coarse greywacke, composed of
rounded grains of quartz in a basis of clay-slate, to a fine-grained
clay-slate with a fibrous or silky lustre. The greywackes are of a

* Whilst these facts show that part of the igneous formations in the Ochils pre-
ceded, and that part accompanied the formation of the Old Red Sandstone, there
is full evidence that other portions are younger than the Red Sandstone, and indeed
even than the Coal. It is also right to mention that some observers consider the
trappean conglomerates as marking an older, the quartzose conglomerates a
newer stage in the Red Sandstone. (See Page’s Advanced Text-book, p. 174.)

192 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

blue colour; the slates often bluish or greenish grey, weathering
brown on exposure. Both rocks contain iron-pyrites in cubical
crystals or disseminated in small grains, and also scales of mica.
The slates show very distinct division-planes, or foliation, with a
very predominant dip at 70° to N. 10° W., but the inclination
ranging from 55° near Comrie to 85° on the north near the syenite,
and the direction of the dip from N. 15° E. to N. 55° W.

Before noticing some other peculiarities in the slates, it is better
to complete the section by describing the granite, or rather syenite,
in the north. This rock rises high up on the declivities of Ben
Chonzie (2922 feet high), and occupies a great part of the valley of
the Lednock. Generally it is a fine-grained syenite, composed of abun-
dant felspar and hornblende, with scales of black mica and a little
quartz. In some varieties, as that used in building the Melville
Monument, the hornblende is in great measure replaced by mica,
and the stone has then a white or grey colour. It has been com-
pared to the grey granite of Aberdeen, but the resemblance is
merely superficial. In the Comrie syenite the felspar is more pre-
dominant, and often forms distinct porphyritic crystals ; hornblende
seems always more or less present, and the quartz is far more subor-
dinate than in the grey Aberdeenshire granite. In truth, it seems
more closely related to the felspar-porphyry or trap group, than to
the true granites of the central Grampians. Its peculiar character
is better seen in other varieties, which are fine-grained mixtures of
red felspar and green hornblende, with very little quartz or mica. A
vein or mass of this kind occurs in Dunmore Hill, near the Monu-
ment, chiefly composed of red crystalline felspar*.

Some of the effects of the syenite on the slate near it are very
interesting. It appears occasionally to send veins of considerable
extent far into the midst of the slate mountains, and finer veins are
seen ramifying through the slate irregularly in various directions.
On the position of the slate it does not appear to have produced
much change, as the beds near it are on the whole conformable in
dip and strike to those more remote from it. More marked is the
change in the mineral character of the rocks as seen in tracing them
along the Lednock from Comrie to the vicinity of the syenite. As
they approach the igneous rock the slates gradually become harder
and more crystalline. Then lenticular masses of red felspar and
quartz, like a binary gneiss, become intermixed with layers, more or
less continuous, of the blue slate, till at length the whole rock is
converted into a fine-grained gneiss. Even the coarser greywackes
are so altered in aspect as,in many places, to be readily mistaken for
the syenite.

11. Bedding or Cleavage (?).—In examining the section just de-
scribed, and other sections in the slates, considerable difficulty is
often felt as to the true character of the division-planes seen in them.

* See, for the position of this syenite, Dr. Macculloch’s Geological Map of Scot-
land, or my own Map. It is omitted, along with the other igneous rocks in this
vicinity, in the “ Sketch of a New Geol. Map,” &c., by Sir R. I. Murchison and
Mr. Geikie.

NICOL—-SOUTHERN GRAMPIANS. 193

Are these planes of deposition and bedding, or a true slaty cleavage *
distinct from, and independent of the stratification? Or are theso
two structures here coincident? This question is of very consider-
able interest in relation to the true structure of this locality, and of
the Highlands generally. It has too often been assumed, without
proof, that all the marked division-lines in the metamorphic strata
of the Scottish Highlands are lines of deposition, and much error
and confusion has thus been produced. Near Comrie, this question
is not easily decided, as the rocks, chiefly exposed in natural sections,
or quarries of small extent, furnish few precise data for its determi-
nation. Still even there the great regularity in these planes, and the
intimate manner in which they pervade the entire mass of the rock,
correspond more to cleavage than bedding. Other planes of struc-
ture, too, may be observed in these rocks. One set of these showa
very predominant dip west by compass, or W. 25° to 30° S., and
-thus with a strike to N. 30° W., almost at right angles to the direc-
tion usually assigned to the strata in this region. This dip is very
clearly seen in the coarse greywackes at the foot of Loch Earn, and
also in the contorted mica-slate at St. Fillans Church. ‘The latter
rock consists of thin, undulating lamine, dipping N. 27° W., but
intersected by other planes dipping W. 27°S. parallel to the bedding
of the slates. Similar planes dipping generally W.S.W. are obser-
vable in the whole valley from Loch Earn to Comrie, but near the
latter place the dip is more nearly west. In the valley of the Led-
nock a second set of division-planes also occur, but far less regular in
position.

The slate-quarries wrought in the Aberuchil Hills, in Glen Artney,
to the south-west of Comrie, offer better evidence on this question.
These slates are of a light bluish-grey colour, with a fine granular,
almost compact texture, occasionally becoming fibrous or minutely
erystalline. The cleavage is very distinct, so that the slates appear
scaly, or as if made up of very flat and thin lenticular plates. The
cleavage is cut obliquely by other planes, some very distinct, others
little more than mere striz, or hghter and darker lines. Where
very numerous and close, these give the slates a glossy, fibrous aspect.
The more distinct lines are readily traced in hand-specimens, and
appear as great curves on the exposed faces of rock in the quarry.
They do not intersect the cleavage at any fixed angle, but range
from 15° to 45°, and 60° in some instances which I measured. These
curved lines seem to me to represent the planes of deposition, whilst
the slates are wrought on the true slaty cleavage. The dip of the
cleavage is N. 12° to 27° W., thus parallel to the foliation of the

* Tt has been affirmed that true slaty cleavage does not exist in these meta-
morphic strata. Mr. D. Sharpe had great merit in directing attention to its occur-
rence in many parts of the slates, though in some points going further than I can
find good reason for following. (See Quart. Journ. Geol. Soc. vol. viii. p. 126, and
Phil. Trans. 1852, p. 445.) In the Quart. Journ. Geol. Soc. vol. xv. p. 113, I
described this structure in the slates of Easdale and Oban, where a marked
parallelism in the cleavage is combined with remarkable convolutions in the
beds. Compare, for cleavage in the Aberdeenshire slates, Rep. Brit. Assoc. for
1859, p. 118.

VOL. XIX.—PART I. 0

194 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

slates at Comrie, and proving that it too is cleavage and not stratifi-
cation. The position of the other planes is less definite from their
curvature, but they seem on the whole to dip S.E., and the large
rock-masses in some of the neighbouring hills appear also to dip
in that direction. The subjoined figure (fig. 7) may give some
imperfect idea of the contortions in the beds in one part of these
quarries. The borders, represented as seen in the quarry, are nearly
in the line of cleavage. ;

Fig. 7.—Contortions in Slate, Aberuchil Quarry.

On the whole, therefore, I conclude that the chief division-planes
seen in the slates near Comrie are those of cleavage, and not of
deposition. The dip of this cleavage is predominantly N. 10° W.,
and the direction W. 10° S. to E. 10° N., and thus oblique to the
general course of the slate on the south flank of the Grampians.
The strike of the beds, as marked by the other division-planes,
N. 30° W., withaS.W., or more rarely N.E. dip, is still less conform-
able to the usual course of the slates. This deviation may perhaps
be caused by the intrusion of the Glen Lednock syenite, though, as
stated, it appears to have exercised no very marked influence on the
position of the slates *.

12. Mica-slate of Loch Earn.—The relation of the clay-slate to the
mica-slate formation is not very clearly shown in any of the sections
I examined in Strath Earn. Mica-slate appears near St. Fillans
Church, but soon again gives place, higher in the valley, to clay-
slate and greywacke. This mica-slate, as already noted, besides a
very distinct foliation, much twisted and contorted, as 1s common
in mica-slate, shows also other division-planes parallel to the bed-
ding of the clay-slates. Mica-slate predominates along the north
bank of Loch Earn, but the rocks are much concealed by wood and
vegetation, and the strata greatly disturbed, probably by intrusive
greenstones. So irregular are the beds, that at first it seems almost
impossible to discover any dominant dip or direction. On further
examination, however, the direction EK. 22° N. comes out as the
average result of the whole; or, excluding a few dips nearly at
right angles to the others, a mean direction of E. 40° N., with a

* The strike of these beds is thus parallel to that of the gneiss on the N.W.
coast of Ross and Sutherland, which it has been supposed to characterize as an
older group ; but see my paper, Quart. Journ. Geol. Soc. vol. xvii. p. 110.

NICOL—-SOUTHERN GRAMPIANS. 195

preponderance of dips to the south, but nearly balanced by dips to
thenorth. The dips are frequently at low angles; and, on the whole,
_ TL have no doubt that on the north side of Loch Earn the mica-slate
forms a marked anticlinal axis, probably the continuation of the axis
of highly contorted beds noted above on Loch Long, Loch Lomond,
and Loch Lubnaig. The limestone, formerly quarried on the upper
part of Loch Earn, appears to lie deep in this series, and is probably
overlain by the greater part of the mica-slate, both higher and lower
on the loch. This limestone is large-grained, crystalline, and of a
grey, or rather mixed white and black colour. It 1s wholly unlike
the Leny limestone near Callander, but closely resembles some of the
limestones in the mica-slate of Cantyre. The limestone is also wrought
at Edinample, on the south side of Loch Earn, and also runs N.N.E.
for some miles up Glen Vech. The dip, generally at low angles,
varies, however, even in the main quarry, from N. 57° W. to
S. 67° W. The limestone seen on the south side of Loch Tay, also
in the mica-slate, is probably the continuation of this deposit, whilst
the beds on the north side of that lake, dipping below Ben Lawers,
are the same series brought up by a fault*. This view is repre-
sented in the diagram, fig. 8.

Fig. 8.—Section from Loch Earn to Loch Tay.

Loch Tay. Loch Earn.

a. Limestone. * Trap.

As already stated, the relation of the clay-slate to the mica-slate
is not clearly exhibited in any single section. At the foot of Loch
Earn, near St. Fillans, the clay-slate and greywacke have a very
constant dip W. 32°S., and consequently a strike N. 32° W. This,
as formerly noted, is the general direction of the stratification in the
slates, and nearly at right angles to the direction just deduced for
the mica-slate (EK. 22° N. or, better, E. 40° N.). This strike of the
mica-slate more nearly corresponds with the strike of the other set
of planes, or the foliation of the clay-slate, which we found E. 10° N.,
but still deviates from it, on what I consider the better determina-
tion, by 30°. Besides, whilst the dip of the mica-slate is predomi-
nantly to the south, that of the clay-slates is very constantly to the
north. We must therefore conclude that in Strath Earn the mica-

* In my Guide to the Geology of Scotland, p. 170, I stated that ‘‘ Loch Tay lies
in a valley of elevation ;” and Sir R. I. Murchison says that it “‘ lies on an anticlinal
fold” (Note to New Sketch-map, p. 17). In the section on my Geological Map
of Scotland, the strata on both sides of the loch are represented as dipping N:W.
This is the result of my observations round Killin, where that section crosses the
valley of Loch Tay.

02

196 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

slate is a distinct formation from the clay-slate, separated from
it both by its lithological and physical characters and its geological
position and relations.

Before leaving this vicinity, some notice must be taken of the
veins of trap which form a most striking feature in its geology.
Several of them are seen near Comrie, as in the bed of the Lednock
and on the road to the Melville Monument. In this line three, or,
probably, four of these dykes occur, generally consisting of black,
columnar basalt, decomposing in globular concretions. Their direc-
tion is E. and W. by compass, or a little to the south of east (EH.
17° N. true), and they often show an inclination (60° to 90°) to the
north. Their breadth varies from 20 to 30 yards, but they run for
great distances nearly in the same direction; some of those in the
Lednock, near Comrie, crossing the valley of the Earn two miles
further up, and then running into the Aberuchil Hills beyond. On
Loch Earn similar dykes, chiefly of grey greenstone, are common
with a parallel direction, and probably pass by Loch Rattachan
into the upper valley of the Lednoch, where similar E. and W. trap-
dykes again occur. We might be disposed to connect these dykes
with the earthquake-phenomena so common at one time near Com-
rie*, were it not that similar and nearly parallel dykes traverse the
whole chain of the southern Grampians from the east coast, near
Aberdeen, to the west coast of Bute and Cantyre.

13. Dunkeld and Blavrgowrie.—Further to the north-east, near
Birnam and Dunkeld, the clay-slate and greywacke also dip towards,
and apparently under, the mica-slate. It was this curious appearance
which induced me many years ago to state that “the strata seem
in some places to have been completely reversedy.” I again drew
attention to this relation of the strata in 1858, observing, however,
that ‘‘ The very distinct cleavage of the [clay-] slate, obscuring the
stratification and often mistaken for it, makes it very difficult in
many places to determine the true position of this rock”’t. A similar
section is seen on the Ericht, above Blairgowrie, in the lower part
of Glen Shee. Here the Old Red Conglomerate, broken through by
trap-rocks, is beautifully exposed in the precipitous gorges in the
pleasure-grounds of Craighall. Further up, the river traverses the
clay-slate, quarried near Cally Bridge, and dipping north-west
towards the mica-slate. Probably a fault intervenes between the
two formations, but I have not examined the district so as to speak
with confidence.

* A register of the time of occurrence and the direction of these earthquake-
shocks was kept by Mr. Patrick Macfarlane, of Comrie, whose kindness in show-
ing me the very ingenious apparatus for marking the intensity and direction of
their motion (some of it his own invention) I take this opportunity of acknow-
ledging. The fullest account of them is given in some valuable papers by Mr.
Milne-Home, in the Edin. New Phil. Journ. vol. xxxi., &. Compare Geol. of
Scotland, pp. 257, 258. They have recently become rare, or, rather, have ceased, to
the great relief of the natives, who found that they repelled strangers from visit-
ing one of the most picturesque localities on the outskirts of the Grampians.

+ Guide to Geol. of Scotland (1844), p. 169.

+ Note on Geol. Map of Scotland, p. 3.

NICOI—SOUTHERN GRAMPIANS. 197

A similar relation occurs at the extreme north-east termination of

the chain between Stonehaven and Aberdeen, in the section on the

- sea-coast described by me in a paper formerly read to the Society*.
Referring to it for further details, I shall now make a few general
remarks on the sections described.

14. Relation of the Old Red Sandstone.—The first point I would
notice is the relation of the Old Red Sandstone to the primary or
metamorphic strata. Some years ago I showed that in Cantyre the
Red Sandstone rests conformably on the mica-slate , and has, in part
at least, been elevated along with it. It is therefore not improbable
that these deposits are among the oldest unaltered red conglomerates,
and distinct from other red sandstones that rest on them. On the
mainland from Joch Lomond to Stonehaven the sandstones are sepa-
rated from the slates by a great line of fault; and I donot remember
any place where the sandstones are seen resting immediately on the
older rocks. Very often, as in the Comrie section, a great intrusion
of trap intervenes, and, though less marked in other localities, a
band of igneous rock might probably be traced almost continuously
from sea to sea. Near the line of junction the sandstone has been
forced up at a high angle, and dips away from the primary strata.
It is often a hard, coarse conglomerate, but mixed with finer beds,
and in many places forms a range of lower hills skirting the great
Grampian chain. The position of the sandstone implies that the
strata forming the primary mountains on the north have not merely
been elevated, but have undergone a great lateral expansion, or push-
ing out to the south-eastt.

15. Clay-slate and Mica-slate—tThe relation of the clay-slate to
the mica-slate is more complex and difficult of explanation. In Can-
tyre clay-slate does not appear, having, as it were, been split off from
the mica-slate by the granite-eruption of Goatfell,in Arran. Further
north-east, as formerly stated, the two formations run side by side
along the whole southern base of the Grampians. But in Bute and
on the Gareloch both formations dip 8.E., and the clay-slate rests on
the mica-slate almost or altogether conformably, and at low or
moderate angles. On Loch Lomond the two formations are nearly
vertical, but both have still a southerly inclination, so that the clay-
slate continues to rest on the mica-slate. At Callander both forma-
tions dip north, and now the clay-slate apparently below the mica-
slate. At Comrie the two formations are unconformable, and both,
perhaps from the intrusion of the syenite, have a strike oblique to
their ordinary course. At Dunkeld, Blairgowrie, and other places, to
Stonehaven, the clay-slate again dips north, towards, and apparently
under, the mica-slate. There is thus a most remarkable anomaly
in the two portions of the chain. The clay-slate, which at the
western extremity covers the mica-slate, and is thus the newer for-
mation, is at the eastern end covered by it, and is there apparently

* Quart. Journ. Geol. Soc. vol. xi. (1855) p. 544.

+ Nicol, on Geology of Cantyre, Quart. Journ. Geol. Soc. vol. viii. (1852)
p. 410.

¢ Nicol, on Eastern Grampians, Quart. Journ. Geol. Soc. (1858) vol. xi. p. 549.

198 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the older. It seems a ready solution of the difficulty to declare both
formations identical, and to affirm that there is no normal order or
arrangement in them. This, however, is a mere evasion, not a solu-
tion, of the question. The mica-slate and clay-slate are too distinct
to be thus conjoined ; and Dr. Macculloch, who first pointed out (more
strongly, I suspect, than facts will warrant) their alternations and
transitions, fully admits their claims to be considered distinct geo-
logical formations. Besides, the difficulty, evaded in words, really
recurs in another form. How is it that the more metamorphic
portion of the series, which is lowest in one place, is highest in the
other? Still more, the bed of clay-slate is known and quarried at
so many points along the line from Bute to Stonehaven, that its
physical continuity can scarcely be doubted; and the question recurs,
how is it that this bed, which in the west forms the highest part of
the series, appears in the east as the lowest ?

In further considering this curious phenomenon, the first point
for inquiry is, what is the normal order of the two formations? Is
the clay-slate regularly the upper or the lower deposit ? The analogy
of other localities leads us to believe that the clay-slate is the higher
and newer formation; and the lower inclination and more regular
dip of the beds in Bute and on the Gareloch confirm the view that
the strata there are in their normal position. The reversed position,
therefore, seen at Callander and other points to the north-east must
be abnormal. We thus again return to the second question, How
has this peculiar position of the clay-slate been effected? Now I am
inclined to regard this infraposition of the clay-slate as, in part, only
apparent. Besides the great fault intervening between the red
sandstone and the clay-slate, other faults, approximately parallel to
it, run through the clay-slate, along which the dykes of trap and
other igneous rocks have found their way to the surface. The pri-
mary strata have thus been divided into longitudinal sections, and
each section having been tilted up from the south, the rocks all
dip north, towards, and apparently under, the centre of the chain.
But at other places, and especially at Callander, a real infraposition
of a portion of the clay-slate takes place, caused I believe by a com-
plete folding over or reversal of the beds. The first portion of the
strata in the Pass of Leny has been raised up from the south, and
dips normally to the north-west. Near the foot of Loch Lubnaig
there is a fault, and immediately beyond it the whole strata have
been folded over, so that the clay-slate comes to dip under, or rather
to be folded up in, the mica-slate. This change has taken place in
the country to the south-west, and, it would appear, in a gradual
manner, the strata rising from a dip of 40° or 50° on the Gareloch
to 80° or 90° on Loch Lomond, and at Callander being turned com-
pletely over to the south.

There are two subsidiary facts supporting this view of these re-
lations. First, the highly inclined position of the conglomerate and
red sandstone proves, as stated above, that they have been acted on
by a force from the north-west, not merely raising up the beds, but
pushing them in a south-east direction,—that is, such a force as the

NICOL—-SOUTHERN GRAMPIANS. 199

reversal of the beds on the north-west supposes. Second, the mica-
slate also shows that it has undergone an action conformable to this
supposition. The enormous twisting and contortion of the mica-
slate has long been considered as one of its most characteristic
features; but it has been seldom observed that there is within these
beds a similar twisting and contortion of the minuter lamine or folia.
Not only are the beds, as such, bent and curved, but within these
beds a second set of contortions—convolutions, asit were, of another
order—have taken place. Now any force acting from below would
evidently merely bend or curve the strata, and thus pull out or
lengthen their mass, and could not thus convolute or fold up the beds
on themselves. Such folds or convolutions imply a force acting on
the beds laterally, not vertically ; and not raising them up, but forcing
the ends or sides together*. Such a force, however, is exactly the
one required to fold the mica-slate over on itself and on the clay-
slate, and to raise up the red sandstone as seen on the south-east.
Were it necessary to assign an agent for this compression, I should
point, partly, to the great outbursts of granite in the central region
to the north-west, and, as even more influential, to the great com-
pression which the strata must have undergone when taken down
into those interior regions of the earth’s crust where the chief labo-
ratories of metamorphic action are situated f.

16. Central Gneiss and Quartzite—The next formation we have
to notice is the great central formation of gneiss. In this I include
most of the quartzite on its margin, as, although distinct in mineral
character, these two rocks in this region do not appear to me suffi-
ciently separate in other respects to be regarded as two independent
geological formations. This view was stated by me in the note to
my Geological Map of Scotland, and this central gneiss, with its asso-
ciated quartzite and limestone, referred to a newer formation, “not
older than the Lower Silurian period”’?. At the Leeds Meeting of
the British Association in 1858, I also brought forward sections
proving that “in the central region of Scotland, from Aberdeenshire
to Argyllshire, the great formation of gneiss, with limestone and
quartz-rock, overlies the mica-slate, and does not dip under it as
usually represented. In particular, the gneiss of the Black Mount
and Breadalbane Highlands appears to form a wide synclinal trough
resting on both sides on mica-slate, and thus to be an overlying and
younger formation”’§. Although these views differed widely from

* This was long ago proved by Sir James Hall’s simple experiment—all the
more demonstrative from its simplicity.

+ A similar view was proposed in reference to the section at the S.E. extre-
mity of the Grampians in my paper in Quart. Journ. Geol. Soe. vol. xi. p. 547.
Subsequently (Paper at Leeds Meeting of Brit. Assoc., Proceedings for 1858,
p. 96, and Note on Geol. Map of Scotland) I was inclined to regard the clay-slate
as normally the lowest bed ; but the difficulties in the way of this supposition, and
further examination of the localities have caused me to revert to my former view.

t Note on Geol. Map of Scotland, pp. 2 and 4.

§ See Report of the Twenty-eighth Meeting of the British Association, held at
Leeds, 1858, Transactions of the Sections, p. 96; also Report of the Twenty-
ninth Meeting, held at Aberdeen, 1859, Transactions of the Sections, p. 119.

200 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

those then entertained by the highest authorities in Scottish geology,
I have as yet seen no reason to recede from them, and shall now
bring forward some of the facts on which they are based. I must,
however, pass over several sections which, though I regard them as
favouring my views, I have not yet been able to examine thoroughly.

17. Tyndrum and Black Mount.—The relation of this gneiss to
the mica-slate is well seen between Tyndrum and the Black Mount.
Near Killin, at the head of Loch Tay, the strata, principally mica-
slate, mixed with hornblende-slate and limestone (the latter, as
already stated, probably the continuation of the beds seen on Loch
Earn), dip at low angles (30°-40°) to N. 25° W. The same dips,
though more irregular, continue along Glen Dochart to the hmestone
near Crianlarich, where there is probably a synclinal fold. From
this place to Tyndrum the general dip of the strata is to the S.E.
Round Tyndrum the rocks are true mica-slate, intersected near the
mines by a vein of quartzose hornstone or felspar-porphyry running
about E. 30° N. Following the road to the north-west, the mica-
slate is well seen, intermixed with a few beds of quartzite, and still
dipping at 30° or 40° to 8. 40° E. A little beyond the village there
is a dyke of greenstone running about E. 10° 8S. At the top of the
ridge the dip becomes first easterly, and then gradually folds over to
the north and north-west*. In passing down the glen to Urchay
Bridge the rock changes to gneiss, and is seen distinctly resting on
the mica-slate on both sides of the valley. No true quartzite inter-
mediate between the gneiss and the mica-slate, as represented by
Dr. Macculloch, was seen in this line of section. On the hills to
the south-west great protruding veins of quartz occur, which Mr.
Thost informed me range for great distances across the country.
Beyond the Urchay, the gneiss continues by Inveroran and King’s
House to the top of Glencoe, and, though often concealed in the low
moors, has its position well marked in the mountains on the west.
This section left no doubt on my mind that the gneiss forming the
great central region of the Black Mount overlies the mica-slate of
Tyndrum and Loch Tay, and thus, as stated, is a newer formationy.

18. Glen Shee and Braemar.—The same relation of these two
formations appears to me to exist in the valley of the Tay and its
tributaries ; but as I have not been able recently to re-examine some
of the sections there, I shall pass to the valley of Glen Shee (fig. 9),
where the connexion of the mica-slate of the southern Grampians
to the gneiss of the central mountains is well seen.

The greater part of this glen lies in the mica-slate, the beds
showing a general inclination to the north, though much concealed

* Thus, my observations at intervals to beyond Urchay Bridge gave 30° to
BH. 17° N.;.22° to B. 27°. N; 37° to. B..37° N.; 10° to H. 52° N.; 20° to B:
77° N.; and 30° to N. 27° W.

+ It is right, however, to mention that, in their “ Sketch of a New Geol. Map of
Scotland,” Sir R. I. Murchison and Mr. Geikie make it an older formation. It
will be seen that the tract of country coloured by them as 2’ 1+ in this place
nearly corresponds with the outline of the gneiss and quartzite as drawn by Dr.
Macculloch and myself. The continuous limestone-zone, laid down in their
map as overlying the gneiss, was not observed by me.

NICOL—-SOUTHERN GRAMPIANS.

in the lower valleys by detritus and occa-
sional convolutions. North of the Inn at
the Spittal I found a black carbonaceous
shale, in highly contorted beds, but dipping
60° to N.12° W. This rock closely resem-
bles the black shales of Oban and Easdale,
described by me in 1858*. It appears to
overlie the mica-slate, and thus confirms
the view that the clay-slates are the higher
and newer formationt. The part of the
section, however, to which I wish specially
to refer lies further up the glen, and on to
the Braemar Mountains. ‘The slates con-
tinue up Glen Beg to the fovt of the steep
pass over the Craig Well. Here a bed of
bluish-grey limestone, with numerous veins
of cale-spar, crops out, dipping at a high
angle to the north-west. This is overlain
by beds of gneiss passing up into quartzite,
which forms the higher portion of the
mountains. Near the summit-level of the
ridge veins of red felspar-porphyry are seen,
running from EK. 30° to 35° N. to W. 30° to
35° S$. Further down, near Ben Turk
Bridge, a grey micaceous limestone appears,
dipping at 70° to 8. 45° E. From this place
to Braemar the lower part of the valley con-
sists of gneiss, with veins of granite, but
overlain by beds of blue or grey compact
limestone, and this in turn by a white
quartzite or altered sandstone, often much

iron-tinged. The whole of the formations

seem to be conformable, and though occa-
sional high angles occur, yet taken generally
they dip at low angles to the south-east.
The gneiss appears merely the more meta-
morphic lower portion, and the quartzite
the less metamorphic and higher portion of
one great formation. Further north, beyond
the River Dee, as shown in the section, it
rests, still at very low angles of from 5° to
10° or 15°, on the granite of the Ben-Mac-

* Quart. Journ. Geol. Soc. vol. xv. (1858) p. 111.

t I described this rock at the Meeting of the Bri-
tish Association in Aberdeen in 1859 (see Report of
that Meeting, Transactions of the Sections, p. 118),
aud exhibited some fine specimens presented by Mrs.
Farquharson of Invercauld. It has since formed
the subject of a paper by Sir R. I. Murchison and
My. Geikie, Quart. Journ. Geol. Soc. vol. xvii. (1861)
pp. 226 & 232.

Z

Fig. 9.—Section from Glen Shee to Braemar Mountains.

Cairn Drochet.

Dee Valley.

Glen Clunie Hills.

Craig Well.

Glen Shee.

201

No
as
* RK *® Granite

Gneiss and Quartzite.

Mica-slate.

* Dykes of porphyry and trap,

b. Black carbonaceous shales.

a. Limestone.

202 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

dhui and Cairn Gorum Mountains. So little does it appear to have
been affected by these great igneous masses, that I have been al-
most disposed to believe that it may have been deposited on the
granite at a period subsequent to its consolidation. Be this as it
may, there is no doubt that this great formation of gneiss, lime-
stone, and quartzite rests on the mica-slate of the southern Gram-
plans, and is thus a newer formation. JI have also no doubt that it
is a continuous portion of the same great gneiss and quartzite forma-
tion which we have seen in the Breadalbane Highlands overlies the
mica-slate of Loch Tay and Glen Dochart.

19. Clay-slate of Loch Creran.—I shall not at present follow this
series of deposits north into Aberdeenshire and Banffshire, but turn
now to its relation to the slate-rocks of the south-west. These are
by no means so clearly seen as might be wished, probably in conse-
quence of the great eruptions of igneous rocks of diverse kinds and
of very different ages. In the south-west it abuts against the
granitic mass of Ben Cruachan. Near Dalmally and Loch Awe, this
mountain is skirted by schistose rocks, but these I regard as belonging
to the mica-slate formation more probably than to the gneiss. Beyond
this granite mountain-group, in the angle between Loch Creran and
Loch Leven, there is a great development of schistose beds, classed
partly as clay-slate, partly as mica-slate. A fine section of these
beds is exposed near Appin and along the shores of Loch Creran.
At Port Appin quartzite appears on the shore and extends north-
east along the Linnhe Loch. Generally it is composed of distinct
grains of quartz in a finer quartz basis, with a few crystals of iron-
pyrites or felspar, the latter well marked by weathering to an opaque,
white colour. In some places, however, the quartzite is a mere
mass of quartz-veins with no marks of stratification, and in many
cases may almost be regarded as a binary granite composed of abun-
dant quartz with a little felspar. Where most distinctly stratified it
dips 60° or 70° to W. 20°S8., and thus runs in a direction N. 20° W.
Proceeding east towards Loch Creran, mica-slate, often talcose, begins,
and forms the great mass of the country with very little diversity of
character. It first dips E. 35° to 40° 8., but, about two miles east
from Appin, forms a synclinal, beyond which the dip is very predo-
minantly W. 30° N. at angles ranging from 45° to 60°. The beds
are strongly undulated, and in many places show a transverse cleavage
orgrain. This peculiar character is beautifully seen on the weathered
surface of the rock near Creigan Ferry, where it approaches in mineral

aracter to gneiss. The two sets of planes dip nearly in opposite
directions,—the one at 55° towards N. 52° W., the other 438° towards
S. 52° E.; and in another place, the first at 56° towards N. 64° W.,
the second at 20° towards 8. 64° E, The first is probably the true
dip, as it is the more continuous, and also as it is parallel to the
change in the mineral character of the beds. Great veins of quartz
also run along these divisions or bedding. In either case the mica-
slate in this locality is unconformable to the quartzite, as clearly
shown by the direction of the beds. This is—

NICOL—-SOUTHERN GRAMPIANS, 203

In the Quartzite .... N. 20° W.
In the Mica-slate .. N. 30° E.
Difference ...... 50°

The position of the mica-slate has probably been determined by the
eruption of the granite of Ben Malugage, one of the northern outliers
of the Ben Cruachan Mountains. Round this granite a zone of gneiss
is laid down; but I had not an opportunity of examining this wild
region so as to speak confidently of its position.

The most remarkable feature in the rocks of this region is the
double foliation or structure which they exhibit. Nowhere have I
seen this peculiarity more strongly marked in the crystalline strata.
In some specimens, layers of a more quartzy nature alternate with
others that are more micaceous. In the quartzose layers only one
set of lines is seen, which may be regarded as the true bedding. In
the more micaceous layers, which on the whole are parallel to the
former, there is a second set of lines oblique to the first, and pro-
duced by the alternation of folia of mica and quartz. Both sets of
lines are of the same nature, produced by the alternation of different
mineral substances, and the chief distinction is that the first is more
continuous than the second, which is cut off by the quartz-layers
even where very thin. In this respect they resemble the bedding
and false bedding in ordinary strata. ‘These lines differ essentially
from cleavage, either in a rock or simple mineral, inasmuch as
their number and position are definite, whereas in cleavage (mark-
ing only a minimum of coherence in a certain direction) the mass
separates along parallel planes indefinite (or rather infinite) in num-
ber and position. This peculiar double structure is not confined
to the mica-slate of this locality, but is well seen also in the
similar beds near Loch Leven on the north, and Loch Craignish on
the south. It must form an element of much importance in all
speculations on the origin and history of the rock. The two struc-
tures so closely correspond, that we can scarcely doubt that the cause
producing the foliation of the rock on the great scale has also pro-
duced this cross foliation on the small scale. If the one be an effect
of crystallization; or of mechanical action, subsequent to the deposi-
tion of the beds, so must also be the other. It is also of conse-
quence as proving that the foliation of the mica-slate may not in
all cases coincide with the bedding, but be more or less oblique to it.
So much is this the case, that occasionally the inner foliation is highly
convoluted or twisted, whilst the outer planes of stratification remain
more nearly even or plain. From not observing this fact, many in-
accurate determinations of dip and direction have been given.

20. Loch Leven and Glencoe.—North of Loch Creran lie the valleys
of Loch Leven and Glencoe, so well known for their wild and magni-
ficent scenery, and so interesting to the geologist from the variety of
their igneous rocks. To a superficial observer, merely walking along
the roads, the sections may seem simple enough; but on following
them out into the upper parts of the mountains, where the rocks
are more fully exposed, many anomalies appear. Therefore, though

204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

I have examined this neighbourhood repeatedly, returning to it
again and again in different years, many points in its structure still
appear very obscure. In the slate-quarries on the south shore of
Loch Leven, the principal division-planes dip at 65° to W. 28°S.,
and a corresponding dip is seen in some of the other rocks in the
vicinity. This plane, however, I am inclined to believe, is, in the
slates, that of the cleavage, whilst the true bedding, though very
obscure, dips nearly east. Further up the loch, limestone is quarried,
but the dip is very obscure; and beyond it, towards the foot of
Glencoe, mica-slate is seen very highly undulated, but probably
dipping 8.W. towards and below the clay-slate. The mountains
west of the slate-quarries consist of quartzite intermixed with gneiss,
mica-slate, and limestone, but I found the dips so variable that no
fair average could be deduced. ‘This is not wonderful when account
is taken of the enormous protrusions, in this region, of igneous rocks
—granites, porphyries, and greenstones, of almost endless diversity
in mineral character and age. On the north side of Loch Leven
the clay-slate dips to 8S. 40°-50° E., but again probably on the
cleavage. Taken as a whole, this region seems too highly disturbed
to throw much light on the relations of the formations. This is
specially true of the quartzites, of which some portions at least
appear rather a binary granite of quartz with a little red orthoclase,
than a stratified rock. It prevails especially in the higher parts of
the mountains, where the narrow ridges, much steeper and scarcely
broader than the roof of a house, covered with the small loose
angular fragments among which no vegetation takes root, shine in
the sun almost like drifted snow.

21. Fort William and Ben Nevis.—The vicinity of Fort William
and Ben Nevis also presents some interesting sections. The lowest
rock seen on the east side of the Great Glen is probably the gneiss
near Nevis Bridge, which dips at 60° to 8. 10°-15° E., and runs
apparently under the granite of the mountain. The shore of Loch
Eil, south from Fort William, consists of mica-slate alternating with
clay-slate and talc-slate, and dipping generally at 60° or 70° to
S. 50°-55° E. In a few places the beds dip N.W., probably near a
fault or anticlinal axis, running nearly in the direction of the loch.
These beds pass north towards Ben Nevis, where, at the foot of the
mountain, similar slates dip 65° towards 8. 57° E. below the granite,
but separated from it by veins of the black porphyry which forms
the centre prism of the mountain. This porphyry, as has long been
known, is the newer eruptive rock, not merely piercing the granite
in mass, but forming irregular branched veins through it* as in
fig. 10. Generally, however, the strata do not extend far north of
the Nevis River, the slope of the hill consisting of granite inter-
mixed with numerous veins of red and black porphyry. The south

* Nicol’s Geology of Scotland, p. 164. Here also I described the singular
brecciated character of this porphyry as shown on the weathered surface. So
marked is this character, that one is almost induced to speculate on the possibility
of this rock being a huge fragment of some old stratified deposit caught up in,
and metamorphosed by, the granite.

NICOL—-SOUTHERN GRAMPIANS. 205

side of the glen consists of gneiss dipping 50° or 70° to 8. 40°-50° E.
Further up, the red granite, still full of veins of porphyry, crosses
the stream, and is well exposed at a small fall in the river. Still
higher the valley contracts, and gneiss forms the lower portion on
both sides; the beds much contorted, but dipping on the whole about
70° to 8, 42° E.

Fig. 10.—Porphyry Vein in Granite, Ben Nevis.
(Length about 30 feet.)

The lower portion of Glen Nevis thus consists essentially of gneiss,
dipping, more regularly than might have been expected in the
vicinity of such a mass of granite, to the 8.E. The mountains on
that (the south-east) side of the glen appear generally to be capped
by quartzite, which ought thus to overlie the gneiss. A great part
of this region, however, is now a mere desolate deer-forest, without
house or path, so that even in the finest seasons—and these too
rarely occur for the geologist—it is difficult of examination. In one
of the ravines on the south side of the Glen the following section
was observed (fig. 11).

Fig. 11.—Section of the South side of Glen Nevis.
N. s.

a. Quartzite. c. Red Granite e. Red Granite.
6. Gneiss. d. Mica-slate and Gneiss.

The bottom of the valley is red granite—a branch of that in Ben
Nevis. Itis covered by a fine-grained gneiss or hornstone, probably
altered by the igneous rock, which dips at 60° to S. 27° E., and above
passes into chloritous mica-slates, some dark, others light grey, and
also dipping at 65° to 8. 27° E. These slates are in turn covered
by a bed of red granite, perhaps from 100 to 150 yards wide, which
runs along the face of the southern hills, and in another ravine is
traversed by a vein of the dark Ben Nevis porphyry. The granite

206 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

is again succeeded by fine-grained, grey gneiss much contorted, but
dipping south-east, probably at a high angle. Still higher, beds of
quartzite appear, dipping at 10° to 8. 47° E., and thus, though the
immediate junction is not seen, apparently unconformable to the
gneiss. In others of the surrounding hills the quartzite, readily
recognized by its white colour, also appeared to rest unconformably
on the grey gneiss, but I was prevented from determining this point
by further examination.

About ten miles from Fort William, Glen Nevis is crossed by a
great ridge of rock, through which the river forces its way in a series
of narrow gorges and rugged cascades. ‘This ridge must have been
cut through by the river in some very different condition of the
country, as the valley beyond it les at a much lower level than its
summit, and opens out to the upper part of Glen Treig, by what
would be its natural drainage. Above this ridge a large branch of
the river enters from the south, forming a fine waterfall over an
overhanging cliff. In this place there is another interesting section,
represented generally in fig. 12, though from the incessant rain and
mist I was again prevented following out all its details.

Fig. 12.—Section of the upper part of Glen Nevis.

Mica-slate.

On the north-west is the granite dome of Ben Nevis, pierced by
the porphyry prism that forms the summit of the mountain. To this
succeeds a ridge of mica-slate, dipping at 70° to N. 47° W., and
thus apparently below Ben Nevis. Both in mineral character and
dip these beds correspond with the mica-slate seen in Glen Spean,
above the opening of Glen Roy. The valley forms an anticlinal, as
the strata on the other side dip about 45° to the south, and in the
higher part of the mountains appear to be again covered by the
quartzite.

22. Glen Spean.—In Glen Spean, on the north side of Ben Nevis,
a similar series of rocks is seen, but with some diversity in the
details. In the lower part of this glen the mica-slate dips generally
to 8. 50° E., and contains one or more beds of lhmestone, which are
quarried in some places, and is also intersected by veins of red
felspar-porphyry and granite. Near the mouth of Glen Roy the
dip changes, and the mica-slate further up dips 55° or 60° to N.
50°-55° W. These beds appear to correspond to the mica-slate
seen in the upper part of Glen Nevis. Some of the lofty mountains,
however, on the south, towards Loch Treig, consist of gneiss, which |

NICOL—-SOUTHERN GRAMPIANS, 207

_ am inclined to regard as, in this locality, a lower formation than the
mica-slate, and thus not connected with that in the central region.

The whole of this western region, however, is so much disturbed
by igneous intrusive rocks, and the wild nature of the country, with
the uncertainty of the climate, renders continuous geological inves-
tigation so difficult, that few certain conclusions can be drawn from
the sections as to the relations of the stratified masses. Still, on the
whole, I adhere to the view stated by me in 1858, that the quartzite
and gneiss of the Black Mount and Breadalbane Highlands form a
wide synclinal trough resting on both sides on mica-slate, and thus is
an overlying and younger formation. On the other hand, the gneiss
near Ben Nevis, and probably also that towards Loch Treig, appears to
me an older formation. So also the great gneiss-formation on the
west side of the Great Glen. This singular depression is evidently
the line of a great fault, so that the connexion of the strata on its
two sides is very uncertain. On the upper Loch Eil beyond Corpach -
the gneiss dips to the west, but this is clearly connected with the
granite which forms the hills along the west side of the Lochy.

The mica-slate of Loch Creran, with some similar strata seen in
other parts of the western Highlands, is probably also a peculiar
formation, distinct both from the ordinary mica-slate and also from
the clay-slate. In regard to age, I conjecture—for with so few certain
facts little more is possible—that it is younger than the mica-slate,
and older than the clay-slate.

The clay-slate, limestone, and quartzites of Appin and Balahulish
are, we have seen, unconformable to the mica-slate, and probably an
overlying formation. I still conjoin them with the slates of Easdale
and Islay, though the black carbonaceous beds so common at Easdale
and Oban are not seen at Balahulish, and the deposits also differ in
other respects. Asin 1858, I am still inclined to regard these rocks
as the newest deposits in this region. I then stated that these
slates were the equivalents of the Lower Silurian (Skiddaw Slates)*,
and Sir Roderick I. Murchison has since expressed his concurrence
in this view. These slates and limestones thin out north of Loch
Leven, and do not seem to be represented near Ben Nevis or further
north. The partial beds of limestone quarried in Glen Spean belong
to the mica-slate, and thus to an older group.

23. Geological connexion of the Grampians with other parts of the
Highlands.—Before concluding this paper, I may be allowed to say a
few words on the connexion of these beds with the strata in other
parts of Scotland. In such comparisons we are deprived of one
great means of identification of distant formations by the entire want
of organic remains. Except some obscure indications noticed by me
in a former communication, no traces of organic beings have ever
been mentioned from these beds. We are thus thrown entirely on
the mineral character of the rocks and their geological relations for
any conclusions we may form in reference to these points. There is no
doubt that ultimately all Geology of the primary rocks must depend on
these characters as the basis of its classifications ; but as there is reason

* Quart. Journ. Geol. Soc. vol. xv. (1858) pp. 112, 116.

208 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

to believe that rocks with nearly identical mineral characters may
occur in more than one period, and as the geological connexion of
the strata is often obscure, many difficulties have still to be en-
countered in such investigations.

There seems little doubt that the gneiss of Ben Nevis and the
Great Glen forms a continuous formation with the great mass of this
rock represented, in Dr. Macculloch’s Geological Map and my own,
as running from Inverness-shire through Ross and Sutherland to the
northern extremity of Scotland. In a former paper I have shown
that there is no reason for separating this gneiss from that of the
north-west coast of the mainland or of the Long Island. The chief
distinctions arise merely from the greater predominance of intrusive
igneous rocks, granites and syenites, in the latter, and recur in the
eastern gneiss wherever these igneous masses appear. The mica-slates
of the south have also their representatives in these north-western
regions, where some of the mica-slates, ike the thin, even-bedded
varieties on the Kyle of Tongue, contain garnets. Others, like those
of Ben Hope and Strath Oykell, have more resemblance to the talcose
varieties on Loch Creran. As the mica-slates in the south are a distinct
formation from the gneiss, it 1s probable that this may also be true
of those in the north, where their relations have been less studied*.

The overlying red sandstones and conglomerates of the west
coast. (‘‘ Cambrian” of Murchison) have no representative, so far as
yet ascertained, in the South-west, unless some portions of the red
sandstones in Cantyre belong to the same formation. The quartzites
and limestones that rest on them are Lower Silurian, according to
Mr. Salter’s determination of the fossils found in them by Mr. Peach
and others. As I have ascribed the same age to the slates of Kasdale
and Oban, it would follow that the connected quartzites in the
south-west are, to a certain extent, of the same age with those in
the north-west. This view of the identity of these quartzites,
embodied in Dr. Macculloch’s Geological Map and my own, has also
been adopted in the recent map of Murchison and Geikie. As both
formations are the uppermost in the series, there is, of course, no
improbability in this view; and as this Lower Silurian Period was
evidently of very long duration, and in other regions contains a great
diversity of deposits, the marked difference in some of the phenomena
cannot be held as invalidating it. The most remarkable of these
diversities are, first, the entire absence in the south of the great
underlying red sandstone and conglomerate group of the north. But,
as I pointed out in 1856, this red sandstone is even in the north a
very limited formation, not extending far to the east, where the
quartzite in many places appears resting immediately on the gneiss,

* It is necessary to mention this diversity, as Sir R. I. Murchison appears to
have overlooked the statements to this effect in my former papers, and conse-
quently represents me as maintaining the identity of the gneiss of the west coast
with certain mica- or chlorite-slates. They are identical only so far as both
belong to the great series of metamorphic formations inferior to the red
sandstone and quartzite; but, both in my papers and map, they are represented
as distinct formations, each with its own peculiar features, and, it may be, of
widely different age.

NICOL—-SOUTHERN GRAMPIANS, 209

without its interposition. The diversity in mineral character is of
less importance, though still very considerable. It may in some
measure have arisen from the far less extent of metamorphic action
to which the sandstones (quartzites) in the north have been exposed,
many portions of them being not more altered or more crystalline
than the ordinary sandstones of the Coal-formation. To this more
powerful metamorphic action we may also ascribe the more marked di-
versity of, and the entire absence of organic remains in, the southern
limestones and quartzites,—a want which prevents us from feeling
perfectly assured of the identity of these two formations. Whatever
view we may take of this question, it is, however, certain that the
quartzites and slates of the south-west cannot be of more recent
date than the lower portion of the Silurian. As the gneiss and
mica-slate are inferior and older formations, we are thus compelled
to carry them back into a still more ancient period in the history of
the earth. There is indeed nothing in the mere thickness of these
deposits to prevent us regarding them, as I was formerly inclined to
do, as the altered representatives of the lower portion of the Silurians
of the south, as the clay-slates were of the upper portion,—but the
break in the conformity of the formations, seen in many places, is
opposed to this view. The analogy of nature too in other regions,
where the lowest Primordial zone of life rests unconformably on
upturned, and evidently far more ancient, crystalline or metamorphic
strata, strengthens this view of the great antiquity of the gneiss and
mica-slate of the Scottish Highlands. This is especially true of
Scandinavia, in which we find a great gneiss-formation identical in
many respects with that of Scotland, and probably at one time even
in geographical connexion with it. The conviction has thus been
forced on me, that in the north of Scotland there is a much longer
series of formations—deposits dating from a far more early period
in the history of the earth—than might at first be imagined. Thus,
as our knowledge of the geological structure of Scotland becomes
more precise, we find that, asin every other field of geological science,
the duration of the earth, as measured by successive phenomena,
irresistibly expands, and we are more and more taught to feel how
impossible it 1s to comprise, in the narrow framework of our partial
and merely temporary systems, the majestic series of evolving events
that have filled up the untold ages which have left their traces in-
scribed even on the crust of this little globe of earth.

VOL, XIX.—PART I. jg

210

DONATIONS

TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From October 1st to December 31st, 1862.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

American Journal of Science and Arts. Second Series. Vol. xxxiv,
No. 101. September 1862. From Prof. B. Silliman, For.Mem. GS.

J. Lubbock.—Ancient Lake-habitations of Switzerland, 161.

G. J. Brush.—Tenth Supplement to Dana’s Mineralogy, 202.

——. Amblygonite from Hebron in Maine, 243.

J. D. Hague.—Phosphatic Guano-islands of the Pacific Ocean, 224.

Forchhammer.—Saltness of the Sea, 272.

Thallium, 275.

H. B. Geinitz’s ‘ Dyas,’ &c., noticed, 280. -

Crinoidea from the Upper Helderberg and Hamilton Groups of New
York, 282.

C. F. Rammelsberg.—North-American Meteorites, 297.

W.S. Church.—Ascent of the Volcano of Candarave, Peru, 300.

Anvers. Bulletin de la Société Paléontologique de Belgique. Vol. i.
pp. 81-128. . 1862.

Bosquet’s ‘ Entomostracés fossiles de la craie de Maéstricht,’ noticed,
95

—— ‘Cirripédes récemment découverts dans le duché du Limbourg,
Haarlem,’ noticed, 96.

——- ‘Entomostracés fossiles des terrains tertiaires de la France et de
la Belgique,’ noticed, 96.

De Koninck.—Brachiopodes carboniféres de Belgique, 97.

Nyst.—Crag des environs d’Anvers, 99.

A. Nytterhoeven.—Crane humain, extrait d’une tourbiére prés de
l’Escaut, dans la Flandre-Orientale, 111 (plate).

Assurance Magazine. Vol. x. Part5. No. 49. October 1862.

DONATIONS. 211.

Atheneum Journal. Nos. 1823-1835. ©

Notices of Meetings of Scientific Societies, &c.

Meeting of the British Association, 432, 463, 498, 532.

G. C. Wallich’s ‘ North-Atlantic Sea-bed,’ noticed, 455.

D. Wilson’s ‘ Pre-historic Man,’ noticed, 625. ne

R. Mallet’s ‘ Great Neapolitan Earthquake of 1857,’ &c., noticed, 835.

Berlin. Zeitschrift fiir die gesammten Naturwissenschaften. Band
xvii. 1861.

C. Bischof.—Die Inystallinische Schiefergruppe mit einigen Bezie-
hungen auf den Harz und die Alpen, 128,

Band xix. 1862.

C. Bischof.—Ueber die silurischen Bildungen des Unterharzes, 383.

G. Suckow.—Kzystallographisches und Chemisches, 242 (plate).

W. Trenkner.—Ueber das Vorkommen des Kohlenkalkes bei Grund
am Harz, 1 (plate),

Se
°.

Boston. American Academy of Arts and Sciences. Proceedings.
- Vol. v. pp. 241-884, 1862.

F. H. Storer and J. M. Ordway.—Frozen Well at Brandon, Vermont,
290,

British Association for the Advancement of Science, Report of the
Thirty-first Meeting of the, held at Manchester in September
1861. 1862,

R. Mallet.—Transit-velocity of Earthquake-waves, 201 (2 plates).

T. Dobson.—Explosions in British Coal-mines during the year 1859,
236 (plate).

W. eaten Athens to account for the Physical Condition and
the Fall of Meteorites upon our Planet, 15. 7

R. P. Greg.—On M. Haidinger’s Communication on the Origin and
Fall of Aérolites, 13.

H. H. Vivian.—Microscopic Observationson theStructure of Metals, 34.

W. Fairbairn.—Temperature of the Earth’s Crust as exhibited by
Thermometrical returns obtained during the sinking of the deep
mine at Dukinfield, 53 (plate). .

W. Hopkins.—The Theories of Glacier-motion, 61.

Daubeny.—Evolution of Ammonia from Voleanos, 77.

J. H. and G. Gladstone.—Aluminous Mineral from the Upper Chalk
near Brighton, 79.

Russell and Matthiessen.—Vesicular Structure in Copper, 92.

Smith.—Difficulties in the way of separating Gold from Quartz, 92.

J. Tennant.—Meteorie Iron from Mexico, 93. ;

Voelcker.—Composition of Crystallized Moroxite, from Jumillo, near
Alicante, 93. |

R. I. Murchison.—A ddress to the Geological Section, 95.

W. H. Baily.—Palzontological Remarks upon the Silurian Rocks of
Treland, 108,

T. W. Barrow.—Bone-caves of Craven, 108.

E. W. Binney.—Geological Features of the neighbourhood of Man-
chester, 109, _ .

J. Bonwick.—Extinct Volcanos of Australia, 109.

A. Brady.—Flint Instruments, &c., 110,

A. Bryson.—Aqueous Origin of Granite, 110.

pp DONATIONS.

British Association for the Advancement of Science. Report, 1861

(continued).

C. R. Gordon.—The Laws discoverable as to the Formation of Land
on the Globe, 112.

C. Gould.—Results of the Geological Survey of Tasmania, 112.

A. H. Green.—The Faults of a portion of the Lancashire Coal-field,
113.

Hagen.—Fossil Insects of England and Bavaria, 113.

R. Harkness.—Old Red Sandstone of South Perthshire, 114.

. The Sandstones and their associated Deposits of the Valley or
the Eden and the Cumberland Plain, 115.

D, Milne-Home.—Elongated ridges of Drift, common in the South of
Scotland, called “ Kaims,” 115.

E, Hull.—Isomeric Lines, and the relative distribution of the Cal-
careous and Sedimentary Strata of the Carboniferous Group of
Britain, 116.

J. B. Jukes.—Progress of the Geological Survey in Ireland, 117.

J. G, Marshall.—The relation of the Eskdale Granite at Bootle to
the Schistose Rocks, &c., 117,

G. H. Morton.—Pleistocene Deposits of the Districts around Liver-
pool, 120.

C. Moore.—Notes on two Ichthyosauri, 121.

W. Haidinger.—Present State of the Imperial Geological Institution
of Vienna, 121,

R. Owen.—Dinosaurian Reptile (Scelidosaurus Harrisoni) from the
Lower Lias of Charmouth, 121.

. Remains of a Plesiosaurian Reptile (Plestosaurus Australis) from
the Oolitic:Formation in the Middle Island of New Zealand, 122.

W. Patterson.—Certain markings in Sandstones, 123.

W. Pengelly.—New Bone-cave at Brixham, 123.

-——. Recent Encroachments of the Sea on the shores of Torbay, 124.

—. Relative Age of the Petherwin and Barnstaple Beds, 124.

——. Age of the Granites of Dartmoor, 127.

J. Phillips.—Post-glacial Gravels of the Valley of the Thames, 129.

T. A. Readwin.—Gold of North Wales, 129.

Richardson.—Details of the Carboniferous Limestone, as laid open
by the Railway-cutting and Tunnel near Almondsbury, north of
Bristol, 150.

J. W. Salter.—Nature of Sigillarie, and on the Bivalve Shells of the
Coal, 131.

R. H. Scott.—Granitic rocks of Donegal, 181.

H. Seeley.—The Elsworth rock, and the Clay above it, 152.

W.S. Symonds.--Some phenomena connected with the Drifts of the
Severn, Avon, Wye, and Usk, 183.

Vaughan.—Subterranean Movements, 134,

W. Whincopp.—The Red Crag Deposits of the County of Suffolk,
considered in relation to the finding of Celts, in France and
England, in the Drift of the Post-pliocene period, 154.

J. T. Wilkinson and J, Whitaker.—The Burnley Coal-field and its
fossil contents, 135.

A. B. Wynne.—Geology of Knockshigowna in Tipperary, Ireland, 135.

J. Yates.—The Excess of Water in the Region of the Earth about
New Zealand, 136.

C. T. Beke.—Volcanic Eruption on the Coast of Abyssinia, 186.

E. Belcher.—Glacial Movements noticed in the vicinity of Mount
St. Elias, on the North-west Coast of America, 186.

DONATIONS. 213

British Association for the Advancement of Science. Report, 1861
(continued).
R. Bridge.—Great Earthquake at Mendoza, 20th March, 1861, 187.
Shafiner.—The Spitzbergen Current, and Active and Extinct Glaciers
in South Greenland, 198.

Cacn. Annuaire de l'Institut des Provinces. SecondeSérie. Vol. iv.
1862.

G. Cotteau.—Progrés de la géologie en 1860, 72.

De Villeneuve.—Théorie de la formation géologique des divers sols,
134. :

——. Découverte de débris de l'industrie humaine dans des terrains
contenant des débris d’animaux vertébrés, 143. :

Barufli—Horizon géologique du diluvium dans lequel on a trouvé
des haches en pierre et autres objets fabriqués, 290.

Calcutta. Journal of the Asiatic Society of Bengal. New Series.
pee. 911, 112: 1862; Nos. 2°& 3.

W. T. Blanford.—Visit to Puppa doung, an extinct volcano in Upper
Burma, 216 (map).

W. Theobald.—On some stone implements from the Andamans, 323
(2 plates),

Cambridge (U.S.). Memoirs of the American Academy of Arts and
Sciences. New Series, Vol. viii. Part 1. 1861.

Canadian Journal. New Series. No. 41. September 1862.

Chemical Society. Journal. Vol. xv. Parts 10-12. October-
December 1862.

Colliery Guardian. Vol.iv. Nos. 92-104.

Notices of Meetings of Scientific Societies, &c.

Coal and Ironstone in the International Exhibition, 265, 306, 326, 365.

Government Inspection of Mines, 266, 295, 315.

Meeting of the British Association, 270.

Coal in Australia and New Zealand, 275, 334, 354, 453, 473.

G. C. Greenwell.—Timbering, Tubbing, and Walling of Shafts, 336,

Colonial Departments in the Exhibition, 347.

Lighting Mines with Gas, 355.

Literature of the Coal- and Iron-trades, 367.

Geologists’ Association at the International Exhibition, 376.

Discovery of the Cleveland Iron-stone, 376.

G. C. Greenwell.—Ventilation of Mines, 385.

W. W. Smyth.—Lectures on Mining, 386, 406, 425, 446, 466, 486, 503.

Glasgow School of Mines, 415.

Statistics of Coal in North America, 415.

‘Transactions of the North of England Institute of Mining Engineers,’
noticed, 417.

‘ Mineral Statistics for the year 1861,’ noticed, 425.

W. C. Truran’s ‘Tron-manufacture of Great Britain,’ noticed, 427.

R. Hunt.—Coal and its products, 433.

Working of Coal-mines, 445.

T. P. Teale.-—Atmosphere of the Earth during the Carboniferous
Period, 490.

Mineral-resources of the United States, 494,

Colliery-ventilation, 508,

B14 DONATIONS.

Critic. Vol. xxv. Nos. 629-631. October-December 1862.
Notices of Meetings of Scientific Societies, &c.
Meeting of the British Association, 154.
T. L. Phipson’s ‘ Phosphorescence in Minerals, &e.,’ noticed, 149.
G. C. Wallich’s ‘ North-Atlantic Sea-bed,’ noticed, 169.
J. Smith’s ‘ Newer Pliocene and Post-tertiary Geology,’ noticed, 169.
* - D: Wilson’s ‘ Pre-historic Man,’ noticed, 170.

Dublin, Journal of the Geological Society of. Vol. ix. Part 2.
1861-62.
A. Smith.—The Blowpipe, its History and Use, 223.
G. C. Mahon.—Duties of Mineral-agents, 236.
R. H. Scott.—Granitie Rocks of the South-west of Donegal, 285.
E. H. Blake.—Primary Rocks of Donegal, 294 (plate).
W. H. Baily.—Lower Silurian Fossils in Meath, Tipperary, and
Clare, 300 (plate).

. Transactions of the Royal Irish Academy. Vol. xxiv.
Part 2. 1862,

Edinburgh, Proceedings of the Royal Society of. Vol. iv. Session
1861-62.

J.D. Forbes.—Climate of Palestine in Ancient and Modern times, 511.

Tait.—Molecular arrangement in Crystals, 535.

D. Brewster.—Pressure-cavities in Topaz, Beryl, and Diamond, and
their bearing on Geological Theories, 548.

J. Duns.—Recent Landslip, 560.

J. H. Balfour.—Bark of Araucaria imbricata, with special reference
to Paleontology, 577.

A. Geikie.—Carboniferous volcanic rocks of the Basin of the Forth,
582.

A. Bryson.—Danger of hasty generalization in Geology, 604.

D. Brewster.— Vegetable formations in Calc-spar, 610.

W. Thomson.—Secular cooling of the Earth, 610.

, Transactions of the Royal Society of. Vol. xxii. Part 1.
1861-62.

D. Brewster.—Pressure-cavities in Topaz, Beryl, and Diamond, 39.
——. Formations in Calc-spar, 97 (plate).
W. Thomson.—Secular cooling of the Earth, 157 (plate).

Geologist. Vol. v. Nos. 58,59. October-December 1862.

Notices of Meetings of Scientific Societies, &e.

R. N. Rubidge. —Metamorphosis of Rocks in the Cape Town District,
South Africa, 366.

S. P. Woodward.—Barrettia, a new fossil shell from Jamaica, 372
(2 plates).

W. H. Bensted.—Geology of Maidstone, 378, 447.

Geological Notes in the ‘Great Exhibition, 382, 408.

S. J. Mackie. —Dragon-tree of the Kentish Rag, 401 (plate).

-——. Bos frontosus, 441 (plate).

H. Mitchell.—Restoration of Pteraspis, 404.

JT. Davidson.—Scottish Jurassic, Cretaceous, and Tertiary Brachzo-
poda, 443 (plate).

Meeting of he British Association, 416, 456.

Correspondence, 406, 450; Notes and Queries, 396, 425, 468.

Reviews, 397, 434, 472.

DONATIONS, 915

Heidelberg. Verhandlungen des naturhistorisch-medicinischen Ver-~
eins zu Heidelberg. Band ii. No.6. 1859-62,

Institution of Civil Engineers. Abstracts. 1862-63. Nos. 1-4, 6.
——,. Premiums. 1861-62.

Intellectual Observer. No. 9. October-December 1862.

Notices of Meetings of Scientific Societies, &c.

Glacial Origin of Lakes, 228.

Last Elevation of Scotland, 228.

Artesian Wells in the Desert of Algiers, 228.

Method of Determining the age of Fossil-groups, 275.

S. P. Woodward and A. Cochrane.—Fossil Human Skeleton from
Guadaloupe, 280.

H. Woodward.—Feathered Fossil from Solenhofen, 313 (plate).

Lausanne. Bulletin de la Société Vaudoise des Sciences Naturelles,
Woh, vi... No. 48.. 1861.

Vol. vi. No. 49. 1862,

Nicaty.—Roches et fossiles du petit Atlas, 220.
E. Renevier.—Dessins sur toile, 232.

. Quelques dépéts récents d’eau douce, 249.
Planchon.—Fossiles de Meximieux (Ain), 254,
J. Delaharpe.—Question glaciaire, 264.

Linnean Society. Journal of Proceedings. Vol. vi. No. 24, No»
vember 1862.

Lisbon. Memorias da Academia Real das Sciencias de Lisboa.
Classe de Sciencias Mathematicas, Physicas e Naturaes.. Nova
Serie. Tom. ii. Parte 1. 1857.

J. M. de O. Pimentel.—Memoria sobre a produccéo do sulphato de
soda no volcao da Ilha do Fogo no Archipelago de Cabo Verde.
C. Ribeiro.—Reconhecimento geologico e { ydralogisd dos terrenos

das visinhangas de Lisboa (plate).
J. de Aldama.—Informe sobre la mineria de la Provincia de Malaga

em 1848,

oe
.

Nova Baio: Bowie i. Parte 2. 1861.

C. Ribeiro.—Minas de Carvao de pedra de 8, Pedro da Cova, do
Cabo Mondego, &c. (plate).
Minas metallicas de Portugal (5 plates).

Liverpool, Proceedings of the Literary and Philosophical Society of.
No. 16. 31st Session, 1861-62.

J. Yates.—Excess of Water about New Zealand, 14.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xxiv. Nos. 161-163. October-December 1862.

J. B. Jukes.—River-valleys of the South of Ireland, 323.

S. Haughton.—Granites of Donegal, 323.

T. H. Huxley.—Stalk-eyed Crustacean from the pean oa 323.
——. Premolar Teeth of Diprotodon, 324.

oy
e

°16 DONATIONS.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series,
Vol. xxiv. Nos. 161-163. (continued).

J. Powrie.—Old Red Sandstone of Fifeshire, 324.

E. W. Binney.—Upper Coal-measures in Ayrshire, 324.

J. Nicol—Southern Grampians, 324.

S. H. Beckles.—Footprints from the Wealden, 325.

R. Thornton.—Geological Notes on Zanzibar, 325.

W. Carruthers.—Section at Junction-road, Leith, 325.

W. Denison.—Death of Fishes in the Sea during the Monsoon, 526.

A. C. Ramsay.—Excavation of the Valleys of the Alps, 377.

J. Thomson.—Crystallization and Liquefaction, 395.

J. H. Pratt.—Truth of the Fluid-theory of the Figure of the Earth,
409,

L. de Koninck.—Fossils from India, 491.

ki. Hodgson.—Deposit in the Iron-ore Mines near Ulverstone, 492.

F. Applegath.—Geology of a part of the Masulipatam District, 492.

J. G. Sawkins.—Association of Granite with Tertiary Strata, near
Kingston, Jamaica, 492.

London Review. Vol. v. Nos. 118-130.

Notices of Meetings of Scientific Societies, &c.

Meeting of the British Association, 291, 306, 318, 328, 352.
J. Challis’s ‘Creation in Plan and in Progress,’ noticed, 326.
Minerals at the Exhibition, 365.

T. L. Phipson’s ‘Phosphorescence,’ noticed, 504.

D. Wilson’s ‘ Pre-historic Man,’ noticed, 520.

Longman’s Notes on Books. Vol.u. No. 313. November 30, 1862,

J. E. Woods’s ‘Geological Observations in South Australia,’ noticed,
285,
H. Worms’s ‘ Earth and its Mechanism,’ noticed, 291.

Manchester Geological Society. Transactions. Vol. iii. Index. 1862.
: . Vol. iv. No.1. Session 1862-63.

Mechanics’ Magazine. New Series. Vol. vii. Nos. 197-209.
October 3rd to December 26th, 1862.

Notices of Meetings of Scientific Societies, &c.
Meeting of the British Association, 211, 223.
Glacier-phenomena, 230.

Explosions of Fire-damp, 343.

Salt-well in Ohio, 344.

W. King.—The bed of the Atlantic, 364.

Melbourne. Public Works, Roads, and Railways’ Circular. No. 8.
~ September 25, 1862.

Milan. Atti della Societ&a Geologica residente in Milano. Vol. i.
1859,

A.e G, B. Villa.—Sulla distribuzione oro-geografica dei molluschi
terrestri nella Lombardia, 84.

G. Omboni.—Intorno alla Carta geologica della Lombardia, 97.

E. Paglia.—Sugli strati del terreno sottoposto al letto attuale del Po,
109.

A. Stoppani,—Rivista geologica della Lombardia, 190 (plate),

DONATIONS, 217

Milan. Atti della Societa Geologica residente in Milano (continued),

A. Bossi.—Intorno alle Argile, agli altri minerali ed ai fossili di
Maggiora, 317. Ba!

A. Bertolio.—Di un nuovo minerale d’origine organica, Kramerite,
B24.

G. e F. Sandberger’s ‘ Petrefatti del sistema Renano nel Nassau,’
noticed, 352. :

L. Pareto’s ‘Terreni al piede delle Alpi,’ noticed, 338.

——, Atti della Societa Italiana di Scienze Naturali. Vol. ii,
Anno 1859-60. 1861.

G. Omboni.—Sul terreno erratico della Lombardia, 6 (plate).

A. Stoppani.—Resultati paleontologici e geologici dedotti dallo studio
dei petrefatti d’Esino, 65.

G. M. Cavalleri.—Sulla densita delle varie parti costituenti il globo
terrestre, 116.

A. Bertolio.—Di un grasso fossile di Rio-Janeiro, 140.

E. Sergent.—Sulla densita della materia nell’ interno del Globo, 169.

B. Gastaldi.—Su alcune Ossa di Mammiferi fossili del Premonte, 213

late).

ea cans Dolomia del Monte San Salvatore, 233.

G. de Mortillet.—Plus anciennes traces de homme dans les lacs et
les tourbiéres de Lombardie, 250.

G. Omboni.—Gita geologica nei dintorni del Lago d’Iseo, 302.

—. Il congresso dei Naturalisti Svizzeri in Lugano, 312.

E. Paglia.—Sulle colline di terreno erratico, 337 (plate).

G. A. Pirona.—Sulle antiche morene del Friuli, 348 (plate).

Vol. ii. Anno 1861. 1862.

B. Gastaldi.—Cenni su alcune armi di pietra e bronzo, 11.
G. de Mortillet.—Carte des anciens glaciers du versant Italien des

Alpes, 44 (plate).
A. Stoppani.—Sulle condizioni generali degli strati ad Avicula con-
torta, 86.

G. Omboni.—I ghiacciaj antichi e il terreno erratico di Lombardia,
232 (3 plates).

B. Gastaldi’s ‘Epoca glaciale miocenica,’ noticed, 313.

F. de Bosis.—I minerali utili delle Marche, 327.

—. la grotta degli Schiavi, 360 (plate).

A. Senoner.—Catalogo delle meteoriti esistenti nell’ i. r. gabinetto
mineralogico di Vienna, 444.

G. de Mortillet.—Note sur le crétacé et le nummulitique des environs
de Pistoja, 459 (plate).

Giunta consultiva per la formazione della carta geologica del regno
d'Italia, 468.

——. Memorie del Reale Istituto Lombardo di Scienze, Lettere, ed
Arti. Ser. 2. Vol. ii., fase. 6,7. 1861.

E. Lombardini.—Studj sull’ origine de’ terreni quadernarj di tra-

sporto, 449,
—. —. Ser. 2. Vol. ii., fasc. 15-20. 1862.
———s . ‘Ser, 2.-° Vol. ii., fasc. 1—4. -.1862.

G. Curioni—Intorno agli scisti bituminosi della valle di Setarolo, 12.

OQ. Ferrario.—Analisi chimica degli scisti bituminosi della valle di
Setarolo, 15,

918 DONATIONS.

Mining and Smelting Magazine. Vol. ii. Nos. 10-12. October-
December 1862.

Gruner and Lan.—Manufacture of Pig-iron in Scotland, 193.
G. Darlington.—Minera Mining Field, Denbighshire, 207, 269.
H. C, Salmon.—TIlustrated Notes on Prominent Mines, 211.
The Seton Mining District, 277, 333.

Abstracts and Reviews, 223, 284, 344.

Correspondence, 299, 359; Notes and Memoranda, 360.

Montreal.- Canadian Naturalist and Geologist. Vol. vii. Nos. 4, 5.
August, October 1862.

C. F. Naumann.—Origin of the Primitive Formations, 254.

J. W. Dawson.—Footprints of Lnmulus and the Protichnites of the
Potsdam Sandstone, 271.

M. C. White.—Microscopic Organisms in the Siliceous Nodules of
the Palzeozoic Rocks of New York, 281.

Proceedings of Scientific Societies, 320.

M. H. Perley.—Geology and physical characteristics of Newfound-
land, 321.

J. Hall.—Cattskill Group of New York, 377.

C. Robb.—Superficial deposits of Canada, 382.

E. Billings.—Remarks upon Prof. Hall’s ‘Contributions to Paleon-
tology,’ 389.

E. Jowett.—Age of the so-called Old Red Sandstone of New York,
395.

Munich. Sitzungsberichte der k. bayer. Akademie der Wissenschaften
zu Minchen. 1862. Part I. Hefte i, 11.

Paris. Annales des Mines. Gime Série. Vol. i. Liv. 3. 1862.

Bulletin de la Soc. Géol. de France. Deuxiéme Série. Tom.
Rimste oo toe 4.1 sa

A. F. Nogués.—Recherches sur le terrain jurassique des Corbiéres
(fin), 513.

Daubrée.—Formation contemporaine de pyrite cuivreuse 4 Bagnéres-
de-Bigorre, 529.

L. Zejszner.—Sur le Pachyrisma Beaumonti, 529 (plate).

H. Coquand.—Sur la convenance d’établir dans le groupe inférieur
de la formation crétacée un nouvel étage entre le néocomien pro-
prement dit et le néocomien supérieur, 531.

Ch. d’Alleizette.—Sur la craie et la mollasse du Jura bugeysien dans
les environs de Nantua, 544 (plate).

A. Damour.—Sur la Tcheffkinite de la cote de Coromandel, 550.

Ed. Hébert.—Sur lage du calcaire de Rilly, 552.

Delesse et Laugel.—Revue de géologie pour l’année 1860, 556.
Gosselet.—Sur quelques gisements fossiliféres du terrain dévonien de
VArdenne, 559.
L’abbé Pouech.—Sur la grotte ossifére de 1’Herm (Ariége), 564 (plate).
De Verneuil.—Sur l’inapplicabilité du nouveau terme Dyas au systéme

Permien, 599.

Talabardon.—Sur la prétendue découverte d’un gisement d’or a
Saint-Perreux (Morbihan), 615.

A. Dolfus.—Sur une nouvelle espéce de Trigonie de l’étage kimmé-
ridgien du Havre, 614 (plate).

Fh Ebaaaeee le terrain houiller des environs de Decize (Niévre),
615.

DONATIONS, 219

Paris. Bulletin de la Soc. Géol. de France (continued).

J.Marcou.—Remarques sur les expressions Pénéen, Permien, et Dyas,
621.
Albert Gaudry.—Note sur les débris d’oiseaux et de reptiles trouvés
a Pikermi, 620 (plate).
P. de Cessac. saiftaa aie géologique du département de la Creuse,
, 640.
Bourgeois.—Distribution des espéces dans les terrains crétacés de
Loir-et-Cher, 652.
J. Capellini. —Etudes stratigraphiques et paléontolopiques sur V’in-
fra-lias dans les montagnes du golfe de la Spezia, 675.
P. de Rouville.—Sur lage essentiellement triasique des dépéts gyp-
seux secondaires du midi de la France, 683.
Guillebot de Nerville.—Sur le ‘ bone- bed’ de la Bourgogne, 687.
J. B. Noulet.—Sur le calcaire miocéne lacustre de Narbonne, 705.
J, Schlumberger.—Dent de Ceratodus runcinatus, Plien., 707 (plate).
A. Laugel.—La faune de Saint-Prest prés Chartres, 709.
Ch. Lory.—Sur le gisement des gypses des environs de Vizille (Isére),
720.

——. Liste des Membres de la Soc. Géol. de France. Juillet
1859.

Comptes Rendus hebdomadaires des Séances de l’Académie
des Sciences. Tom. lv. Nos. 1-11.

Supplément aux Comptes Rendus des ee de Académie
des Sciences. Vol. i. 1861.

Bronn.—Distribution des corps organisés fossiles, &c., 377.

Mémoires de Académie des Sciences de l'Institut Impérial
de France. Vol. xxxii. 1861. With atlas.

. Mémoires présentés par divers savants 4 l’Académie des
Sciences. -Vol. xvi. 1862.

C. Ste.-Claire Deville et F. Leblanc.—Composition chimique des
’ gaz volcaniques, 225.

Vol. xvii. 1862.

Daubrée. — Etudes et expériences synthétiques sur le “métamor-
phisme, 1.

Parthenon. -Vol.i. Nos. 23-35. 1862.

Notices of Meetings of Scientific Societies, &c.

The Gold-mines of Egypt, 714.

G. C. Wallich’s ‘North-Atlantic Sea-bed,” noticed, 720.

Meeting of the British Association, 722, 746, 779.

Gold from Victoria, 812.

D. Wilson’s ‘ Pre-historic Man,’ noticed, 838.

Tracks and Trails, 850.

Fossil Mammalia in South Africa, 880.

J. von Gumpach’s ‘True Pagans and Dimensions of the Earth,’
noticed, 943.

The Archeopterys, 971.

T. L. Phipson’s ‘ Phosphorescence,’ noticed, 972.

—see
e

220 DONATIONS.

Parthenon. Vol.i. Nos. 23-35. 1862 (continued).

H. Werms’s ‘The Earth and its Mechanism,’ noticed, 973.

The progress of Transatlantic Science, 1004.

J. Smith’s ‘Researches in Newer Pliocene and Post-tertiary Geology,
noticed, 1006.

D. T. Ansted and R. G. Latham’s ‘Channel Islands,’ noticed, 1025.

J. E. Woods’s ‘Geological Observations in South Australia,’ noticed,
1101.

Aids and Impediments in Science, 1103.

Philadelphia. Proceedings of the American Philosophical Society.
Vol. vii. No. 64. May—December 1860.

F, Peale.—Indian Arrow-heads, flint Knives, &c., 411.

Vol. viii. Nos. 65,66. January—December 1861.
W. M. Gabb.—Synopsis of the Mollusca of the Cretaceous forma-

tion, 57.
F. Peale.—Stone Implements of the Indians of North America, 265,
Dubois and Eckfeldt.—Natural dissemination of Gold, 278.
Lesley.—Limestone-bed on the Brandywine River, 281.

Transactions of the American Philosophical Society. New
Series. Vol. xu. Part 2. 1862.

Photographic Journal. Nos. 126-128. October-December 1862.

Plymouth.. Annual Report and Transactions of the Plymouth In-
stitution, and Devon and Cornwall Natural History Society.
1861-62.

W. Pengelly.—Red Sandstones and Conglomerates of Devonshire,
Part 1., 15 (plate).
Puy, Annales de la Société d’Agriculture du. Vol. xxii. 1859.
Aymard.—Roches a bassins dans la Haute-Loire, 341.

Quarterly Journal of Microscopical Science. New Series. No. 8.
October 1862.

Royal Asiatic Society of Great Britain and Ireland. Vol. xx. Part 1.
1862. :

Royal Geographical Society. Proceedings. Vol. vi. No. 5. 1862.

Royal Horticultural Society. Proceedings. Vol. 11. Nos. 10, 11.
October and November 1862.

Royal Society. Proceedings. Vol. xii. No. 52,

St. Petersburg. Bulletin de l’Acad. Imp. des Sciences de St. Péters-
bourg. Vol. iv. Nos. 3-6.
H. Struve.—Zusammenstellung einiger Untersuchungen von Stein-

kohlen aus dem Kistengebiet des nordlichen Theils stillen Oceans,
337,

DONATIONS, OUT

St. Petersburg. Mémoires de l’Acad. Imp. des Sciences de St.
Pétersbourg. Vol.iv. Nos. 1-9. 1861.

N. v. Kokscharow.—Ueber den russischen Monazit und Aischynit
(4 plates).

——, Verhandlungen der k. Gesellschaft fiir die gesammte Mine-
ralogie zu. Jahrgang 1862.

E. Steinfeld.—Tabellen fiir die Berechnung der Ableitungszahlen, 1.

——. Ein Melanit-Krystall aus Pitkaranta, 57.

P. Pusyrewsky.—Russische Apatite, 59.

Tjutschew.—Analyse eines Sumpferzes, 72. ‘

B. de Marny.—Geognostisch-geographische Skizze des Bergreviers
Kataw im Ural, 75 (plate).

Mineralogische Neuigkeiten vom Ural, 82.

A. Pusyrewsky.—Neue Fundorte der Morpholite in Finnland, 83.

W. Beck.—Analyse einiger russischen Mineralien, 87.

N. vy. Lawrow.—Notiz iiber den Salzsee Elton, 95 (plate).

T. v. Ssawtschenkow.—Der Paligorskit, 102.

E. Sochting.—Zur Paragenesis des Glimmers, 105.

Ueber Einschliisse in den Krystallen russischer Mineralien,

126.

H. J. Holmberg.—Ueber die Fortschritte der Mineralogie in Finn-
land, 144.

B. de Marny.—Geognostische Beschreibung des Hiittenbezirks von
Ufaleisk, 157 (plate).

——. Geognostische Beschreibung des Reviers des Sserginschen
Hiittenbezirks, 193 (plate).

C. Pander.—Die Steinkohlen an beiden Abhingen des Ural, 230 (plate).

VY. Meller.—Ueber den geognostischen Horizont des Sandsteins von
Artinsk, 263 (plate).

Society of Arts. Journal. Vol. x. Nos. 515-521.

Notices of Meetings of Scientific Societies, &c.
W. P. Jervis—The Mineral Fuel of Italy, 685.
Meeting of the British Association, 687, 699.
Australian Exploration, 726.

on MOle me eNGSs O22—pe 7 :

B. H. Paul.—Utilization of Peat, 32.

R. Hunt.—Mines, Minerals, and Miners of the United Kingdom, 84,
J. Tennant.—List of British Minerals, 111.

J. Y, Watson.—British Mining, 118.

ee, . List of Members, 1862.

Stockholm. Kongliga Svenska Vetenskaps-Akademiens Handlingar.
New Series. Vol. ui. Part 2. 1860.

——. Kongliga Svenska Vetenskaps-Akademien, Ledamdter.
May 1862.

--—. Ofversigt af Kongl. Vetens—Akad. Forhandlingar. 18 Ar-
gangen, 1861. :

202 DONATIONS.

Strasbourg. Mémoires de la Société des Sciences Naturelles de
Strasbourg. Vol. v. Parts 2 and 3. 1862.

J. Keechlin-Schlumberger et W. P. Schimper.— Mémoire sur le
__ terrain de transition des Vosges (30 plates).
Fée.—De l’Espéce.

Stuttgart. Wiirttembergische naturwissenschaftliche Jahreshefte.
Jahbrgang xvii. Hefte 1-3. 1862.

Von Kurr.—Ueber den Kalk zum Betelkauen, 30.

Binder.—Ueber die geologischen Verhaltnisse des Tunnels zwischen
Heilbronn und Weinsberg, 45.

Eser.—Ueber ein Schadelstick eines Keupersauriers, 47.

Fraas.— Ueber den Lehm, 59.

Die tertiaren Hirsche von Steinheim, 113 (2 plates).

Bruckmann.—Stadtische Kohlenstadelquelle zu Ulm und die Ent-
fernung des Uebelstandes, 135.

Fraas.— Der Hohlenstein und der Héhlenbir, 156.

Giimbel.—Die Streitberger Schwammlager und ihre Foraminiferen-
Einschlisse, 192 (2 plates).

Sydney Morning Herald. Vol. xlvi. No. 7579. Sept. 20, 1862.

W. B. Clarke’s ‘Reports on the discovery of Gold in Australia,’
noticed, 4.

Vienna. Jahrbuch der k.-k. geologischen Reichsanstalt. Band xii.
No. 3. 1862.

T. v. Zollikofer.—Die geologischen Verhaltnisse des siidéstlichen
Theiles von Unter-Steiermark, 311 (plate).

J. Jokély.—Die Quader- und Planer-Ablagerungen des Bunzlauer
Kreises in Bohmen, 367.

. Pflanzenreste aus dem Basalttuffe yon Alt-Warnsdorf in

Nord-Bohmen, 379. lit

Allgemeine Uebersicht iiber die Gliederung und die Lage-
rungsverhaltnisse des Rothliegenden im westlichen Theile des
Jiciner Kreises in Bohmen, 381.

——. Das Riesengebirge in Bohmen, 396 (plate).

K. v. Hauer.—Arbeiten in dem chemischen Laboratorium, 421.

Verhandlungen der k.-k. geol. Reichsanstalt, 233.

II. PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 3rd Series. Vol. x.
"Nos. 58-60. October-December 1862.

W. Denison.—Death of Fishes in the Sea during the Monsoon, 320,
G. C. Wallich’s ‘ North-Atlantic Sea-bed,’ noticed, 380. pee

Bronn und Leonhard’s Neues Jahrbuch fiir Min., Geog., Geol., und
_ Petrefaktenkunde. Jahrgang 1862, Heft 5. 1862.

A. Streng.—Ueber den Gabbro und den sogenannten Schillerfels des
Harzes: Abtheil. 1., 518 (plate). 7

DONATIONS. 223

Bronn und Leonhard’s Neues Jahrbuch fiir Min., Geog., Geol. und
Petrefaktenkunde. Jahrgang 1862, Heft 5 (continued).
T. Kjerulf und T. Dahll—Ueber das Vorkommen der Eisen-Erze
bei Arendal, Nis, und Kragero, 557 (plate).
E. Kluge.—Ueber die Periodizitiit vulcanischer Ausbriiche, 582.
Letters ; Notices of Books, Minerals, Geology, Fossils, &c,

Edinburgh New Philosophical Journal. New Series. Vol. xvi.
No. 2. October 1862. |
G. S. Silliman.—Origin of Aérolites, 227.
A. Bryson.—Danger of Hasty Generalization in Geology, 260.
J. M‘Bain.—So-called raised Sea-beach near Leith, 269.
G. P. Scrope’s ‘ Volcanos,’ noticed, 286.
J. B. Jukes’s ‘Student’s Manual of Geology,’ noticed, 290,
Geological Survey of India, 317.
Coal raised in India, 318.

Institut, ’. 17° Section. Nos. 1499-1505.
——. 2°Section. No. 322. |
Paleontographica. Herausgegeben von H. y. Meyer. Band x.

Lief. 4. 1862.

R, Ludwig.—Actinozoen und Bryozoen aus dem Carbon-Kalkstein
im Gouvernement Perm, 187 (11 plates).

Ill. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.

Abstracts from the Meteorological Observations taken in the years
1860-61, at the Royal Engineer Office, New Westminster, British
Columbia. Edited by Col. Sir H. James. 1862. From the Se-
eretary of State for War.

Anon. On Unity of System. PartI. 1862.

Beke, C. T. A few words with Bishop Colenso on the subject of
_ the Exodus of the Israelites and the position of Mount Sinai.
1862.

Binney, E. W. Additional Observations on the Permian Beds of
South Lancashire.

——. On Sigillaria and its roots. 1861.

Brody, G. O. St. The Weston-super-Mare Catalogue of British
“Shells, &c, 1859.

Catalogue. A Descriptive Catalogue of the Rock-specimens in the
Museum of Practical Geology, with explanatory notices of their

_ nature and mode of occurrence in place. By A. C. Ramsay, H.

_ W. Bristow, A. Geikie, and H. Bauerman. 3rd edition. From
the Director-General of the Geological Survey of Great Britain,

224 DONATIONS,

Catalogue. Catalogue of the extensive stock of old, rare and curious
books of T.O. Weigel. Part i1.: History, Geography and Travels,
Numismatics. 1862. From Messrs. Williams and Norgate.

——. Official Descriptive Catalogue of the Products of the King-
dom of Italy exhibited at the International Exhibition. 1862.
From W. P. Jervis, Esq., F.GS.

Repertorium der Literatur tiber die Mineralogie, Geo-
logie, Paliontologie, Berg- und Hiittenkunde Russlands bis zum
Schlusse des xviii. Jahrhunderts. Bearbeitet von Ernst von Berg.
1862. From the Mineralogical Institute of St. Petersburg.

Crawford, J. W. Geological Report upon the Wairarapa and East
Coast Country, Province of Wellington, New Zealand. 1862,
From the Colonial Government.

Dawson, J. W. Alpine and Arctic Plants. 1862.

—-—. On the Footprints of Zimulus as compared with the Prot-
ichnites of the Potsdam Sandstone, 1862.

--—, On the Pre-carboniferous Flora of New Brunswick, Maine,
and Eastern Canada. 1861.

Delesse. Recherches sur l’eau dans l’intérieur de la terre. 1861.

—— et A. Laugel. Revue de Géologie pour Vannée 1860, 1861.
From M. A. Laugel, F.GAS.

Favre, A. Cartes géologiques des parties de la Savoie, du Piémont,
et de la Suisse voisines du Mont-Blane. 1862.

Freke, H. An Appeal to Physiologists and the Press. 1862.

Gaudin, 0.-T., et C. Strozzi. Contributions 4 la Flore fossile
Italienne. Sixiéme Mémoire. 1862.

Geinitz, H. B. Ueber Thierfahrten und Crustaceen-Reste in der
unteren Dyas, oder dem unteren Rothliegenden, der Gegend von
Hohenelbe, 1862.

Gibb, G. D. A Visit to Reculver, in Kent. 1862.

Grabau, E, Cenni sulla Proprieta e la Legislazione delle Miniere.
1860. From L. Horner, Esq., F.GS.

——., Le Miniere dell’ Elba e l’Industria del Ferro in Italia. 1860.
From L. Horner, Esq., F.GS.

——-—, Sulla Proprieti e Legislazione delle Miniere Osservazioni in
replica ai Signori Senatori Pogei e Marzucchi e Prof, Savi e Me-
neghini. 1861, From L. Horner, Esq., FANS.

DONATIONS. 225

Hall, J., and J. D. Whitney. Report on the Geological Survey of
the State of Wisconsin. Vol.i. 1862. From the Legislature of
the State of Wisconsin.

Helmersen, G. v. Die Alexandersiule zu St. Petersburg. 1862.
——. Noch ein Wort tiber die Thulaer Steinkohle. 1861.

Hitchcock, E., E. Hitchcock, jun., A. D. Hager, and C. H. Hitchcock.
Report on the Geology of Vermont; descriptive, theoretical, eco-
nomical, and scenographical. 2 vols. 1861. From the Legis-
lature of the State of Vermont.

Hull, E. The Coal-fields of Great Britain; their history, structure,
and resources; with notices of the coal-fields of other parts of the
world. 2nd edition. 1861.

Jervis, W. P. The Mineral Resources of Central Italy, including
a description of the Mines and Marble-quarries. 1862.

Jukes, J. B. Address to the Geological Section of the British Asso-
ciation at Cambridge, Oct. 2,1862. 1862.

Korizmics, L. A few particulars regarding some of the chief Pro-
ductions of Hungary. 1862. From the Commissioners for Hungary
at the International Exhibition of 1862.

Laugel, A. La faune de Saint-Prest, prés Chartres (Eure-et-Loire).
1862.

M‘Gill University. Statement of the Board of Royal Institution
Governors of the M‘Gill University, Montreal, in relation to the
financial condition of the University, 1862. 1862. From Dr.
J. W. Dawson, F.GS.

Malaise, C. Note sur quelques ossements humains fossiles et sur
quelques silex taillés. 1861.

Marcou, J. Letter to M. Joachim Barrande on the Taconic Rocks
of Vermont and Canada. 1862.

The Taconie and Lower Silurian Rocks of Vermont and
Canada. 1862.

Marsh, O. C. Catalogue of Mineral Localities in New Brunswick,
Nova Scotia, and Newfoundland. 1862.

Omboni, G. Cenni sulla Carta geologica della Lombardia. 1861.
——. I ghiacciaj antichi e il terreno erratico di Lombardia. 1861.

——. [Review of Cantoni.] Nuovi principj di Fisiologia vegetale.
1861.

[Review of Gastaldi.] Epoca glaciale miocenica. 1861.
VOL, XIX.—PART I. Q

226 DONATIONS.

Owen, D. D., R. Peter, 8S. S. Lyon, J. Lesley, L. Lesquereux, and
E.T.Cox. Fourth Report on the Geological Survey in Kentucky,
made during the years 1858 and 1859. 1861. From the Legis-
lature of the State of Kentucky.

Prestwich, J. On the Loess of the Valleys of the South of England
and of the Somme and the Seine. (Abstract.) 1862.

Readwin, T. A. On the Gold-bearing Strata of Merionethshire.
1862.

Report. Annual Report of the Board of Regents of the Smith-
sonian Institution, showing the operations, expenditures, and con-
dition of the Institution for the year 1860. 1861. From the
Smithsonian Institution.

Annual Report on the Improvement of the Harbours of
Lakes Michigan, St. Clair, Erie, Ontario, and Champlain. By J. D.
Graham. 1860. From Col. J. D. Graham.

——. Results of Meteorological Observations made under the
direction of the United States Patent Office and the Smithsonian
Institution from the year 1854 to 1859 inclusive. Vol. i. 1861.
From the Smithsonian Institution.

Thirteenth Annual Report of the Regents of the University
of the State of New York, on the Condition of the State Cabinet
of Natural History, and the Historical and Antiquarian Collec-
tions annexed thereto. 1860. From T. A. Cheney, Esq.

——. Report upon the Colorado River of the West, explored in
1857 and 1858 by J. C. Ives. 1861. From the Senate of the
United States.

——. Report upon the Physics and Hydraulics of the Mississippi
River ; upon the protection of the alluvial region against overflow ;
and upon the deepening of the mouths. Prepared by A. A.
Humphreys and H. L. Abbot. 1861. From the Secretary for
War of the United States.

Rose, G. Ueber eine neve kreisférmige Verwachsung des Rutils.
1862.

Rutimeyer, L. Eocine Saugethiere aus dem Gebiet des schwei-
zerischen Jura. 1862.

Sedgwick, A. A Lecture on the Strata near Cambridge and the
Fens of the Bedford Level. 1862.

Smith, J. Researches in Newer Pliocene and Post-tertiary Geology.
1862.

Smithsonian Miscellaneous Collections. Vols.i.toiv. 1862. From
the Smithsonian Institution.

DONATIONS. 227

Szabé, J. Egy continentdlis emelkedés és Siilyedésrol] Eurépa dél-
keleti részén, 1862.

Wallich, G. C. The North-Atlantic Sea-bed: comprising a Diary
of the Voyage on board H.M.S. Bulldog, in 1860; and Observa-
tions on the Presence of Animal Life, and the Formation and
Nature of Organic Deposits, at great depths in the ocean. Parti.
1862.

Woods, J. E. Geological Observations in South Australia; prin-
cipally in the district S.E. of Adelaide. 1862. From Messrs.
Longman & Co.

Worms, H. The Earth and its Mechanism: being an account of
the various proofs of the rotation of the earth. 1862. From
Messrs. Longman & Co.

“gat. niy Bonae anaes io pees bis fone aul ad. me
asites. Garmult: type)’ ad : goaatebirie aly phi. ‘wae
To aGrenatis shroiisan ae ‘ SARE END PSE CHT Ged

pet Ans id pcr A,
, (. ie ee
ye Ee Ret oF

LYNUOU 2 eK 1 ei

TVA IO2 PAA DOLORY FHF

A oY Ol ha Amel Sa RATS, vn, srl ta

Sauk dh YET ORR fet eRe oe) ee ee
: att with Wer Bakes on ae rh:

‘2 Stihl ae ab pea het) £05 | TPRAY NM

37 Baur Ones STS rea tarts Sih
a, GOL Ata Ot EF Ge sen ae ae ee

oe Bite garish ead y

beta rade’ vit. sift rte 4 andl pent aids 30 hesist de, ats
vi moitenrt s bailes ad taomls y yaa pigeon ot zi sth
pod asvowed vat SH Yo earrot srs lia Yo sata Kodera
asttg? toseg tontt erlang e08 therrsey ott

Rd. alle aaa) 20.08 ae ayay adepes P

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

JANUARY 21, 18638.

Edward Brooke, Jun., Esq., Oakley House, Edjerton, Huddersfield ;
John Brunton, Esq., C.E., Engineer of the Scinde Railway; Alfred
Hewlett, Esq., Mining Engineer, Haigh, Wigan; Thomas Wardle,
Esq., Leek Brook, Leek, Staffordshire ; and George Worms, Esq.,
17 Park Crescent, Portland Place, were elected Fellows.

The following communications were read :—

1. On the Upper Srturntan PassaGe-Beps at Lintey, Saxop.
By Grorex E. Roserts, Esq., and Joun Ranpat, Esq.

[Communicated by the President. |

A zone of thin-bedded, often conglomeratic, sandstones, forming the
passage-bed between two great formations, is frequently found to
include within its series of deposits one or more bands of shell- or
bone-breccia. Perhaps the most important of these zones is the
one which lies between the mudstones of the Upper Silurian series
and the lowest Old Red Cornstone, the most northerly extension of
which forms the subject of this paper. This, from the number and
variety of its organic contents, may almost be called a formation by
itself. The continuance of Silurian forms of life is, however, too
strongly marked to permit any division of it from that great series
of deposits. On the other hand, its uppermost layers are allied, by
physical constitution and fossil contents, so nearly with the overlying
VOL. XIX.—PART I. R

230 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

Old Red, that, although this new exposure at Linley adds to our
knowledge of the series, it does not, in our opinion, enable us to
draw a more definite boundary-line between the Silurian deposits
and the Old Red Sandstone.

In commenting generally upon these passage-beds, we cannot
choose a more fitting preface than the following passage from
‘ Siluria ’ :—

‘“‘ During the accumulation of nearly all the Silurian deposits of
Britain, which were characterized by a certain fauna, the bottom of
the sea was, to a wide extent, occupied by dark- and grey-coloured
sediments. At the close of that period a great change occurred, over
large areas, in the nature and colour of the submarine detritus. In
and around the Silurian region, for example, the dark-grey mud was
succeeded by red silt and sand, the colour being chiefly caused by the
diffusion of iron-oxides in the waters ” (2nd edit. p. 270).

The characters of this more or less iron-tinged zone have had the
careful attention of many geologists, more especially as regards the
fossil contents of the lowest and, hitherto, best-known layers, in
which the bone-bed of the Upper Ludlow shales is so noticeable a
feature.

The important exposures of the uppermost division, in which
the rocks described in this paper occur, at and near Ludlow, and
at Ledbury, have revealed enough to show it to be by far the more
important series of the two, whether we consider it with regard to
its greater thickness, variety of mineral composition—indicating an
era of more frequent physical changes,—or for containing the remains
of more highly organized animals. At Ledbury, Cephalaspid Fishes
seem to have been the chief inhabitants of the water; while at
Ludlow, remains of Pterygotus and other Crustaceans occur plenti-
fully in and near this “upper bone-bed.” At Linley, remains of
those Fishes known as Plectrodus, Onchus, Ctenacanthus, &c., charac-
terize the zone, and no Crustacean remains have yet occurred.

The position of the beds at Linley is shown by sections along
the course of Linley Brook, a stream which falls into the Severn at
Apley, four miles north of Bridgnorth. Opposite Linley Hall the
Upper Ludlow rock is exposed in the sides of a little gorge formed
by the stream, the dip being 8.8.W. Here it is traversed by two
sets of joints, one N.E. to 8.W., the other W.S.W. to E.N.E. Lower
down the brook, near the “ Holly Bush,” a more extended section
may be obtained. ‘The dip is here 15° to the S.E.

The series exposed in this sinuous gorge ranges from the true
Aymestry rock, which forms, in places, the bed of the brook, to the
Upper Coal-measures, capped with northern drift and scratched
boulders. The coal-seams are but two in number, and of poor
quality. .One or more beds of jointed freshwater limestone lie
among the clays. The exact junction of these coal-measures with
the Old Red we failed to discover, though at a point high up the
north bank, near the “ Holly Bush,” the line of fault marked down
by the Geological Survey, as dividing the two systems, is traceable
in the steeper inclination of the Coal-measure clays.

1863.] ROBERTS AND RANDALL—PASSAGE-BEDS AT LINLEY. 231

Fig. 1.—Sketch of the Upper Ludlow Rocks and the Passage-beds at
Innley Brook.

- ao, git

The numbers refer to those attached to the beds in fig. 2.

In connecting the higher beds of this series with the true Old
Red Sandstone, it is worth remarking that the lowest Cornstone
of the Old Red at present known occurs interstratified with the
plant-bearing grits (d in the Linley series) at Trimpley, two miles
north-west of Kidderminster. If, therefore, these bands of inorganic
breccia have any value as dividers of the series, we have here the
proved position of one, relatively to underlying deposits, hitherto most
difficult of arrangement.

On the fossil contents of the series three observations may be
made :—firstly, the abundance of Lingule, occurring in two condi-
tions—as well-preserved shells upon the surfaces of the shales, and
as layers of triturated shells; secondly, the importance of the Fish-
fauna of the upper bone-bed, which has yielded the largest spines,
yet discovered, of the forms figured by Sir P. G. Egerton from the
corresponding bed at the Paper Mill, Ludlow*, together with some
fragments of solid bone (ribs ?) two inches in length; and, thirdly,
the entire absence, so far as we have been able to make out, of Crus-
facean remains. Even the lower “ bone-bed,” which has furnished,
from its outcrop at Ludlow and all other exposures, such numbers of
Astacoderma, does not appear to contain a trace of these bodies ; for,
though subjected to careful scrutiny by Dr. Harley and ourselves, it

* Quart. Journ. Geol. Soc. vol. xiii. Pl, X. p. 289.
R2

232 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 21,

yielded little else beside the dermal studs of Thelodus, fragments of
Lingule, and a large percentage of ferruginous inorganic grains.

A section of about 80 feet, through the Old Red to the lowest
Silurian bed exposed, gives us the following series of deposits * :—

Fig. 2.— Vertical Section of the Beds exposed at Linley Brook.

a. Northern drift with boulders. ft. in.
b. Upper coal-measures, containing a band

of limestone.
e. Red clays, unfossiliferous . . 6 0
d. Light-coloured grits, with Plant-re-

mains—Juncites ?, Lycopodites, Ke. . 20 O
e. Hard micaceous grits, somewhat flaggy,

and charged with Fish-remains. (THE

Upper BoNnzE-BED.) 4
Jf. Flagstones bearing current- -markings 1
g- Micaceous sandy grits with Lingule . O1
h. Greenish, irregularly laminated rock

1

Oo moo ©

with conglomerate . :

i. Hard calcareous grit with ‘thickly dis-
seminated greenish aa and nese
broken Lingule . . 1

k. Laminated light-grey micaceous and
sandy shales. . . «at peroneal

1. Grey micaceous grit. . 0

m. Micaceous sandy clays, coloured "by
peroxide ofiron . . 6

n. Yellowish sandstones (Downton series)
with Beyrichie and Lingule, and in-
cluding two or more ferruginous bands
containing large quantities of the der-
mal studs of Thelodus, fragments of
LTingule,and minute crystals of quartz.
(THE LOWER or LUDLOW BONE-BED.)
Clusters of Modiolopsis Senn satis
occur at the base of thisrock . . 8 0

o. Hard calcareous shales with Fish-re-
mains, Lingule, &e. . 6 0

p. Flaggy beds of i impure limestones, with
Serpulites longissimus. oo: ue Upper
Ludlow.) . et CS

q. Hard, impure limestone. (Aymestry

: series, )

eo Ao oe

* In these sections, Lingula cornea ranges up to
the summit of the bed ce.

1863. ]. - ROBERTS—CRUSTACEAN TRACKS, 233

2. On some Crustacean Tracks from the Otp Rep Sannsrone near
Luptow. By Gzores E. Roserts, Esq.

[Communicated by the President.]

I LATELY received some sandstone-slabs from the Lower Old Red
Cornstones, obtained by Mr. Alfred Marston, of Ludlow, which ex-
hibit more clearly than is usual tracks and trails of Crustacea. They
were obtained from a somewhat noted quarry at Bouldon, a village
seven miles north of Ludlow. Mr. Marston has furnished me with
the following details of the Bouldon section :—
Fig. 1.— Vertical Section of the Beds exposed at Bouldon Quarry,
near Ludlow.

LRA

90 A Ee
. ra J

«470% ofa
"Oho oF,

-
-_
=)

,
#0?

a. Rough coarse conglomerate; a few Fish-remains
(Pteraspis, Cephalaspis)

6. Fine-grained sandstone with Pteraspides .

ce. Rubbly beds

d. Fine-grained sandstones with Preraspides

e. Micaceous sandstones

J. Thin-bedded fine sandstone with : TRACKS OF Crvs-
TACEANS . nity Sereda agree

g. Fine-grained shales . hg Se ee ea a

h. Lowest Cornstone; remains of Fish and Crus-
taceans ; Pteraspis and Cephalaspis abundant,
Pterygotus scarce.

HHO

oo

A zone of fine-grained and thin-bedded deposits, indicating qui-
escent conditions and shallow water, is thus seen dividing two con-
glomeratic beds, the lower of which I am inclined to regard as the
rock wanting above the plant-bearing bed at Linley, but which is
seen to accompany that deposit at Trimpley, in Worcestershire, and
elsewhere.

The Crustacean tracks occur as casts abundantly upon the under
surface of the thin sandstone-layer, f, of the above section.

Of the three or more varieties, the most important in size and
distinctness (fig. 2) is a shghtly curved trail about 14 inch in width,
formed by two series of oval or, rather, flask-shaped prints, 1 of an
inch long, each bearing a number of transverse wrinkles parallel
to the direction of the trail. The prints taper inwardly, and have
a slight upward curve at the same end. Their distance from each
other varies, as also does the height of the cast, but these inequali-
ties may be regarded as results of peculiarities of the condition of
the surface which received them.

The indentations made by another Crustacean (?) upon the slabs
(see fig. 3) are longer and more sharply ended, and show a nearer

234 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 21,

Figs. 2-4.—Crustacean Tracks from the Old Red Sandstone of
Bouldon. (Natural size.)

——<—— J
=

‘ibe
Pal
dn io ah.
sad ies hale

et) Z
e Voie OP
vee

an A
a

vk wat then
Nh

Quart. Journ. Geol. Soc. Vol. XIX. Pl. X.

el SKETCH-MAP or a PART or LOCHABER.

eee Parallel Roads.

WB 0141 Debtas |

G28 Glacier-moraines and Moraine-deltas.
Log Syenite of Glen Spear.

Direction of the glacial strie.

— => Outlets of the old Lakes.

*
BRITISH MILES
oO 1 2 3 4 oj 6 7 é ] 1
y ae i n === I 1
R oy F
\
: \ }
\
een

Lochan
a —4

“WM

1863. | JAMIESON——PARALLEL ROADS OF GLEN ROY. 235

resemblance to those described and figured by Mr. Salter, from the
Lingula-flags, as the trail of Hymenocaris vermicauda ?*

The track of an apparently smaller Crustacean (?) (fig. 4) consists
of ovate prints, stamped in a more regular serial order. In none of
these is there any evidence of tail-markings, in the existence of any
central rib or ridge, like that which appears in the trail of the Cli-
mactichnites of the Potsdam Sandstone, or in that of recent Limulv.
Long, slender impressions also appear upon the sandstone-surfaces,
having coriaceous interiors, and being probably the casts of Sertu-
larian zoophytes.

The Bouldon quarry is certainly the richest exposure of these
track-bearing sandstones, and should therefore be carefully worked ;
for in the absence or, at least, paucity of organic evidence as to the
Crustacean fauna of the Old Red Sandstone, we are forced to content
ourselves with the examination of secondary and indirect witnesses.

3. On the ParatteL Roaps of Grsn Roy, and their PLace in the
History of the Guactat Pertop. By Tuomas F. Jamieson, Esq.,
F.G.8., Fordyce Lecturer on Agriculture in the University of
Aberdeen.

[PLATE X.]

ConrTENTs.

1. General appearance of the ‘ Roads.’
2. The different theories.
a. General review of the theories.
6. The marine theory.
ce. Agassiz’s theory.
3. Place of the Parallel Roads in the history of the Glacial period.
a. Relation to the period of chief submergence—Hskers and Osar.
b. Relation to the 40-feet Raised Beach of Argyleshire and to the
‘Raised Beaches’ of Norway.
. Height and horizontality of the Parallel Roads.
. Difficulty as to a dam of ice.
. Central Asia during the Glacial period. Its glacial lakes and inland
seas.
. Intensity of glacial action in the West Highlands
. Recapitulation.

CON Hoe

§ 1. General appearance of the Roads.

In the Highlands of Scotland there is a district called Lochaber,
embracing a range of bare hilly country in the south-west of Inver-
ness-shire. In this district lies the little valley of Glen Roy, famous
for certain curious features in its scenery.

High up on both sides of this glen three lines appear, one above
another, and some distance apart. They are perfectly level, strictly
parallel, and run along the bare mountain-sides as neatly as if drawn
with a ruler and pen. They sweep round the shoulders of the hills,
wind into their side-recesses, and encircle all the upper part of the
valley, everywhere preserving the same rigid parallelism and the
same undeviating horizontality. A sight so curious and unusual

* Quart. Journ. Geol. Soc. vol. x. p. 208. .

Quart. Journ. Geol. Soe. Vol. XIX. Pl. X.

SKETCH-MAP or A PART oF LOCHABER.

—_——Farallel Roads
WB 012 Dettas K
GE Glacier-moraines and Moraine-deltas.
Syenite of Glen Spean . 2
ween Direction of the glacial stria.
—> Outlets of the old Lakes.

BRITISH MILES

W West, imp.

a

236 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

strongly arrests the attention of the spectator. These lines look all
too mathematically regular for the work of nature, and yet they
seem on too grand a scale to have been traced by mere mortal hands.
One might fancy he had wandered into fairy-land, and caught the
genius loci practising geometry on the hill-sides. No wonder then
that the imaginative Highlanders ascribed them to the ancient heroes
of their race, and saw in these lines the hunting-roads of Fingal and
his companions, that they had made for chasing the deer. In their
native language they call them ‘ Casan,’ or ‘ the footpaths’; for, on
climbing up to them, they are each found to consist of a green ledge,
or narrow terrace, jutting out from the face of the hill; so that they
actually serve as convenient tracks for walking on.

Pennant, I believe, was the first to draw attention to these sin-
gular appearances, and, before they were well known, various con-
jectures were started to account for them; but an attentive ex-
amination of the district by Dr. Macculloch* and Sir Thomas Lauder-
Dick*+ at once showed that these ‘‘ Parallel Roads”’ must have been
formed by water that had once filled the glen to the height of the
uppermost line, and had subsided step by step till it- reached the
lowermost, leaving its water-mark in these shelves as the traces of
its ancient shore. But then arose the difficulty, how to account for
the water. As you walk down the glen and draw near its lower
extremity the two upper lines vanish, and no sign of them again
appears; in like manner the lowest line, which now becomes more
faint, after being traced into the larger valley called Glen Spean, of
which Glen Roy is a branch, also vanishes before reaching the mouth
of the Spean valley, leaving no trace of any barrier to account for
the retention of a lake to the necessary height; and so deep and
wide is the gap that would have to be filled up, that any attempt to
account for the gradual wearing down, or wasting away, of any mass
of earth or rock that could have occupied the void strikes one at
once as utterly hopeless. Another little valley, called Glen Gluoy, in
the immediate neighbourhood, and branching off from the Great
Valley of the Caledonian Canal, is also marked in a somewhat simi-
lar though less striking manner. Here only one decided line is
seen, although there are likewise some faint traces of a lower one.
This Glen Gluoy line is a little higher than any of those in Glen Roy,
and towards the mouth of the long narrow valley, which resembles
a profound trench cut among the hills, it seems to reach the very
brow of the ridge, and then ceases; but the flanks of the hills on
either side show not a vestige of any protruding mass that could
have filled up the deep gulf between. There is no narrow rocky
gorge, no mound of earth, nothing, in short, but the smooth slopes
of grass and heather, with the sheep nibbling quietly on the hill-
side. Had any barrier of earth or rock existed here in times so
recent as these shelves would appear to indicate, it is incredible it
could have been so completely cut away as to leave no trace what-
ever of its former existence. The question then occurs, If these
are the marks of old lakes, what could have retained them ?

* Geol. Trans. ser. 1, vol. iv. p. 314. ft Edin. Roy. Soc. Trans. vol. ix.

1863. | JAMIESON——-PARALLEL ROADS OF GLEN ROY. 237

§ 2. The different Theories.

a. General review of the theories—It was scarcely possible in the
first examination of such a subject to escape errors, and some of
those Dr. Macculloch fell into greatly enhanced the difficulty at-
tending it, so that although both an able geologist and an acute
reasoner, and believing a lake to be the cause, yet he found himself
quite baffled to account for either its existence or disappearance.
Sir Thomas Lauder-Dick, himself a very excellent observer, and
aided by the local knowledge of Mr. Macdonell of Insch, had made
a nearer approach to the true conditions of the problem, but was
unable to offer any more probable explanation as to how the lakes
were retained or emptied, than was to be got by supposing some
great displacements or dislocations of the adjoining district. But
there is not a jot of evidence that any such have taken place since
the period of these lakes. No fault has anywhere been detected in
the lines ; and they are so horizontal and undisturbed that, even apart
from many other objections, these circumstances alone are incom-
patible with the notion of great convulsions having rent the sur-
rounding district.

Another theory is that which appeals to diluvial agency. A great
inundation, it has been said, flowing over the country from the west,
might have left these marks as it gradually subsided. This was Sir
George Mackenzie’s idea* ; and very recently Mr. H.D. Rogers*, Pro-
fessor of Natural History in the University of Glasgow, has suggested
something similar, only that he thinks it was during the rise of this
great inundation that the thing was done. A great heave of the
Atlantic’s bed might have sent a volume of water across Scotland,
and as it poured through the glens it might, it is said, have grooved
these lines on their sides. In support of this, Professor Rogers states
that the lines consist of deep grooves in the earthy covering of the
hills, and are most distinctly and deeply indented in the sides that
look down the valley, disappearing altogether in the recesses or
deeper corries that scollop the flanks of the mountains ; and, further,
that certain traces of what is called false bedding, or oblique lami-
nation, in the gravel-beds indicate a current flowing in the required
direction.

So far, however, from the lines being faintest on the N.E. faces
of the hills, or being absent in the side recesses, it so happens that
these are often the places where they are most beautifully seen.
This is remarkably the case on the hill of Bohuntine, in the lower
part of Glen Roy, where all the three lines are strongly marked on
the N.E. face of the hill, the two upper vanishing entirely round
the other side, which looks down the valley. And in the side re-
cesses of Glen Turrit the shelves are as clearly seen as anywhere else.
Indeed, Professor Rogers seems to have overlooked the fact that, in
regard to the two lower lines, there is no outlet for this current at
the head of Glen Roy; for, owing to the rise of the ground, they

* Edin. Phil. Journ. January 1848.
¥ Lecture before the Royal Institution, March 22, 1861.

238 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 21,

meet the bottom of the valley long before reaching its extremity.
Glen Roy itself is thus a long recess, forming a complete cul-de-sac
in respect of these two lines, so that no current rushing up the glen
from its mouth to its head, it seems to me, could account for them
even on the Professor’s own theory. Moreover the lines are not,
properly speaking, grooves. They are not due to matter cut out of
the hill, but to matter deposited. They consist, wherever I have
been on them, of buttresses, or small narrow terraces, formed by the
check which the waters of the old lake gave to the descent of the
débris washed into it by the rains and streams, as Macculloch long
ago pointed out. They are, if I might use the expression, the con-
tinuous deltas formed by the rains and other atmospheric agents.

The false bedding in Glen Roy, of which Professor Rogers speaks,
I did not see, nor in the sections of gravelly matter that I examined
did I find anything to indicate a current up the glen. During the
time of the highest line, however, the surface-water of the lake
would have had a determination towards the col beside Lochan
Spey. But, apart from all these objections to the facts brought for-
ward in favour of this diluvial theory, there is abundant evidence
that no such transitory action can account for the phenomenon in
the numerous large deltas that exist, chiefly along the lowest line,
where the side streams had poured their débris into the old lake.
These furnish sufficient evidence, as has been often pointed out, that
the water occupied the glen for a very considerable time. Other
facts will be adduced in the course of this paper, all pointing
to the same conclusion. And if this be not enough, another strong
objection rests in the horizontality of the lines, which is so complete
that none of the engineers who have been employed to test it have
been able to allege any deviation from a dead water-level. Sir
Thomas Lauder-Dick, Mr. Milne-Home, and Mr. Chambers all had
surveyors with them, all of whom came to the same conclusion. Mr.
D. Stevenson made a section along the middle road for a distance of
nearly 32 miles, from Glen Turrit downwards, and throughout
that extent the road was found to be perfectly horizontal. He and
his assistants were there for a week, at Mr. Milne-Home’s request,
on purpose to test this very matter.

That any flood, or diluvial body of water set in motion by an
earthquake, and rushing up a rugged inclined plane, could have
traced lines so neat and so level as these, is to me quite incredible.

Another mode of explanation presented itself in supposing the sea
to have been the agent. Sink the country to the level of the highest
line, and we should have a sea-margin corresponding to it ; and then
as the land gradually emerged, successive coast-lines might be traced
corresponding to all those we find. On the mountains of Wales sea-
shells of existing species had actually been obtained, imbedded in
sandy layers, at a height greater than would be necessary even for
the most elevated of these parallel roads, and had been allowed by
many geologists as evidence of a recent submergence to the required
extent ; so that there was nothing objectionable in the idea so far,
while the mode in which it accounted for the absence of all barriers

1863. | JAMIESON—-PARALLEL ROADS OF GLEN ROY. 239

told strongly in its favour. This was the theory of Mr. Darwin *,
who urged it so forcibly, and handled so well the difficulties that
arose on every side when it was attempted to place barriers of earth
or rock in any of the required positions, that his explanation met
with general acceptance, and appears to be still the one most in
favour.

A Swiss visitor, however, came and offered quite a new suggestion.

This was Agassiz +, who, living in sight of the snow-clad Alps, and
awakened by the teaching of Venetz and Charpentier to a perception
of the former vast extension of their glaciers, had much enlarged
our acquaintance with the ice-world, and had come over to Britain
to see whether he could find any trace of glaciers in a country where
none now occur. These traces he met with in abundance, and
nowhere more clearly than in Lochaber, which he visited in com-
pany with Dr. Buckland in 1840. Perceiving that the lines occupy
certain glens where the hills are comparatively low, and that ranges
of higher mountains encircle them on the W. and 8. +, fronting the
opening of the valleys where the lines terminate, and that Ben
Nevis, the loftiest of them all (where the snow still lingers even in
the hottest summers), guards the entrance of the main valley, the
idea struck Agassiz that this curious phenomenon, that had puzzled
so many able heads, must be due to glacier-lakes, instances of
which were known to him in the Alps. Ice, in short, had been the
barrier that no one could find, and which, on the approach of a more
genial climate, had melted before the heat of the sun, and vanishing
left << not a wreck behind.”
- Here was an explanation no one had thought of. The visit of its
author, however, was too hurried to enable him to work it out.
He merely pointed to the evidence of a former glacier having pro-
truded from Glen Treig across the valley of the Spean as one
element in the solution of the problem, suggesting that the ravines
of Ben Nevis would probably account for the rest.

Admirably as this seemed to meet the difficulties of the case, yet
few were prepared to admit such a development of ice in this
country. Had the lines been in the Alps or the Himalaya, the ex-
planation might have been at once accepted ; but to suppose that
our little hills could have given birth to so large ice-streams seemed
to exceed all probability. Accordingly, though the parallel roads
have since been repeatedly examined by Messrs. Robert Chambers $
and Milne-Home||,and Professor Rogers, and although all three came
away differing with one another as to how they originated, yet they
agreed upon this point, that the theory of Agassiz was quite inad-
missible,—the two latter even declaring that no evidence whatever
existed of the supposed glaciers, at all events not in the places
where their presence had to be assumed. And it was pointed out
that the glacier from Ben Nevis, which Agassiz had laid down in his

* Phil. Trans. 1839. + Edin. New Phil. Journ. vol. xxxiii. p. 217.

{ In the map accompanying this paper, the engraver has failed to bring out
this feature so distinctly as in the MS. sketch.

§ Ancient Sea Margins, 1848. || Edin. Roy. Soc. Trans. vol. xvi. p. 395.

240 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

little map, would not serve his purpose, inasmuch as the lowermost
line extended beyond it.

Here then was no approach to agreement; and Sir Charles Lyell,
in summing up his lucid sketch of the controversy, correctly ex-
pressed the state of the case when he said, ‘“‘ This problem, like many
others in geology, is as yet only solved in part; a large number of
facts must be collected and reasoned upon before the question can
be finally settled.” *

These words will serve as an excuse for reopening the discussion.
The matter is one of interest, not merely as a local curiosity. It is
so connected with the history of the last great geological changes
that to leave it unsettled is not only an opprobrium to our geologists,
but is also a confession of our inability to give any clear account of
these events. Unsolved it is a source of perplexity and confusion,
whereas, if once fairly understood, it would help us much in unra-
velling the history of the great ice-period.

Accordingly Sir Charles Lyell suggested to me, when in London in
1861, to visit the district in order to get more evidence on the sub-
ject; and this was further urged by Mr. Darwin, who candidly ad-
mitted that, not having glacier-action in view when he was there, he
had since, to some extent, doubted his own observations. He fur-
nished me with some useful maps and memoirs bearing upon the
problem, and hkewise indicated several points worthy of particular
attention.

Having myself been long desirous of seeing these curious lines, I
took the first opportunity I had of carrying out these suggestions ;
and to that intent devoted a holiday ramble to Glen Roy in August
1861, and another in July of the following year.

b. The marine theory.—tThe first good sight I had of the parallel
roads was from the shoulder of Bohuntine Hill, in the lower part of
Glen Roy, near a place known as “the Gap.” Looking up Glen
Roy from this station, the three lines are beautifully seen, running
along both sides of the glen with unbroken regularity. Here I was
much impressed with the extreme neatness and precision of the
markings. These clear narrow lines seemed to me altogether too
fine and neat for the effect of a sea-margin, subject as it is to a
continual rise and fall of tide. On the west of Argyleshire there
is a fine old coast-line, about 40 feet above the present, which
every one admits to be due to the sea, but it has a very different
character from these Roads of Glen Roy.

Here are no cliffs, no caves, no banks of well-rolled shingle, no
rude notching of the rock. Wherever the lines pass across a rocky
face of gneiss, they die out or become so faint that they can scarcely
be traced. This fact has been allowed by all the visitors who have
attended to it, by Macculloch, Lauder-Dick, and Darwin. In the
narrower land-locked parts, where the water had been least ruffled
by the prevailing south-west wind, the little terraces, of which these
lines consist, jut sharply out from the hill, almost perfectly flat and

* Manual of Geology, ord edit. p. 89.

1863. | JAMIESON—-PARALLEL ROADS OF GLEN ROY. 241

level, as is well seen along the western side of the valley, from the
Gap up to Glen Turrit ; where, however, the valley is wide, and has
been exposed to the westerly gales, the terraces are broader, ruder,
and more shelving. This is seen on Tom Brahn, and in the Spean
valley above Tiendrish, for example.

The general appearance then of the Roads did not, at first sight,
exhibit that erosion which I should have expected from a coast-
line. There is a marked absence of well-rounded shingle, less of it
indeed than I have observed along the margin of existing fresh-
water lakes. This absence of any strong erosion has been generally
admitted ; but there is at one place a certain amount of rounded
rock, upon which the author of the marine theory built a good deal,
as evincing an amount of abrasion that no mere freshwater lake
could have accomplished. This is near the entrance to Loch Treig,
where the lower line only occurs; and this was one of the points Mr.
Darwin wished me particularly to attend to.

But the rounding of the rocks here I found to be clearly due to
glacier-action. This, indeed, Mr. Darwin himself had begun to
suspect. It extends, as I have shown in another paper, for many
hundred feet up the hill on both sides of the entrance; the line
here, and around Tom-na-fersit, being formed by a thick terrace of
gravelly débris abutting against the ice-worn rocks. Until, however,
the contingency of ice-action in Britain was thought of, it was, of
course, almost unavoidable to attribute this effect to water. Some
rounded rocks occur also at the gorge near the head of Glen Roy,
owing to the same cause, the scoring being in many places quite
visible. On the flank of Craig Dhu the glacial markings are often
very finely displayed close above and below, and even on the very line
itself. But I nowhere found any decided notching or cliff that I
could assign to the action of the old lake.

There was another feature that seemed to bear against the pre-
sence of the sea. ‘This was the state of the deltas in the upper part
of Glen Roy. The fine preservation of these is very remarkable.
One upon the east side of the glen, below the shooting-lodge of
Dalriach, is especially worth notice. Its surface comes up to the
level of the lowest line, and it protrudes from the little ravine that
gave it birth nearly halfway across Glen Roy, bulging out lke an
artificial mound, compact and clear in outline as when first formed,
save that the stream from which it was originally deposited has now
cut a great gash through its midst. The fan-shaped margin shows
that the water it dropped into had no strong set or current, either
up or down the glen. If it had, the débris would have curved more
or less up or down the valley; whereas it has disposed itself almost
equally all round the mouth of the little stream, the tendency being,
if any way, down the glen. Now it seems to me that the continual
swaying up and down of a sea-loch subject to the tides, is incom-
patible with all this. So far as I have observed, delta-matter car-
ried into the sea, or into a salt-water lake, is levelled and spread
out to a much greater degree. Its bearing upon the notion of a
deluge sweeping up the glen is still more obvious. There is a fine

242 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

little delta of the same kind in Glen Collarig, and also a large one at
the mouth of the Rough Burn in Glen Spean.

A further way of testing the matter presented itself.

Had the lakes been freshwater, they should each have had an out-
let for the discharge of their excess, and we ought to be able to
point out the channels along which the streams descended to a lower
level. Now this can be done for all the three Glen Roy lines,
and likewise for that of Glen Gluoy. It has been ascertained that
the latter, which is the highest of all, coincides in level with the
watershed at the top of its glen*; so that were Glen Gluoy filled to
the height of its line, the water would pour over this col or summit-
level down a hollow, called Glen Turrit, into the upper part of Glen
Roy. The fall from this col to the highest line in Glen Roy is,
according to Messrs. Milne-Home and Chambers, nearly thirty feet.
The overplus of the Glen Gluoy lake would, therefore, run into that
of Glen Roy. That this was actually the case is well confirmed by a
huge old delta at the mouth of Glen Turrit, coinciding in its upper
surface with the lowest of the Parallel Roads. This delta is out of
all proportion to the size of the stream. Standing at the junction of
the Turrit and the Roy, I estimated the water in the latter at fully
three times as much as that of the Turrit. Seeing then that the
channels of the two streams are similar in character, the Roy should
have had much the larger delta. Instead of that, the delta of the
Turrit is more than twice as big as that of the Roy. It is a consider-
able mass, some furlongs wide, with a flat surface, and a front rising
at its centre ninety feet above the bottom of the valley—a striking
proof how long the lake must have existed. Deep terraces of delta-
matter fill the glen here at all the lateral openings, and the scene
strongly reminds one of Dr. Hooker’s sketch of the terraces in the
Yangma valley (Himalayan Journal, vol.i. p. 242).

With regard to the uppermost Glen Roy line, it was ascertained
by Sir T. Lauder-Dick, and the fact has been further verified by Mr.
Darwin, that it coincides with the watershed at the head of Glen
Roy. So that were Glen Roy filled with water to the level of its
uppermost ‘road,’ the lake would have discharged its excess over
this col into Lochan Spey.

Again, the middle line of Glen Roy coincides (as was first pointed
out by Mr. Milne-Home) with the col at the head of Glen Glaster,
a little valley which branches off to the eastward from the lower
end of Glen Roy. This point I verified myself, and found the line
to be just on a level with the watershed, or, more accurately, a foot
or two above it. The parting of the waters is in a flat swampy hol-
low, over which peat is now growing. Here a small stream rises,
and flows eastward down a hollow into the Rough Burn, which en-
ters Glen Spean opposite Loch Treig. The fall, or descent, of the
stream from this Glen Glaster col to its junction with the Rough
Burn is, by an aneroid observation, about seventy feet. The trace
of an old channel is here visible, that looks to have belonged to a

* More accurately, it is a foot or two above it; see Darwin, Phil. Trans. 1839,
p. 42.

1863. | JAMIESON—PARALLEL ROADS OF GLEN ROY. 243

good-sized stream. It is now overgrown with swampy turf, which
hides the nature of the bottom. It is interesting to observe that a
large old delta occurs at the mouth of the Rough Burn at a level
corresponding with the lowest of the Parallel Roads; the top of the
delta rising, however, above the line which marks the west side of it.

This third or lowest of the Parallel Roads of Glen Roy extends
into the valley of the Spean, and, passing the old delta just men-
tioned, seems to have stretched eastward beyond Loch Laggan to a
place called Makoul, where the watershed occurs that divides the
basin of the Spean from that of the Spey. Sir Thomas Lauder-Dick
first showed the connexion of the line with this watershed, pointing
out that here must have been the outfall for the water of the old
lake, when it stood at the height of the lowest Parallel Road. This
conjecture appears to be perfectly correct. Owing to the broken,
rocky nature of the ground, the line can only be traced faintly here
and there. Nevertheless we have this large delta at the mouth of
the Rough Burn. There is also another of far greater size at the
west end of Loch Laggan, where the entrance,of the Gulban River
had formerly been. This is the largest of all the deltas. It is a
wide-spreading mass of silt and gravel, the front of it rising about
twenty feet above the surface of Loch Laggan, but it slopes gradu-
ally backwards to a height of about fifty feet. These two deltas,
together with other traces, afford good evidence that a lake had filled
all this part of the Spean valley to the height of the lowest Glen
Roy line. It further appears, from levellings executed for other
purposes by the Ordnance Survey, that the altitude of the water-
shed near Makoul corresponds with that of this line. There is no
reason then to doubt that this was the outlet of the lake when it
stood at the lowest Parallel Road. Now, when we come to examine
this spot, we find evidence of a large stream having flowed out there.
Some low rocks of gneiss, sprinkled with birches, occupy the hollow
bordered by a steep hill on the north side. These crags have been
ice-worn at a former period, as can still be perceived, but the traces
of subsequent water-action are unmistakeable at a level correspond-
ing with what had been the old outlet of the lake. The glacial
markings are effaced, and the rock worn into smooth, sinuous curves,
with something like incipient pot-holes. These water-worn ledges
are strewed with well-rounded balls of stone, as large as cocoa-nuts
—the mullers that had ground the rocky surface—lying just where
the eddy had left them; and, in the recesses and sheltered bends to
the east or lee side of the crags, large heaps of pebbles, intensely
water-rolled, afford good proof that a strong brawling current had
long gone out here. On ascending the knolls of gneiss above the
level of the old outflow, these appearances vanisn. No water-
rolled pebbles are to be seen, no washed gravel, no water-worn
rocks, no tendency to pot-holing, but merely a thin covering here
and there of coarse earth with angular bits of stone. Had this
watery action been due to the sea, it would not have been confined to
the level [have mentioned, but would have extended, at least during
the period of the two higher lines, to a greater elevation.

244 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

On going eastward the features of a deserted river-valley increase.
The rocky banks recede on either side, and a flat level space occu-
pies the centre, now covered by peat. Beds of water-worn pebbles
occupy the bays and curves at the sides, and, further on, old river-
meadows present themselves, with alluvial flats running close up to
the rocky masses that rise abruptly from their margin, and all the
signs of a river-course are seen but the river itself, which has dis-
appeared. I quite agree, therefore, with Mr. Milne-Home, who has
hkewise described this spot, that the evidence of a deserted water-
course 1s here very plain.

But it will be seen, on referring to the map, that a stream called
the Pattag enters the head of Loch Laggan, and turns round close
by this watershed. It may therefore be said, admitting all this
evidence of a current flowing out here, might it not be merely the
old channel of the Pattag, that might easily be supposed, by a slight
diversion of its course, to have here turned eastward into the Spey,
instead of wheeling round, as it now does, into the head of Loch
Laggan ? .

The answer to this is that the deserted channel is far too large to
be due to a small stream like the Pattag, for it is such as a river
like the Spean or the Lochy might have produced. But perhaps a
better answer may be derived from a consideration of the old delta
of the Gulban already mentioned, for the height of it proves that a
lake must have formerly extended to Makoul, and consequently had
its outfall there.

We have evidence, then, in regard to each of the Parallel Roads,
that it coincides with an outlet where the water might have escaped
to a lower level. And, where the point has been attended to, it
appears that the lines just eaceed the height of these outfalls suffi-
ciently to admut of a certain depth of water passing out. This four-
fold proof tells very strongly, I think, in favour of the view that the
lakes were freshwater. A short line which Mr. Darwin discovered
in a gully near Kilfinnan coincides in like manner with the water-
shed between it and another valley.

The fact of the drop, or descent, of 20 or 30 feet from the Glen
Gluoy line to the highest one in Glen Roy has always been felt as a
difficulty, 1f we suppose the Roads to be sea-beaches ; for why should
there be no coincidence between the lines in these two glens, both
haying been so favourable for the preservation of the beaches? And
why, indeed, should these four lines be absent in all the other glens
of Scotland ?

But Glen Roy presents an exceptional character to our other
mountain glens, not only in respect of its parallel roads, but also on
account of its great beds of silt and gravel, and, still more, the won-
derfully fine deltas at the mouths of its lateral ravines. All these
local peculiarities—the lines, the deltas, and the heavy banks of silt
and gravel—bespeak a local cause, such as a freshwater lake, and
not a universally present one like the sea. It has further been
pointed out, as another formidable objection to the marine theory,
how improbable it is that this region should have been heaved up

1863.] JAMIESON—PARALLEL ROADS OF GLEN ROY. 245

some 1200 feet or so, and yet have preserved its horizontality so
perfect that all the observations hitherto made have failed to detect
any fault in the lines, or any deviation from a dead water-level.

The absence, therefore, of any good positive evidence in favour of
the marine theory, and so many considerations urging themselves
against it, seemed to me to render it untenable.

c. Agassiz’s theory.—Let us now see what help is to be got from
the glaciers; and first as regards Glen Gluoy. This glen opens into
the great valley of the Caledonian Canal (or ‘the Great Glen,’ as it is
called in pre-eminence), right opposite Loch Arkaig. A glacier, then,
issuing out there might have blocked up Glen Gluoy; or we may
conceive the Great Glen itself to have been the bed of a large ice-
stream, fed by the lateral valleys.

I therefore went to Glen Arkaig, and at its very mouth, close to |
Loch Lochy, found the gneiss much ground down, as if by ice coming
from the west. From this to the Lake is known as ‘the dark mile,’
the road winding along the bottom of the glen beneath the shade
of oak, birch, alder, and ash. On reaching Loch Arkaig I ascended
the hill on its north side, and found the gneiss much ice-worn as
far up as I went, which was about 700 feet above the lake. The
crystalline schist is here highly mineralized and of a very metamor-
phic nature. The bedding seems nearly vertical, and the layers
often twisted and gnarled. These rocky masses show an evident Stos
Seite, as Sefstrom would have called it, the west faces being smoothed
down, and the eastern more rugged and unworn. The scores and
strie have mostly weathered out, but I succeeded in finding some
well-marked instances, the direction being up and down the valley.
This was nearly 400 feet above the Loch; and, judging from the ap-
pearance of the ridge as far up as I could see, the glacial action had
extended to a great height. There was an absence of any super-
ficial detritus, and also of large boulders. Glen Arkaig shows a wide
basin encompassed with large, broad-flanked hills. The ridge be-
tween it and Glen Garry is very high, three of the peaks reaching
about 3000 feet, and the highest exceeding that a little. Glen
Arkaig, therefore, would seem to possess the qualities suited for
turning out one of the largest glaciers in the district. This, then,
was so far favourable.

On coming to examine the mouth of Glen Gluoy, I found on the
north side, upon the angle of the ridge between it and Loch Lochy,
glacial scores pointing W. 25° N., as if caused by a pressure of ice
from Loch Arkaig. This was at a height of about 260 feet above
the bridge, the markings being discovered by tearing off the peel
of turf that covered the rock, so as to expose a fresh surface. On
walking up the glen to the point where Glen Fintaig branches off, I
found scores here and there, generally parallel to the valley; but on
the spur of the hill that divides Glen Gluoy from Glen Fintaig, the
scoring runs right up and down the slope that faces down the valley.
This had been previously noticed by Mr. Milne-Home, who attri-
buted it to diluvial action.

I now examined the shoulder of the hill between the mouths of
VOL, XIX,—PART I, s

246 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 21,

Glen Gluoy and Glen Spean, and on the angle of the ridge, between
Loch Lochy and the Spean (known, I believe, as Strone-y-Vaa), I
found the rock much worn in many places, as if by the pressure of
ice from the west. The surface, however, of these masses has
yielded to the influence of the weather, so that it required much
search to discover any reliable markings. Several clear instances I
did at length find. At an elevation of probably 800 or 900 feet
glacial scoring occurred, pointing W. 5°N., a little lower W. 20° N.,
running not horizontally, but up and down the slope, as if by ice
mounting over it from Loch Lochy. Again, W. 26° N., W. 45° N.,
and W. 12° N., pointing generally towards the mouth of Glen
Arkaig. Further round the angle of the hill towards Glen Spean
and lower down, W. 15° N. and W. 45° N., or due N.W.; and the
western sides of the rock being most worn showed that the action had
come from that side, and not down the Spean Valley. The rocks
were also most bared where the pressure of a glacier, wheeling round
from the Great Caledonian Valley into the mouth of Glen Spean,
would have applied most strongly. All this seemed to show that
the Glen Arkaig glacier not only blocked up Glen Gluoy, but also
largely contributed to close the mouth of Glen Spean.

Ataplace called Brackletter, on the south side of the Spean, near
its junction with the Lochy, I observed glacial scores pointing more
nearly due west, but still inclining a little to north, as if caused by
the pressure of ice from Glen Lui, a valley lying to the south of
Glen Arkaig, and opening in front of Glen Spean.

The south side of the Spean, from its mouth eastward to Loch
Treig, is bounded by a range of lofty hills, which may be looked upon
as an extension of the Ben Nevis ridge. The highest peaks exceed
3000 feet in height, but they are not disposed around a basin that
could collect their snows into one ice-stream. The most extensive,
however, of the numerous gullies that intersect their flanks is “‘Corry
N’Eoin” (the ‘‘ Bird-Corry ”’), a grand place to the east of a large
mountain called the Aonach More. This ravine presents a series
of rocky amphitheatres, or great caldrons, whose walls have been
ground down by the long-continued action-of the ice. The quartz-
veins are all shorn to the level of the rounded gneiss, and streaked
with fine scratches pointing up and down the hollow, These signs of
glacial action extend far up the rocks on either side. Ishould have
therefore considered it a good objection to Agassiz’s theory, had any
of the parallel roads been visible in this gully. But it is interesting
to remark, that although the lowest line can be traced from Loch
Treig all along to here, yet it stops short just as it approaches the
entrance of this ravine, and further west I could not trace it. The
conclusion, therefore, seems reasonable, that the extension of the
lake was cut off here by a glacier issuing from Corry N’Eoin, and
on the opposite side by the ice of Glen Arkaig and the Great Glen
flowing over the shoulder of Strone-y-Vaa to near Tiendrish, where
the line on the north side of Glen Spean vanishes.

Probably all the Great Caledonian Valley was at this time filled
with ice, from its summit-leyel at Loch Oich to Fort William; the

1863. | JAMIESON—-PARALLEL ROADS OF GLEN ROY, 247

glaciers I have indicated forming a large proportion of the main
stream. This then would close up the mouths of Glen Gluoy and
Glen Spean ; and so long as the ice exceeded sufficiently the height
of the watersheds at the top of the glens, these cols would determine
the level of the water in the lakes.

But in Glen Roy there are three lines, and this barrier across the
mouth of Glen Spean, although it might serve for the lowest, leaves
the two higher ones unaccounted for. In order that a lake could
exist in Glen Roy at the height of the upper lines, something must
have prevented the water escaping by Makoul, and also by the Glen
Glaster Col.

In order to explain this we must go to Loch Treig. Let us sup-
pose a glacier issuing from the mouth of Glen Treig, and let it pro-
trude across Glen Spean until it rests on the hills upon the north side
of that valley. This would cut off all outlet to the eastward, both
by Glen Glaster and Makoul; and, so long as the icy barriers main-
tained a sufficient height, the water fillimg Glen Roy would have to
escape by the col at the top of that Glen into the head of Strath-
spey. This col, therefore, would determine the level of the lake,
and keep it at the upper line as long as this state of things lasted.

Now let the Glen Treig glacier shrink a little. This would open
the Glen Glaster Col, and let out all the water above its level. That
watershed would now determine the height of the lake, and there-
fore keep its surface at the middle line so long as this second state
of matters lasted.

Then let the Glen Treig glacier shrink again, until it withdrew
out of Glen Spean. That valley being now clear, the water would
eseape by the outlet at Makoul, which would then determine the
level of the lake, and keep it at the lowest line so long as the ice-
stream across the mouth of Glen Spean maintained itself of suffi-
cient height. When this latter finally gave way, Glen Roy would at
length be emptied.

Grant then these two ice-streams, one in the Great Caledonian
Valley and the other at Glen Treig, and the problem of the Parallel
Roads can be solved, provided we allow that glaciers have the power
to dam such deep bodies of water as must have occupied Glen Gluoy
and Glen Roy.

Now there is good reason to believe that both of these glaciers
existed. Indeed the evidence for that of Glen Treig is probably
more complete than for any other glacier in the kingdom. I have
in a former paper detailed part of that evidence* ; I have shown how
the rocks at the entrance are intensely worn for many hundred feet
up the hills on either side, presenting in their rounded outlines,
scored surfaces, and perched boulders, all the marks of glacier-action.
The profound pool of Loch Treig, lying in a deep rock-basin, is,
adopting the views of Professor Ramsay, a still further proof. But
it was not until my last visit that I was aware of some remarkably
fine moraines that demonstrate still more forcibly the former pre-
sence of the ice, and which I shall now describe. I am the more

* Quart. Journ, Geol. Soc. vol. xviii. p. 170. :
S

248 PROCEEDINGS OF THE GHOLOGICAL society. (Jan. 21,

induced to do so, because some foreign savants have said on visiting
Scotland, “‘ You have the glacier-mud, the transported boulders, the
roches moutonnées, and the striated pebbles ; and your ice-scored and
polished rocks differ in no respect from those of the Alps. All these
we have seen and admit; but where are your moraines? ”

The glacier on issuing from the narrow gorge at the end of Loch
Treig dilated immensely, and, in doing so, the right flank of it had to
pass over a rough expanse of syenite forming a bit of low, rocky
ground in the middle of Glen Spean; but the surrounding hills are
of mica-schist with veins of porphyry. ‘This syenite has the pro-
perty of breaking up into large cubical blocks, often of immense size.
These have been swept before the advancing mass of ice, and have,
along with other débris, been disposed into long mounds, forming a
sort of semicircular arch, or great horse-shoe, with a sweep of some
miles. These concentric bands mark out most distinctly the former
edges of the glacier, as it shrunk from time to time with the return
of a milder climate. And it is instructive to observe how, in some
places, the ice has pushed this zone of blocks before it, uphill, off
the parent rock, and left them upon the mica-schist on the north side
of Glen Spean.

The best view of these moraines is to be got by walking along
the footpath, or pony-road, that goes eastward from the entrance
to Loch Treig, along the base of the hill towards Badenoch. Having
proceeded about a mile or more along this tract, you will find your-
self at the summit-level of the road, where it crosses these moraines.
Here they start out from the hill into the wide low moor that occu-
pies the bottom of the valley, and from this point they may also be
traced slanting upwards across the slope of the hill towards the
gorge of Loch Treig; showing how vastly the pent-up ice had dilated
on issuing from the narrow pass. Here the stuff consists of the
débris of the mica-schist with bits of porphyry, but blocks of
syenite soon mingle with it, and become more and more plentiful.
Two chief lines of moraine now appear, stretching far out into the
plain with a gentle curve, and hold on with surprising regularity for
a long way. Outside of these, older hillocks of similar origin may
be traced for a considerable distance, showing that the glacier had
at one time been of much greater extent. But these two are so
perfect and well-defined as to indicate a long abiding of the ice at
their margin. ‘The outer one is the largest, rising in some places
sixty or seventy feet above its base, and forming a narrow steep-sided
mound. Blocks of all sizes, up to fourteen feet in length, stick out of its
surface, mixed with lesser débris of mica-schist and gneiss. The
inner moraine runs alongside of this one, in some places approaching
so closely as to mingle with it,in others receding 200 yards or more.
It contains less small débris, and is often composed wholly of large
blocks of syenite, many of them from five to ten feet, some of them
fifteen to twenty-five feet in length, which give it a very striking
appearance, forming a long pile of blocks like a ruined breakwater.
The biggest piece I saw was twenty-six feet in length; it lay on the
top of some smaller fragments, and a little wounded lamb had taken

1863. ] JAMIESON-—PARALLEL ROADS OF GLEN ROY, 249

refuge in the recess beneath it. Within this moraine there is a wide
smooth space, like a bay, almost destitute of boulders for a con-
siderable distance, and overgrown with a green swampy turf; show-
ing that the glacier had made a considerable retreat without halting
long enough anywhere to leave much debris.

These two moraines, after being traced for a mile or so out into
the moor, become less regular, and gradually merge into the boulder-
covered surface. Their curve seems to indicate that the glacier had
crossed the Spean near a place called Gorstan. On the north side of
the valley two crescent-like zones, evidently a continuation of those
I have been describing, stretch eastward from the spur of Craig Dhu
to near Ben Caoran (pronounced Ben Hourin, meaning the Rowan-
tree Hill). We might liken the two curving mounds to a double
rainbow, and the outer hillocks to the supernumerary bows.

It seems to me that these moraines, together with the ice-worn
gorge, afford about as good evidence of the former existence of the
Glen Treig glacier as a fossil skeleton does of the former existence
of the living animal.

The position of the outer hillocks shows that the ice must have
pressed against the hills on the north side of Glen Spean, so as
to have blocked up the outlet for the water by the Glen Glaster Col,
and boulders of the syenite are numerous in the hollow beside it.
The inner ones in hke manner demonstrate that gradual shrinking
of the ice which the theory requires.

These parallel moraines are as fine a sight to a geologist as the
Parallel Roads themselves, and no one who goes there should omit
seeing them. Those at the mouth of the Larig Leachach Glen are
also well worth a visit.

There are no such fine moraines at the mouth of Glen Spean ; but
the greater part of the extensive moor called Unichan, or Aonachan,
is overspread with what appears to be glacial débris, partly modified
by falling into the water of the old lake. The same is the case high
up on the shoulder of the ridge all round from Tiendrish towards
Loch Lochy. Large boulders are scanty, although onc is met with
here and there; the stuff being mostly a rubbish of mica-schist—a
rock which furnishes a smaller débris with few great blocks.

The character of a moraine depends, of course, upon the rocks that
furnish it, and the striking features of those I have described are in
a great measure due to the accident of the glacier haying to pass
over the rough tract of syenite. Much also depends upon the moraine
being formed (to borrow a chemical phrase) in the dry way ; for when
the stuff from the glacier falls into a lake or pool, its features assimi-
late to those of an aqueous deposit—a circumstance that has misled

many good geologists.

The immense ‘accumulations of gravel about ie and the
mouth of Loch Treig seem to partake of this mixed character, being
probably the terminal moraine-matter of the glaciers of Glen Treig
and Corry Laire when they protruded into the margin of the lake.

At Inyerlaire, and around the large rocky knoll called Tom-na-
fersit, they have been finely terraced by the action of the water when

250 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

at the level of the lowest Glen Roy line. But I ascertained that the
terraces close by the end of Loch Treig do not correspond in height ;
they do not, in fact, form part of this Parallel Road, but are about
30 feet above it. This seems difficult to account for except by sup-
posing these heaps of débris to have been piled up by the glacier to
such a height as to dam Loch Treig, after the ice withdrew, to a level
exceeding the height of this ine. The outpour of the lake would
then wear through them; but it has not even yet cut its way to the
very bottom, for the lake is still partly retained by these banks of
gravel.

On tracing the gravelly accumulations up the Laire Glen, I found
that they became terraced or flattened at the level of the lowest
Parallel Road (which is the only one seen in Glen Spean), but ex-
tended up the glen continuously above the level of this line, assum-
ing an irregular hillocky outline, and becoming gradually coarser
and of a less water-worn character—assuming, in short, the natural
aspect of old moraines. It is interesting to note that none of the
syenitic boulders occur here. At a deep section of one of these banks
at the mouth of Corry Laire, below the level of the line, I noticed
that the stuff was heaped together in a highly inclined sloping
manner; the mass consisted of coarse water-worn gravel, very
pebbly, and the pebbles indicated a considerable amount of water-
rolling. ‘This want of horizontal stratification, and the somewhat
earthy character of much of the sand, were the chief differences I
could perceive between it and ordinary water-bedded gravel.

The melting of the ice from time to time, aided by heavy rains,
would send floods of water over the old moraines, and might thus
produce great quantities of rolled gravel in the neighbourhood.

The meeting of the moraines with the lowest Parallel Road at the
mouth of the Larig Leachach is also well worth studying. ‘The ice of
this short glen seems to have protruded in much the same way, for
the outer mounds are fringed with the gravelly terrace of the Road.
Something of the same kind is also seen at the next corry to the west,
called Corry Vaddie. But at the time of the two uppermost lines,
which mark a period of severer cold, all these glaciers must have
advanced far out, and perhaps filled the whole of the lower part of
Glen Spean, and hence the absence of the two upper lines there.
Glen Gluoy, even, and the basin of Loch Laggan may have been then
filled with snow and ice, and some of the higher side ravines of Glen
Roy may have had their sheets of ice, or glaciers of the second order.
This, it seemed to me, might have been the case with a corry on the
west side of Glen Collarig, near which the two upper lines cease, one
of them quite suddenly ; the terrace of which it consists bulging out
at its termination as if it had there met the ice. The watershed at
the head of Glen Collarig seems also to be formed partly by old
moraines from an adjoining corry, but these belong probably to a
period antecedent to any of the Glen Roy lines.

Seeing the many fine deltas along the lowest of the Glen Roy lines,
I was struck with the remarkable absence of these accumulations
along the two upper ones. I do not think the shorter course of the

1863. | JAMIESON—-PARALLEL ROADS OF GLEN ROY, 251

rivulets sufficient to account for this. As far as I remember, there
is an absence of delta-matter in Glen Turrit at the level of the two
upper lines. Perhaps this may be explained by remembering that
the two upper lines mark severer glacial conditions, when the hills
would be more covered with snow, and perhaps abound less in
running water. Glen Gluoy, as I have said, might then be filled
with snow and ice; consequently there would be no lake discharging
into Glen Turrit, and hence no delta-matter. Hence also the fainter
mark of the Glen Gluoy line.

Glen Gluoy and Glen Roy are both very narrow glens, not having
basins fitted for feeding glaciers; it is probable, however, that, at
the upper extremity of the latter, traces of glaciers may be found
interrupting the mark of the highest line, but circumstances pre-
vented me from examining that locality properly.

Mr. Darwin, in his memoir, alludes to some horizontal mounds or
patches of earthy matter near the cols, and at a higher level. Mr.
Robert Chambers also lays much stress on certain horizontal markings
in Glen Spean, above any of the Parallel Roads. Some of these I ob-
served. An instance of such is distinctly seen high up on the front
of Ben Chlinaig when viewed from Bohuntine. I, however, ascer-
tained that these short lines on Ben Chlinaig were neither quite
horizontal nor perfectly parallel. I therefore think they have arisen
from some other cause than what formed the roads of Glen Roy. I
am of opinion that many of these cases are connected with that
-former great extension of the ice which preceded the period of the
Roads. They may mark the edge of those great ice-fields that for-
merly filled the valleys, being either lines of moraine matter or stuff
accumulated in lateral pools between the ice and the hill-sides. These
glacier-pools occur in various situations, and their geological effects
have been well pointed out by Charpentier *.

A large glacier must have issued from Glen Nevis, and, owing to
the great height of the hills there, must, I should think, have pro-
truded across the mouth of the great valley of the Caledonian Canal,
after the ice had shrunk out of the mouth of Glen Spean. This
would continue to dam the water to a certain height, and may afford
the explanation of those broad terraces in the lower part of Glen
Spean, some of which are very noticeable. They differ in character
from the Parallel Roads, and few of them exceed an altitude of
400 feet above the sea. There is a fine fragment of one about that
height at Brackletter, and also at Auchnaderry, near bridge of Roy,
and several at lower levels. It is worthy of remark that these
terraced accumulations all cease on approaching the mouth of Glen
Nevis. They are also absent in Glen Gluoy, and in the lower part
of Glen Arkaig. If they are of marine origin, why do they vanish
at these places ?

§ 3. Place of the Parallel Roads in the history of the Glacial Period.
a. Relation to the period of chief submergence.—Believing the Parallel

* Essai sur les Seas pp. 64 & 257. See alsolAgassiz, Etudes sur les Gla-
ciers, pp. 217-288

252 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

Roads to have been formed by freshwater lakes, I was now anxious
to ascertain what relation in time these lakes bore to the great sub-
mergence that seems to have overspread so much of Britain and
Ireland during what has been called the Drift-period. The preser-
vation of the deltas in the upper part of Glen Roy, and the way in
which the pebbles lie on the water-worn ledges of the outlet east from
Makoul, just where the eddying outflow of the lake seems to have
left them, appeared to me to show that neither the sea nor any
diluvial catastrophe had, since the time of these lakes, approached the
level of the lower line, which, in round numbers, we may call 850 feet
above the present tide-mark.

Seeing that Glen Nevis opens upon the head of Loch Eil, which is
now an arm of the sea, I thought an examination of it would afford
some further light upon this question. If Lochaber partook in the
submergence, and if this submergence occurred after the glaciers had
finally disappeared, then some trace of the sea’s presence should be
found in Glen Nevis, either in the shape of marine strata, or in the
moraine-hillocks being levelled by the inroad of the waters. Even
supposing no shell-beds could be detected, yet some shingle beaches
or stratified beds of clay and sand might be looked for.

It was, therefore, with a good deal of curiosity that I walked up
the Glen some five or six miles to try this point. The result was
that I found nothing to show that the sea had ever occupied the
glen since the glacier left it. The moraine-hillocks, even near the
mouth of the glen, have all their original roughness, and are dotted
with boulders just as they are in the Larig Leachach. There are no
high terraces of silt, or gravel, no beds of brick-clay; but there are
irregular mounds of débris covered with big stones, and the torrents
that scar the steep sides of Ben Nevis are still pouring down their
shoals of gravel. The stream in the bottom has likewise accumulated

a slight depth of alluvial loam in the flatter parts of the v alley ; ; but
of the sea’s presence I saw no trace.

The same remarks will, I think, apply to the lower part of Glen
Arkaig, judging from whatI saw during my hasty visit to that locality.

Both Mr. Darwin and Professor Ramsay have expressed their
opinion that in Wales the glaciers made a considerable advance after
the great submergence which left the shells on Moel Tryfan, and
these later glaciers, they maintain, have swept the marine drift out
of many of the valleys there. Adopting this opinion, we might
suppose some such re-extension of the glaciers to have swept all
trace of the sea out of Glen Neyis.

If the glacier-lakes of Lochaber were not formed during the
shrinking of the great ice-covering which preceded the submergence,
we may suppose them also to belong to this later period. The un-
disturbed horizontality of the Parallel Roads is in favour of this view,
for we should hardly have expected them to be so perfect had they
shared in all the ups and downs of the later Phocene period. This ~
second advance of the ice would also account well for the absence of
all high-lying beds of marine shells in the more mountainous parts
of Scotland. If, therefore, the Parallel Roads are the beaches of

1863.] JAMIESON—PARALLEL ROADS OF GLEN ROY. 253

glacier-lakes belonging to this later period, some beds of marine
drift with sea-shells may yet be discovered underneath the lacustrine
silt and gravel of Glen Roy.

A considerable amount of glacier-action after the chief submergence
of the drift-period would also explain a circumstance that has always
seemed to me remarkable, namely, the absence of any clear trace of
the upper limit of this submergence. One would think that, however
indistinct the intermediate halting-places might be, yet the upper-
most shore-line ought to be more clearly marked. But if we suppose
the ice to have made a decided advance after the emergence of the
land, it is clear that it would blot out all trace of the old shores, so
far as it extended. I believe we owe the first suggestion of this
explanation to the fertile mind of Mr. Darwin.

This re-extension of the glaciers would also enable us to account
for much of the valley-gravel without the aid of marine action. I
have pointed out in a former paper some features of this upper rolled
gravel that mere river-action, however prolonged, does not account
for. But if we can call in the agency of glaciers for these features,
we might explain the superficial accumulations of our Highland
valleys (I am not now speaking of our lower grounds) simply by
glaciers followed by a very long period of river-action. Extensive
effects might have arisen from the occasional bursting of glacier-
lakes, and also from the melting of the ice, if it thawed rapidly.
Pools and lakes would be formed by the moraine-mounds left along
the valleys on the shrinking of the ice, and these would obstruct the
drainage to some extent, but would be afterwards modified by the
rivers gradually cutting through them.

Might not some of those curious accumulations known as eskers,
osar, and kaims have been formed by this re-extension of the ice
ploughing into the old marine beds, and forcing them up into long
narrow mounds? In some regions these may have arisen from the
glaciers terminating in the sea, forming a kind of marine moraine ;
and, if the end of the glacier floated, fine mud and sea-shells might
gather beneath it.

b. Relation to the 40-feet beach of the West Coast——Another ques-
tion presented itself. It is well known that a fine old coast-line
occurs along the border of Argyleshire, about 40 feet above the
present beach, marking a long pause of the sea at that level. What,
then, is the relation of this old beach to the time of the Parallel
Roads, and the glaciers connected therewith ?

I observed that this 40-feet beach fringes the head of Loch Eil
distinctly on both sides up to Fort William, and can be traced on to
the entrance of Glen Nevis. It is well marked close beside the
bridge at the mouth of the Glen, and appears to extend quite across
it on towards Bannavie, forming a broad shingly margin along the
base of the moraine hillocks. These, however, above that level,
preserve their original irregular surface dotted with boulders.

This 40-feet beach is therefore later than the Glen Roy lakes, and
later than those large glaciers whose moraines I have described as so
remarkable in Glen Spean.

254 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

On the east side of Loch Eil, just half a mile to the south of Fort
William, I came upon a section of this 40-feet beach, laid open by a
small stream cutting through it, which seemed to me especially inter-
esting on account of a bed of marine shells it contained.

These shells are at a height of about 11 feet above present high-
water-mark, and about 50 yards or so from the shore. They are
imbedded in the lower part of a stratum of greyish stony clay,
resting immediately upon the solid schistose rock.

This clayey stratum is about 5 feet thick, and is covered by some
sand and gravel which are not well exposed. At the bottom are the
shells, which are very numerous, many of them broken and decayed,
especially the larger kinds, but many of the smaller perfect. They
appear to have been mostly empty or ‘ dead’ shells, being filled with
shelly mud, and many of them have been pierced by boring mollusks.
They lie in a gravelly matrix of small schistose fragments and clayey
sand. In the upper part of the bed the clay is purer, with few stones
and no shells.

The following is a list of the species I collected. For the identifi-
cation of some of them I am indebted to Mr. J. Gwyn Jeffreys,
F.RBS.; F.G.8., &e.

1. Astarte elliptica, Brown ............ Numerous.
2. compressa, MMeNe. <..s.cessnacsas Four specimens, mostly perfect.
3. Pecten Islandicus, Miiller............ Numerous; all small young shells.
4. Anomia ephippium, Linn. ......... Several.
5. Modiola modiolus, Linn. ............ Plentiful.
©: Wucula ...22..- RN Aa ea BO One valve, like WV. nucleus.
Ge) GMMONE cc sat tack eau eM can secenee One fragment of a large species, appa-
rently C. marmoreus.
8. Acmea virginea, Miiller ............ Several.
9. Puncturella Noachina, Linn. ...... Two specimens.
10. Trochus cinerarius, Linn............. Several, both old and young.
11 GUMIGUS,, T6829 wikceoucenes Two or three.
¥2: Lacuna vincta, Mont. .....2..c4.000: Numerous.
13. Littorina littorea, Linn. ............ One full-sized specimen.
14. PUGS; 600i. caoccmnaewraegenees A few.
15. Turbo expansus, Brown ........645 Several. Mr. Jeffreys informs me this
is the same as Littorina squalida of
Brod. and Sow.
16. Natica clausa, Sow. ......s.scese.e808 Several.
17. Bela pyramidalis, Strem ............ One specimen.
18. Mangelia Holbellii, Moller ......... Seven specimens.
19. Rissoa striata, Mond. ..............0000 One.
20. Buccinum undatum, Jinn. ......... A few.
' 21. Trophon clathratum, Linn. ......... Numerous.
22. scalariforme, Gould ............ One fragment. Mr. Jeffreys thinks it
may be an aged specimen of Trophon
Gunneri, Lovén.
OS, WebiMUs isis src etadss atien sca snes tek Some spines and plates.

The prevalence of the Littorinw and Lacuna, together with the
general character of the group, afford fair evidence of a shore-line,
while the fact that the most common Jittorina is the Arctic variety,
or Turbo expansus of Brown, together with the number of Pecten
Islandicus, Natica clausa, Mangelia Holboella, and the presence of

1863. | JAMIESON—PARALLEL ROADS OF GLEN ROY. 255

other shells not ranging now so far south as Britain, show the assem-
blage to be of a decidedly more northern character than what now
haunts our coast.

As the assemblage is a littoral one, I see no reason for doubting
that it belongs to the period represented by this 40-feet old coast-
line, probably the earlier part of that period. It is just the sort of
collection that might be expected at the depth of a few fathoms along
such a line of shore, were the sea somewhat colder than it is now.

This bed of shells, I should think, must at all events be of later
date than the time when those large moraines were formed in Glen
Spean, which I have described in a former part of this paper; for
the glacier of Glen Nevis, when at a corresponding state of develop-
ment (and probably the ice of the Great Glen itself), could not but
have extended past this spot, and would have consequently destroyed
this shell-bed, seeing that there was nothing to shelter it.

The Scandinavian peninsula ought at that time to have had a
development of glaciers corresponding to its higher latitude and
elevation. Are we therefore to suppose that the elevated beds of
arctic shells and raised beaches described by Keilhau, Bravais, Lyell,
and others, occurring along many of the fiords from the Naze to the
North Cape—are we to suppose these to be posterior to the time of our
latest glaciers? How otherwise could so many of them have escaped
destruction by the ice, those, for example, near Trondheim and on
the coast of Finmark? If the glaciers that formed the large moraines
in Glen Spean were later than the chief submergence which covered
so much of Ireland and Britain, and left its arctic shells hundreds of
feet above our present coast-line, then surely an equivalent extension
of the ice in Scandinavia would have swept these Norwegian beaches
and shell-beds out of the positions where many of them occur.
Might we therefore synchronize some of these with our old 40-feet
coast-line of Argyleshire and its northern shells? This would indi-
cate a greater elevation of the land to the eastward since the time
of that old beach.

§ 4. Height and Horizontality of the Parallel Roads.

We are indebted to Mr. Robert Chambers for the first good mea-
surement of the height of the lowest line. Mr. Joseph Mitchell, C.E.,
of Inverness, at his request sent Mr. William Paterson, one of his
surveyors, to carry a series of levellings up to it from Loch Lochy.
The result gave 847 feet above the sea for the height of the lowest
of the Parallel Roads of Glen Roy. The measurement seems to have
been taken at the western extremity of the line, and, so far as I can
learn, would seem to refer to high-water-mark, although this is
perhaps uncertain. The space between the lowest and the middle
line of Glen Roy was levelled by Dr. Macculloch and by Mr. D.
Stevenson and found by both to be 212 feet, thus giving (847+212)
1059 for the height of the middle line. The distance between the
middle and the uppermost line is, according to Macculloch, 82 feet,
and according to Mr. Stevenson, 80. Taking the mean of these, we
get (1059+ 81) 1140 feet above the sea for the highest Glen Roy line.

256 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 21,

The space between the highest Glen Roy line and the one in Glen
Gluoy does not appear to have been so carefully ascertained. Sir
Thos. Lauder-Dick states it at 12 feet. Dr. Macculloch, who in this
case used a barometer, also makes it 12 feet; but Messrs. Chambers
and Milne-Home found it to be fully 29 feet. There is a fainter
trace of a lower line in Glen Gluoy, which, according to Mr. Easton,
C.E., is 200 feet below the upper one. I find that a rough aneroid
observation of my own made the distance between them a few yards
more. Professor Rogers also made some measurements of the Glen
Gluoy lines, and found that neither of them corresponds with those
in Glen Roy, but I have not seen any detail of his results.

The shelf in the gully near Kilfinnan is, according to the baro-
metrical measurement of Mr. Darwin, 40 feet above the highest Glen
Roy line.

The Ordnance Survey haying carried a line of spirit-levelling along
the Loch Laggan road from Dalwhinnie to Spean Bridge in 1858, I
availed myself of their bench-marks to test the height and horizon-
tality of the lowest line, which extends into Glen Spean. The bench-
mark on Roy Bridge is 308:97 feet above the mean sea-level at
Liverpool, or say, in round numbers, 309 feet. From this point I
carried a line of spirit-levelling up to the inner angle, or upper border,
of the terrace of the lowest Parallel Road on the west side of an ad-
joining eminence called Meal Derry, and found it to be 545 feet
above the Ordnance-mark on Roy Bridge. The terrace here is rudely

marked, and so obscure when one is upon it, that its upper outline
could not be ascertained within a foot or two; I therefore took sights
to various parts of the line in the immediate neighbourhood where it
was best defined, namely, on Ben Chlinaig and on Bohuntine Hill,
and found that I could not anywhere safely make the upper rim of
the marking exceed the height I have mentioned. This then gives
(5454309) 854 feet above the mean level of the sea for the height
of the line in the neighbourhood of Roy Bridge. If Mr. Chambers’s
height 1s above high - water, this would just about correspond with
his ‘statement.

I next went to the delta at the mouth of the Rough Burn, which
is about six miles east from Roy Bridge, and found the upper border
of the same line there (which is distinctly marked on the west side
of that delta) to be fully 10 feet higher than an Ordnance bench-
mark on the road near it. This bench-mark is 851 feet above the
mean sea-level, which gives 861 feet for the height of the line. The
trace of the same line at Inverlaire, which is clearly seen from this
spot, seemed to be equally high. But the top of the terraces at the
end of Loch Treig was distinctly higher; as nearly as I could ascer-
tain, they are about 885 or 888 feet. This fact I have mentioned in
a former part of this paper.

The breadth or vertical height of the line on the delta of the
Rough Burn is about 6 feet, so that its lower border is higher than
the upper border of the same line in the neighbourhood of Roy Bridge.

Assuming then the Ordnance-levellings to be perfectly trustworthy,
this would seem to show that the lowest of the Parallel Roads rises

1863. ] JAMIESON——PARALLEL ROADS OF GLEN ROY. 257

slightly—or about 1 foot in a mile—as we trace it eastward. Iwas
unfortunately unaware of the Ordnance-levellings when at Loch
Laggan and Makoul, otherwise I should have tested this point there,
but hope to be able to do so at some future time. Mr. Milne-Home,
however, says that, by barometrical measurement, the height of the
line is 21 feet above the highest point of the channel at Makoul, and
as the Ordnance-levelling indicates 851 feet for the height of the
watershed there, this would give (851+ 21) 872 feet for the altitude
of the line at Makoul. There is therefore some ground for suspecting
that this rise to the eastward extends to Makoul, and in a similar
proportion to the horizontal distance. The verification of this inter-
esting question, however, requires further investigation. Should a
rise to the eastward be actually established, one might speculate upon
its connexion with what I have hinted concerning the raised beaches
and shell-beds of Norway.

§ 5. Objections to a Dam of Ice.

The greatest difficulty that I find in supposing the Parallel
Roads to have been formed by glacier-dammed lakes arises from a
consideration of the depth of water the ice had to retain; for it is
evident the moraines were too insignificant to have done much of the
duty. One might think the hydrostatic pressure of a column of
water some hundreds of feet high would have forced an escape
beneath the ice. If, however, the height or thickness of the glacier
were sufficiently in excess of the depth of water, I imagine there
would be pressure enough to keep it in. The difficulty may also be
lessened by supposing the grinding of the ice to have considerably
deepened the bottom of the Great Glen since the time of at least the
higher lines.

Some low rocky eminences stretch across the mouth of Glen
Spean and Glen Gluoy, and may have blocked them up to some
extent before the gaps around them were ground out by the ice.
Our knowledge of glacier-action is but recently acquired, and has
been derived chiefly from a study of one region, namely Switzerland.
Until a country like Greenland or Spitzbergen has been examined,
our acquaintance with the geological effects of land-ice will be very
imperfect. I, therefore, do not think the objection I have stated is
sufficient to counterbalance the amount of evidence in favour of the
theory.

§ 6. Central Asia during the Glacial Period.

If I am right in my explanation of these Glen Roy lines, it is
clear that many stratified accumulations, presenting all the features
of aqueous deposits, might be heaped up in pools or lakes confined
by the ice in situations where, without this agency, we could not
fancy any body of fresh water to have existed. I have no doubt
this has been a fertile source of delusion in countries formerly over-
spread with glaciers. In such regions many of the supposed proofs
of the former presence of the sea far inland, and at great heights,
whether drawn from parallel roads, perched boulders, gravel ter-

258 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan, 21,

races, or stratified beds of earthy matter, are inconclusive. And I
think Dr. Hooker, in his valuable ‘ Himalayan Journal,’ has rightly
explained, by glacier-action, many such phenomena in the Sikkim
valleys. From the disposition of the rivers and the mountains in
Northern India and Thibet, it seems to me that there may have
arisen some glacier-lakes in those countries on a very large scale.
The great alluvial plain of the Upper Sutlej, for example, which
Col. Strachey has described and referred to marine action, may
haye been accumulated in a great lake dammed up by glaciers and
moraine-matter from the high mountains below Bekhar*. The
upper reach of the Bramahpootra and many other valleys may have
been blocked up in a similar way.

More important effects, however, than these must have flowed
from the refrigeration of the climate of Central Asia during the
glacial period, and which I have not seen noticed. The great basin
of the continental streams, larger than the area of Europe, is re-
markable for its inland lakes from whence no streams ever reach
the ocean, owing to the great heat drying up the water. Now this
heat and dryness being much lessened during the glacial period,
there must have resulted a much smaller evaporation, which would
no longer balance the inflow. These lakes therefore would swell
and rise in level, and thus the Caspian, the Aral, and the Balkash
might have spread until they became more or less connected into a
wide inland sea, discharging its overplus into the Euxine, or along
that depression skirting the east flank of the Ural noticed by Hum-
boldt. This rise of the Caspian, damming back the waters of the
Volga and other streams, would occasion large deposits of alluvial
matter over the surrounding flat regions, and account for many of
the freshwater beds that occur there. The other great Asiatic de-
pression to the north of the Kuenlun Mountains would likewise be
filled up with water, and it is somewhat curious to find that the
Chinese have a tradition that Lake Lhop once drained into the
Hoang Ho.

The sandy deserts of Central Asia are probably the dried-up beds
of these inland seas,

§ 7. Intensity of Glacial Action on the West side of Scotland.

So far as I have observed, the traces of glacier-action are much
more striking in the West Highlands than in the east of Scotland. It
has occurred to me that as the amount of rain along the west coast
far exceeds that on the east, so in former times the precipitation of
snow may have been in like excess. Hence larger glaciers would
be the result. The volume of the streams in Lochaber in relation

* Quart. Journ. Geol. Soe. vol. vii. pp. 306-308. Since writing the above, I
have read Dr. Thomson’s description of this locality in his ‘ Travels in W. Hima-
laya and Tibet,’ and his account confirms me in the opinion above expressed.
The ice of the Piti and Parang valleys has been probably instrumental in dam-
ming the Sutlej near Lio. The lacustrine clays of the Upper Indus may like-
wise be explained by supposing that valley to have been blocked up below Rondu
by the ice of the Gilgit valley, whose glacier seems still to descend lower than
any other in the W. Himalaya. (See 'Thomson’s Travels, 1852, p. 482.)

1863. | JAMIESON—PARALLEL ROADS OF GLEN ROY. 259

to the areas they drain often drew my attention, and the wetness
of the climate is (eaperto crede) something remarkable. During the
glacial period the west side of Scotland may have also had a greater
relative elevation, which would further increase the size of the
glaciers.

The clearness of the evidence in Lochaber leads me to think that
those accumulations in the glens of Braemar which I examined and
described in 1859, and of whose origin I then felt doubtful, cannot
be marine, but must be attributed to freshwater action and the
agency of glaciers*.

§ 8. Recapitulation.

To recapitulate, then, the following are the conclusions I have
been led to by my examination of Lochaber :—

1st. That the Parallel Roads are the beaches of freshwater lakes.

2nd. That these lakes seem to have arisen from glaciers damming
the mouths of the valleys and reversing their drainage.

3rd. That the date of these lakes is posterior to the great land-
glaciation of Scotland.

4th. That neither the sea nor any diluvial catastrophe has, since
the time of the lakes, approached the 850-feet line, Therefore the
chief submergence of the glacial period must have preceded the
formation of the roads, or else not haye been so extensive as to
reach them.

5th. The glens of Ben Nevis do not appear to have been occupied
by the sea since the glaciers finally left them.

6th. The 40-feet raised beach of Argyleshire extends to Fort
William, and is later than the large glaciers.

7th. The Mollusca of this old 40-feet coast-line were of a more
northern character than those now inhabiting our shores.

I hope some geologists who have studied glacier-action may be
induced to yisit this most interesting tract, and either confirm or
disprove the above conclusions,

For the information of intending visitors, I may mention that there
is an inn at Spean Bridge, and another at the east end of Loch Lag-
gan; also one of smaller size at Bridge of Roy. The locality can be
best approached by leaving the Caledonian Canal steamer at Gair-
lochy, near the mouth of the Spean, and walking or driving up to
Spean Bridge, a distance of three miles. There are good hotels at
Bannavie and Fort William. |

* Even the deep mass of stratified matter on the flank of Meal Uin, near
Killiecrankie, described by me in the Quart. Journ. Geol. Soc. vol. xvi. p. 359,
and which I thought a good evidence of marine action, from the insuperable
difficulties of supposing any ordinary freshwater lake to have existed in that
locality capable of explaining it, may possibly be accounted for by supposing it
to have been lodged in a deep pool filling the gully, and confined between the
mountain and the side of a large glacier occupying the valley of the Tummel.—
See Charpentier’s Essai sur les Glaciers, p. 64, for an explanation of similar
occurrences in the Alps; also Lyell’s Antiquity of Man, p. 245; and Agassiz,
Etudes sur les Glaciers, pp, 217-288.

260 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 4,

Frpruary 4, 1863.

William Babington, Esq., and Clement Le Neve Foster, Esq.,
Geological Survey of Great Britain, 28 Jermyn Street, 8.W., were
elected Fellows.

The following communications were read :—

1. On a Wymna-pen at Wooxry Horr, near Watts. No. Il. By
W. Boro Dawkins, Esq., B.A. Oxon., F.G.S., of the Geological
Survey of Great Britain.

ConTENTS.
I. Introduction. 3. Introduction of the Organic
II. Excavation of the Cave. Remains into the Cave.
1. The Antrum. 4, Position of some of the Re-
2. The Passage B. mains.
3. The Passage C. 5. Introduction of Red Earth.
4. The Passage D. B. Special description.
5. The Vertical Passage H. 1. Jaws and Teeth of Carnivora.
6. The Physical Features of the 2. Perissodactyla.
Cave. 3. Artiodactyla.
III. Organic Remains. 4. Proboscidea.
A. General Review. IV. Results of the Excavations.
1, Table showing the distribution J. The ancient Physical Geogra-
of the Bones. phy of the district.
2. Table showing the distribution 2. Evidences of Human Occupa-
of the Jaws and Teeth. tion.

&. Conclusion,

§ I. Introduction.

Freire certain that the results of my former imperfect excavation
of the Wookey Hole Hyzna-den, already brought before the Society*,
were but the earnest of further discoveries, I, together with Mr.
James Parker, of Oxford, and Mr. Henry Catt, of Brighton, deter-
mined to explore the cave thoroughly, and to convey its contents
completely out. This we were enabled to do in April and May last,
by the courtesy of its owner, Mr. Hodgekinson.

§ IL. Excavation of the Cave.

1. The Antrum.—We commenced by completely clearing out the
large antrum or entrance-hall (see fig. 1). On the left-hand side,
and near the entrance, we discovered teeth of Ursus speleus, Mam-
moth, Hyena spelea, and especially of Rhinoceros tichorhinus, which
greatly predominated over the rest. Associated with these were
numerous implements and a few ashes of bone. The area where
these were found is represented in the ground-plan (a, fig. 1). As
we dug our way towards the vertical passage F (see figs. 1 and 3), we
found that the cave extended between it and the left lateral branch
A. Here a tusk of Elephas primigenius was discovered, about 2 feet
5 inches in length, and greatly incurved. Its position is shown by
the transverse section (fig. 2).

* Quart, Journ. Geol. Soe, vol, xviii. p. 115.

1863. ] DAWKINS—HYENA-DEN NEAR WELLS. 261

Fig. 1.—Ground-plan of the Hyena-den at Wookey Hole.

Dolomitic conglomerate. Position of the traces of man.

Undisturbed red earth.

Bone-bed *,

. Upward-tending Branch.
. Left lateral Passage.

. Upward-tending Branch.
. Right-hand Branch of B.
Vertical Passage.

. Vertical Fissure.

- ——. The numbers attached to these lines of section correspond
with those of the figures in which the sections are given.

~------------ . The figures attached to these lines give the breadth and
height of the cave in feet and inches.

gH Yan >

* These explanations also refer to the same symbols, where they occur, in the
following figures.

VOG, Xik——P An. 1. Tt

262 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 4,

Fig. 2.—Transverse Section in the Antrum of Wookey Hole.

a. Roof.

b. Red earth, containing a large quantity of stones, and but
few organic remains, 2 feet in thickness, and extending
within 1 or 2 inches of the roof.

e. Red earth, with irregular layers of album greecum and
peroxide of manganese, and containing the Elephant’s
tusk, together with teeth, and numerous splinters of
bone; 7 to 8 inches.

d. Red earth, containing stones and a few organic remains ;
4, feet.

e. Floor, worn by water and corroded by carbonic acid.

On the right-hand side of the cave we found some more imple-
ments, at the spot marked ¢ in fig. 1, underlying layers of peroxide
of manganese and comminuted bone, as in the case of those which I
described in my former paper.

Fig. 3.—Longitudinal Section in the Antrum of Wookey Hole.
N.N.W. 8.S.E.

= Grey clay, containing stones,

, Red earth, contaming
but no bones *.

stones and bones.

The longitudinal section (fig. 3), taken along the line marked 3—3
in the ground-plan (fig. 1), shows the relation which the flints of
area c held to the contents of the cave—the scattered bones and
stones,—the complete filling-up of the cave to its roof; and the
change in the colour of the sediment in, and the absence of organic
remains from, the vertical passage F, described in my former paper.

We had now cleared out every portion of the antrum except that
between A and F, and had found that the contents extended up to
the roof everywhere except in this latter locality, where there was
an interval of from three to four inches. This interval was traversed
by stalactites, which formed in some places a smooth undulating
drapery with stony tassels, in others miniature pillars extending
down to the débris and, as it were, propping up the roof. Their
pedestals, as they gradually expanded upon the débris, formed round
plates of stalagmite, and, where they met, became a continuous

* These explanations also refer to the same symbols in the following figures.

1863. | DAWKINS-—HYENA-DEN NEAR WELLS. 263

crust—the “ pie-crust” of Dr. Buckland. In this interval were
hazel-nuts, bearing tooth-marks of Rodents, together with the bones
of recent Frogs. With this exception, the section was the same as
the transverse section, fig. 2. The layers of album grecum con-
tained round balls, as at Kirkdale. The splinters of bone at this point
began to increase in size, and became also, proportionately, more
numerous than the teeth. In places an infiltration of carbonate of
lime had cemented organic remains, stones, and matrix into one hard
mass. In one fragment of this breccia, now in the Brighton Museum,
are a tusk and a carpal of Hlephas primigenius, the coronoid process of
the right ulna of Rhinoceros tichorhinus, and the base of the antler
of Cervus Guettardi *; in another, the shaft of the radius of a Rhi-
noceros, side by side with the antler of Cervus Bucklandi—a second
variety of Reindeer ; in a third, two scapule, an ilium, and ischium
of Rhinoceros tichorhinus, together with a coprolite and the lower
jaw of Hyena spelea. The vertical passage F now took the form of
an oblique fissure, which presented every appearance of being con-
nected with some rabbit-burrows vertically above it.

2. The Passage B.—We were now at the entrance of the small
constricted passage B (see figs. 1 and 4), which branches off almost

Fig. 4.—Longitudinal Section of the Passage B.

a. Dark-red earth. e. Red earth, containing stones
6. Bone-bed. and a few bones.

at right angles to the antrum. A spot a little to its right gave the
following section, fig. 5.

Fig. 5.—Transverse Section of the Passage B.

a. Roof.

b. Red earth, containing stones and but few bones, 1 foot
8 inches in thickness, ata distance of from 4 to 5 inches
from the roof, and under a crust of stalagmite.

. A mass of conglomerate fallen from the roof.

. Red earth, with irregular layers of album grecum and
large stones, which are a continuation of those men-
tioned in the previous section.

e. Red earth, full of stones, and containing but few bones.

J- Ploor.

29

As we dug our way deeper inwards, the stalagmitic crusts became

* T have retained this term for a variety of C. tarandus, as sanctioned by the
usage of Dr. Falconer, in his paper on the Gower Caves, Quart. Journ. Geol.
Soe. vol. vi. p. 489.

T2

264 PROCEBDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 4,

more and more intermittent, until they were reduced to a few
rounded pedestals. At this point began the bone-bed, a layer of
matted bones, teeth, and coprolites, in all stages of decay; some
perfectly sound, others too much decomposed to be handled (see
figs. 1 and 4). Its relation to the other members of the same sec-
tion is as follows:—Immediately upon the water-worn and acid-
worn conglomerate-floor was red earth (e, figs. 4 and 6), 2 feet in
thickness, and, as usual, containing few organic remains, but nu-
merous stones; upon this lay the bone-bed (6), from 3 to 4 inches
thick, with the junction-line rather irregular, and containing a few
stones in its lower part ; next came a layer of dark-red earth (a), from
3 to 4 inches thick, very loose and friable, and having upon the
surface a few rounded stalagmites, and a few stalactitic pillars ex-
tending through the interval of from 3 to 4 inches, which separated
it from the roof.

The bone-bed extended
horizontally across the pas-
sage, with an average width

Fig. 6.—Transverse Section across
the Passage B.

of 7 feet and a length of eer en! rears anne
14 feet, affording, therefore, > 7s." eee _—
a square area of 98 feet. .-| i
The enormous quantity of :-< =

organic remains present can-
not be estimated even by the
large number we have pre- oil eee es
served. The 243 bones, the See ee ee
64 jaws, and 240 teeth ob-
tained from it are to be ‘f pares earth. || Je: Het cakes:

. ne-bdeda. stones .
looked per merely geen: i bs Undisturbed red carte
small fraction of the whole.

3. The Passage C.—Having now exhausted the bone-bed, as we
worked onwards we found that the passage B bifurcated, the smaller
branch, C (see fig. 1), going onwards and gently upwards, the larger
branch, D, stretching at right angles from it, and having a gentle
dip of 6° to the south. In the former we met with a second bone-bed
(see figs. 1 and 4), which continued undiminished in thickness until it
rested upon the floor, and thinned out at a distance of 5 feet from
the bifurcation. At the entrance of C the section was identical
with that in B, the red earth (rather more clayey, and containing
more stones) resting upon the acid-worn and water-worn floor, and
supporting the bone-bed, immediately above which was a thin layer
of dark friable earth. This, at the further end, owing to the thin-
ning out of the beds underneath, was superimposed directly upon
the floor, until it hkewise thinned out. The bone-bed extended
through the whole width of C, affording a square area of about 15
feet. Besides bones, it yielded 8 jaws of Hyena, and 46 teeth and
41 bones of various animals. The passage was but 15 or 16 inches
high, and about 3 feet in width; it gradually narrowed until, at a
distance of 12 feet from the bifurcation, a stalactite, about 6 inches

1863. | DAWKINS—HYZNA-DEN NEAR WELLS. 265

long, had reached the floor and formed a vertical bar, as if to forbid
further ingress. The last portion of this branch, for a distance of
about 6 feet, was perfectly free from sediment, and was covered
here and there with stalagmitic crusts.

4. The Passage D.—Having explored C as far as we could crawl,
we commenced clearing out D, and discovered a third layer of or-
ganic remains presenting the same section as the former bone-beds,
except that the dark layer was absent in places, and the bone-bed
was in immediate contact with the roof. Besides an enormous
quantity of bones, it yielded 45 jaws and 120 teeth. It occupied
the whole of the width of D, and its edge rested on the floor of the
eastern side. Its average width was 6 feet, its length 14 feet; and
its square area was, therefore, 84 feet (see figs. 1 and 7).

Fig. 7.—Longitudinal Section of the Fig. 8.—Transverse Section in
Passage D. the Vertical Passage K.

n

f. Sand. d. Grey clay.
For the explanation of the other symbols see Figs. 2-6.

As we approached the further end of the bone-bed, the red earth
became of a paler hue and of greater tenacity; the stones also be-
came larger, and the organic remains more rare. At its further edge
was a layer of fine sand (f, fig. 7), 4 inches in thickness, underlying
grey clay (d), full of large stones, and containing a few large bones.
This latter extended completely up to the roof (see fig. 7), and was
20 inches in thickness.

5. The Vertical Passage E.—¥From this point up to the vertical
passage E (see fig. 7), a distance of 4 feet, there was not the slightest
vestige of bones or teeth. The stiff grey clay (d, fig. 8) rested upon
the horizontal layer of sand on the floor of the cave (f). In the
former a most beautifully polished piece of chert from the Mountain-
limestone was found, which, as its surface is very irregular, appears
to owe its polish to friction upon some soft substance. Dr. Buckland
would have called it a rubbing-stone*. In the latter, also, there
were numerous angular pieces of chert from the Mountain-limestone,
associated with peroxide of manganese. The vertical passage took
the form of a vault (fig. 7), 6 feet in height and 4 in width, and was
represented overhead by an opening, 1 square foot in extent. Here
our exploration ended.

* In the bears’ dens of Zahnloch and Gailenreuth similar traces of polishing
were found, which Dr. Buckland assigns, without hesitation, ‘to the skin and
paws of antediluvian bears” (Relig. Diluv., second edition, pp. 132, 137).

266 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 4,

6. The Physical Features of the Cave-—The ground-plan* and
sections exhibit the more important features of the cave, namely,
the horizontal antrum traversed by a fissure filled with cale-spar,
side by side with the “‘ step” of conglomerate; the oblique and but
partially filled passage C, similar in these respects also to A; the
vertical and completely filled passages E and F, totally devoid of
organic remains and full of grey clay; the places where the contents
have not been disturbed, and many other phenomena which brevity
compels me to pass over.

§ IIL. Organic Remains.
A. GrnerAL Review.

1. Table showing the Distribution of the Bones in the Cave.

| Antrum. | Passage B, Passage C. Passage D.| Total.
CARNIVORA. | 7
Hyena spelexa ......... 4 4 1 5 14
Welige): (ooo 2s eta. 1 2 As 3 6
Ursuseese. oer ee ee. 1 : ane 1
Meles taxus .....02.062 1 1
Canis fupus' ..2.2..00222 92 4 6
C.. vulpes: tsc<h. here 3 3
PROBOSCIDEA.
Elephas primigenius... 4 2 1 3 10
PERISSODACTYLA.
Rhinoceros tichorhinus) 32 144 22 38 236
WQUUB) feser 2 San asent nso 6 33 3 | 3 45
ARTIODACTYLA, ‘

Bose Sek ede ass 12 27 10 LIA 66
Cervus tarandus } ...... “pe SE oar ets os
Ca elaphus $< se5 << Bes ee es sa sit

| Ceryusy, Si. ware seas 8 20 4 9 41

| S$ —|—__——-

otal 7 .ses6/s ants 73 233 41 82 429
|

* For many of the measurements in the ground-plan I am indebted to my
partner in the work, Mr. James Parker.

t The absolute accuracy of these numbers is not to be depended upon, on
account of the great difficulty in discriminating between the carpals and tarsals
of the larger Deer and those of the smaller Oxen.

t The skull of a Reindeer bearing an antler of Cervus Guettardi, in the Taunton
Museum, proves that the latter is a variety of the former. Cervus Bucklandi,
Owen, a species based upon a small fragment of antler, and characterized by the
brow-antler being “34 inches from the lower extremity or base ’’ of the beam
[Owen, Foss. Mamm. fig. 200, p. 485], is by no means satisfactorily separated
from C. tarandus, in which the brow-antler varies greatly even in the same indi-
vidual (see Coll. Surgeons’ Hunt. Cat. 3512). C. Guettardi is probably founded
on a young, and C. Bucklandi on an old antler of the Reindeer.

§ There is no evidence that Strongyloceros speleus is a distinct species from
Cervus elaphus,

1863. ] DAWKINS—HYNA-DEN NEAR WELLS. 267

2. Table showing the Distribution of Jaws and Teeth in the Cave.

Antrum. |Passage B.| Passage C.|Passage D.| Total.

CARNIVORA. Jaws. Teeth.| Jaws. Teeth. J aws. Teeth,|Jaws. Teeth.|Jaws. Teeth.
Hyeena spelea ......... 26 229; 46 67/ 8 7| 41 39 121 342
Welis'spelita 60.) .252...)3-: balls Aas te oe OSLO ESS Br ss 9
ST a es re eres (eee BE Bbetih a) bended Wy cise fit aes ves 1 ce 1
Ursus speleus ..... ... De die lat Retehet aS ol. 24
Prats AECIOB ........5<<3| ++- Dea ace co ate bone lcs 1
UU la ee 1 Dae Rl ee ee ee eet 2
Canis lupus ............ 1 aod cos (em) PEROT eI eng NIA.
PRBMUMDES (i poccsie.5..05, MNMON A ee PU Ne alee OE Wee breee hele ad etd er) 2

PROBOSCIDEA.
Elephas primigenius...} ... Poy ke. Flere wists. lao, OO
PERISSODACTYLA.
Rhinoceros tichorhinus!s 38 88] 4 63]... 10]... 29] 7 190
R. hemitcechus, Fale...| ... i FS ae 2S Ral ew Seana oe 1
EG gos oce cover ic asien)- vos ZU A OB ns. ~ BA act ORL GA . S62
ARTIODACTYLA.

Bos primigenius ......| ... 14]... 3 see Bil Ose EL) Pea TES
(Pa | es eee MS icce teed deen lip tet paktoteltaece iW eto I aud 1
Megaceros hibernicus | 2 18) 7 4} aa A ee em
Cervus tarandus* ...... SE) ma te se ace dh Geta alta Rae (nai ih Sted Dh trees
EO rs ora
hl eas ae a 7

(i) 39 612) 64 236] 8 46) 44 120 1/155 1014

3. Introduction of the Organic Remains into the Cave.—I shall
now briefly consider the method by which the contents of the cave
were introduced ; and first the organic remains.

The 800 or 1000 bones, including splinters, which we obtained,
form no index to the vast quantity that crumbled to pieces on expo-
sure to the air. Table No. 1 shows the distribution of the 429
which I have catalogued; and Table No. 2 shows the distribution
of the teeth and jaws in the cave. A glance at them will show
that, on the whole, the remains of any given animal, if abundant,
are not confined to one spot in the cave, but are pretty evenly dis-
tributed, and lie large with small, the more with the less dense,
not in the least degree sorted by water. There is no evidence of the
Bear succeeding to the Hyzna, or the Felis to the Bear, in the occu-
pation of the cave; or that the latter retired hither to die, as in
some of the caves of Germany; or that any of the Herbivores fell
into the open swallow-holes, and so left their remains, as in the
Hutton and Plymouth caves. On the contrary, the numerous jaws
and teeth of Hycna, the marks of those teeth upon every one of the
800 to 1000 bones, upon the 155 jaws, and even upon the great

* C. Guettardi and C. Bucklandi are merely varieties of C. tarandus, under
which they are here classed.
t See Buckland, Rel. Diluy.

268 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 4,

majority of the teeth, show that they alone introduced the remains
which were found in such abundance.

4. Position of some of the Remains.—A glance, however, at the
vertical sections will show that some of the remains are not now in
the exact position they occupied in the days of the Hyzna. The
maximum distance of the bone-layers from the roof is but eight
inches, a space manifestly too small to allow of the Hyzena devour-
ing his prey ; while in many instances the remains actually touched
the roof. This, indeed, has been used as an argument in favour of
their having been introduced by water from some unknown reposi-
tory. On this supposition the introducing current of water must
either have passed down the vertical passages or through the hori-
zontal mouth of the antrum. In the former case the three bone-
layers would not have been found in the narrow passages, but would
have been swept out into the wide antrum, where the force of the
hypothetical current must have abated. In the latter case the great
bulk of the remains would have been found in the antrum, and not
in the smaller passages and innermost crannies of the cave. But,
apart from this evidence, the absence of marks of watery action
upon the organic remains, and especially of that sorting action which
water, as a conveying agent, always manifests, and in no case more
remarkably than in the lower jaws of the Stonesfield Mammals,
makes the hypothesis of their introduction by water untenable *.

The evidence, indeed, as to the cause of the position of some of
the remains is most conflicting. Their condition, their distribution
in the cave, and especially the presence of two gnawed rami of the
same lower jaw of Hyena, found a few feet apart in the passage B,
of two gnawed fragments of the same upper jaw of the Irish
Elk, also found apart in the passage D, of the right and left lower
molars of the same Elephant, and the right upper and lower molars
of a second, also in the passage D, all prove that the organic remains
were not introduced by water. On the other hand, the horizontality
of the layers, the presence of layers of peroxide of manganese, of
the red sediment, and of the sand, show that water certainly was
an agent in rearranging and introducing some of the contents of the
cave. The only solution of this difficulty that I can hazard is the
occurrence of floods during the occupation by the Hyznas, and per-
haps for some time afterwards, similar to those which now, from
time to time, take place in the caverns of the neighbourhood.

5. Introduction of the Red Earth.—A few years ago the outlet of
the stream flowing through the great cavern at Wookey Hole was
blocked up, and the water rose in it to a height of upwards of sixteen
feet, and left a horizontal deposit of red earth similar, in every
particular, to that of the Hysna-den. Now, if we suppose that
similar floods were caused by an obstruction in the ravine below
the Hyzna-den, it may have been flooded just as the upper galleries

* The caverns of the Liége district, explored by Dr. Schmerling, were filled,
without exception, by the action of water, and contain in many cases water-worn
bones. Schmerling, Recherches sur les Ossements Fossiles découverts dans les
Cavernes de la Province de Liége, vol. 1. pp. 18, 19.

1863. ] DAWKINS—-HYZNA-DEN NEAR WELLS. 269

of the great cave; and the water, laden with sediment, entering from
time to time, might have elevated the layers of matted bone and all
the scattered remains on the surface, while the current was insuffi-
cient to disturb the stones or to affect, to any extent, the deposit of
former floods. The buoyancy of the organic remains is not required
to be greater by this hypothesis than is demanded by that of their
having been introduced by a current through the swallow-holes.

But if water introduced the red earth, it is certain that it had
nothing to do with the introduction of the stones. As the red
calcareo-magnesian cement of the dolomitic conglomerate supplied
the red earth, so did its imbedded pebbles of limestone supply the
latter. Either angular or water-worn, they are in the same state
as they were when they formed integral parts of the roof, sides, and
floor of the cave, with the exception that they have been worn by
carbonic acid, and exhibit a network of calc-spar, stems of Crinoids,
and shells of Spirifers in strong relief. It is needless to repeat that,
had they been once set in motion, these organic remains must have
been ground to powder.

B. Sprciat Description.

1. Jaws and Teeth of Carnivora.—t shall pass on now to a brief
consideration of the jaws and teeth, omitting, for the sake of brevity,
all mention of the bones. Amongst the Carnivora*, Felis spelea is
represented by four teeth of the molar series, and six canines. As
the difference in the length of the crown of the large upper canine
as compared with the largest of the lower ones (1:1 inch) is greater
than the difference in an adult tiger (0-4), these teeth may indicate the
presence of two species. This difference is, I think, too great to be
owing to mere sexual peculiarities. There is no evidence as to
whether they belonged to the Lion or the Tiger; for P.M.3, in
its size, approaches the corresponding tooth of Felis tigris; in the

* Comparative Measurements of Canines of Felide and Urside.

S &¢ |e |e
pels |g ae hs
= =| pina | ian =| .
et eee to te eee
S-S/10 3/8 | 0009/5 &
te Se Se EA Sree | el Ss
e2igezeif Sis osm
35 a ~ Se ey
Rte oie atest ©
6 s 2 o + os o
Slow co) Weir: 38
oe Q | ° re 2\5 o a ¢
8 \"s wos; aH |g
SI | 2 asnml|SPrle
D Gs} oO Oo 7
i gle == aie (= ia A
in. | in. | in. | in. | in
Felis spelea. Upper canine.................68- 5°5 | 3°4 | 2°5 | 3:0 | 3°9 | maximum.
Heliss sp. Lower, Cunine ...0..4. 000. ss 0sesce9ss 4-2 | 2°4 | 1:4 | 2°8 | 2-7 | mmimum.
Ursus speleus. Upper canine................. 6:0 | 3:3 | 1°7 | 4°3 | 4°3 | maximum.
ae re Lower canine................. 5-6 | 3°2 | 1-4 | 42 | 3°7 | maximum.
U. Leodensis (Schmerling). Lower canine | 4°9 | 2°2 | 1:4 | 3°6 | 2°7
J. arctos. Tower canine 22.07.05.65.0 oS AA 24 | 23 |) 31.) 2:5

The upper canine of Felis spelea has the apex of its fang truncated as in a
corresponding tooth of Felis tigris in the Museum of the Royal College of
Surgeons (4535 of Cat.) and as another in the Oxford Museum.

270 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 4,

narrowness of its anterior as compared with its posterior talon, it
approximates to Felis leo.

The 121 jaws and 342 teeth of Hycna spelea, the normal inha-
bitant of the den, show how numerous those animals were, and for
how long a time they inhabited the cave. <A selected set of rami
shows all the changes in their dentition, from youth to old age. The
two oldest have each lost one of their two bone-crushers: the one
has lost P.M.4, and its alveolus is partially filled up; the other has
lost P.M.3, and its alveolus is completely obliterated by osseous
tissue. In the three youngest jaws are seen the stages by which
the small deciduous molars were replaced by the large and perfect
permanent dentition—the most admirable for crushing bone that
could be desired. In one lower jaw ofa Hyena in its prime the per-
fect dentition of the right ramus is preserved; both rami were found
some feet apart in the bone-layer in the passage B. In a second
ramus of an older animal the angle and the greater part of the
coronoid process are preserved—the only instance of their having
escaped the teeth of the Hyzna. In a third, covered with tooth-
marks, the broken M.1 has been partially thrust out of its alveolus by
the teeth of the animal that devoured its possessor. As, however, it
was fortunately exposed on the floor to the calcareous dripping from
the roof, it is firmly cemented in its place by stalagmite. Of the
upper jaws, also arranged according to age, one shows the perfect
premolar series, a second the small true molar which disappears early
in the Hywnide, a third the diseased stump of P.M.4. The in-
flammation resulting from the fracture of the latter has greatly con-
stricted the supraorbital foramen.

The Canide are represented by Canis lupus and C. vulpes. The
three jaws and two teeth of the latter indicate a size similar to that
of the existing species, while the four jaws and three teeth of the
former indicate a superiority of size.

The Melide are represented by Meles tawus, of which one humerus
only was found. This may be of a date far posterior to that of the
other remains.

Of the Urside twenty-seven teeth and two jaws were discovered,
the larger canines equalling, if not surpassing, in size the largest
from Germany; and the molar teeth, of which one upper molar is
larger than any from Gailenreuth or Quinger, in the Bucklandian
Collection, belong to the gigantic Cave-bear, Ursus speleus. A lower
canine also indicates the presence of a second species of Bear,
U. arctos*. Of the equivocal remains, one jaw is closely allied to
that from Bacton in the British Museum?; and a canine with a thin
compressed fang is identical with that figured by Dr. Schmerling as
Ursus leodensist, though slightly larger in every dimension.

* Comp. Schmerling, op. cit. vol. i. pl. 8. p. 8. In the collection of my
friend Dr. Spurrell I recognized a lower canine of U. arctos, from the Crayford
gravel-pits.

t+ Comp. Owen, Brit. Foss. Mamm. fig. 35.8, p. 106.

t Comp. Schmerling, op. cit. vol. i. p. 94, pl. 8. fig. 8. Whether U. leodensis
is a valid species or not, I can offer no opinion.

1863. | DAWKINS—HYENA-DEN NEAR WELLS. 271

The tooth-marks upon the remains of the Carnivores prove that
they were preyed upon by the Hyzenas.

2. Perissodactyla.—Of the Perissodactyle Herbivores, the solidun-
gulate division is represented by Equus fossilis, of which four jaws
and 362 teeth were found, while the multungulate division contains
Rhinoceros tichorhinus and R. hemitechus. Seven jaws and 190
teeth belong to the former of these. The molars present points of
great interest. One series of M.3 shows the inconstant size and
form of the posterior column (Collis tertius of Brandt), which, rudi-
mentary in some, passes gradually to the summit of the crown in
others, and finally, in an abnormal specimen, circumscribes a second
deep cavity on its posterior aspect. One of the M.2 is also abnor-

mal. In it the entrance of the principal valley is closed up, leaving
the valley so characteristic of Rhinoceros as an insulated cavity in
the middle of the tooth. The upper milk-molars are remarkable for
a cusp at the wide entrance of the valley, quoted by Professor Owen
as one of the characteristics of ft. leptorhinus. The lower jaws prove
that in no stage of the dentition was the first premolar developed.
The jaws from Lawford and Thame, figured and described by Pro-
fessor Owen (Brit. Foss. Mamm.) as containing the premolar dentition,
are really young jaws with the deciduous dentition. The first milk-
molar in the Lawford specimen is mistaken for the first premolar,
which, as yet, has not been proved to exist*. Of R. hemitechus but
one fragment of a left upper milk-molar was found, for the identifi-
cation of which I am indebted to Dr. Falconer.

3. Artiodactyla.—The Artiodactyle division of Herbivores is largely
represented. Sixteen teeth attest the presence of Bos primigenius,
while one upper molar, smaller in every dimension than the rest,
may possibly belong to a second species of the Bovide.

Twenty-three teeth and twelve jaws are preserved of Megaceros
hibernicus. One specimen of a right lower ramus shows, besides
the perfect molar series, a curious freak of nature. P.M. 2, instead
of being in its natural position, has come up hind foremost, the ante-
rior part occupying the place of the posterior, the inner side that of
the outer. The fragments of the upper jaw containing M. 1, 2, 3 were
found dissociated in the passage D.

Cervus Guettardi, C. tarandus, and C. Bucklandi are represented
by antlers, some of which have been torn violently from the skull,
and not shed by necrosis, as are all those found at Kirkdale. The
fact that in the Williams Collection, at Taunton, there is a skull of
Cervus tarandus, bearing on the left side an antler? of C. Guettardi,

* Pallas, indeed, and Fischer doubt the existence of the first premolar.
Brandt comes to the conclusion that it is absent from the adult. On the other
hand, Cuvier, without ever having seen it, states that it exists, on the authority of
Adrian Casper ; and Blainville (Ostéographie, p- 107) ascribes four premolars
to R. tichorhinus.

t+ Comparative measurements :—

Right side. Left side.
Burrito beramier’ He Wee Cg ar’ oO”
Ban isiromeadicr se States SO 82. ore, ZOO
Circumference above burr . .. .3 2 2 8
Circumference of brow-antler at base . 1 8 [es

272 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 4,

and on the right its own normal antler, shows that the latter is but
a variety of the former, consequent upon the irregular position of the
brow-antler. The correspondence also of the antler-basements of a
skull belonging to the former with the bases of necrosed antlers of
CO. Bucklandi may indicate that this is a second variety of the same
species, consequent on varying age. Antlers also indicated the pre-
sence of Cervus elaphus. Some of the teeth also correspond with
those of C. elaphus ; but I cannot affirm without hesitation that they
undoubtedly belonged to that animal.

4. Proboscidea.—The twenty-four molars and six tusks of Elephas
primgenius belonged in the main to young individuals. The longest
tusk was 2 feet 5 inches in length; the oldest molar was composed
of seventeen plates, four of which were supported by the anterior
fang.

IV. Results of the Excavations.

1. The Ancient Physical Geography of the District—The group of
animals just noticed throws great light upon the physical geography of
the district in the days of the Hyena. In the absence of the Beaver
and the Otter, of the Water-rat and the Hippopotamus, we may see
that then, as now, there was no river in the immediate vicinity.
The great preponderance of the Horse and Rhinoceros is very remark-
able. The great number of the former, compared with the few in
the Kirkdale Hyzena-den, may perhaps show that they were more
numerous in the west than in the north of England*. Both indi-
cate the existence of an extensive plain in the neighbourhood; while
the various species of Cervide point to woodlands on the flanks of the
Mendips, and encroaching on the plain at their base. But this evi-
dence does not stand alone. The physical configuration of the west
coast of Somerset, the mammalian remains found at low water at
St. Audries, the jaws of Rhinoceros tichorhinus at Taunton, associated
with oak, ash, and alder, prove that a level district extended in those
days, with but lttle interruption, from the Mendips to the Devonian
range of the Quantocks, and advanced westwards into the British
Channel, and possibly into the Atlantic. The higher grounds of
South Wales, in the Mountain-limestone of which bone-caves are so
numerous, probably formed its northern boundary.

The Mountain-limestone borders of this great plain would obviously
be most favourable for the habitation of the large numbers of Car-
nivores—the Hyzenas, the three, if not four, species of Bear, the two
species of Felis, the Foxes, and the Wolves. We should naturally
expect to find them here in greater variety and numbers than in
any less favourable place.

Subsequently to this came a great depression of the district, followed
by a gradual upheaval, the evidences of which time does not permit
me to bring forward. In neither the marine deposits of the one, nor
the lacustrine deposits of the other, have I detected any of the fauna
of the bone-cave, with the exception of the Fox, the Irish Elk, and
the Red Deer. Thus the paleontology of the district shows that the
date of the cave was prior to a submergence of the immediate

* See List of Remains from Kirkdale, ‘ Reliquie Diluviane.’

1863. | DAWKINS—HYZNA-DEN NEAR WELLS. 273

vicinity, while Rhinoceros hemitechus here, as at Kirkdale, associ-
ated with R. tichorhinus, may perhaps refer it to the earlier part of
the newer Pliocene period*.

2. Evidences of Human Occupation.—Let us now pass on to the
evidences of human occupation. All the ashes and implements were
found in positions, near the mouth of the cave, where man himself
may have placed them (see figs. 1 to 8), with the exception of an
ash of bone imbedded in the earthy matrix between the canine tooth
and a coprolite of the Hyzna, and cemented to a fragment of dolo-
mitic conglomerate. This was found far in the cave, either at the
entrance of the passage B or in the middle of the passage D. The
latter passage yielded the only rolled flint without traces of man’s
handiwork. The materials out of which the implements were made
were used pretty equally. All the spear-heads were of flint; all the
sling-stones of chert from the Upper Greensand; while the flakes
consisted of both, used indifferently. Besides these three typical
forms, which were most abundant, is a fourth, im form roughly
pyramidal, with asmooth and flat base, and a cutting edge all round.
Of these we found but two examples, both consisting of chert. In
form they are exactly similar to some hundreds found in a Celtic
village at Stanlake, and to others I discovered in a cemetery of the
same date at Yarnton, near Oxford. They strongly resemble a cast
I have of one found by M. Lartet in the cave of Aurignac. Were it
not for this similarity, I should look upon them as accidental forms.
The rest are mere splinters, irregular in form, and probably made
in the manufacture of the various flint and chert implements. All
the flint implements have been strangely altered in colour and
structure, either by heat or, as is more probable, by some chemical
action. Without exception, the old surfaces present a waxy lustre
(by the absence of which forgeries are easily detected), the colour is
of a uniform milk-white, and the ordinary conchocidal fracture is re-
placed by that of porcelam. Some are not harder than chalk. I
have obtained weathered and calcined flints from Sussex in which
similar changes are observable, and in which the difference in the
results of chemical action and heat can hardly be detected. The
chert implements, on the other hand, show no traces of any such
changes, but are similar in colour and structure to the rocks from
which they came—the Upper Greensand of the Blackdown Hills.

The inferiority of workmanship, on comparison with the imple-
ments of Amiens and Abbeville, and of Hoxne, may possibly indicate
a higher antiquity, and certainly shows that the Wookey Hole savages
were of a lower order than the Flint-folk of the valley of the Somme,
or of Suffolk. If also the complete whitening and the total absence
of conchoidal fracture in these implements, as compared with the
fracture and natural colour of those from the above well-known
localities, in which the decomposition is but skin-deep, and causes
but a waxy lustre, be any evidence of antiquity, the former are of a
far earlier date than the latter.

* Comp. Dr. Falconer, “On the Ossiferous Caves of the Peninsula of Gower,”
Quart. Journ. Geol. Soc. vol. xvi. p. 491.

274 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 4,

All the fragments of calcined bone, with the exception of one
already mentioned, were found near the entrance (see fig. 1), and ina
place more suitable for a fire than any other in the cave. I can
identify none of them as human. ‘The coarse texture, the structure,
and the thickness of one indicate a fragment of a long bone of Rhi-
noceros *, All resemble many splinters strewn about in other parts
of the cave, which are not calcined, but were evidently introduced by
the Hyzenas. The calcination may therefore be due to the accident
of their lying upon the surface at the time the fire was kindled. The
presence .of the ashes indicates the occupation of the cave by man.

3. Conclusion.—The whole body of evidencet tends to prove that
man, in one of the earlier stages of his being, dwelt in this cave ; that
in it he manufactured his implements out of flint from the chalk-
downs of Wilts, and from the less fragile chert from the Greensand
of the Blackdown Hills, and arrow-heads out of the chert and the
more easily fashioned bone; and that, beyond all doubt, he was a
contemporary with the extinct fauna found, with the traces of his
existence, in the cave. Then after an interval, in which much of
the fauna became extinct, and in which the whole of the district
was considerably depressed, we again meet with traces of man in the
coarse pottery and the human teeth found by Dr. Buckland in the
great Wookey Hole cavern{. And, lastly, the discovery of coins of
Allectus, Comes littoris Saxonici, together with skeletons near the
Hyzena-den, brings us down to the fourth or fifth century after
Christ. Thus Paleontology shades off into Archeology, and that into
History, and each, taking up the thread where the other dropped
it, shows the intimate relation between sciences formerly considered
to have little or no bearing upon each other. Until, however, there
are data for estimating the magnitude of the breaks in the suc-
cession, it is impossible to reduce the interval between ourselves and
the Flint-folk to the scale of time used in history. The supplanting
of one species by another, and the oscillations in the level of the
surface, prove that the lapse of time was enormous, but they do not
warrant us in reducing it to any definite number of years.

2. On the Discovery of ParapoxipEs 7m Brirarn.
By J. W. Sartsr, Esq., F.G.S., A.L.S.

Durine a few days’ holiday in South Pembrokeshire last summer, I
went to the neighbourhood of St. David’s. I wished to see the
Cambrian and Lower Silurian beds recently mapped by Mr. T. Ave-
line, and to learn if they presented the same characters as the corre-

* Possibly it may have belonged to Hlephas, but its coarse texture seems to
me to indicate Rhinoceros.

t For arguments on the relation of the traces of man to the organic remains,
see Quart. Journ. Geol. Soc. vol. xviil. p. 119.

{ See Rel. Diluv. p. 165.

1863. ]

SALTER——PARADOXIDES IN BRITAIN.

Paradoxides Davidis (one-half the natural size).

()
ml

UNM!
emu

276 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 4,

sponding beds in North Wales. On this point I hope to have an
opportunity of laying some particulars before the Society. My
object now is only to point out the locality and geological place of a
gigantic Trilobite long looked for in Britain, and lately, I must say
accidentally, found by me. I believed I was working at Solva Har-
bour, in Llandeilo flags*, but by good fortune I had landed instead in
a parallel creek a mile to the westward, at the junction of the red
and purple Cambrian grits with the Lingula-slates.

Porth-rhaw is a small boat-creek, a mile 8. of Whitchurch, on
the St. David’s road. Black slates occur on both sides of it; but on
the west side they pass into and rest upon the red and purple Cam-
brians ; on the east they form magnificent cliffs of vertical or highly
curved slates and flags. Sometimes these cliffs show sheets of rip-
pled rock 150 feet to the water’s edge. Though much curved, the
general dip is to the east and south-east; but I have not traced the
slates further in this direction than the Cradle Rock ; nor could I find
fossils except at one point, where they are in hundreds. This was
at Porth-rhaw, before mentioned, in the black vertical rocks on the
east side of the little creek. A boat may reach them easily ; but,
except at low water, it is not very easy to walk down to them.

The fry of some large Trilobite first attracted my attention, and
then, by looking along the ledges, I found fragments (head, body-
rings, labrum), but none perfect, of the largest species of Paradox-
ides known—scarcely excepting the great P. Harlani, from near
Boston. Agnostus accompanied it as usual, being the smallest, as
Paradoxides is the largest, Trilobite of the Primordial zone.

I shall describe the species (for it is new), with full figures, in a
forthcoming Decade of the Geological Survey; and only now sub-
join a short diagnosis, and a reduced figure from a drawing by Mr.
C. R. Bone.

ParapoxipEs Dayipis, spec. nov.

P. pedalis et ultra, maximus, glabella clavata, sulcis duobus solum perfectis. Oculi
submediant, parvi. Thorax axe fere ut pleura lato, hec recta, apicibus recurvis,
nec abrupte flexis, sulco mediano valde obliquo marginem attingente. Cauda
lata. Labrum angulis eaternis biangulatis.

Locality.—Lower Lingula-flags, Porth-rhaw, St. David’s, Pem-
brokeshire (1862); also Solva Harbour, west side.

There has been a single specimen of Paradowides for a long time
in the Collection of the Geological Survey. It is a much smaller and
more slender species; for P. Davidis is robust in all its parts, and
has a broad axis, like the Bohemian P. spinosus. The small species
in questiont was found in N. Wales by A. C. Selwyn, Esq., now
Director of the Geological Survey of Victoria; but the exact locality
was never ascertained, nor could the species be again met with. I
recommend my North-Welsh friends (after one of whom, conspicuous

* T have since found that the black Lingula-flags, with Paradoxides, extend

to Solva Harbour.
+ P. Forchhammeri (see ‘ Siluria,’ 2nd edit. p. 45, fig. 5, 2).

1863. | WRIGHT—ECHINID OF MALTA. 277

for his zeal and kindness, I name the species*) to work at the lower
black slates in the neighbourhood of Ffestiniog, not far above their
junction with the Cambrian beds, where they will surely meet with
these species.

The following succession of beds, in ascending order, in the Pri-
mordial zone, has now been established in Wales, and it is the same
in South as in North Wales :—

Red and purple grits, becoming intermixed with ; :
some greenish-grey sandstones where they pass up rey) (Geological
into y).

1. Lower Lingula-fiags. —A thick mass of black ( Lingulella, rare.
shales, very uniform in its upper part, but with } Olenus, common.
much sandstone in the lower; probably accumulated | Agnostus, common.
in deep water. Paradoxides Davidis.

2. Middle Lingula-flags.—A thick series of hard | Lingulella Davisit, abun-
light-coloured sandstones, with ripple-markings, dant.
worm-tracks and burrows, and other evidences of ) Olenus, rare.
having been accumulated in shallow water. Hymenocaris, abundant.

( Olenus, many species.

3. Upper Lingula-flags.—A thin series (not more | Agnostus, abundant.
than 300 feet at most) of fine black shales, crowded < Conocephalus.
with small Crustaceans; shells very rare; deep water. | Dikellocephalus.

\ Orthis, small species.

The best general section in the neighbourhood of St. David’s is at
Whitesand Bay, where the Cambrian Rocks and Lingula-flags are
seen to be overlain by a lower member of the Llandeilo formation,
of which and its corresponding beds elsewhere there is not space here
to treat properly ; I hope to do so shortly.

The constant occurrence of the same large forms of Trilobite
(generally, too, accompanied by the minute Agvostus) in the lowest
strata in which anything like a fauna is known, of different species
in each district, and yet distributed so widely in Europe and America,
is surely a curious fact, in any view of the origin or distribution of
species. Both these genera depart widely from the general type of
the Trilobites.

3. On the Fossil Ecurxty x of Matra. By Tuomas Wrieut, M.D.,
F.R.S.E., F.G.8. With Notes on the Miocene Bens of the Istanp ;
by A. Lerrm Apams, A.M., M.B., Surgeon of H.M. 22nd Regiment.

[The publication of this Paper is postponed. ]
(Abstract. )

Tue Echinoderms described in this paper by Dr. Wright were dis-
covered by Dr. Leith Adams during a careful examination of the
strata and geological features of Malta. A description of the Mio-
cene beds was given by the latter gentleman, in which he stated his

* David Homfray, Esq., of Port Madoc, Caernarvonshire, who, together with
Mr. F. Ash of the same place, has for many years successfully explored the Pri-
mordial zone and the overlying beds.

VOL. XIX.—PART I. U

278 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 18,

reasons for not accepting entirely the classification of them proposed
by Captain Spratt, and followed by Earl Ducie in his Geological Map
of the Maltese Islands. He divided the Miocene strata into the
following subdivisions:—1l. The Upper Limestone; 2. The Sand
Bed; 3. The Marl; 4. The Calcareous Sandstone; 5. The Lower
Limestone; and again subdivided the Upper Limestone into three
parts. Dr. Wright gave diagnoses and detailed descriptions of forty
species of Echinide, four of which are new; and Dr, Adams added
a Table showing their stratigraphical distribution.

Fesrvuary 18, 1863.

John Rand Capron, Esq., Guildford; Julius Haast, M.D., Govern-
ment Geologist, Christ Church, Canterbury, New Zealand ; Thomas
Hood Hood, Esq., Member of the Legislative Council of Queensland,
Australia ; John Randall, Esq., Madeley, Salop; and Samuel Wright,
Eisq., Cockermouth, were elected Fellows.

The following communication was read :—

On the Mippir and Upper Litas of the DorsEetsHirE Coast*.
By E. ©. H. Day, Esq.

{Communicated by R. Etheridge, Esq., F.G.S. ]
ConrTENTs.

I. Introduction.
1. Sir H. De la Beche’s subdivision of | 2. The Middle Lias.

the Dorsetshire Lias. 3. The Upper Lias.
I. Descriptions of the Sections.
1. Black Ven. 5. Fourfoot Hill.
2. Stonebarrow Hill and Westhay Cliff. | 6. Burton Cliff.
3. The Golden Cap. 7. Generalized Section.
4. Down Cliffs.
III. Distribution of the Organic Remains.
1. The Belemnite-beds. _7. The Brown Sands and Sandstones.
2. The Green Ammonite-beds. 8. The Marlstone with its Pleuroto-
3. The Three Tiers. maria-bed.
4, The Shell-bed. 9. The Upper Lias Limestone.
5. The Starfish-bed. 10. The Cephalopoda-beds.
6. The Grey and Brown Sands with | 11. Conclusion.
Nodules.

§ L. Introduction.

1. Sir H. De la Beche’s subdivision of the Dorsetshire LInas.—
The only published section giving details of the Lias formation of
Dorsetshire, at present in existence, is one made more than thirty

* For an account of the Lower Lias of Dorsetshire, &., see Quart. Journ. Geol.
Soe. vol. xvi. p. 374, &.; and vol. xvii. p. 494, &e.—Ebpir.

1863. ] DAY—LIAS OF DORSETSHIRE. 279

years ago by the late Sir Henry De la Beche*. When I undertook
the investigation of the geology of the coast in the neighbourhood
of Lyme Regis, I soon found that that section, though according
well with certain general facts, was, owing to the rapid progress of
geological knowledge, and the consequent changes in our system of
classification, utterly useless to students. The divisions and sub-
divisions of De la Beche were founded solely on lithological grounds,
whereas those of the present day are based in great measure upon
paleontological considerations. He classed all our Upper and nearly
half our Middle Lias with the Inferior Oolite Sands +, and he sub-
divided the Lias, as then understood, accordingly. As he had classed
sands with sands, and marls with the Lias, so he divided the latter
into “ Upper Lias Marls ” (which, under the present system, include
both the Middle and Lower Lias Marls), “ Lias Limestones ” (which
correspond to a subdivision of the Lower Lias), and “ Lower Lias
Marls” (which are the ‘‘Avicula contorta series,” no longer regarded
even as Liassic).

The section quoted gave to the entire Lias Formation of Dorset-
shire a thickness of 600 feet; our present acceptation of the term
includes between 1000 and 1100 feet of strata.

The plan which I have adopted, in order to lay clearly before the
Society the extent and character of these deposits, is to give, in the
first place, a description of them lthologically as they appear in the
successive cliffs; and, in the second, to point out, in a generalized
vertical section, the paleontological features which characterize the
subdivisions and strata. To avoid confusion, I will premise what I
understand by the terms Middle and Upper Lias.

2. The Middle Inas.—As this term is now accepted, it may be
defined as that portion of the Lias Formation which les between the
strata containing Ammonites raricostatus, Ziet., as the predominant
form below, and those characterized by Ammonites communis, Sow.,
above.

Thus defined, the Middle Lias of this neighbourhood presents a
mass of beds which, though including two great and Lithologically
well-marked subdivisions, is on the whole very distinct, both in its
lithological appearance and in most of its fossils, from the beds above
and below. The Marlstone and the Middle Lias Sands are generally
understood to occupy this interval, or, at least, the greater part of it,
throughout the South-west of England; but, in the district under
consideration, these beds do not occupy more than two-fifths of the
gap, the larger part being filled up by a mass of marls. Throughout
the rest of England, moreover, I believe the total thickness of this
member of the Lias amounts to much less than in this district, where
it includes upwards of 500 feet of strata.

Such an increased development, and other characters very much

* Geol. Trans. 2nd series, vol.ii. 1829; also, Report on the Geology of Corn-
wall, Devon, and West Somerset, 1839.

t Owing to this classification, fossi!s from the Middle Lias have been given
as from the Inferior Oolite of Bridport (vide Rhynchonella serrata, Pentacrinus
gracilis, &c., in Morris’s Catalogue of British Fossils).

v2

280 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 18,

in accordance with those of the Continental types, appear to ap-
proximate our Middle Lias more closely to foreign equivalents, than
that of any other British section hitherto examined; and this is
what we might expect to find at the point where our English beds
approach nearest in distance to foreign shores ; on the other hand,
such an approximation in character would lead us to hope that we
might here meet with organic forms hitherto supposed peculiar to
the Continental Lias.

3. Lhe Upper Lias.—This division, as defined by Continental
geologists, commences with the strata containing Ammonites com-
munis, Sow., and terminates with those containing A. jurensis, Ziet.
It thus rests upon the zone of A. spinatus, Brug., and is in turn
covered by that of A. Murchisone, Sow. Like the Middle Lias, the
Upper Lias of Dorsetshire presents us with two lithological sub-
divisions, the lower one argillaceous, the upper one sandy; but their
special characters will be given in the sequel.

§ IL. Descriptions of the Sections.

1. Black Ven.—The first section in which the Middle Lias is seen
as we proceed eastward from Lyme Regis, and upwards in the order
of stratification, is in a cliff called Black Ven, situated between Lyme
Regis and Charmouth. Above the beach, nearly opposite the highest
part of the hill, there is a succession of cliffs of Lias capped by Green-
sand (a, fig. 1). The lower portion of these cliffs, to the height of
180 feet, is of a dark slaty-blue colour, and consists of the “‘ Lower
Lias Marls” (7); it contains the zones of Ammonites Brookii, Sow. (the
local equivalent of A. T'urneri, Sow.), A. obtusus, Sow., A. oaynotus,
Quenstedt, and A. raricostatus, Ziet., all well defined. Above these
beds is a mass of marl, forming a cliff or wall, the dull-grey tint of
which strikingly distinguishes it from the darker strata below. This
marl, about 90 feet in thickness, is the lower commencement of the
Middle Lias, as well as its most westward extension upon this coast.

On a closer examination we find, however, that the base of the
above-mentioned wall (2) is blue and not grey, its real colour being
concealed by the crumbling away of the beds above. Nevertheless
the Middle Lias, as above defined, commences at the very base,
where certain Lower Lias fossils cease and Middle Lias forms appear.
This change occurs in some tiers of limestone (2, &) upon which
the wall or cliff rests. Between two of these beds of stone, in about
eighteen inches of marl, a great number of compressed and metallic
specimens of A. raricostatus occur, and this, as far as I know, is the
highest limit of that form. The next alternate layer of marl is full
of Belemnites; and here I think the Belemnite-beds may be fairly
assumed to commence, and with them the Middle Lias.

In the 30 feet of blue marl above (2), a very elongated Belemnite,
B. longissimus, Miller, is the characteristic fossil. This blue marl
gives place to some irregular beds of impure semi-indurated lime-
stones of a grey colour (g), and these are succeeded by grey marls (f),
becoming shaly in the upper portion. The shales (¢), 6 feet thick,
are very full of Belemnites, as is also the thin band of limestone

1863. ] DAY—LIAS OF DORSETSHIRE. 281

(d, the “ Belemnite-stone”’) by which they are capped. Above this
stone there are some 15 or 20 feet more of grey marl (c), upon
which rests the base of the Cretuceous Series.

Fig. 1.— Vertical Section of the Middle Inas at Black Ven,

. Greensand, chert, and Drift, about . st
. Green Ammonite-nodules.

9 Greymane apse olts 2) i) yew te [tay eee
!. The Belemnite-stone.

She Belonmite-shale wy ot.) 220 2 oe G
Gireysmarle ey Ys (eater Leto +26

. Impure limestones, in uncertain and ir-
regular beds formed by the induration of

the light-coloured ca!careous marls 14 to 18
. Blue marl containing Belemnites longis-
simus, Millev . . 3. 28h) Gos 3B
;. Limestone and marl with Belemnites,

. Limestone and marl with Ammonites
raricostatus.

lower ia), -: ... - Same pabouty18)

Middle Lias, about 94 feet.

The Lias thus terminates in Black Ven at a height of about 270
feet above the sea. The road from Lyme to Charmouth, where it
passes through the east ‘“ Cuts,” is about 70 feet above the highest
of the Lias. From this point the beds are somewhat steeply denuded
towards the valley of the Char, so that we soon lose the Middle Lias.
The Lower Lias beds dip gently in the same direction, that is, to-
wards the east ; and, at the mouth of the river, we find a fault which
throws them down some 50 feet more in the same direction.

2. Stonebarrow Hill and Westhay Cliff—tThe base of the Middle
Lias is met with in Stonebarrow Hill at the height of about 80 feet
above the sea (m, fig. 2), and the Belemnite-stone (y) at about
80 feet above that again. At 16 feet over the Belemnite-stone we
find the first layer of the “Green Ammonite-beds ” (¢)—thus termed
by collectors from the green tint of the cale-spar that fills the cham-
bers of the Ammonites laticostatus, Sow., the characteristic fossil.
Several layers of these limestone-nodules occur in the next 16 or
20 feet. Some of the layers are more persistent than others, and all
are not equally fossiliferous.

Above these nodules the marls continue of the same character
as in the upper part of .the last section (fig. 1) for 75 feet more (d,

282 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 18,

fig. 2), and are then succeeded by three tiers of a fine-grained mi-
caceous stone containing more or less lime (c). This is the first
appearance of mica in the Middle Lias; and from this horizon up-
wards it will be found to occur at intervals up to the highest of the
Upper Lias Sands. The thickness of the blocks in the “Three Tiers,”
as | have termed them, varies much, as does likewise that of the
intervening marl; in the aggregate they measure from 20 to 26 feet.
Above these, in Westhay Cliff, we find some 20 feet more of micaceous
marl (6), which is succeeded by Greensand (a). There is thus a
thickness of about 220 feet of Middle Lias in this hill; and the best
exposure of the beds is to be seen upon Westhay Cliff at, and to the
eastward of, a gully called “ Breakneck.”? From this point to the
eastward the cliff decreases in height, and the beds dip in the same
direction, as far as a little stream called Ridge Water, near which
a piece of broken swampy ground conceals a downthrow to the east,
of about 40 feet. This brings us to Gabriel’s Water, at which com-
mences the fine section of the Golden Cap.

Fig. 2.— Vertical Section of the Middle Lias at Westhay Cliff.
BON Ages hv ey ae |

_j|a@

==
- feet.

a. Greensand, chert, and Drift . . . .about 180

6. Grey micaceous marl . .. . . . 16 to 20

ce. ‘‘The Three Tiers””—micaceous sandstone in
sandy micaceous shale and grey marl—about 20

d. Grey marl (not micaceous) with thin ferru-
ginous seams, and masses of pyritess . . . 73

e. The Green Ammonite-beds—nodules imbed-
ded in grey marls eens esas io

f. Grey marl, as above . .

g. The Belemnite-stone.

h

. Grey shale and layers of marl.

Middle Lias, about 220 feet.
a ey

rr ces

2.0 Grey mark .o3y atte: ae ele
I BS @rey. Lias stone. 2/04, da ie Sea tos
é é Blue marl ~22", 5 : oA Mr eae

im. Limestone with Belemnites; Ammonites rari-
, costatus in the lower beds.

t a. Lower Tiago) =? Ga Ba, PR Satie tO

A

3. The Golden Cap.—tThe principal portion of this hill is based

upon the Belemnite-beds (7, fig. 3), and the marls immediately over
the beach are those containing the Green Ammonite-nodules. Above
these, the “Three Tiers” are here finely developed, and form a remark-

Middle Lias, about 350 feet.

1863. | DAY—LIAS OF DORSETSHIRE. 283

able feature in the cliff, though very uninteresting to the collector.
They are succeeded by 160 feet of grey micaceous marl (d). Two or
three thin bands of mudstone and of occasional nodules occur in the
lower part of this mass; and at rather more than 100 feet over the
‘Three Tiers ” a thicker band (e), containing shells and calcareous
concretions, stands out from the face of the cliff. Underneath this
thick band is a curious and persistent layer of small nodules (f), con-
taining, chiefly, fragments of Ammonites. The mass of grey marls
terminates with a layer made up of shells and fragments of Penta-
erinus ; and this is immediately overlain by a bed of large sandstones
from 4 to 6 feet in thickness, which is again succeeded by large
nodular masses of indurated sand. Over the nodular layer occur
the Middle Lias sands (a), grey and marly in the lower part, but gra-
dually becoming brown and more arenaceous in their upper portion.
Nodules are plentifully scattered through these ferruginous sandy
shales and sands, which are here about 60 feet in thickness, and are
succeeded by Cretaceous beds.

Fig. 3.—Vertical Section of the Middle Lias at the Golden Cap.

Greensands, &c.

a, Grey and Brown sands with nodules .. . as
f b. Starfish-bed.

ce. Shell-bed.

d. Grey micaceous marl with layers of mudstones 160
e. Mudstone with nodular concretions and Shells 4
f. Small nodules containing Ammonites.

Oe ene) Parbe UWers. 2 he ag he in, ea ane
h. Grey marls with the Green Ammonite-nodules 100
z. The Belemnite-stone.

We have, therefore, in the Golden Cap, about 290 feet of grey
marls, capped by about 60 feet of sands with nodules, all belonging
to the Middle Lias.

Passing eastwards over a small upthrow, mentioned by De la
Beche, there occurs, at the Coastguard-station at Seatown, a power-

284 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 18,

ful fault which carries out of sight the marls below the ‘Three
Tiers,” the ‘“‘ Three Tiers” themselves, and part of the micaceous
marls over them.

4. Down Cliffs——In consequence of the fault just mentioned, the
layer of small nodules already noticed in the Golden Cap (f, fig. 3)
is seen in Down Cliffs at a height of about 25 feet from the beach
(3, fig. 4). The overlying shell-containing mudstone (e, fig. 3), of
the hill to the westward, is here represented by an equal thickness
of hard shelly marl (2, fig. 4). The fault has therefore caused a
downthrow of about 200 feet, which great effect is not the result of
several small downthrows, but of one well-defined fracture.

Sixty feet or so over the small nodules, a layer of massive sand-
stones projects from the face of the cliff. These are the Starfish-
stones (0, fig. 3, and 2, fig. 4), so called from the beautiful specimens
of Ophioderma Egerton, Broderip, collected from their under sur-
face. Beneath them is a layer of marl, rich in shells (c, fig. 3, and
k, fig. 4); and above them, and occasionally forming part of one
huge block, are large shaly nodules; the entire series being identical
in character with their equivalents already mentioned in the Golden
Cap. As in that hill also, over these beds is a mass of shaly sands
with nodules (jh, fig. 4), here attaining to a thickness of about 85 feet,
and capped by a band of blue, micaceous, siliceo-calcareous stone (9),
which yields most of the specimens of Ammonites margaritatus,
Montf., sp., that are collected here, and which I therefore term the
“‘ Margaritatus-stone.”’ Resting upon this layer is a bed of marl (f),
the grey or blue tint of which renders it a more prominent feature
in the section than its thickness of only 6 feet would lead one to
expect. This argillaceous deposit forms a remarkable break in the
series of sands, which recur over it (d, e); above, however, they are
less calcareous, quite as micaceous, and of a more decidedly brown
colour than those below.

Over these upper sands, which are frequently indurated into
massive blocks of sandstone rather than into nodules (d), and which,
from the “ Blue Band” upwards, measure about 70 feet in thick-
ness, is a mass of very micaceous grey marl or clay (c*), about 18 feet
in thickness. This is capped by a remarkable band of stone (1), the
lower portion of which is in great part a conglomerate, the pebbles
being imbedded in a more or less ferruginous matrix, with oolitic
granules. In places, however, this part of the bed assumes more the
appearance of the Marlstone of other districts; it is separated from .
the higher portion of the stone by a seam of iron-ore, seldom more
than an inch in thickness, but occasionally becoming thicker, and
then containing a remarkable assemblage of Mollusca amongst the
water-worn pebbles. This “ Pleurotomaria-bed,” as I have termed
it, and the underlying equivalent of the Marlstone appear not to be
persistent through the section, but the upper portion of the bed of
stone can be traced throughout. This higher part is composed of
thin bands of a hard, dense, almost chert-like limestone, separated
by thin Jamine of yellow ochreous clay; the whole, however, being
consolidated into one block. The entire thickness of the associated

1863.]

Upper Lias, about 210 feet.

Middle Lias, about 275 feet.

DAY—LIAS OF DORSETSHIRE. 285

Fig. 4.— Vertical Section of the Middle and Upper Lias at Down

© bo

ct

d

Cliffs.

feet.
a. Drift (Thorncombe Beacon). . . . 15
BU pper tienes SEED
G. WPBEP WAAR Clay ype wi se anc ag mee E
GF AOAy (FANG ARC) each ay «tee. 2D
d. Blocks of indurated sand. . . .. 8
e. Light-brown sands . . . ... . 60
FowimUe NEES Ls 5 ict ee (estes ER
g. Margaritatus-bed . . . . + ted

h. Marly sands, with many tiers of Sad®
nodules in the upper part, and beds of
irregular and laminated sandstones
un GHG TOWEE oo oe ts or at 8. har. <7 OO

7. The Starfish-bed. . . . . . .4t06
k. The Shell-bed. .
1. Grey micaceous marls (Toad’s Cove) . 90

1. Upper Lias stone and the Marlstone.
2. Band of hard marl.

h 3. Layer of small nodules.

286 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 18,

marlstone and limestone (belonging to the Upper Lias) varies from
2 to 3 feet *. This extraordinary band of stone, thus including the
boundary-line of two formations, is interposed between portions of
the same great clay-deposit, since above it there is a mass of grey
micaceous marl (¢) precisely similar in character to that below. This.
marl is continued upwards for about 70 feet.

We have already seen that blue marl, similar to that of the Lower
Lias, is continued some 20 feet into the Belemnite-beds of the Middle
division; here, on the contrary, we find the higher limit of the
latter, as defined by fossils, carried upwards into a clay-deposit most
certainly belonging in the mass to the Upper Lias. We thus see
that the organic and inorganic conditions characteristic of two con-
tiguous groups do not always possess the same boundary-line.

Over the great clay-bed last mentioned there are about 140 feet of
sands(b)—brown, micaceous, and with close-set tiers of large nodules,
and layers of indurated sandstone. These are the sands which, till
within the last few years, have been called “ the Sands of the Inferior
Oolite,” but which are now, as is well known, generally assigned
. to the Upper Lias. The highest of these beds immediately under-
lying the Inferior Oolite have been, in the section under consideration,
completely denuded, the total height of the hill being completed by
a few feet of drift (a). Passing under the height of Thorncombe
Beacon, we find the Down Cliffs section sloping away gradually to
the eastward. The beds are cut through by the Valley of Eype, but
without any fault.

5. Fourfoot Hill.—In this hill, at a little distance to the eastward
of “‘ Kype’s Mouth,” we come suddenly to a very strong fault, which
carries out of sight not only as much of the Middle Lias as is not de-
nuded, on the one side, but, on the other or eastern side, brings down
the highest beds of the Inferior Oolite below the level of the beach,
with upwards of 200 feet of Fuller’s Earth and Forest Marble resting
upon it. As there is a thickness of more than 200 feet of Lias in
the one cliff, and as the interval between those beds and the upper-
most of the Inferior Oolite cannot be much less than 300 feet, we
may estimate this fault as a downthrow of nearly, if not more than,
500 feet, and this too in one great fracture.

The Lias beds of the western side of the fault include the brown
sands nearly up to the Upper Lias Stone; but, as the only portion of
the section not obscured is to be seen in the faulted face, where the
beds are much displaced and coated with the débris of the fault, it
is difficult to say much about this, the most easterly extension of
the Middle Lias on the Dorsetshire coast.

No more of the Lias is seen till we approach Bridport Harbour,
where the Upper Lias Sands are brought up again by a fault corre-
sponding to that of Fourfoot Hill, though not equalling it in mag-
nitude.

* R. Etheridge, Esq., of the Geological Survey, being engaged, in the summer
of 1861, in making a section of the Lias strata near Lyme Regis, was the first to
discover the existence and true position of the Upper Lias in this cliff, though
he did not then suspect the character of the under part of the block in which he
found the Upper Lias Ammonites.

1863. ] DAY—LIAS OF DORSETSHIRE. 287

In the first cliff east of the harbour, there is a thickness of about
120 or 130 feet of sands with nodules, cut into a perpendicular cliff.
Probably some of the highest nodules of the sands cap this cliff, as I
have seen a few fossils in blocks fallen from the summit, and as the
Inferior Oolite is found a very short distance inland.

6. Burton Cliff.—tIn this section there is the same thickness of.
sands as in the last-mentioned cliff, but here capped by the Inferior
Oolite and Fuller’s Earth. As much discussion has taken place in
England upon the correctness of the classification which assigns
these sands to the Upper Lias, and as I believe some amount of
doubt was at one time expressed, not only upon the deductions
drawn from the assertions made upon this point, but even upon
those assertions themselves, I am happy to be able to add my testi-
mony to the truth of one point which was formerly called in ques-
tion, namely, the existence of a bed containing numerous Ammo-
nites, of species assigned on the Continent to the Upper Lias, lying
in the sands a few feet under the lowest beds of the Inferior Oolite.
From the geologist who first pointed out this Ammonite-bed, it is
frequently called the Cephalopoda-bed of Dr. Wright *; and I have
now found it in this district, not only in Burton Cliff, but under-
lying the Inferior Oolite of Chideock Hill, of Poorstock, and of Stoke
Knap, near Broad Windsor.

Only the highest nodules of the sands are fossiliferous, and the
uppermost tier of all is a persistent bed of sandstone, containing
much lime and densely charged with the casts of Ammonites and
other shells. Under Burton Cliff, on the occasion of a visit thither
in the company of my friends Dr. Wright + and Robert Etheridge,
Esq., we found the bed of stone here mentioned still attached to the
base of the limestone containing Ammonites Humphriesianus, Sow. ;
the zone of A. Murchisone, Sow., being here absent. In the other
localities above given, I have found the same bed underlying the
zone last mentioned, the absence of which, in Burton Cliff, appears
to be the exception in this district.

7. Generalized Section.—With the last section ends my description
of the lithological characters of the Middle and Upper Lias of this
coast, which divisions I have thus traced, from the first appearance
of the lower, in the cliffs of Black Ven, to the point of disappearance
of the upper, near the village of Burton-Bradstock.

I now propose to condense these several sections into one gene-
ralized diagram, in which I shall endeavour to point out how the
fossils are distributed through the successive beds of varying litho-
logical character.

Commencing from below, there is first a great mass of marls con-
taining more or less persistent beds of limestones, or limestone-
nodules, but all without a trace of mica. This mass, nearly 200
feet in thickness, as seen in Westhay Cliffs, is terminated by a de-
posit of lime, sand, and mica, forming the “ Three Tiers.” Over this

* See Quart. Journ. Geol. Soc. vol. xii. p. 292, and vol. xvi. p. 3.

+ I have to thank Dr. Wright, with whom I first visited some of the sections
described, for his kindness in determining many specimens, which I submitted
to him, illustrative of these strata.

Middle Lias.

"so 0 QQ rr Ke

rn

288 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. pRebeis;

Fig. 5.—Generahized Section of the Middle and Upper Las of the
Dorsetshire Coast.

i ) mt cr dé Ammonites variabilis, D’ Orb.

A. primordialis, Schloth.

+ Upper Lias Sands.

(
|
|
|
|

nN
5
ae

+]

oO
io
laf
5)

Upper Lias f A. defrons, Brug. A. communis, Sow.
Stone. A. serpentinus, Rein. | A. crassus, Phil.
f Pleurotomaria-bed. | A. annulatus, Sow.
KBlazlstone ‘| Nodular marlstone. | A,
4d Meera SS A, Bechei, Sow.

ie spinatus, Brug.

g |
= |
a )
3 : gq ...Margaritatus-bed. \ A. fimbriatus, Sow.
~
2 |
: |
:
... Starfish-bed.
...Shell-bed. A. margaritatus, Montf.
1

)

|

pe stb

bane Three Tiers. |
r

|

|

\ eecee erases eet eseeseee Bion
— | Belemnite-beds. A, Henley.
... Belemnites longissimus, Miller.

‘|. Lower Lias Marls.

é A, Loscombii, Sow.

mM eo

a

Era

©

s |

= A. brevispina (non Sow.), A.
| a | Green Ammonite- Bechei, Sow., A. laticostatus,

if beds. A, heterogeneus, A. Davei.
) ...A. Taylori?, A. fimbriatus, A.

radians, Schloth.

1863. | DAY—LIAS OF DORSETSHIRE. 289

is a series, 180 feet thick, of grey marls, which are micaceous, but
without sand. Capping these, in Down Cliffs, is the Starfish-bed,
above which begin the Middle Lias Sands; at first these are very
argillaceous, but higher up, and over the intercalated band of blue
marl, they become more purely siliceous. This mass of sand, above
and below the band of marl, is altogether 170 or 180 feet in thickness.
A great clay-deposit next succeeds, the lower 20 feet of which belong
to the Middle, and the remaining 70 feet to the Upper Lias; the boun-
dary of the two divisions, as I before explained, being discoverable in
an intercalated band of stone. Over the clay-deposit, I include in
my section some 150 feet or more of siliceous sands, densely charged
with nodules, the highest tiers of which are slightly calcareous, and
capped by asolid bed of stone containing also some proportion of car-
bonate of lime. These latter, the Cephalopoda-beds, underlie another
formation.

§ IIL. Distribution of the Organic Remains.

1. The Belemnite-beds.—The lower portion of the great mass of
marl without mica includes these beds, in some of which Belemnites
occur more abundantly than in any other bed of the Lias; in the
words of De la Beche, “‘ seams composed of little else than their re-
mains are seen on ledges, dry at low tide, at the foot of the Golden
Cap.” The lowest portions of these beds contain chiefly the Belem-
nites longissimus, Miller, but in the higher ones many species are
intermingled; and it is more especially these higher beds, imme-
diately underlying the Belemnite-stone, and that band itself, which
deserve attention. In the beds below, excepting Belemnites, fossils
in a recognizable form are rare ; compressed Ammonites and their im-
pressions are abundant, but not in a state to be of much service to
the paleontologist. I cannot therefore pretend to give any precise
information as to the characteristic Ammonite of this zone. I believe,
however, that fragments of A. Henleyi, Sow., do occur throughout
it. In the Belemnite-shales and -stone, however, there is an abun-
dance of recognizable fossils. The only place where anything like
a full and speedy insight into the contents of these beds can be ob-
tained is on the beach between the Golden Cap and Seatown when
a favourable wind has cleared away the shingle which generally
conceals them. Belemnites elongatus, Miller, is, perhaps, the most
common form. Another very frequently occurring species is B.
clavatus ; but I suspect that some, at least, of the specimens known
by this name are only the young of other species. B. longissimus,
Miller, is also a form of frequent occurrence. Of other varieties
there would appear to be many; but, in the present state of our
knowledge regarding these fossils, I may be excused from venturing
on further determinations. One fossil, however, found in the stone,
calls for special investigation. I allude to the fossil figured and de-
scribed by De la Beche (Geol. Trans. 2nd series, vol. ii. pl. 4. fig. 4)
as an Orthoceras*. My specimens indicate that it is more closely

* In his ‘Report,’ p. 224, De la Beche records it again as ‘‘ Orthoceratites ?
elongatus.”

290 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 18,

allied to the Belemnite,—De la Beche’s determination having been
founded, as his figure shows, upon a very imperfect specimen. Allied
though it be to the Belemnite, yet I think that it must be looked
upon as generically different, since it not only differs in the out-
ward form, but also in the internal structure of the guard. The
very elongated proportions of the phragmacone also differ from any
that I have seen associated with true Belemnites*.

In these layers of shale there are also considerable numbers of
Lthyncholites, which are assigned by local collectors to the animal of
the Belemnite. As they differ considerably from those of the Nau-
tilus found in the Lower Lias, I am inclined to think that the local
assignment of these to the dibranchiate Cephalopods may be correct ;
but more evidence is required upon this point.

Associated with the above remains occur very many Ammonites
and Nautili. Amongst the former are large and crushed specimens
of A. fimbriatus, Sow., old and young specimens of A. Becher, Sow.,
and occasionally one of A. Loscombii, Sow.; this is likewise the chief
horizon of A. Henleyr, Sow., which however occurs also in the over-
lying marls. Many forms of small pyritized Ammonites are found
in these beds, and several species of Nautilus are also to be met with
herein.

Gasteropodous shells are common, the most frequent species being
the Trochus Gaudryanus, D’Orb., and Pleurotomaria eapansa, Sow. sp.
Amongst the Conchifera, Crenatula ventricosa and Nucula variabilis (?)
are the most abundant forms. Brachiopoda are likewise abundant,
but so crushed and deformed as to render identification difficult.
Upon a specimen of Ammonites Henleyi in my possession, from these
beds, there is a numerous colony of very small Cranie ; and in several
other instances I have observed the same form upon fragments of
the same species of Ammonite, as likewise upon a specimen of Am-
monites Becher from the beds above.

Of the Vertebrata, good specimens of both Saurians and Fish have,
I am told, been obtained from these beds, though I have been un-
able to find any authentic specimens. The Saurian of which bones
are most frequently found is the Jchthyosaurus tenuirostris, ConyD. ;
I. communis, Conyb., also occurs. Both of these species are like-
wise met with far down in the Lower Lias.

Of Fish, I have seen fragments of the genus 2chmodus from these
beds.

Pentacrinus basaltiformis, M7ller. Plicatula spinosa, Sow.
Terebratula numismalis, Lam. Pecten, several species.
Rhynchonella. Cucullea.

Craniz, upon Ammonites Henleyi. Nucula variabilis (?), Sow.
Crenatula ventricosa, Sow. Pleurotomaria anglica, Sow.

Hinnites velatus, Goldf. expansa, Sow.

* Since writing the above, I have been fortunate enough to obtain the pen of
the creature, associated with the phragmacone and guard. This not only fully
corroborates my supposition that the animal was generically different from the
Belemnite, but presents us with an unknown and extraordinary modification of
pen-structure, which Professor Huxley has kindly undertaken to explain in a
description of the new fossil.

1863. ] DAY—LIAS OF DORSETSHIRE. 291

Trochus imbricatus, Sow. Nautilus inornatus, D’ Ord.
Gaudryanus, D’ Ord. semistriatus, D’ Ord.

Turbo. Belemnites clavatus, Blainv.

Chemnitzia Periniana, D’ Ord. ‘longissimus, Miller.

Ammonites Bronnii, Rom. — elongatus. Miller.

—— furticarinatus, Quenst. —— acuarius, Schloth.
Nodotianus, D’ Ord. brevirostris, D’ Orb.
Grenouillouxi, D’ Orb. Rhyncholites.

—— Henleyi, Sow. Xiphoteuthis Bechei, Huxley, MS.

— Bechei, Sow. Geoteuthis, sp.
laticostatus, Sow. /®chmodus.

— Loscombii, Sow. Ichthyosaurus communis, Conyd.

—— fimbriatus, Sow.
And several undetermined species.

2. The Green Ammonite-beds.—These beds, and the higher por-
tion of the non-micaceous marls, contain an assemblage of fossils
having many species in common with the beds below. Peculiar to
them amongst the Cephalopoda are Ammonites laticostatus, Sow., and
its aged and extraordinary variety A. heterogeneus, Y. & B. (A. hy-
bridus, D’Orb.), a species locally known as A. brevispina (but not of
Sowerby, nor yet I think a mere variety of A. laticostatus), and A.
Davei, Sow., which is one of the most scarce Ammonites of our
locality.

tenuirostris, Conyb.

Inoceramus, n. sp. Ammonites Daveei, Sow.
Chemnitzia Carrucensis, D’ Ord. , Sp.

Pterocera liasina, D’ Ord. Nautilus semistriatus, D’ Ord.
Acteonina, sp. Belemnites compressus, Voltz.
Straparollus, sp. — longissimus, Mi//.
Ammonites Bechei, Sow. Aptychi of Ammonites.

— Loscombii, Sow. Ichthyosaurus.

— laticostatus, Sow. Plesiosaurus.

— heterogeneus, Y. § B.

3. The Three Tiers—These beds are very unfossiliferous, espe-
cially in the Golden Cap. The bones of Saurians are, however, occa-
sionally met with, as also Belemnites and the casts of phragma-
cones, and occasionally an impression or fragment of Ammonites
margaritatus, A. Loscombu, or of A. fimbriatus occurs in some of
the blocks.

In the marls over them traces of but few fossils are seen, until
we come to the layer of small nodules, which contain Ammonites of
several species, and other shells. The shelly mudstone above con-
tains, as far as I can judge, the same forms as occur again in the
Shell-bed. °

4, The Shell-bed.—This bed underlies the Starfish-stone, and in it
I have found a rich collection of Mollusca, chiefly Conchifera. The
only two species of Ammonites which I have obtained from it are
A, margaritatus and A. Thouarsensis, D’Orb. One or two species
of Belemnites complete the list of Cephalopoda. Some small species
of Pleurotomaria, Trochus, and Chemnitzia occur not unfrequently ;
but the most abundant shells are those peculiar to this zone, which
extends from the small nodules to the Starfish-stone. Numerous
genera are represented, as the accompanying list shows. Fragments

292 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 18,

of Pentacrinus and the spines of Cidaris contribute largely to make
up the bed. Cidaris Edwardsii, Wright, a species very frequent in
the Lower Lias, occurs here.

Pentacrinus Johnsonii, Austin. Nucula aurita, Quenst.
Cidaris Edwardsii, Wright. Unicardium cardioides, Phil.
Crania. Lucina.
Terebratula cornuta, Sow. Astarte.

numismalis, Las. Pullastra.
Rhynchonella furcillata, Theod. Venus pumila?, Oppel.
Avicula novemcosta, Brown. Tsocardia.
Lima pectinoides, Sow. Pleurotomaria anglica, Sow.
Hinnites velatus, Goldf. araneosa, Desi.
Modiola. expansa, Sow.
Hippopodium, young. Nerina.
Cucullea elongata, Sow. Cerithium.

inxquivalvis, Goldf. Chemnitzia.

cancellata, Phil. Ammonites Thouarsensis, D’ Ord.
Sanguinolaria vetusta, Phil. —— margaritatus, Monitf.
Cardinia, sp. Belemnites clavatus, Blainv.
Pholadomya, sp. Teeth of Hybodus.

5. The Starfish-bed.—Besides the Ophioderma Egertoni, Broderip,
this stone affords a closely allied species, or variety, O. tenuibrachiata,
Forbes. These Echinoderms are collected, as I have already stated,
from the under side of the large blocks ; in reality the layer beneath
which they occur is but a portion, a few inches thick, of the entire
stone, and this portion is a more pure sandstone than the part above.
As far as one can judge, the thin deposit of purer sand is as local as
the occurrence of the imbedded Starfish, and hence the two pheno-
mena appear attributable to the same cause. This consideration, the
peculiar situation of the Echinoderms, and the positions in which
they occur in the stone, lead me to imagine that we have in this
case a true instance of a sudden and accidental deposit and destrue-
tion of life, in contradistinction to the gradual and regular mode in
which most geological masses were accumulated.

6. The Grey and Brown Sands with Nodules.—In these we find
here and there a considerable number of organic remains; in some
places, lumps composed chiefly of the joints of the stems and arms of
Pentacrinus Johnson, Austin; in others, masses of Rhynchonelle of
small size. Intermingled with these are small Gasteropoda and Con-
chifera, together with fragments of larger shells. The latter, such
as Gryphea Maccullochu, Sow., and Pecten equivalvis, Sow., occur
very perfect and fine in these sands. Plicatula spinosa, Sow., which
is found in every collection of fossils from the Belemnite-beds up-
wards, is here abundant and fine.

In the topmost layer of the nodules, or the “‘ Margaritatus-stone,”
Ammonites margaritatus occurs very large, and occasionally well
preserved; as is also A. fimbriatus, with which it is associated.
From the overlying blue marl I have scarcely seen a fossil, so that
I cannot say whether it belongs palzontologically to the sands below
or to those above.

Terebratula cornuta, Sow. | Rhynchonella tetrahedra, Sow.
quadrifida, Lam. Lingula Beanui, Phil.

1863. ] DAY—LIAS OF DORSETSHIRE. 293

Crania, sp. Chemnitzia, sp.

Gryphza Maccullochii, Sow. Nautilus semistriatus, D’ Ord.
Avicula novemcosta, Brown. Ammonites fimbriatus, Sow.
Lima, sp. margaritatus, Monff.
Plicatula spinosa, Sow. Fragments of Crustacea.

Pecten equivalvis, Sow.

7. The Brown Sands and Sandstones.—In these, masses of fossils
occur, chiefly collected from the outside of the blocks of sandstone.
Ammonites spinatus, Brug., is now the characteristic Ammonite, and
with it are associated some peculiar Phasianelle and the magnificent
Pinna Hartmanni. I have two crushed fragments of Ammonites
Bechei from this zone, and one of Nautilus semistriatus, D’Orb.

Ammonites spinatus, Brug. Pinna Hartmanni, Zier.
Bechei, Sow. Goniomya rhombifera, ave

Nautilus semistriatus, D’ Orb. Avicula, sp.

Belemunites, sp. Pecten, sp.

Phasianella, two species. Plicatula spinosa, Sow.

In the 18 feet of clay over the sands I have found no fossils.

8. The Marlstone with its Pleurotomaria-bed.—These beds amply
atone for the poverty of the bed beneath. Ammonites spinatus is
still the characteristic Ammonite, occurring here in great variety.
Associated with this most variable and truly Middle Lias form I have
obtained specimens of several Upper Lias Ammonites, such as A,
communis, Sow. and its several closely allied forms, A. radians,
Schlotheim, and even A. serpentinus, Rein. ; the first-named species,
though not so plentiful, is represented by far lar ger individuals than
in the Upper Lias stone itself. Beautiful as are the Ammonites
of this bed, the Gasteropoda are still more remarkable. They are
most perfectly preserved, but, owing to the character of the matrix,
they are very difficult of extraction. My list, as given below,
includes many species of Pleurotomaria and Trochus, with several of
Turbo, Straparollus, Phasianella, Chemnitzia, &c. Amongst these
are included many of those beautiful shells, figured and described
by Deslongchamps and D’Orbigny, from the Middle and Upper Lias
of Calvados. Nor are the Conchifera much less remarkable, though
even fewer good specimens are obtainable. Many appear to be un-
described species, whilst some are forms but rarely met with; such
are Sanguinolaria cuneata and S. vetusta, figured by Professor Phillips
from the Yorkshire coast.

The shells and the pebbles of the conglomerate are coated with
Serpule, and the water-worn stones are perforated by Lithodome.

Brachiopoda are also well represented. Spirifera Walcotti, Sow.,
and S.rostrata,Schloth., occur, though rarely. Terebratula Edwardsii,
Dav., is common, and J. subpunctata, Dav., very fine. Several
other Marlstone species are represented: 7. resupinata, Sow., how-
-ever, Which is common in this zone in many localities, is here alto-
gether absent ; 7’. cornuta, Sow., elsewhere abundant, is here scarce,
being apparently replaced by its variety 7. quadrifida, Lam., which
latter here appears also to have attained to a greater size than else-
where in England, thus approaching to its Continental types. Rhyn-
chonella serrata, Sow., rare elsewhere, is here not uncommon.

VOL. XIX.—PART I. x

294 PROCEEDINGS OF THE GEOLOGICAL, SOCIETY. [ Feb. 18,

Nor is this bed, so valuable in the abundance of its paleontological
evidence, less suggestive of physical facts. The thin and interrupted
bed which I consider to be the representative of the Marlstone, the
pebbles and small boulders imbedded therein, the perforations of the
Inthodomi, the masses of shells here and there collected into hollows,
as it were, of the underlying rock, the Serpule covering the shells
and pebbles, and the very intermixture of Upper Lias species, all
point to a sea-bottom upon which, for a long period, little or no de-
posit took place; the water-worn fragments which lie upon it, on
the contrary, indicating that, during that period, previously formed
Strata were again destroyed. From what I have seen of the junc-
tion of the Middle with the Upper Lias, both here and at Glaston-
bury in Somersetshire, I have been led to believe that, immediately
previous to the deposition of the Upper Lias, some disturbing cause
for a time changed the direction of the currents which had brought
here the mud and sand of the Lower and Middle divisions, and that,
in place of continuing gently to lay down these deposits, the action
of the water was for a time, and over certain districts, confined to
the destruction of beds previously formed and consolidated*.

Serpula, two species. | Gryphza gigantea, Sow.
Apilocrinites ? | Myacites unionides, Goldf.
Pentacrinus ? | ——, two other species.
Holectypus hemispheericus, Desor. | Mytilus, sp.

Thecidea Moorei, Dav. | Modiola, several species.

Terebratula punctata, Sow. _ Goniomya,sp. (aspera, Etheridge, MS.).
subpunctata, Dav. | Tsocardia, sp.

—— numismalis, Lam. | Cypricardia, sp.

—— quadrifida, Lam. Ceromya, sp.

— Moorei, Dav. Cardinia concinna, Stutchb.

cuneata, Stutchb.

cornuta, Sow.
Listeri, var. hybrida, Stwtchb.

Edwardsii, Dav.

Rhynchonella tetrahedra, Sow. Cardita, sp.

serrata, Sow. Unicardium cardioideum, Phi//.

subconcinna, Dav. f | Sanguinolaria vetusta, Phdl/.

furcillata, Theodor. cuneata.

Moorei, Dav. | Mytilus hippocampus, Y. & B.

eynocephala, Richard. | Cardium truncatum, Sow.

— acuta, Sow. , sp. (Dayii, Etheridge, MS.).
Spirifera rostrata, Sch/oth. Arca, sp.

Walcotti, Sow. | Cucullea ineequivalvis, Goldf.
Lingula, sp. | Pholadomya ambigua, Sow.
Perna, sp. _ Lithodomus, sp.

Lima punctata, Sow. | Trochus Gaudryanus, D’ Ord.
antiquata, Sow. | monoplicus, D’ Ord.

Pecten dentatus, Sow. epulus, D’ Ord.
textorius, Schloth. | —— Emylius, D’ Ord.

Sie Eolus, D’ Orb.

» S}
Hinnites velatus. Goldf. Mariz, D’ Orb.

Gryphza Maccullochii, Sow.

* Since the above passage was written, I have found a notice of this bed, which
I had previously overlooked, in a paper by Buckland and De la Beche, “ On the
Geology of the Neighbourhood of Weymouth, &ec.” It shows clearly to what
formation these beds were in those days assigned, and that the conglomerate-bed
and its meaning had been studied years ago by those eminent observers. (See
Geol. Trans. 2nd ser. vol. iv. p. 31.)

1863. | DAY—LIAS OF DORSETSHIRE. 295

Turbo Itys, D' Orb. ' | Turritella, two species.
Nireus, D’ Ord. | Chemnitzia, sp.
Midas, D’ Ord. Pitonillus, sp.
Pleurotomaria mirabilis, Des/. Ammonites crassus, Phi//.
precatoria, Desi. communis, Sow.
—— bitorquata, Des/. | —— Holandrei, D’ Ord.
sulcosa, Des/. spinatus, Brug.

rustica, Des/. —— fimbriatus, Sow.
procera, D’ Ord. : serpentinus, Pez.
—— pinguis, D' Ord. (?). radians, Rezn.

—— rote.lxformis. Raquinianus, D’ Ord.

expansa, Sow. sp. | Belemnites, several species.
Straparollus sinister, D’ Ord. Ancyloceras, sp.
, sp. Fish-scales and fragments of Crustacea.

Piesanditn’ two species.

9. The Upper Lias Iamestone.—In the lower part of the Upper
lias Limestone, that is, immediately over the ferruginous seam, I
have found Ammonites serpentinus, Rein., in some abundance, though
badly preserved.

In the upper part of the same stone occurs Ammonites bifrons,
Brug., which I have not met with below, associated with several other
Upper Lias species of Ammonites, Gasteropoda, and Brachiopoda.
Terebratula, a small species. |) Ammonites bifrons, Brug.
Rhynchonella Bouchardii, Da». | Raquinianus, D’ Orb,

Moorei, Dav. | —— radians, Rein.
Leptena liassina, Bouchard. / —— communis, Sow.
Crania, sp. | — serpentinus, Rein.
Cardinia, sp. | —— complanatus, Brug,
Astarte elegans, Sow. Holandrei, D’ Ord. .
Trochus trimonilis, D’ Ord. | Nautilus, sp.

/€gion, D’ Orb. |

In the Upper Lias Clay I have found no fossils, and it may be
observed that I have riot met with any trace of the fish-bed of
Ilminster and Dumbleton in our series of beds.

10. The Cephalopoda-beds.—The lower and greater portion of the
Upper Lias sands have afforded me no fossils, excepting a few
impressions of Ammonites radians; but in the topmost part, or
Cephalopoda-beds, I have found several species of Ammonites. <A.
Jurensis, Ziet., A. opalinus, Quenstedt, and A. variabilis, D’Orb.,
are all forms ussioned to the ‘ Jurensis-stage’ of Continental geolo-
gists, and the fossils of other classes associated with these Ammonites
all belong rather to the Upper Lias than to the Inferior Oolite.

Ammonites Jurensis, Z2e7?. Goniomya, sp.

variabilis, D’ Ord. Pecten barbatus, Sow.

opalinus, Quenst. Terebratula, sp.
Nautilus latidorsatus, D’ Ord. Rhynchonella tetrahedra ?; Sow.
Belemnites, two species. —— cynocephala, Richard.

Myacites unionides ?, Goldy.

11. Conclusion.—_If we now review the chief feattires of the dif-
ferent lists of fossils given above, we shall be able to obtain a better
idea of the vertical distribution of particular forms (see fig. 5).

To begin with the Ammonites. These, with some exceptions,
have more or less restricted ranges, and in no case does the range of

an Ammonite equal that of some of the most widely distributed Con-
x2

296 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 18,

chifera. Ammonites Henleyi, Sow., A. laticostatus, Sow., and several
other species characterize the Belemnite-beds and some of the beds
immediately above them. Ammonites Davei, Sow., occurs only in the
Green Ammonite-beds, in the uppermost layer alone of which is found
the form locally known as A. brevispina. A. margaritatus, Monttf.,
appears with the sand and mica in the “‘ Three Tiers,” and disappears
again with a deposit of marl; its place is, however, on the recurrence
of sand, supplied by a closely allied form, A. spinatus, Brug. This
species is succeeded by A. serpentinus, Rein., and that again by
A. bifrons ; after which is a wide gap assignable to no particular
form. Above this interval A. Jurensis occurs, underlying the zones
of the Inferior Oolite. But though these and most Ammonites have
their zones well marked and restricted, it is not so with all. For
instance, A. Loscombii appears with A. Henleyi, abounds with A.
laticostatus, and goes some way up into the range of A. margaritatus,
where it makes its last appearance in the layer of small nodules
below the shelly marl. It thus passes through most of the grey
marls, but does not reach to the permanent appearance of the sand.
A. fimbriatus and A. Bechet are still less restricted, the latter ap-
pearing in the Belemnite-beds, and showing itself, in occasional
specimens, as far up as the sands of the ‘ Spinatus-zone’ ; the former
ranging still more widely, from the same starting-point up to the
very summit of the Middle Lias. These forms are thus found not
only in strata some hundreds of feet apart, but in the highest and
lowest of a series of at least four of the more restricted ranges.

But if the ranges of the Ammonites are not very limited, neither
I apprehend are those of some of the other Cephalopoda ; Nautilus
semistriatus I find ranging coextensively with Ammonites Becher, and
I cannot distinguish some of the Belemnites of the Marlstone from
those of the Belemnite-beds.

In the Gasteropoda and Conchifera we find the vertical ranges of
several species of very various extent ; but they do not appear to me
to coincide so much with the distribution of particular Ammonites as
with other accidental circumstances. The Conchifera of the Belemnite-
beds occur also in the Green Ammonite-marls, but not in the shell-
bed under the sand, excepting such a ubiquitous form as Plicatula
spinosa, Sow. Some of the Gasteropoda, on the other hand, occur
also in the Pleurotomaria-bed associated with Ammonites spinatus.

The Shell-bed under the Starfish-bed has, as I have said before,
many forms peculiar to a zone lying above the frequently mentioned
“layer of small nodules” and below the sands, but many of its
species occur again above, and these are represented by far finer spe-
cimens in the sands. It would thus appear that Ammonites marga-
ratatus occurs in two faunas, which, though blending together at their
junction, are yet very distinct. In the lower part of the ‘Spinatus-
zone’ there appears to be a different fauna from that of the sands
below, and in its upper portion occurs the most remarkable collection
of Mollusca of any in the Lias. Along with many new and curious
forms are others that I have observed in some one or other of the
Middle Lias beds below. And yet, with all the diversity in the extent

1863. | _ MURCHISON—PERMIAN OF BOHEMIA. 297

of the various ranges, we cannot help feeling surprised at meeting here
with species that occur far down in the Lower Lias. Such however
are, amongst others, Lima punctata, Sow., Lima pectinoides, Sow.,
Cardinia hybrida, Stutchb., and Spirifera Walcotti, Sow., all of
which I have myself found in the ‘ Angulatus-beds’ to the west of
Lyme. What makes the appearance of these forms so high up the
more remarkable is that I have not found them in intermediate
strata. The few fossils that I have cited from the Upper Lias and
the Cephalopoda-beds do not justify any observations beyond those
I have already made—at least, not on the present occasion.

The higher forms of life—fish and reptilia—occur so sparingly in
our Middle Lias, that in these likewise there are no materials upon
which to generalize.

The questions which arise upon the facts of the distribution of
fossils, as herein given, are to my mind of the greatest interest and
importance. It would be impossible, however, to treat of such ques-
tions in a satisfactory manner without extending my observations
beyond the scope of the present paper. In a future communication
I hope to lay before the Society some speculations upon the history
of the Lias, which have originated in a consideration of the distribu-
tion of inorganic materials and organic forms throughout that forma-
tion in this district. The details into which I have entered in this
paper have been for the purpose of describing some of the less-known
facts upon which I have based my theoretical views.

I cannot conclude this paper without expressing my obligations
to my friend Robert Etheridge, Esq., F.R.S.E., F.G.S. The sections
which he had made, and the knowledge which he had acquired upon
the spot before I began my work, he kindly placed at my disposal
for reference and comparison ; the many fossils which I have entered
on my lists have all been submitted to his examination ; and before
I completed my paper, he kindly went over the various sections with
me, so as the more authoritatively to give me the support of his
judgment as to the correctness of my measurements and descriptions.

Marcu 4, 1863.

Francis Drake, Esq., Leicester; Il Commendatore Devincenzi,
Member of the Italian Parliament, Ministry of Agriculture and
Commerce, ‘lurin; Cav. C. Perazzi, Royal Corps of Mining Engineers,
Turin; O. C. Marsh, Esq., M.A., 14 Linkstrasse, Berlin ; and John
Watson, Esq., Whitby, were elected Fellows.

The following communication was read :—

1. On the Permian Rocxs of Norru-EasterN Bonemia. By Sir
Roperick I. Murcutson, K.C.B., F.R.S., F.G.S., &c., Director-
General of the Geological Survey of the United Kingdom.

Lithological Characters.—The Permian rocks of Bohemia differ from
those of North-western Germany in not comprising a calcareous

298 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 4,

member containing marine remains, to represent the German Zech-
stein, or Magnesian Limestone of Britain. They have all, therefore,
been referred by native geologists to the Roth-todt-legende, or what
I call Lower Permian. Being furnished by my old friend M. Haidinger
with the Map of the Austrian Geological Survey of the tract lying
to the south of the Riesengebirge, I endeavoured to complete my
acquaintance with those deposits which, in a previous year, I had
seen in the environs of Braunau and Charlottenbrunn, on the south-
eastern slopes of the same chain. On this occasion I examined
them on the line of railroad from Pardowitz and Josefstadt to Liebe-
stadtl and Semil; which railroad, having a direction from S.W.
to N.E., exhibits a complete transverse section of the whole group.
I was accompanied by Dr. Anton Fritsch, of Prague, whose accom- .
plishments as a naturalist and geologist were of the greatest ser-
vice, and without whose assistance in talking his native Bohemian
language I could have acquired little information on the spot.

In 1857, M. Emil Porth described these deposits in a memoir pub-
lished in the ‘ Jahrbuch der k. k. geologischen Reichsanstalt’*. First
enumerating the varieties of crystalline and metalliferous pene of
which the souther n portion of the Riesengebirge1 is composed, he shows
how the lowest member of the ‘ Roth-liegende,’ or his ‘ conglomerate,’
dips away from the older chain at angles varying from 20° to 48°,
with some intercalated shale-beds containing Plants. He speaks of a
bed of bituminous schist or ‘ Brandschiefer’ near the base of the series,
which contains remains of Fishes and Plants and gypsum-crystals.
Above these he notices a succession of particoloured argillaceous
sands and clays, containing copper-ores; and then the peculiar sand-
stone which is termed ‘ arkose’—1in parts a coarse grit, and partly
conglomeratic, with some manganese. In other parts this so-called
arkose is a sandstone with interpolated layers of dark-red and white,
fine-grained sands, and small courses of limestone. Then follow
sands and argillaceous beds, limestone, marls, and other bituminous
schists ; the culminating masses of the whole group being deep-red
shale and micaceous sandstone, with harder siliceous beds. Besides
these varied deposits, M. Porth mentions thick bands of regular inter-
stratified igneous rocks, chiefly the melaphyr-porphyry, with amyg-
daloids and traps, quartzose porphyry, bands of basalt, &c.

The most recent, however, of the descriptions of the Roth-legende
of this tract is by M. Jokely, and was published in 18627. This
author (who surveyed the tract, and prepared the Austrian geological
map thereof, with which I was obligingly furnished by M. Haidinger,
as stated above) divides the Roth-hegende into three principal parts.
The uppermost of these consists chiefly of hard shales and marl,
with some sandstone, a little limestone, and some harder siliceous
beds; the second of other and darker-coloured marls, shales, and
sandstones, passing down into arkose-grit and sandstone; and the
third of bituminous shale (Brandschiefer and Schiefer), intercalated

* Bericht iber seine diesjahrigen geologischen Aufnahmen in Nord-dstlichen

Bohmen, Seite 701.
+ Jahrb. derk. k. geol. Reichsanstalt Wien, 1862, No. 5, p. 381.

1863. ] MURCHISON——PERMIAN OF BOHEMIA. 299

with and resting on sandstone and the coarse lower conglome-
rate.

My own method of dividing the series, such as it was presented to
me in a section from the south of Liebestadtl to Semil, is as follows,
irrespective of the exact places of the igneous rocks in other dis-
tricts :—I1st. Overlying red marls and sandstones (see figure, p. 301,
Nos. 1-5), which in the sequel will be noticed as possible equivalents
in time of the Zechstein of Northern Germany. 2nd. Dark-coloured
bituminous shale, with some limestone, coal, and many organic re-
mains, including numerous Fishes, and passing into sandstone and
grits, with abundance of Plants (6-10). 3rd. Lower sandstones and
conglomerates (11-13).

This triplex series has been subdivided by the Austrian Surveyors
into eight parts, each part distinguished on the map by a different
colour. To these are to be added the igneous rocks called melaphyr-
and felsite-porphyry, as well as certain members of basaltic rock;
whilst thin seams of coal and limestone also form integral parts of
this compound group*.

* As my inspection of this tract was hasty, I cannot pretend to affirm that
the details which I describe in this section are applicable to the whole of the
wide Permian region lying to the south of the Riesengebirge. According to the
table of colours in the Austrian Geological Map, No. IX., the tract around
Liebestadtl is occupied by sandstone and schist, marked No. 14, whilst two other
subdivisions, whichyonstitute the ‘upper stage’ of the Austrian Surveyors, consist
of schists and marls, with hornstone and bituminous schist (Brandschiefer and
brownish-red argillaceous beds), the Nos. 11 and 12 of the map. As I nowhere
saw such an order of superposition, I have not alluded to it. In fact, all the
dark-coloured schistose and bituminous rocks which I saw between Liebestadtl
and Semil pass distinctly wxder the sandstone to the south of the Liebestadtl
station, and rest on older sandstones and conglomerates. It is, indeed, evi-
dent, from an inspection of the two Austrian maps only (Nos. LX. and X.),
that the general succession is that which I have indicated. Thus, in the eastern
portion of the sheet No. IX., we find that on the flanks of the crystalline rocks
of the Riesengebirge, the lower conglomerates and sandstones, with some schists,
are followed by other sandstones, tle arkose of the authors, and, thirdly, by the
widely spread red sandstones and marls (the No. 14 of the Austrian Table),
which range from Trautenau and Pilnekaw on the east to Liebestadtl and
Lomnitz on the west.

Again, one of the arkose-sandstones, which underlies No. 14 on the north,
or towards the Riesengebirge, rises again in the south, and throws the overlying
beds, No. 14, into a trough. Itis specially in the western half of the sheet
No. IX., or the neighbourhood of Hohenelbe, that the bituminous schists occur,
and, where I saw them, they most assuredly underlie the red sandstones and marls
south of Liebestadtl, as in my section. Since the arrows inserted on the map, as
regards this tract, indicate the south-easterly dip correctly, and are in accordance
with my section, it is probable that, in the complication of colours used, an error
may have arisen, for which the original observer is not responsible. The suc-
cession which I found in this section is exactly analogous to that which I for-
merly described as occurring at-Braunau, far to the east, where limestones and
bituminous schists, with Paleoniscus, &c., reposing on older sandstone and con-
glomerate, are surmounted by red sandstone, &e. (See ‘ Siluria,’ 2nd edit. p. 343.)

In the table of colours of the Austrian Geological Map, the igneous rocks
termed felsit-porphyry and melaphyr are placed above all the divisions of this
group, from which I presume that the author, M. Jokely, wished to show that
these eruptive rocks traverse all the strata,and occasionally overlie them. From
my observation, however, I should infer that these rocks are for the most part
regularly associated with several members of the group. Thus, near Semil,

300 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 4,

It seems to me, therefore, that the term Roth-todt-legende, which
was first simply applied to the pebbly unproductive rock beneath the
Zechstein and Kupferschiefer, ought no longer to be applied to such
a diversified series of deposits of various colours and of very different
lithological structure, and which contain copper-ores and many fossils.

Let me here state, that true Carboniferous rocks, with coal, as
worked in the north-eastern part of the territory under consideration,
crop out unconformably from beneath the conglomerate and bottom-
beds of this Permian series.

But to call attention to the tract which I last examined. After
passing an outlier of old and crystalline rocks to the north-west of
Koniginhof, we first halted at the Station of Falgendorf, to the west
of which we made an examination of the harder sandstones of Alt
Paka, through alternations of red sandstone, mapped as arkose by
M. Jokely, and which are overlain, in a fine escarpment, by a zone of
melaphyr and amygdaloid. The latter is followed by very hard
cherty sandstone, and then surmounted by the softer red and greenish
sandstone and marls of Falgendorf, which form the upper members
of the series. As all these strata are inclined to the N.E., and had
been thrown into undulations, a reversed dip might naturally be ex-
pected to occur where these deposits approached the chain of the
older rocks of the Riesengebirge, to which we were travelling.

Such proved to be the case. After passing certain masses of
porphyry and amygdaloid, and on travelling to the N.W., we met
with extensive masses of marls or shales with red sandstones and
marls, occasionally greenish and whitish, which at Liebestadtl* as-
sumed a steady or reversed dip to the S.E., or away from the older
rocks of the Riesengebirge. Between Liebestadtl and Semil the rail-
road lays open so clear a descending section of the whole group, from
the overlying red marls and sandstones to the underlying conglo-
merates which repose on the older slaty rocks, that, after fixing our
quarters at Semil, my companion and myself re-examined on foot
nearly all the intervening cuttings as laid open by the railroad, and
also made excursions to the east of the little town of Semil.

The result, as exhibited in the accompanying section, is simply
offered to convey a clear general idea of.the succession ; it being
understood that in the midway portion of the distance the continuity
of the order is not well exposed.

The following is the descending order of the strata :—

1. Red marls and traces of limestone, with micaceous sandstones,
in parts spotted, in parts flaggy. These beds are of considerable
thickness, and dip to the S.E., being on the limits of the diagram.

basaltic clinkstone forms tabular masses on one of the lower members, midway
to Liebestadtl, with the schists of the central part ; and near Falgendorf and Alt
Paka the melaphyr occupies the summits of hills of red marl and sandstone.
In my section I have only represented these igneous rocks as I saw them in
that particular tract. Most of these may therefore be considered as contempo-
raneous with the deposits.

* At Liebestadtl we profited by the attention of the intelligent clergyman of
the village, the Rev. J. Marishka, who presented to me two good specimens of
fossil Fishes out of his little collection, and was very useful and obliging.

1863.]

Section across the Permian Rocks of North-Eastern Bohemia (5 to 6 miles).

S.E,

Semil.

River Iser.

~ Pansko.

Liebestadtl.

Lower Division.

Middle Division.

Upper Division.

MURCHISON——PERMIAN OF BOHEMIA. 301

This member of the group was not much
examined by us, and I can by no means
affirm that it does not contain fossil re-
mains.

2. Sandstone, becoming more marly
and argillaceous.

3. Thicker-bedded sandstone, passing
down into

4. Dark-coloured shale.

5. Coarser and reddish-brown sand-
stone in dark-coloured shale.

6. Blackish shale, with small nodular
concretions of cement-stone and septaria,
passing down into thin lamine of ar-
gillaceous limestone, with concretionary
potato-stones, Fish-scales, and Copro-
lites.

7. Thin courses of black shale, gra-
duating with dark bituminous flagstones,
with fossil Fishes — Palewoniscus, &e.
(These occur a little to the north of the
Liebestadtl station, at Kostialow.)

8. Sandy and argillaceous dark-co-
loured shale, becoming in the lower part
what is locally called ‘ Thon-schiefer.’
In the lower part is one layer of thin
flinty limestone, concretionary in parts,
and below it the bituminous shale gra-
duates into a true coal, with impressions
of Plants in the associated shale. This
coal was formerly worked to some extent
in the adjacent hill of Cikoasko, though
as exposed on the side of the railway it
is of small thickness.

It is in this portion of the series, and

- particularly in its western extension to

Hohenelbe, that many of the Fishes and
Reptiles have been found which charac-
terize this central member of the group.
The dip here is about 20° to the S.E.

9. Brown shale with strong sandstone
bands of. about 6 feet each in thickness.
These sandstones graduate into the so-
called ‘arkose’ of the Austrian Surveyors,
one of the lower beds of which is a con-
glomerate, with many pebbles of white
quartz. Fossil plants (notably large
stems of Araucarites) occur in the sand-
stones and shales.

10. Courses of ‘ copper-slate,’ contain-

302 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. { Mar. 4,

ing fine blue carbonate of copper, with some ecoaly matter, and
footprints of small Reptiles in the accompanying shale. Copper-
works were formerly in activity here. It isin the extension of these
shale-beds that the best Reptilian footprints have been obtained at
Kalsia, near Hohenelbe.

EN. ’Argillaceous beds, becoming more sandy doers These
occupy a considerable thickness, and are exposed in partial undula-
tions. On the whole, however, they rise to the N.W., and are asso-
ciated with much melaphyr (amygdaloid) and thin-bedded basalt
or clinkstone, which is exposed in great tabular masseg in the hill
called Pansko, and are accompanied by hardened sandstone and
shale ; the whole dipping away to the S.E., from Semil and the
valley of the Iser.

12. Reddish glossy shale, and thin courses of grit, with ripple-
marked surfaces and many Plants (Calamites and Ferns), alter-
nating with bluish- -grey beds. In a dark, papyraceous, leather-like
schist are the lowest Fish-remains, Palewoniscus, &c. ; and the seetion,
as terminated in a north escarpment on the river Iser, exhibits at its
base sandstone and grit, which are succeeded by

13. The bottom-rock of the series. This consists of coarse con-
glomerates of water-worn and well-rounded pebbles of the older erys-
talline rocks of the Riesengebirge, which, alternating with bands of
coarse gritty sandstone, are well seen to the north of Semil. These
beds, of very great thickness, dip under and support all the before-
mentioned succession, and rest in their turn on the subcrystalline,
Paleozoic, or metamorphic rocks of the SSeS ©

Organic Remains.—In his excellent new work, ‘ Dyas’ (to the
name only of which I demur), Professor Geinitz describes the follow-
ing organic remains as belonging to the Roth-todt- hegende, or his
Lower Dyas. A large portion of these fossils occur in Bohemia, and
many species are common to the same rocks in Saxony, Bohemia,
Russia, and other tracts :—

SAURIANS IN THE RoOTH-LIEGENDE. Locatities.
Sphenosaurus Sternbergi, V. Meyer ... Konigratz, Bohemia.
Phanerosaurus Naumanni, V’. Meyer ... Oberlungwitz, near Hohenstein.
Osteophorus Roemeri, V. Meyer ......... Klein Neundorf, Silesia.
Rhopalodon Wangenheimi, sch. ...... Dioma, Bielabei, Corlavisk, and Nischi
Troitsk, Russia.
Murelisomi,Hiehw: 2. sans ce ae Bielabei (Copper-sandstone), Russia.
Deuterosaurus biarmicus, Hichw.......... Klutchewski, Dioma, Bielabei, Russia.
Zygosaurus lucius, Hichw.............-.0.+- Copper-sandstone, W. Ural.
Melosaurus Uralensis, V. Meyer ......... Nischi Troitsk, Russia.
Onchiodon labyrinthicus, Geen. ......... Plauenschen Grunde, Dresden.
Saurichnites salamandroides, Gezv....... Hohenelbe, Bohemia.
laeertaided: Getqs Saad. <n creeds atebee Ebendaher, Bohemia.

Tn all nine genera and eleven species of Saurians in the Roth-liegende ; whilst
in the Kupferschiefer two only, the Protorosaurus and Parasaurus, are known.

* M. Porth estimates these lower beds as being 600 feet thick.

1863. ] MURCHISON—-PERMIAN OF BOHEMIA. 303
FisHes ty THE RorH-LIeGENDE. Localities.

A Sauroid genus, Geini.............cceee es Plauenschen Grunde, Dresden.

Palzoniscus Vratislaviensis, Aq. ......... Klein Neundorf,Rappendorf, Braunau,

Hohenelbe, Bohemia; Erbendorf in
the Palatinate.

——— lepidurus, Ag. .....-2..0.deeseseceenee Klein Neundorf, Rappendorf, Braunau,
Hohenelbe, Bohemia; Erbendorf in
the Palatinate.

—— Blainvillei ,Ag.(Rohani, Hecker)... Semil, Bohemia.

—— obliquus, Hecker ............0.000000 Semil, Bohemia.
MMS, FACOICOT os: 5, rda ss eine wma Semil, Bohemia.
CRIARISMEECCHC? Fo oo cess ceesesceeseee Ebendaher, Bohemia.
ma Mess, FCCKET 5... ccccccccseccnessee Ebendaher. Bohemia.
MBS AG Rosa. Seite vis Hiittendorf, Hennersdorf, and Hohen-

elbe, Bohemia. Also from Pont de
Muse, near Autun, France.

aE NG OUI0 8 sg Saha, sateen sy 0% asian p Hiittendorf,road to Ob Kalna, Bohemia.

Acanthodes gracilis, Beyr. ............00 Klein Neundorf, Hohenelbe, Bohemia ;
Oschatz, Saxony.

Xenacanthus Decheni, Goldf, ............ Klein Neundorf, Braunau, Hohenelbe,

and other places in Bohemia, as well
as at Oschatz in Saxony.

Thus, while nine species of Palwoniscus occur in the so-called
‘ Roth-liegende,’ seven other species of the same genus occur in the
Kupferschiefer or marl-slate at the base of the Zechstein. Is the
one set to be considered of marine, and the other of freshwater
origin? or may they not all be of estuarine characters ?

The north-eastern part of Bohemia is characterized by an abun-
dance of the stems of the large silicified fossil trees, Araucarites.
In former communications I have alluded to the great abundance of
this plant in the escarpments of the Lower Permian rocks south of
the Harz*. Again, at Radowenz, to the west of Braunau, in
Bohemia, I have alluded to its occurrencey. At the last-mentioned
locality, and also at Peckau, which hes a little to the west of the
line of section just described, the bed of indurated sandstone
in which these great plants are included being at the surface,
and nearly horizontal, the huge stems are seen to be spread over
several acres of land. A large collection of these is to be seen at the
seat of the Prince Lippe-Schoenburg. They are indeed common in
many museums; and one of the largest specimens with which I am
acquainted, measuring 54 feet in diameter, was pointed out to me in
the Zwinger, at Dresden, by Dr. Geinitz.

Referring to the description of the Permian plants by Dr. Géppert,
I would remind my associates that this eminent botanist has shown
that, as a whole, they contain about eight per cent. of Carboniferous
species of plantst. Dr. Geinitz has also come to the same conclu-
sion. Now, independently of the clear order of superposition which
the Upper Carboniferous strata bear to the lowest division of the
Permian, or bottom-beds of the Roth-todt-liegende, any one exa-
mining the public collection at Dresden at once sees that the

* For references see ‘ Siluria,’ 2nd edit. p. 537.
t Ibid. p. 543, { Jbid. pp. 355, 356.

304 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 4,

characteristic fossil Permian plants, such as the typical Psaronites
and Arawcarites, Guglielmites Permianus, Gein., Alethopteris pris-
matifolia, Gein., Walchia pisiformis, Sigillaria Danziana, Gein.,
Neggerathia, and Neuropteris of peculiar species, are all plants of
this particular period, and differ essentially from those of the Car-
boniferous age.

Concluding General Observations.—Though it is out of my power
to make a correct estimate of the thickness of the strata exposed in
the section above described, yet, as the distance from a mile south
of Liebestadtl, where the upper beds have already a dip to the 8.8.E.,
to a spot north of Semil, where the conglomerates or *bottom-beds
of the series still dip in the same direction at an average angle of
about 10° to 15°, is about five or six miles, we cannot but assign
a vast thickness to these deposits, even allowing for a certain
amount of undulation and repetition in the central part of the
section. For in this case the succession is not only one of beds
of red sandstone and pebble-beds with porphyries, such as the geolo-
gists of North Germany have hitherto regarded as the Roth-legende,
but it consists of diversified alternations of sands, marls, bituminous
shales, copper-schists, limestone, hard and soft sandstones, and con-
glomerates, with interpolated porphyries and other igneous rocks.

Any doubt which might have existed as to the thickness of ‘the
whole, as derived from a transverse section like the preceding made
across the strata which are successively exposed at the surface, has,
however, been set aside in other places where no such great variety
in the strata occurs. Thus, near Eisenach, in the borings alluded to
in former communications, 2600 feet of sandstone and conglomerate-
beds were passed through in search of coal*. Recently, indeed, still
more satisfactory evidence has been transmitted to me by Professor
Naumann of Leipzig, who is about to bring out a work descriptive
of the two great divisions into which he separates the Roth-legende
or Lower Permian of Saxony. His upper division, of considerable
dimensions, consists of schistose red clay and marl, sandstone, and
fine conglomerate. A shaft has actually been sunk at Erlbach
through 2200 feet of the lower Roth-liegende only, with its con-
glomerates and interstratified porphyries, claystone, and tufts.

At that depth of 2200 feet true Carboniferous strata were indeed
reached ; but by the last accounts no bed of coal had been found in
them, though the Carboniferous formation had been penetrated to the
additional depth of 400 feet, making the total depth of the pit 2600 feet.

After this last-mentioned positive evidence of the order of super-
position, showing that the lowest member of the Permian rests un-
conformably on subjacent Carboniferous strata, coupled as the fact is
with the demonstration of Professors Goppert and Geinitz that the
fossil flora of these beds is distinct from that of the Coal-period, and
also with the physical proofs brought forward by Geinitz as to the
clear and unconformable separation of the two, it is to be hoped that
my able contemporary, M. Beyrich, will no longer class the Roth-
liegende with Carboniferous deposits.

* See ‘ Siluria,’ 2nd edit., p. 333.

1863. | MURCHISON—PERMIAN OF BOHEMIA. 305

In Germany, as in Britain, there are two zones of the Carboni-
ferous group, each of which has been clearly described by Geinitz.
The lower of these, which Professor Sedgwick and myself showed, in
the year 1839, to be of the age of our Mountain-limestone, has been
elevated with, and is conformable to, the Paleozoic rocks (Devonian
and Silurian) beneath it,—a phenomenon which ranges, indeed,
through Germany and France. The other, or overlying, coal-field,
like that of Bohemia and Saxony, is quite unconformable to the lower,
and is also quite unconnected with the base of the Permian,—it
having been clearly shown by Geinitz that its surface was abraded
before the lowest portion of the Roth-todt-liegende was deposited ;
whilst the latter formation contains within it rolled fragments,
derived from the uppermost coal-strata in the environs of Dresden.
It is thus proved that the Permian group is independent of all the
subjacent Paleozoic rocks, as established by stratigraphical and pale-
ontological data.

In concluding this sketch of the Permian rocks of Bohemia, let me
add a remark or two on the physical and geological conditions under
which these deposits may have been accumulated. Unlike the Per-
mian rocks of Northern Germany and England, the conglomerates,
sandstones, shales, marls, and limestones which constitute the so-
called Roth-liegende of Bohemia are not overlain by the Zechstein
with marine shells. Nor, as in Russia, do we meet with alternations
of deposits which were unquestionably marine with others which, from
their plants and some of their included remains, were probably of
lacustrine and terrestrial characters, showing rapid alternations of
level.

That portion of the Bohemian deposits which is most richly charged
with fossils has, from the character of its imbedded animal remains.
been referred by Geinitz to a freshwater origin. But if it be granted
that the small lizards which formed the impressions called Saurich-
nites are of terrestrial origin, is it settled that all the Fishes which
have been enumerated lived in fresh water? I confess that on this
head I am very sceptical, after seeing what has transpired respecting
the fishes of the Old Red Sandstone of Scotland, which for a time
were believed to have lived in fresh water, but which in Russia have
been found associated with unquestionably marine shells. Leaving,
however, naturalists to settle these points by some direct working
out of the true affinities of these fishes, I may state that my friend
Sir P. Egerton is of opinion that the Palwonisci were probably fishes
that lived in estuaries. On this point I would observe that, after all,
these Bohemian ichthyolites do not differ essentially from those of
the copper-slate of Northern Germany, which constitutes the natural
base of the Zechstein, just as the marl-slate is the bottom of the
purely marine Magnesian Limestone of England. Now, what if,
in this great development of Permian strata in Bohemia, the upper
red marls and sandstones of considerable thickness, which there
overlie the bituminous and cupriferous schists with Fishes, should
be found to contain a few sea-shells like the red Permian marls
at Manchester, and of forms like those in the Zechstein? Why, then

306 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 18,

the conclusion would fairly be drawn, that in Bohemia, as to the
west of the Pennine chain in England, there exists a full Permian
series, but with a different mineral-development from that of North-
ern Germany.

Throwing out this hypothesis as a caution, I would only add that
the well-rounded pebbles of the coarse and fine conglomerates, which
compose the lowest member of the group, seem to me to have been
formed by the waves of a sea beating on the shore of an estuary,
adjacent to which exuberant forests prevailed, with trees like the
Araucarites and Guglelmites, which must have required a genial
if not a warm climate to bring them to their large dimensions.
When we also consider that these water-worn sediments are at
intervals interlarded with outpourings of igneous matter, in the
form of porphyries, basalts, tuffs, and amygdaloids, we have before
us nearly all the material data for speculating upon the condition of
large portions of the surface of the northern hemisphere at the close
of the Paleozoic era, and antecedent to the origin of those new orders
of Animais and Plants which began to prevail in Mesozoic times.

Marca 18, 1863.

Samuel Baines, Esq., Holroyd House, Lightcliffe, near Halifax ;
Hilary Bauerman, Esq., Geologist of the North American Boundary
Survey ; Robert Mushett, Esq., Royal Mint, Tower Hill; and Frank
M‘Clean, Esq., B.A., C.E., late Scholar of Trinity College, Cam-
bridge, 2 Park Street, Westminster, were elected Fellows.

The following communications were read :—

1. On the CorrEtation of the several Susptvistons of the Inrertor
OouitE in the Mippie and Sours of Enexanp. By Harvey B.
Horr, MD k.G:s.

(Abridged.)

Introduction.—The Inferior Oolite in the South of England compre-
hends two well-defined subdivisions: namely, an upper member,
consisting of light-coloured, coarse-grained, more or less thin-bedded
or flaggy oolite, containing few fossils, and those chiefly in the form
of casts; and a lower member of hard, brown, ferruginous lime-rock,
often much speckled with ovoid grains of peroxide of iron, and
abounding in fossil remains. The relationship which these two beds
hold with respect to the other members of the Inferior Oolite has
been differently viewed by geologists.

The late Mr. Strickland evidently regarded the lower brown fos-
siliferous limestone as the equivalent of the Cephalopoda-beds of
Haresfield Hill*. -

On the other hand, Dr. Lycett, referring to the same bed at
Dundry, remarks that, “‘ considering the position of the Mollusca-
bed beneath the Freestones, and overlying the Cynocephala-stage, it

* Quart. Journ. Geol. Soc. vol. vi. p. 250 (1850), as quoted by Dr. Wright.

1863. | }OLL—INFERIOR OOLITE. 307

may approximately be placed upon the parallel of the Cheltenham
ferruginous pisolite.” *

More recently, Dr. Wright communicated to the Geological Society
a paper in which these lower beds at Dundry form the type of his
“‘zone of Ammonites Humphriesianus,’ while the white-oolite beds
above constitute his “‘ zone of Ammonites Parkinson.” The former
he has referred to the horizon of the Upper Freestone of the Northern
Cotteswolds, and the latter to that of the Trigonia- and Gryphite-
grits.

The result of my own investigations is at variance with each of
these views; and, having followed the beds stratigraphically along
the line of their outcrop, I shall endeavour to show that their true
position is higher in the series than is stated by any of these geolo-
gists, and that they are, in fact, the southern extensions of the
Upper and Lower Ragstones of Mr. Hull, the uppermost of which is
not represented in the typical section at Leckhampton, having risen
above the level of the country, and cropped out before reaching the
brow of the hills.

Southern side of the Mendips.—On the southern side of the Mendips
the Inferior Oolite nowhere exceeds 28 or 30 feet in thickness, of
which from 8 to 10 feet belong to the lower subdivision. The upper
subdivision immediately underlies the Fuller’s Earth; and its ight
colour, lithological structure, and general poverty in organic remains
readily distinguish it from the hard, brown, more or less massive or
rubbly limestone beneath, which is everywhere very fossiliferous.

Both members are well exposed in quarries and lane-side sections,
along the whele length of the belt of oolite as it ranges through
Dorsetshire and Somerset, but espeéially so in the neighbourhood of
Bridport, Yeovil, Castle Cary, Bruton, and, further to the north, at
Batcombe, and on the hills east of Shepton Mallet. At the “ Half-
way House,” between Yeovil and Sherborne, we find the following
section, which fairly represents the general characters of both sub-
divisions :—

Section at the “‘ Halfway House.”

A. Upper Ragstone. Thin-bedded oolite, with partings of brown,
SenEy, rahe m Clay ete css oa sn see eer fs ee ak 13
B. Lower Ragstone :—
1. Hard, ferruginous, thick-bedded limestone, divided near
the middle by a soft, friable, light-coloured band .... 6
2. Hard, light-coloured, fine-grained, sandy limestone.... 3

The upper part of B contains many Ammonites; and the soft friable
band which divides the bed contains several species of Gasteropods
_in a fine state of preservation, and also Collyrites ringens, C. ovalis,
Hyboclypus gibberulus, Terebratula Phillips, T. spheroidalis, Rhyn-

feet.

* “Cotteswold Hills,’ p.72, 1857. See also Proceedings of the Cotteswold
Club, vol. i. (1853) p. 64.

+ “ On the Subdivisions of the Inferior Oolite of the South of England, com-
_ pared with the equivalent beds of that Formation on the Yorkshire coast,”
Quart. Journ. Geol. Soc. vol. xvi. pp. 17 & 24 (1859).

308 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Mar. 18,

chonella spinosa, and, more rarely, R. acuta, Sow.*, R. ringens, and
R. Forbesii, with many other shells. The fossils of the lower part
of the bed are chiefly Conchifera. .

Following the escarpment of the hills northward, past Blackford
and Yarlington, we meet with numerous exposures in one or both of
these beds, and near Castle Cary and at Hadspen the lower one was
formerly extensively quarried. In the former locality the Lower
Ragstone contains Clypeus Agassiz, and in both Clypeus altus occurs,
while in the latter, as also in the quarries near Bruton-Bradstock,
Terebratula spheroidalis is met with in immense numbers. Ammo-
nites are rare.

At Sunny Hill, near Pitcombe, between Castle Cary and Bruton,
in a quarry above the Railway Station, we find the following section,
which, as it is at some distance from the last, will serve to show the
persistence with which these two subdivisions preserve their cha-
racters.

Section at Sunny Hill.

A, Upper Ragstone. Coarse, white, flaggy oolite..... Re 6
B. Lower Ragstone :—
1. Hard, brown, thick-bedded, highly fossiliferous limestone 12
2. Hard, sandy, compact, light-coloured limestone, with a
FEW: OBST, 3-4-5) 40d covershar deta ae heen eae ae 2

In this quarry the fossils of the Lower Ragstone are chiefly Con-
chifera and Brachiopoda. It is worthy of remark that the only
Ammonite observed was Ammonites Parkinson. Among the fossils
noticed were Rhynchonella spingsa, R. angustata, Terebratula Phil-
lipsu, T'. spheroidalis, Gryphea subloba, Desh., Ostrea pixiformis,
Wr., Lima gibbosa, Trigonia costata, Pholadomya Heraulti, Holectypus
hemisphericus, &. The bed No. 2, or basement-bed, contained a
few fossils, very difficult to extract.

In the quarries around Bruton, and in the railway-cutting near
the church, both series of beds are exposed, as also on the road
through the Hedgestock turnpike-gate to Batcombe, and at Creech
Hill. At the latter locality, ascending the hill from Lamyat, through
a deep lane-cutting in the Ammonite-sands, to the brow of the hill,
the lower fossiliferous limestone, not well exposed, is seen above the
sands, and above this the Upper Ragstone, which is here about 15
feet in thickness, and is, in part, a tolerably thick and evenly bedded
rock, while some of its beds exhibit lines of oblique lamination.
About the middle of tltese upper beds there is a layer in which the
fossils have the shell preserved.

The hard, pale-coloured, sandy limestone which formed the base-
ment-bed of the Lower Ragstone in the sections at the “‘ Halfway .
House” and at Sunny Hill does not appear to be continued much
further to the north, as it was not observed at Creech Hill, and is
- absent at the Vallis Farm, 14 mile north-west of Frome, where, in
the quarry on the right bank of the stream, the Lower Ragstone is

* Tam not aware that this fossil has hitherto been recorded as an Oolitic
species.

1863.]

8.8.W.

Generalized section of the Inferior Oolite from Cheltenham to Bath.

NN.E.

Bath and Dundry..-.------—-

Doddington Park.---------

Cross Hands Inn. ---~----

£iorton:--=——=—== |

Avening. --~—----

Nailsworth.---—----

Rodboro’ Hill.----- =

Stroud..----- L

Sporebed Hill. ____. lil

Painswick. ---.- 1 Hl

h
Leckhampton.--- i

HH
iM |

Cheltenham...- i 5

Cleeve..-. a

&
Notting Hill ____- ss

VOL. XIX.—-PART I.

SS
——

——S =>

= ———

mi

SSS
——

——
om

Pe ss aa
rir

a
thir

6 Upper Freestone.

b. Lower Ragstone.

f. Pea-grit.

e. Lower Freestone.

d. Oolite-marl.

a. Upper Ragstone.

HOLL—INFERIOR OOLITE. 309°

seen separated from uptilted Car-
boniferous strata by alternate
layers of more or less compacted
clay, with pebbly bands, resting »
on a bed of conglomerate, beneath
which Mr. C. Moore, of Bath, de-
tected a thin stratum containing
Avicula contorta*.

North side of the Mendips.—Be-
tween the Mendips and the valley
of the Avon the same beds continue
to represent the Inferior Oolite,
and are well exposed in the rail-
way-cuttings between Wells and
Ammersdown, and, in a series of
roadside-quarries, on to Radstoke, -
and further north, by the side of
the canal near Dunkerton, at the
foot of the Viaduct Bridge near
Limpley Stoke, and at Widcombe
Hill, near Bath. In all these lo-
calities they continue to preserve
those general features which serve
to distinguish the one from the’
other. In the neighbourhood of
Dunkerton the Upper Ragstone is
about 20 feet in thickness, and
contains Corals of the genera Ana-
bacia, Stylina, and Isastrea.

The outlying patch of Inferior
Oolite at Dundry Hill is connected
with this portion of the main body
of the range by the smaller patches
of the Barrow Hills, Stanton Prior,
and Timsbury. At Dundry the
light-coloured, partly flaggy, partly
thick-bedded oolite which caps
the hill belongs to the upper sub-
division, and in certain layers at
the top of the hill contains Corals
of the same genera and species as
the similarly situated beds in the
neighbourhood of Dunkerton and
Bath. Beneath this we find beds
of rubbly and ferruginous lime-

* This interesting section has been
given in detail in Mr. T. R. Jones’s re-
cent Monograph of Fossil Estherie
(p. 74), published by the Palsontogra-
phical Society. ; :

x.

310 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 18,

stone belonging to the Lower Ragstone, and having a somewhat
greater aggregate thickness than in other parts of the country; but
this may possibly be more apparent than real, and owing to some
slight settlement of the hard ragstones, around the flanks of the hill,
upon the yielding sands and Upper Lias clays beneath.

The Cotteswolds.—Passing across the valley of the Avon, we are
able to trace these beds past Dryham Park to the quarry half a
mile east of Doddington Ash, where the junction of the two Rag-
stones is well exposed, the lower one abounding in fragments of
Trichites.

But, two miles further to the north, im the lane leading from the
‘ Cross Hands’ Inn to Old Sodbury, the Ragstones are seen under-
lain by about 6 or 8 feet of thin-bedded white oolite, the lower beds
of which are made up, in part, of comminuted shells. It rests
upon a yellowish sandy bed, 2 or 3 feet thick, containing casts of
Gresslya; beneath this are the brown-coloured argillaceous Cepha-
lopoda-beds, with Belemnites and casts of Ammonites. Nearly the
whole thickness of this white oolite is seen in the lane-side cutting.
The Lower Ragstone crops out in the field above the section, and is
also seen a little further along the lane, while the Upper Ragstone
and overlying Fuller’s Earth are exposed in a quarry opposite
the inn.

This white oolite, when followed northward, is seen gradually to
increase in thickness, and its relationship to the Ragstones may be
well studied in a quarry near Horton Rectory, while its basement-
beds and its junction with the upper part of the Cephalopoda-beds
are exposed in the lane half a mile south of the Rectory.

Section near Horton Rectory.

A, Upper Ragstone. White, thin-bedded, friable oolite...... 12
B. Lower Ragstone. Massive, hard, brown limestone, in two
or thrée beds, with matty dossils:., -en) eso about 10
C. Freestone. Thick-bedded white oolite, used for building-
SLOIE ..iihce » aceiah ele jab ai ccues coe ee ee ee 12
D. Yellow sandy rock, containing Grresslya .............. 2 to3
E. Cephalopoda-beds (Ammonite-sands or Upper Lias sands).
Alternate beds of marly, more or less indurated, and rubbly
rock, speckled with oolitic grains of peroxide of iron, and
containing Belemnites and Ammonites; 8 feet exposed .. 8

The Lower Ragstone is here crowded with fossils, among which
are Trigonia costata in great numbers, Lima proboscidea, Ostrea
Marshu, Trichites, Belemnites, Rhynchonella spinosa, Rhynchonella
quadriplicata, &e. The lower beds of the underlying Freestone con-
tain a small Pecten in great abundance, which occurs also in the
same position at Hawkesbury and Leckhampton.

A similar section exhibiting both the Ragstones, overlain by the
Fuller’s Earth, and resting upon the Freestone, which is probably
2 feet in thickness, is seen near Hawkesbury, on the road to Pool

art.

1863. ] : HOLL—INFERIOR OOLITE. 311

The Freestone continues to increase in thickness as we proceed
from the last section to Wotton Underedge, being 35 or 40 feet
thick at Coneygore Wood, a mile north of the town. Continuing to
thicken towards Frocester and Painswick Hills, it acquires its full
development in the vicinity of Cheltenham, where it constitutes the
<‘ Building Freestone” of Leckhampton. The overlying Ragstones
at the same time gradually rise to higher levels, and at Coneygore
Wood crop out before reaching the brow of the hill, but may be
found on higher ground half a mile further along the read, towards
the Rushmire turnpike-gate.

From the section in Coneygore Wood and the sides of Symond’s
Hall Hill, the upper of the two Ragstones may be followed north-
ward to Nympsfield and Avening, and along the sides of the Vale of
Nailsworth, where it becomes identified with the “‘ Upper Ragstone”’
or “Clypeus-grit” of Mr. Hull*, and the “ Pholadomya-grit” of
Mr. Lycett?, the casts of Pholadomya and Homomya and the re-
mains of Clypeus (Nucleolites) Plotii especially characterizing this
highest zone in the northern part of the Cotteswolds, but being by
no means common south of the Valley of Stroud.

In like manner the fossiliferous hmestone immediately beneath it
is continued onward to Rodborough Hill, where it becomes continuous
with the Trigonia- and Gryphite-grits of Messrs. Wright, Lycett,
and others, and the Lower Ragstone of Mr. Hullt. In the neigh-
bourhood of Nympsfield this latter has associated with it a band of
hard pale-coloured limestone, crowded with Rhynchonella spinosa.

In the vicinity of Wotton, as at Symond’s Hall Hill, the Lower
Ragstone rests directly on the Building Freestone ; but, crossing the
high ground on the east to the Vale of Nailsworth, we find, in the
smaller tributaries of Horsley and Avening, a few inches of the Oolite-
marl, with its characteristic Terebratula fimbria, underlying the base
of the Ragstone, and resting upon 4 or 5 feet of pale-coloured ar-
gillaceous limestone, which graduates downwards into the Freestone.
This is the earliest appearance of the Oolite-marl in the southerly
direction, and a little further down the valley it begins to be sepa-
rated from the base of the Ragstone by the interposition of some
more or less sandy oolite belonging to the Upper or “ Bastard”’ Free-
stone. This latter, at Nailsworth, is about 3 feet in thickness; but,
passing along the valley to Stroud, both it and the underlying Oolite-
marl gain in thickness and importance, and separate the Ragstones
more and more widely from the Lower Freestone.

. At Rodborough Hill the Lower Ragstone is about 10 or 12 feet in

thickness. The basement-bed is crowded with Conchifera, and con-
stitutes the Lower Trigonia-grit, or lowest of the three members into
which it has been subdivided. As we proceed northward, however,
both this and the middle, or Gryphite-grit division, increase in thick-
ness. At White’s Hill, near Randwick, Mr. Lycett has estimated it
at 5 feet. At Kimmersley Castle it is somewhat more, and contains

* Memoirs of the Geological Survey, “Geology of parts of Wiltshire and
Gloucestershire,” p. 10.
t ‘Cotteswold Hills,’ p. 68. t Op. cit. p. 10. ;
~

312 PROCEEDINGS OF THE GEOLOGICAL socrety. [ Mar. 18,

many Conchifera in a good state of preservation ; but it attains its
greatest development at Leckhampton Hill.

Over a considerable portion of the north-western part of the
Cotteswolds, especially towards the verge of the hills, the Upper
Ragstone has been denuded, and it is only beneath the isolated
patches of Fuller’s Earth, brought down by faults, that it occurs, and
in these localities it is seldom well exposed. It may be seen, how-
ever, to the east of the fault at Cold Comfort, and still better on the
hills beyond Andoversford.

The cropping-out of this bed before reaching the verge of the hills
in the neighbourhood of Cheltenham appears to haye led Dr. Wright
to overlook it altogether*.

I quite agree with Dr. Wright in his suggestion that, away from
the western escarpment of the hills, the Upper and Lower Trigonia-
grits haye come into contact, as the great Oyster-bank which consti-
tutes the Gryphite-grit extends only from the vicinity of Rodborough
Hill to Cleeve Cloud, and eastward to the neighbourhood of Andovers-
ford; but the Lower Ragstone, as seen in the quarries between the
latter place and Hampen, consists chiefly of the Upper Trigonia-grit,
having at its base a bed, from 1 to 2 feet in thickness, of very hard,
brownish limestone, pierced everywhere by small vertical tubes, pro-
bably the work of some species of Annelid. These Lower Ragstone-
beds may be seen in situ on the Stow Road, a mile and a half east of
Andoversford, and again half a mile beyond Naunton Inn, and on
the top of a hilla mile south-west of Aylworth, where its junction
with the Upper Freestone is exhibited.

But above this Lower Ragstone, and resting upon it, there is seen,
over all the country around Naunton and Turk Dean, and west of
North Leach, a higher bed, 15 or more feet in thickness, of very
coarse-grained, rubbly, white oolite, containing fossils in abundance,
but not in great variety. This is the northern extension of the
Upper Ragstone, which has here become fossiliferous and more
coarsely oolitic. The lower part of the bed is crowded with Tere-
bratula globata, and the central portion contains Clypeus Ploti in
great numbers. In going from Naunton Inn to Harford Bridge,
we cross in succession the outcrop of the Upper Freestone, the Lower
Ragstone, and then the Upper Ragstone to the Fuller’s Earth, and we
again find the two latter, on the opposite side of the stream, in the
lane above Harford.

The Upper Ragstone is well exposed at Aylworth, where it has
been brought down to a lower level by faults, and also by the side
of the road leading from Turk Dean to Aston, where an upper bed
is exposed, made up of badly preserved fossils imbedded in coarse
white oolite. Clypeus Plotii is most abundant in the middle portion
of the bed.

The junction of the Upper Ragstone with what remains of the
Lower Ragstone is well seen in a quarry by the side of the Roman
Foss-way, near the fifth milestone aus Stow, where we find the
following section :—

* Quart. Journ. Geol. Soc. vol. xvi. pp. 38 & 43.

-1863.] HOLL—INFERIOR OOLITE. 313

Section near Stow. feet.

A. Coarse, rubbly, white oolite, becoming darker-coloured to-
wards the base, and containing in its lower portion great
numbers of Terebratula globata, Lima gibbosa, and Pecten

(2 SE PRs 2s 2 ee 8
B. Very hard, compact, brown limestone, covered on its upper
surface with a large flat species of Gsicen:<..A-.. aiaiday hte 3

C. Lower Freestone te the bottom of the section.

The Lower Ragstone is here reduced to 3 feet in thickness, and
rests upon the Lower Freestone, the intervening members having
thinned out between this place and Turk Dean. A mile further to
the south-west, in the quarries above Clapton, this subdivision has
nearly reached its extreme limit in this direction ; some hard, brown,
sandy rock, with fossils, and a mere trace of the basement-bed being
all that remains to represent the Lower Ragstone. At Little Ris-
sington both this and the underlying Freestone have entirely thinned
out, and the Upper Ragstone rests directly on the Upper Lias clay ;
but north of Stow, on the road to Moreton, there is still some portion
of the Lower Freestone remaining.

Fossits oF THE Upper RAGSTONE.

Nerinza, sp. . . . . .« Little Rissington.
Myacites, casts of three species . » » Naunton, Aston, &e.
Gresslya abducta, PAill.? (cast) . . Aston, Clapton.

Homomya gibbosa, Sow. (cast). . . Aston, Naunton.
Pholadomya Heraulti, 4g. . . . . Aston, Naunton, Little Rissington.
Dewalquei, Zyc. . . . . . « Little Rissington.
Isocardia (cast) . . . . . . © . Stow, Aston.
Astarte elegans, Sow. . . . . . .« Aston.
ae hice. 12) Os ee.
Trigonia angulata, Lye. '?. . . . . Abundant around Naunton, Aston, &c.
costata, Park.. . . » « . Little Rissington.
Nucula variabilis, Phill.?. . . . . Aston.
Lima duplicata, Bach 3 ch sxe. awe
gibbosa, Sow.. . . . «. +» « Naunton, Stow, Aston, &e.
Pee SOW, 5 oo Mas ce fie) » Aston.
NEOPM, OW. soe: oo a ASOD.
Ostrea acuminata, Sow. . . . . « Stow, Naunton, Aston.
Terebratula globata, Sow.. . . . . Very abundant everywhere.
Rhynchonella angulata, Sow. . . . Naunton, Stow, Aston.
concinna, Sow. . . pore “o. ABER.
Serpula, sp. . - Clapton.

Nucleolites (Clypeus) Plotii, Klein . Abundant every where.
Echinobrissus clunicularis, Lhwyd . Aston.

Holectypus depressus, Lamk. . . . Aston.

Isastrea limitata, Z.g¢ H. . . . . Aylworth.

Anabacia orbulites, Lamk. . . . . Naunton, Stow.
i Se ules? me DEON.

The * Rolling Bank” Quarry.—Dr. Wright has referred all the
fossils of the Rolling Bank Quarry to the U. pper Freestone beds of
Cleeve, and considers them to be the northern equivalents of the
Conchiferous Lower Ragstone of Dundry, Yeovil, &c.* That this is

* Quart. Journ. Geol. Soe. vol. xvi. p. 18.

314 PROCEEDINGS OF THE GEOLOGICAL society. [ Mar. 18,

not so, however, is, I think, made manifest by a careful examination
of all the beds which occupy the interval between the Oolite-marl and
the base of the Ragstone, where they occur im situ. Leaving the
Rolling Bank Quarry, which has been opened into “ tumbled oolite”’
resting upon the Upper Lias Clay, and ascending the hill in an
easterly direction, we come to two quarries situated in the Lower
Freestone, and in the higher of the two, distant from the Rolling
Bank Quarry about 200 paces, the Oolite-marl occurs, 9 or 10 feet
thick, resting upon the Lower Freestone, and overlain by 5 feet
of the Upper Freestone. The hill rises only a few feet above the top
of the quarry, and a little further on, at the very summit of the hill,
is a second quarry. The lowest beds on the western side of this
quarry belong to the base of the Upper Freestone, and, formerly, a
portion of the upper part of the Oolite-marl was also exposed.
These beds, which dip slightly towards the east, pass upwards into
a brown, calcareous, sandy rock, the uppermost stratum of which is,
in parts, composed entirely of yellow and brownish sand. Resting
upon this, and immediately under the turf, on the eastern side of the
quarry, is the Lower Trigonia-grit, with Terebratula wmpressa, Tri-
gonia costata, Goniomya angulifera, Ceromya Bajociana, Myacites,
Gresslya, and many other fossils.

These beds are again seen in a third quarry, a little further on in
the same direction. Eleven feet of rock are here exposed, the upper
three feet of which are sandy and ferruginous, and similar to the top-
beds in the last quarry. The lower eight feet consist of brown sandy
oolite, moderately thick-bedded. Neither the uppermost nor the
lowermost beds can be seen; but, close by, at only 3 or 4 feet
higher elevation, the junction of the former with the Lower Trigonia-
grit may be seen in some small superficial excavations which have
been made in searching for the sand, which here and there occurs at
the top of the Upper Freestone.

The junction of the Upper Freestone with the overlying Lower
Trigonia-grit is, however, better seen in a number of small pits
along the north side of the ravine which lies a little to the right.

From all these exposures the following section may be con-
structed :—

Section of the Rolling Bank Quarry.

A. Lower Trigonia-grit. feet.
a. Rubbly limestone, with many fossils—Corals, &c. ..
6; Brown and, blue.clay.e.j.23 2 Heemt-t eee see eee 1 to 2

B. Upper Freestone.
a. Hard, brown, coarse-grained limestone, with frag-

ments of Shells, not persistent ............ 6 in. to 2
6. Yellow and brownish sand, with lenticular masses of
NeTMMSGOMme YS USE EH ES ck AR Te SY a 3

c. Ferruginous arenaceous limestone and sandy oolite,
the lowest bed pierced by the vertical tubes of
Annelidsraboutie eee. 8s SS oe eee ee ee 14

1863. | HOLL—INFERIOR COLITE. 315

C. Oclite-mazrl. feet.
a. Pale-coloured, argillaceous limestone, with Tere-
bxpkulee fla brtie sila Se. ceils siren k stay op ene oe 3 to 4
b. Cream-coloured marl, with Terebratula jfimbria,
Conals, ers ho Sana ug ns eer cy aiieia of Sic Stu oon x

D. Lower Freestone.

The hill is capped by Gryphite-grit, with Gryphea subloba, Desh.

Thus, at Cleeve, a series of beds of very unstable character occupies
the interval between the top of the Oolite-marl and the base of the
Lower Ragstone, and represents the Upper Freestone of Leckhamp-
ton; but nowhere, in these beds 7 situ, do we find any of the fossils
of the Rolling Bank Quarry. Apart, however, from this negative
evidence that these beds are not on the same horizon as the Conchi-
ferous limestones of Dundry, we have the fact that this Lower Rag-
stone may be traced continuously from Dorsetshire, through Somer-
setshire, and along the escarpment of the Southern Cotteswolds, up
to the Trigonia-grits of Rodborough and Leckhampton Hills.

The Rolling Bank Quarry has been excavated into an accumu-
lation of fallen débris which has collected at the foot of the oolitic
cliffs, and consists chiefly of Lower Ragstone; and nearly all the
fossils that are found there belong to this subdivision.

The Pea-grit—The lowest member of the Inferior Oolite is the
Pisolite, or Pea-grit, which immediately underlies the Lower Free-
stone. This bed has been generally stated to thin out at Notting
Hill. Its southern limits have been somewhat more variously de-
fined. Its northern attenuation at Notting Hill is true, however,
only as regards its pisolitic structure, as the bed itself, although no
longer pisolitic, appears to underlie the Lower Freestone of the
Bredon outlier.

Below the brow of the eastern extremity of the hill, above Aston,
Rhynchonella cynocephala, Rich., the small dwarfed variety similar
to the one which occurs at Wotton Underedge*, is found in de-
tached blocks of hard limestone; but I have not been able to find
the bed in situ. This is the most northern locality at which this
fossil has hitherto been met with in the Cotteswold district. Further
round the hill, above Elmley Lodge, there is a bed of hard, yellow,
sandy limestone, some layers of which are full of fragments of Pen-
tacrinus and spines and plates of Echinoderms, with some fossils
entire. Terebratula plicata is the dominant fossil, but the valves
are usually separated. Still further on, beneath the ancient encamp-
ment of Bredon Tower, nearly 10 feet of this bed is exposed,
having the Lower Freestone resting upon it. On the surface of the
blocks, besides the fragments of Crinoidea and Echinoidea, are many
specimens of Cricopora verticillata, Mich.?, and other Bryozoa.

To whatever position the grey and yellow limestone with Rhyn-
chonella cynocephala may be assignable, the bed above referred to
belongs, I think, to the Pea-grit.

Towards the south the Pea-grit ceases to be pisolitic, or is only

* The specimen, with part of the matrix, is in the author’s cabinet.

316 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 18,

very slightly so, at Painswick Hill. Beyond this itis represented by
yellowish sandy limestone and ferruginous oolitic rock, which, near
the Horseponds, are less than 20 feet, and at Haresfield Hill are
about 12 feet in thickness. At Frocester Hill, the light-brown
sandy rock, with casts of Gresslya and Pholadomya, overlying a hard
fossiliferous bed, together about 74 feet in thickness, is all that re-
mains to represent the Pea-grit of Crickley Hill; and the 2 or 3
feet of yellowish sandy rock, with Gresslya, which was seen under-
lying the Freestone in the sections at Horton, and near the Cross
Hands Inn, probably belongs to the same zone, and indicates the
approaching southern limits of the bed.

All these beds thin out in a south-easterly direction, as already
shown by Mr. Hull*. The Upper Ragstone alone crosses the valley
of the Evenload, and in Oxfordshire is the only representative of the
Inferior Oolite, but finally it thins out in the vieinity of the Cher-
well, The Lower Ragstone was seen to have nearly reached its
eastern limits at the quarries above Clapton, and is absent at Stow,
Seizincote, and Bourton-on-the-hill. The Upper Freestone and
Oolite-marl are on the eve of disappearing at Condicote and Turk
Dean, and do not extend southward further than Avening; while
the Lower Freestone is seen thinning out at Stow, Sherborne, and
near Doddington Park, ten miles north of Bath. The northern and
southern limits of the Pea-grit have already been indicated. East-
ward it ceases to be pisolitic before reaching Dowdeswell, beyond
which the bed has not hitherto been recognized. |

Geographical Distribution of the Fossils.—The fossils of the Upper
Ragstone, as far as they are at present known to me, have been >
already enumerated. Those of the Lower Ragstone have been re-
corded by Dr. Wright, Mr. Lycett, and Mr. Hull. With respect to
the lists given by Dr. Wright, however, it must be borne in mind
that the Humphriesianus-zone of Dorsetshire and Somerset, and the
Parkinsoni-zone of the Northern Cotteswolds, are on one and the
same geological horizon.

The geographical distribution of the fossils of the Lower Ragstone
is very unequal, and many of the species and even genera, although
abundant, are altogether local. The Ammonites, for instance, are
numerous only in a few localities in the southern part of the district ;
elsewhere only scattered individuals are met with, and not more
frequently than they are in the northern part of the Cotteswolds +.

* “On the South-easterly Attenuation of the Lower Secondary Formations
of England,” Quart. Journ. Geol. Soc. vol. xvi. p. 71.

t+ With respect to Ammonites Parkinsoniand Ammonites Murchisone, these
fossils are by no means so restricted in their range in time as some authors sup-
pose. A. Parkinsoni is stated by Mr. Lycett to occur in the Pea-grit “ but
sparingly” (Cotteswold Hills, p. 37). It has been met with in the Lower Rag-
stone of Somersetshire, and occurs very generally in the Upper Trigonia-grit of
the Northern Cotteswolds. A. Murchisone was found by the officers of the
Geological Survey in the Lower Ragstone of Leckhampton and Stanley Hills
(Hull, Geol. Cheltenham, p. 48), together with 4. Sowerbyi, A. concavus, and
A. Dorsetensis, and in the Upper Ragstone near Churchill, in Oxfordshire
(Geol. of Coumtry around Woodstock, p. 13). On the authority of Professor

1863.] PORTER—OXFORD CLAY. 317

Among the Brachiopoda, we find Terebratula Buckmani, Dav., in
great abundance at Cleeve, Leckhampton, and Sherdington. Tere-
bratula Wrightii is equally gregarious, as in the Perna-bed at Cold
Comfort ; but it is only sporadically distributed elsewhere in the
neighbourhood, and does not occur in the south. Near Andovers-
ford, a small Zerebratula, probably a dwarfed variety of 7. ornitho-
cephala, is met with in great abundance, and more sparingly so at
Leckhampton, but I have not found it anywhere else. In the
southern part of the district we find Terebratula spheroidalis occur-
ring in the same great abundance at Hadspen and Bruton-Bradstock,
while in neighbouring quarries they are by no means numerous.
The Gasteropods are mostly southern forms, while the conditions of
the sea-bottom upon which the calcareo-argillaceous beds of the
Lower Trigonia-grit were deposited appear to have been favourable
to the life of the Anatinide. Of the Echinoderms, most of the
species of the northern part of the Cotteswolds are different from
those of the southern side of the Mendips, and instead of Clypeus
(Nucleolites) Plotii, Hyboclypus caudatus, Pedina rotata, and Holec-
typus depressus, we find Clypeus Agassiz and C. altus, Hyboclypus
gibberulus, Holectypus hemisphericus, Collyrites ringens, and C. ovalis,
and others that are not, or only rarely, found in Gloucestershire.
Omitting, however, these local and also the rarer forms, most of the
more common and characteristic fossils on both sides of the Mendips
are identical *.

In this communication I have endeavoured to show the relationship
the several subdivisions of the Inferior Oolite hold with respect to
each other,—and that the conclusions that have been arrived at by
some writers on this point, based on the evidence of fossils only, are
not borne out when the beds come to be traced stratigraphically
from one end of the Oolitic range to the other.

2. On the OccurRENcE of large Quantities of Foss Woop in the
Oxrorp Cay, near PerersorovcH. By H. Porter, M.D., F.G.S.

[ Abstract. ]

Tue author gave a short description of the Oxford Clay area in the
neighbourhood of Peterborough, and mentioned the properties which
caused it to be worked, in the parishes of Eye, Thorney, Whittlesey,
Stanground, Fletton, and Stilton, for the manufacture of bricks and
tiles. The clay is very fossiliferous at all these places, the most
abundant remains being those of Belemnites Puzosianus, Gryphea dila-
tata, Ammonites Elizabethe, A. Duncani, A. convolutus, A. cordatus,
A. fluctuosus, A. hecticus, A. Comptoni, and a few other species of

Morris (Cat. Brit. Foss.), it occurs at Chideock, Sherborne, and Dundry,
localities where the Ragstone is the lowest member. Both 4A. Parkinsoni and
A. Humphviesianus have been found in Yorkshire in beds which are probably
younger than the Inferior Oolite of Gloucestershire.

* Some of the Inferior Oolite forms of Somersetshire pass upwards into the
Fuller’s Earth—Hyboclypus gibberulus, Collyrites ovalis, and Holectypus de-
pressus being not uncommon in this bed near Bruton.

318 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 18,

Ammonites which Dr. Porter had not been able to determine. There
were also Cerithium Damonis, Serpula vertebralis, Belemnites gracilis,
Pecten, 2 sp., Nucula, Corbula, Avicula, abundant remains of [chthyo-
saurus, Plesiosaurus, Pliosaurus, and Steneosaurus (?). The author had
also found a portion of a spine of Ptychacanthus ornatissimus, and a
few palatal teeth of Strophodus subreticulatus. What, however, he
particularly called attention to in this communication was the occur-
rence of large quantities of fossil wood, in pieces sometimes more
than a yard in length, highly bituminous, quite black, having a
fracture similar to jet, and capable of almost as high a degree of polish
as that mineral; it is also exceedingly brittle, and, when exposed to
the air, cracks in all directions. Most of the specimens are flat, and
bear on their surface impressions of Ammonites and other shells.

3. On a new Macrurovs CRUSTACEAN (SCAPHEUS ANCYLOCHELIS) from
the Lias of Lyme Reets. By Henry Woopwarp, Esq., F.Z.S.

[Communicated by Professor Morris, F.G.S.]
[Puate XI. ]

Tuts beautiful and very perfect Crustacean (from the collection of
James Harrison, Esq., of Charmouth) was obtained from the zone of
Ammonites Bucklandi of the Lower Lias of Tape-ledge, near Lyme
Regis.

A complete detached fore-limb of large size, from the collection
of E. C. H. Day, Esq., of Charmouth; an imperfect fore-limb,
and perfect termination to a secondary limb, from the collection of
Capt. Hussey ; together with two fragmentary portions of limbs and
abdomen, from the collection of Mr. J. W. Marder, of Lyme Regis,
are all the remains of this new and very remarkable form hitherto
discovered.

From the length of the fore-limbs, their monodactylous extre-
mities, and also the peculiar spatulate form of the penultimate joint
of the succeeding pairs of limbs, I am convinced of the propriety of
placing it near Bronn’s genus Megacheirus*, many species of which
are described and figured in Miinster’s ‘ Beitrage zur Petrefacten-
kunde,’ Part II., from the Lithographic Limestone of Solenhofen.

That genus has been obtained from the Oxford Clay of Wiltshire
and Normandy, and from the Inferior Oolite and Lower Lias of
Bavaria.

There are, in the British Museum, several examples of the genus
Megacheirus from Solenhofen, and also from the Oxford Clay of Wilt-
shire; but I have only been able to refer to the figures and descrip-
tions given by H. von Meyer and F. A. Quenstedt, of the species

* The name Mecocheirus of Germar (1826) would have been entitied to priority
over Bronn’s Megacheirus (1836), but Germar omitted to give a definite descrip-
tion of his fossil. Megacheirus should also properly include the genus Péero-
cheirus of Bronn, all the Megacheiri being “ wing-fingered,” although the fringe
of hair upon the fore-arms is not always preserved.

MGOOM H SITHHOOTAONV SQYHHdVOS

dur '930\\"M URL IOAA 094 “OP PLUMpPooAA

Id ‘XK TA 90g Joo) usnop yxent)’ | }

tle ka VLG Wet

z

¥

1863. ] WOODWARD—MACRUROUS CRUSTACEAN, 319

found in the Oxfordian Oolite of Normandy *, and those occurring
in the Inferior Oolitet and Lower Lias ¢ of Bavaria.

After careful comparison, I am satisfied that our Liassic Crustacean
is quite distinct from any of these.

ScaPHEUS, gen. nov.

The carapace of Scapheus differs from the nearly smooth cephalo-
thorax of Megachewrus, which is quite destitute of the spines and
prominent rostrum so conspicuous in this fossil; and the smooth,
slender fore-limbs of Megacheirus (considerably exceeding the entire
length of the body) contrast strongly with the more robust spiny
arms and great terminal hooks of Scapheus. In the basal joints of
the outer antenne, the form of the abdominal segments, and the
lamine of the tail, this new genus is also distinguished by well-
defined characters. I propose to name the only known species, re-
presented by Mr. Harrison’s specimen, Scapheus ancylochelis §.

The long monodactylous fore-limbs are quite peculiar to these
fossil genera of Crustacea. The nearest living analogues are found in
the fossorial group Thalassinide, but the resemblance is only evident
in the structure of the limbs and in the hirsute character of both
limbs and abdomen ; the termination of the fore-arms in Scapheus
being similar to Ranina, another burrowing Crustacean of a different
group. The abdomen, however, in nearly all the true fossorial
species is more or less rudimentary, and but little adapted for nata-
tion, whereas in this genus the marginal (or epimeral) portion of
the abdominal segments is as well developed as in Nephrops or
Homarus; and the lamine of the tail and the traces of false ab-
dominal feet also indicate a Crustacean well adapted for swimming.
Taking these points of structure into consideration, we cannot sup-
pose this to have been an habitual burrower, but simply as searching
for its food and concealing itself among stones, for moving which its
powerful fore-limbs seem well adapted, although (from the very
rudimentary character of the fixed ramus of the penultimate joints)
but little suited for organs of prehension.

_The great similarity of the Crustacea of our English Lias with
those from Solenhofen has appeared to me to be a most interesting
point, and I hope hereafter to offer figures and descriptions of several
others not yet enumerated from our Lias, and all analogous to those
of the Upper White Jura of Bavaria.

SCAPHEUS ANCYLOCHELIS, spec. nov.
Cephalothorax one-third longer than deep. Rostrum prominent,

* Palzontographica, vol. i. p. 144. t. 19. f. 2-19.

t Der Jura, p. 520. t. 69. f. 8-11. This species, described by H. von Meyer
under the name of Ewmorphia socialis, from Dives in Normandy, &c., is the same
which Quenstedt describes as Mecocheirus socialis, from the Inferior Oolite of
Bavaria. It is much smaller than M. longimanus from the Solenhofen limestone.

t Quenstedt describes two species from the Lower Lias of Bavaria—Meco-
cheirus grandis, Q. (p. 88. t. 11. f. 15, 16), and M. olifex, Q. (p. 89. t. 11. f. Le LL
consider M. grandis more nearly related to our Lias genus tian to Megacheirus,
so far as Quenstedt’s figures permit me to judge.

§ From oxageds, a “ digger,” and dyxtAoxyAns, “with hooked claws.”

~

320 PROCEEDINGS OF THE GEOLOGICAL socreTy. [Mar. 18,

curving upwards, armed with a double row of conical, slightly curved
spines, nearly 1 inch in length, and extending back to the cervical
furrow, thence in a single row down the median line of the carapace
to the posterior margin. Cervical furrow broad and strong, termina-
ting in a smooth rounded sinus near the antero-lateral margin; the
branchial region divided from the gastric by two slender parallel
furrows, which, passing obliquely down the sides of the carapace,
unite with the cervical furrow near the margin. The posterior and
lateral borders of the carapace are raised, and have a sulcus within
the margin; the surface of the posterior portion is scabrous, of the
anterior portion finely punctate, the antero-lateral portion being
covered with minute irregular spines. Two lines of minute spines
extend forward from the cervical furrow obliquely on each side of the
median furrow towards the rostrum, and another line extends back-
wards and upwards from the posterior margin of the same furrow, on
either side, obliquely to the median line. Eye globular (?), and, from
the size of the orbit, probably large. Outer pair of antenne large,
multi-articulate, 4 to 5 inches long; three basal joints large and
armed with spines. Inner antennz smaller, multi-articulate; basal
joints crushed, and insufficient for description.

The legs forming the first pair are symmetrical, and equal in length
to the entire body; they are scabrous, and armed with several
rows of smooth, strongly curved spines; extremities monodactyle,
the fixed ramus of the penultimate joint being only represented
by a large spine one-fourth the length of the ultimate joint, which is
curved and pointed. The limbs of the second pair are also armed
with spines along their margin; the penultimate joint is flat and
very broad at the distal extremity, the ultimate joint small and
pointed. Third and fourth pairs like the second, but nearly smooth.
The fifth pair is much smaller than the rest, and only very imper-
fectly preserved. Abdomen rather longer than the cephalothorax.
The epimeral portion of the first segment much less produced, and of
the second segment much more produced, than in those succeeding ;
all the segments minutely punctate at, and spinous upon, their
lateral margins. Each segment deeply curved in front to receive a
small polished ball-articulation attached to the posterior margin of
each joint of the abdomen. ‘The tail-lobes are broad, the outer
lamina having a crescent-shaped division near its extremity, bor-
dered by 2 or 3 spines ; the inner lamina is smooth, and the central
lobe slightly punctate, with 2 or 3 small spines along its margin.

False abdominal legs apparently fitted for natation ; but two only
are preserved, and those very imperfectly.

Dimensions.—Length of the carapace 34 inches; greatest depth
13 in. (in profile). Length of the rostrum 2 in. Depth of the first
abdominal segment #in., of the second fin. Length of the abdomen
and tail-lobes 32 in. Length of the outer antenne 4-5 in. Length
of the fore-arm 23 in., wrist 2 in., hand 2 in., finger 13 in.

Length of a detached hand and arm:—arm 23 in., wrist #in., hand
27 in., finger 24 in.

+ {. Soc. Vol_ XIX PLA

| Fipe 5 ET MNS
‘ign NIN SS : an
| Z Gi o AS Ss &
} , Gof WING i, 3
| } 2, ff is
| ( Wr } |

Goruckp ore

% Goahuttee

Wu
»

c= = We 2

NS
mi cy Hr CY

AY ii Wy Z\
oer ih a

whi Ns

WNW Y,
oi HIN yi)
willl!
ATS
WS A
ut Wye
& Hirw AN \ Nii
wes Ny . 4 s
ASI \ ANS WY NUS

‘il Wy
"Go i QW
ie =
CG by, zi
ity
GA
S
ayy y F
\ E
"Wy avy rd
AWW) /
)
)
\
/
{

MAP |
OF TERE RIV IES

OF

BENGAL

Shewing the changes which have taken
place, since Mayor Rennell s Survey.
Lhe River-courses in Black are according
to Mayor Rennell

Those in Red. shew the changes before
and since his time |

1863. | FERGUSSON—DELTA OF THE GANGES, 321

P.S. 27th June, 1863.—Since the foregoing communication was
made to the Geological Society, I have received a copy of Dr. A.
Oppel’s ‘ Paleontologische Mittheilungen,’ Stuttgart, 1862.

The first part of this most valuable work is devoted to a descrip-
tion of Macrurous Crustaceans of the Jurassic formations of Ger-
many, &c., and is illustrated by 38 excellent plates. The author
has, I observe, adopted Germar’s generic name of Mecocheirus in his
descriptions of the Solenhofen Crustacea,

Although Dr. Oppel has added more than 50 new species to the
list of Jurassic Crustacea, none of them agree, even generically, with
that just described from the Lias of Lyme Regis.—H. W.

EXPLANATION OF PLATE XI.
Scapheus ancylochelis, H. Woodw., four-fifths the natural size.

Aprit 1, 1863.

S. N. Carvalho, Jun., Esq., 6 Aberdeen Park, Highbury Grove, N.,
and Wiliam Edwards Wood, Esq., Tamworth Castle, Tamworth,
were elected Fellows.

The Rey. Dr. O. Heer, Professor of Botany in the University of
Zurich ; Sign. P. Savi, Professor of Geology in the University of
Pisa; Sign. G. Ponzi, Professor of Comparative Anatomy and Phy-
siology in the University of Rome; Dr. J. Leidy, Professer of Ana-
tomy in the University of Pennsylvannia; Il Marchese Pareto, of
Genoa; and Professor A. Daubrée, of the Jardin des Plantes, Paris,
were elected Foreign Correspondents.

The following communication was read :—

On Recent Coanexs in the Deva of the GANGES.
By Jamus Frrcusson, Esq., F.R.S.

[Communicated by the President. |

[Puate XII. ]
ConrTENTS.
I. General Considerations. 5. Opening of the R. Jennai.
1. Introduction. 6. Jessore group of rivers.
2. Oscillation of Rivers. 7. Natore group of rivers.
3. Elevation of the Banks of 8. Kishnaghur group of rivers.
Rivers. 9. Changes in the course of the
4. Secular Elevation of Deltas. R. Teesta.
5. Mode in which Deltas are 10, Retrocession of the junctions
elevated. of tributary streams with
II. Physical changes in the Valley of main rivers.
the Ganges. III. Historical evidence of the changes
1. Upheaval of the Madoopore in the Delta of the Ganges.
Jungle. IV. Increase of the Delta seaward.
2. Silting-up of the Sylhet Jheels. 1. Silt held in suspension in
3. Eastern Gap in the seaward Ganges waters.
face of the Delta. 2. Swatch of “ No Ground.”

4. Change in the bed of the | V. Appendix.
Brahmapootyra.

Quart. Journ Geol Soe

ohana
Bian

MYT WSN

Oude Goruckpore
=
°r ogra $
: e Ss
3
i =
~
Thy
i)
Cane, ae
s
Mia
Allahabad
wie
l ining *
oof

=Slionr,

il

APS .
OF THE RIVERS

OF

BENGAL : <

|
|
|
Shewing the changes which have taken
place. since Major Rennells Survey.
The River-courses in Black are according
to Major Rennell
Those in Red shew the changes before

and since his time .

%

322 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Apriady

I. General Considerations.

1. Introduction.—It may seem presumptuous in one who is neither
a geologist nor has any pretension to geological knowledge to ven-
ture to address this Society on a subject so nearly akin to their
special science. My excuse must be that, haying resided for five
years on the banks of one of the most active of the Bengal rivers, I
have had opportunities which are not vouchsafed to every one of
observing their phenomena, and have been a witness of the changes
I am about to describe. I may also, perhaps, be allowed to state that,
when I first became aware of the disturbance that was taking place
around me, I set myself carefully to measure and observe what was
passing ; and, in 1835, made a sketch-survey of the lower Ganges
and Brahmapootra, from Jaffiergunge to the sea. This was published
by Mr. Tassin a few years afterwards, and is, so far as I know, the only
survey that was made—certainly the only one published—between
that made by Major Rennell and the survey now in progress, but
which has not yet been given to the world. I may also mention, in
extenuation, that I have waited for more than a quarter of a century
in order that some one more worthy might undertake the task ; but,
as no one has come forward, | may perhaps be now excused for
venturing upon it.

In order, however, to obviate the reproach of presumption, my
intention is to confine myself wholly to the historical period, and
practically to the time that elapsed between the survey made by the
celebrated Major Rennell, between the years 1780-90, and the survey
now in progress; and though I shall be obliged, occasionally, to
mention facts that may have occurred before the Christian era, they
will be only such as are based on human evidence, and not such as
properly fall within the domain of the geologist.

2. Oscillation of Rivers.—Before describing the actual phenomena,
it may be necessary to call attention to certain principles—not very
recondite, perhaps, but indispensable to a clear understanding of
what is to follow.

The first of these is :—

All rivers oscillate in curves, whose extent is directly propor-
tionate to the quantity of water flowing through the rivers.

An inspection of any good map is sufficient to prove the general
correctness of this dictum, but its consequences have been strangely
overlooked both by engineers and potamologists. Without attempting
to enter into the theory of the question, it may be sufficient for the
present to state, in illustration, that the action of rivers appears to
be the exact converse of that of the pendulum.

The pendulum is a body in stable equilibrium, whose natural con-
dition is consequently that of rest, and, being once disturbed, it seeks
to regain that position; but, the original force remaining, it would
go on oscillating for ever if we could abstract all the natural con-
ditions of friction, resistance of the atmosphere, ec.

A river, on the contrary, is a body of water in unstable equili-
brium, whose normal condition is that of motion down an inclined
plane; and, if we could in like manner abstract all the natural

1863. ] FERGUSSON—DELTA OF THE GANGES. 323

conditions of inequality of surface or of soil, it would flow continu-
ously in a straight line; but any obstruction or inequality whatever
necessarily induces an oscillation, and, the action being continuous,
the effects are cumulative, as those in the pendulum are discumulative;
and the oscillation goes on increasing till it reaches the mean between
the force of gravity tending to draw it in a straight line, and the
force due to the obstruction tending to give it a direction at right
angles to the former.

If this be so, it will immediately be perceived that the extent or
radius of the curves will be directly proportioned to the slope of the
bed of the river. If, for instance, a river were flowing down a
regular slope, through a perfectly homogeneous soil, with a fall of,
say, 10 feet per mile, or 1 in 500, the curves would be so extended
as to appear nearly a straight line on the map. With a fall of 1
foot per mile, the radius of the curve is, as nearly as I can ascertain,
double that of a river with a fall of 6 inches ; and when the fall is
about 3 inches per mile, the direct and tangential forces so nearly
balance one another that the curves are practically semicircles. In
the latter case the chord of the curves is practically four times the
width of the river. Thus a river 1000 feet wide would oscillate
once in 4000 feet in the general direction of its course, and the ex-
tent of its curve, measured along the centre of the stream, is a little
more than 6000 feet. Between a fall of 6 inches and 1 foot per
mile, the oscillation is, apparently, once in about six times the width ;
~ above a foot it rises to one in ten or twelve, above which it is ex-
tremely difficult to find examples uninflnenced by natural obstruc-
tions. It need hardly be remarked that these observations apply to
rivers when their beds are full, which is the only time when they
are shaping their courses *.

There are a number of other consequences flowing from these, to
which I shall not allude here, as they have no direct bearing on the
subject in hand, though it would be extremely interesting if they
were observed and tabulated; for not only would these tables enable
any one on inspecting a map to calculate approximately the slope of a
country, and to estimate the relative importance of every river there
delineated, but they would enable the engineer to regulate their
courses, and the statistician to predict the result of the changes he
sees taking place. To make this clearer, let me take one example. The
Austrian engineers have of late years spent enormous sums of money
in the attempt to straighten the course of the Danube by cutting off
its lateral branches. This has been done by embanking across their
mouths with dykes of fascines and piles. For a time this resists, and
might resist so long as the river finds some other place where it can
readjust its curvature ; but, as these are stopped one after the other,
it bursts through the barriers and resumes its old course. The fact
is, the Austrians are trying to make the whole body of water flow in
curves due only to a portion, and they have hitherto, as might be
expected, found this impossible ; had they taken the trouble to calcu-

* The average width of the Nile between Koum Ombos and Memphis is

324 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Aner ey

late the curve due to the whole body, a few simple groins would
have sufficed for all their purposes. It is precisely the same question
as if it were proposed to make a 10-inch pendulum beat seconds, or
one 39 inches long beat once in two seconds. It can be done by
main force, but the moment the pressure is removed or weakened the
pendulums resume their natural beat; and a clockmaker who con-
structed his clocks on this principle would fail as certainly as the
Austrian engineers.

3. Elevation of the Banks of Rivers.—The second point to which
I wish to call attention is the tendency of rivers in alluvial soils,
especially in deltas, to raise their banks, and so confine themselves
in their beds.

This process has been well described by Sir Gardner Wilkinson
as regards the Nile, and by Sir Charles Lyell for the Mississippi ; but
neither of these gentlemen appear to me quite to have caught, or at
least explained, the true cause. As regards the Ganges certainly,
and the other rivers so far as I can judge, it is owing to the existence
of great sheets of still water in the low lands beyond the banks of
the rivers. These, being still, have deposited their mud, if they ever
had any in suspension ; and being too massive to be set in motion by
the rivers, they reduce the flowing streams to inaction the moment

2000 feet; the average length of oscillation 8500 or 4°25. The slope about
6 inches per mile. The following Table gives the approximate extent of the
oscillation of the Ganges and the three Kishnaghur rivers.

Width of
Distance, | Distance, | stream, Number of| Length of
direct, | per river, | low water,| oscilla- oscillation,

in miles, | in miles. |dry season,| tions. in miles.
in feet.
GANGES.
Allahabad to Chunar ...... 62 104 3500 17 37
Chunar fo Buxar <.. sense 80 113 4000 20 4-
Buxar to Camas. .caccss: 74 96 5000 15 5:
Patna to Monghyr ......... 82 106 6000 113 ic
Monghyr to Rajmahal...... 96 108 7000 10 9°5
Rajmahal to Rajapore ...... 90 100 7000 10 9:
Rajapore to Pubna ......... AO: aes 4000 6 a
Pubna to Jaffiergunge ...... 32 36 3000 8 4-
BHAGARUTTEE.
Chokah to Nuddya ......... 96 120 1200 62 1-5
Nuddya to Chogdah......... 24. 30 2000 9 2°5
Chogdah to Calcutta......... 34 42 3000 11 3
JELLINGHY.
Jellinghy to Nuddya......... 50 112 1000 42 1:2
MATABANGAH.
Ganges to Coomar ...seseee 18 28 1500 9 2:
Coomar to Kissingunge ... 30 50 800 46 2
Kissingunge to Chogdah ...| 24 29 500 47 3

1863. ] FERGUSSON—DELTA OF THE GANGES. 325

they leave their beds, and consequently force them to deposit their
silt in their immediate proximity.

The first consequence of this is, that water resists water far better
than earth does. A river can attack its banks in detail, can eat
them away bit by bit, and carry off the spoil; but the still water,
seizing the silt, forces the river to deposit it exactly where itis most
useful in forming a barrier against further incursions, and so finally
repels its advance.

In India these backwaters are called jheels, and are large sheets
of clear water existing during the cold weather at about the same
level as the river. During the rains they rise nearly parz passu with
the rivers, partly owing to the quantity of rain-water that drains
into them, partly to leakage through sandy strata, partly to small
creeks or openings from the rivers, and partly also from almost all of
them being open at their lower ends, so as to feel the reflex of the
inundation. From all these causes, when the river is at such a
height as to overtop its banks, it meets this body of still water
(fig. 1), and, not being able to set it in motion, it deposits its silt in
the limit between the moving and the still bodies. Even when the
jheel has not risen so fast as the river, a few days’ overflow serves
to restore the equilibrium, and then the deposition goes on as before.
In most parts of Bengal indigo-planters and others avail them-
selves of this interval to cut canals, or khals, through the banks, in
order that the river-water may flow into the jheels, and so raise their
beds and render them fit for cultivation. Even under the most
favourable circumstances, however, the action seldom extends more
than 100 or 200 yards from the banks ; and, when the equilibrium of
water is restored, the silt is deposited in the canal, which requires
consequently to be cleared out every year, and after a few years
the deposit beyond has raised itself to the height of the bank, so
that further progress in that direction is impossible, and the opening
in the bank of the river is then soon completely obliterated.

Fig. 1.—Diagram-section across the Bed of a River.

43

Zz Water
&, containing
o
Ss

Clear water. sediment. River- water. Clear water.

Silt forming the bed of the River.

It is extremely difficult to fix the exact point at which this deposit
begins to take place; but, as far as I have hitherto been able to ascer-
tain, rivers flowing through a country whose slope is more than 6
inches in a mile have rather a tendency to deepen their channels
and abrade their banks, and the land in their immediate proximity
is lower than at a little distance*. At 3 inches in the mile, or

* The fall of the Indus from Attock to the sea being on an sia 1 foot per
VOL. XIX.—PART I.

326 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. | Aprty

under this, the deposit always takes place; and its extent is nearly
in the inverse ratio to the slope.

The exact turning-point of the two systems still remains to be
fixed; but my own impression is, that we are not far wrong in
taking 6 inches as the limit at which the deposit begins to take
place; in many instances, however, 5 or even 4 inches may be taken
as the starting-point*.

4. Secular Elevation of Deltas—The only other point to which I
will venture to call attention is what is called secular elevation,
which I shall endeavour to define.

There was a time, before the formation of the Deltas of the Nile and
the Ganges, when the sea or tide extended to Memphis in the one case,
and to Rajmahal in the other. If at that time the slope of these rivers
had been measured from any fixed point, such as the cataracts in
Egypt in the one case, and the rock of Chunar in the other, it would
have been found that the slope of both of them was very much
greater than it now is, it having been diminished in the exact ratio
in which the ground at the apex of the deltas has been raised—about
80 feet at Rajmahal, and 60 feet at Memphis. Little or no silt was
consequently deposited in the up-country in early times, but every-
thing was swept to the sea, and the extension of their deltas has
consequently been in an immensely more rapid ratio than at present.
But, besides this, for every mile that the delta extended seaward,
the slopes, as shown on the diagram (fig. 2), would tend to become
parallel in a geometric, and not in an arithmetical, ratio. And
when the elbows at Memphis and Rajmahal were completely oblite-
rated, the secular increase must have been infinitesimally small.

Taking first only the mathematical view of the subject—if we
assume a point such as Patna, say 200 miles above Rajmahal, and
that the delta is now extended 200 miles below that point, assuming
also that Patna is now 200 feet above the level of the sea, and Raj-
mahal 100 feet, all which figures are sufficiently correct for ilustra-
tion, it is evident that, if we divide the time since the sea was at
Rajmahal into four equal epochs, the level at Rajmahal during
the first period of the extension of the delta fifty miles seaward
would have risen 40 or 42 feet, during the next 27, during the third

mile, it is not a depositing river. The only part of its course where the slope is
less, judging from the lateral extent of its oscillation, is between Kyrpore and
Sehwan. Between these places it may deposit to some extent, but elsewhere its
course is steep and straight.

* No argument on this subject can be depended upon if derived from obser-
vations on the course of the Nile, the slope of whose bed from the cataracts to
the sea appears to be about 6 inches per mile, for the reason that, between the
bank of the river and the hajar, or desert, the natives have at different times
constructed numerous causeways, as may be seen in the atlas prepared by the
French savants in the beginning of this century, and explained by Sir Gardner
Wilkinson (Journ. Royal Geogr. Soc. vol. ix. p. 432 et seq.). These act as so
many dams or silt-traps during the inundation or depositing season. But for
these dykes, it is by no means clear that there would have been any deposit in
recent times on the plain of Thebes, instead of 7 feet in 1700 years, which Sir
Gardner calculates ; and the variation in the thickness of the deposits in different
places seems to be almost wholly due to these artificial obstructions.,

1863. | FERGUSSON—DELTA OF THE GANGES. 327

Fig. 2.—Diagram illustrating the Secular Elevation of Deltas.

Patna.

O\e Rajmahal.
200 ft.

\

50 miles. 50 50 50 200 miles.

20, and during the last 13 or 14, or less than one-third of what was
due to the accumulation during the first period. But this is far from
representing the whole truth; first, in consequence of the greater
quantity of silt brought down by the river when its slope was 12
inches, which it must have been during the first period, instead of
less than 6 inches as it is now. And, secondly, the area or breadth
of the delta is necessarily less near its apex than at its base, and,
consequently, the area over which the silt had to be deposited much
less than at present.

From these and other minor causes I feel convinced that if we
assumed the deposit to be 50 feet, or one-half, during the first
period, it would be rather under “ee over the mark; and, say, 25
feet during the second, 12 or 13 during the third, and 5 or 6 during
the last of the four periods indicated in the diagram. From tlie
conformation of the ground I should be inclined to assign a higher
rate of progression for the rise of the land of Egypt in the neigh=
bourhood of M emphis. But it is difficult to speculate on the phe-
nomena of that river while we remain so ignorant of the physical
condition of the country from which the inundation proceeds. But
even more uncertainty has been superinduced, as pointed out above;
by artificial obstructions.

All this is assuming that the silt is distributed quite evenly over
the whole delta. This, however, is practically very far from being
the case. The mode in which deltas are raised is by a river, flowing
through some low part of the country, gradually embanking itself,
and then raising its bed till the body of its water is higher than some
neighbouring region; it then falls into this, and, going through the
same process, it fills that depression, and then goes on to the next.
After a long cycle of years it comes back again to the country it first
left, which probably has not risen 1 foot since, while the neighbour-
ing country may have been raised 30 or 40.

From these data it will be perceived how fallacious any conclusions
must be which are drawn from borings into the strata of deltas, and
calculations formed from local superficial deposits. I myself have
seen the bricks which formed the foundation of a house I had built

carried away, and strewed along the bottom of a river at a depth of
Zz 2

328 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. {Apr. 1,

30 or 40 feet below the level of the country. Since then the river
has passed on, and a new village now stands on the spot where my
bungalow stood, but 40 feet above its ruins; and any one who
chooses to dig on the spot may find my “ reliquie” there, and form
what theory he likes as to their antiquity or my age. If we add to
this local disturbance the varying degree of elevation just pointed out
in the secular increase, it must be seen that the problem is of a much
more complex nature than has hitherto been assumed.

5. Mode in which Deltas are elevated.—Independently of the changes
wrought by the varying quantity of water in the different branches
of the deltaic rivers, and the consequent necessity for enlarging or
contracting the extent of their oscillations, there is another class of
changes superinduced by the accidents to which so complicated a
system must always be liable. If one of the tributaries, for instance,
which before fell into the hollow side of a curve presses on the
convex side, if a sand-bank is formed anywhere, or if any natural
or artificial obstruction forces the river to change its bed in any part,
the whole system is so rigid that the alteration is felt in every direc-
tion, both above and below, as far as the alluvial plain extends.

One consequence of any such alteration in the course of the main
stream is, that the initial or terminal oscillation of any tributary or
distributary is continually altering its position, and the oscillations
cut their way through the whole plain* of the river, both in an
upward and downward direction.

Such a river as the Ganges between Patna and Rajmahal must
have eaten through its plain several times since it has occupied its pre-
sent position. But when the delta is so raised as to reduce its slope
from 6 to, say, 3 inches per mile, it is not difficult to foresee a time
when the river will so raise its bed as to be obliged to seek a new
‘‘ plain ” further north, and may again resume the position it once
occupied in the centre of its valley, but from which it has been forced
against the southern hills, by the greater “vis viva” which the
Himalayan streams derive from the rapid slope of their beds and
their preponderating body of water.

None of the rivers of the delta have in historical times, so far as
we know, worked their way twice through the same plains. The first
operation so raises their plains that they generally find it easier to
seek a new course in the lower lands oneither hand; and thestream
in their old beds consequently becoming sluggish, they gradually silt
up and become, after a while, altogether obliterated, except here and
‘there where a reach has been cut off in the process, and remains, like
a fossil, to mark the previous existence in that spot of a river of a
given oscillation, which may still be measured with perfect certainty
in the fragment that is left. It is by this continual shifting of the

plains of rivers that the whole delta is gradually raised to a higher
level.

* By “plain” in this sense is meant the district occupied by the river be-
tween the extreme outward edge of its oscillations on either side. With a river
1000 feet wide, its plain may extend from one to two miles in width, and others
in like proportion, varying, of course, according to the slope of the country.

1863. | FERGUSSON—DELTA OF THE GANGES. 329

This is a curious and complicated process, which I shall now try
to make as clear as I can, by describing the phenomena as they have
occurred in the valley of the Ganges.

II. Physical Changes in the Valley of the Ganges.

1. Upheaval of the Madoopore Jungle—Although the principal
object of this paper is to describe the phenomena resulting from the
deposit of silt by the rivers of Bengal, there is one of a contrary
nature which has had so marked an influence on the river-systems
of the delta that it is impossible to pass it over. The circumstance
J allude to is the upheaval of a large tract of country known as the
Madoopore Jungle, which there is every reason to suppose took
place in very recent times.

This tract extends for about seventy miles due north from the city
of Dacca, which is built on its southern extremity. Its greatest
width in the centre is about thirty-five miles. On its western face
it has a well-defined boundary, and rises in hillocks to a height of
about 100 feet from the level of the alluvial plain along its whole
length ; in the centre its average height is from 40 to 60 feet above
the plain, and it gradually slopes away to the eastward, dipping below
the old bed of the Brahmapootra, and losing itself in the Sylhet Jheels.

The surface of this district is a hard ochreous clay, identical, so
far as I can judge, with the strata found below the peat and recent
deposits at Calcutta, where it exists at a depth of from 70 to 120 feet
below the surface of the soil.

There is, at all events, no @ priort improbability against this up-
heayval having occurred in very recent times. An inspection of the
map will show that it occurred in the axis of the belt of volcanic
action which extends from Narcondam through Barren Island on to
Cheduba and Ramree, and thence to Chittagong and Dacca.

Without going further back than the great earthquake which
occurred at Chittagong in April 1762*, I may remind the Society
that a large tract of land was then submerged, that other parts were
elevated, that two volcanos broke out, and the whole settlement was
shattered, and that at Dacca the shocks were so violent that the
wave from the river swept off a large number of the inhabitants.

It was not then, however, that any upheaval took place, nor at
any period subsequent to the foundation of that city in the beginning
of the seventeenth century by Jehanguire; for its oldest buildings,
though cracked, are not destroyed, as they would have been by such
a convulsion. And how long before that time it occurred we can only
guess by trying to estimate how long it would take the Brahma-
pootra to fill up the Sylhet Jheels to the extent it has done, and by
the uncertain light of native traditions, some of which will be alluded
to in the sequel.

As hinted above, there exists to the eastward of the upheaved
region a depressed area of about equal extent. For a description of
this I cannot do better than refer to Dr. Hooker’s ‘ Himalayan

* Phil. Trans. vol. lili. p. 201.

330 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [pret

Journals’ (vol. 11. p. 256). He sailed for some days among these
Jheels, and found by his barometric levellings that they were very
slightly raised above the Bay of Bengal. Their bottom generally
consisted of accumulations of decaying vegetable matter—incipient
peat—through which he could not reach a bottom by thrusting in the
boat-poles.

It is not necessary here to insist on this depression being the effect
of the upheaval of the Madoopore Jungle, or to inquire whether it
pre-existed ; but I think there can be very little doubt that the dis-
turbance caused by the upheaval was what turned the Brahmapootra
towards the east into these jheels.

A mere inspection of the map is sufficient to establish the proba-
bility that this change must have taken place not very long ago; and
though the length of the course of the Brahmapootra is only half
that of the Ganges (for it is not clear that it has any connexion with
the Sampo of Tibet), still the two rivers are quite equal in volume,
inasmuch as both enter the deltaic plains of Bengal with a ten-
mile oscillation before parting with any of their waters through their
distributaries below Rajmahal on the one river, or at Rangamutty
on the other.

Although equal in volume, the Brahmapootra brings down an
immensely greater quantity of silt than the Ganges—probably one-
half more; as Buchanan Hamilton phrases it, “It is the dirtiest
river I ever saw.” This arises, principally, from the fact that the
slope of the valley of Assam, from Sudya to Goahuttee, appears to
be more than 6 inches per mile. The consequence is, that neither
the principal branch of the Brahmapootra nor any of the tributaries
deposit their silt, but all is swept onwards ; and, owing also to the
greater quantity of rain that falls there than falls to the westward,
the denudation of the land is much more rapid. This condition of
matters will not be changed till the section across the valley opposite
Goalparah has been considerably raised beyond its present level,
or, in other words, till the land between Goahuttee and Goalparah
attains an elevation corresponding to that attained in the valley of
the Ganges about Rajmahal. At present the elevation of the river
at Goahuttee, with 350 miles to run, is apparently lower than the
Ganges at Rajmahal, within 250 miles of the ocean*.

Until this extra elevation takes place, the physical condition of
the valley of Assam will so closely resemble that in which the
valley of the Ganges probably was when the sea was at or near
Rajmahal, that few problems connected with this subject would be
more interesting than to compare the condition of the two valleys,
in so far as materials exist for the purpose.

At that early time the River Ganges must have flowed with greatly
increased velocity nearly in the middle of its valley; but as its slope
and consequent velocity decreased, it was pushed southward against

* The level of the river at Goahuttee is assumed from a long series of baro-
metric observations, checked by those of the brothers Schlagintweit (‘ India,’
vol. ii. p. 103) ; that at Rajmahal, from the levels of the East Indian Railway,
checked by those of the great Trigonometrical Survey.

1863. | FERGUSSON—DELTA OF THE GANGES. 331

the hills by the greater energy of the northern streams, and the mass
of their accumulations, the only southern stream of sufficient power
to keep it off its hills being the Soane.

The Brahmapootra still maintains itself nearly in the centre of its
valley for the greater part of its course, but it must be pushed south-
wards, as the Ganges has been, in the exact ratio in which the
quantity of water flowing from the Himalayas exceeds that draining
from the southern hills; and, as this takes place, the valley must
rapidly be filled up and become habitable, which it hardly can now
be said to be in most parts.

Though it is dangerous to descend to particulars in such matters,
my impression is that hardly more than 4000 or 5000 years have
elapsed since the sea, or rather the tide, was at or near Rajmahal ; or,
to speak more correctly, since the greater part of the province of
Bengal Proper was a great lagoon, like those which exist at the
mouths of the Brenta or the Po, or the Lakes Mensaleh and Boorlos,
at the mouths of the Nile: for there is no reason to suppose that there
did not always exist—in historical times at least—a bar or barrier
where the tides turned somewhere very near where the Sunderbuns
now are; but between this and the apex of the Delta all seems to
have been a tidalswamp. When this was the case, the upper valley
of the Ganges was in the semi-habitable state in which we now find
Assam; and I fancy we can, in history, trace the settlements that
were made one after another, proceeding eastward as the Delta ex-
tended, and, by its elevation, diminished the slope of the bed of the
Ganges to what we now find it.

2. The Silting-up of the Sylhet Jheels—To return, however, to
the Sylhet Jheels. When the Brahmapootra was first turned into
them, they consisted of an immense tract of submerged country,
covered with clean still water of no great depth, and consequently
every particle of silt that was brought into them was seized upon
and deposited; and the Luckia and Megna, which flowed out of
them, must then have been, as they are now, clear and pellucid
streams, as compared with the turbid waters of the two great rivers.

The first effect of this invasion, that we trace on the map, is that
the Soorma and other streams which flowed from Munnipore due
westward, along the foot of the Cossya Mountains, were deflected
southwards, which it was easy enough for the great river to do, so
long as it could take them in detail. It was not until they were all
united in the bed of the Megna, and pressed between the Tiperah
Hills and the upheaved tract, that the real struggle began.

In this case, though the Megna was much the smaller river, it
had certain advantages necessary to be pointed out in order to appre-
ciate the result. ,

The first of these is, that the Sylhet rivers depend wholly on the
monsoon rains for their supply. The clouds, striking early on the
Cossya range, discharge their waters with a violence hardly found
elsewhere ; and, as is well known, from 500 to 600 inches of rain
fall on the slopes of these hills during the three months of the rainy
season. It may also be mentioned that, owing either to the nature

332 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apee,

of the rocks of which these hills are composed, or because the violence
of the monsoon has long ago denuded them of every moveable par-
ticle, these rivers bring down little or no silt even in the height of
the monsoon, and are quite clear in the cold weather.

The Brahmapootra, on the other hand, depends for its floods
partly on the melting of the snow, partly on the far more moderate
and later rains of the valley of Assam, probably hardly exceeding
100 or 120 inches ; having also a longer course te run, it arrived later
at the scene of the struggle, and found the country already occupied by
the waters of the Megna to such an extent as to be able to dam back
its waters for the first month of the rains, and to foree it to deposit its
silt in its own bed. It could not, of course, have done this with any
effect until the large river had reached the higher lands beyond the
jheels to the southward, and with its silt had bridged across the whole
width of the jheel-country, and, by this process, had embanked
itself along the whole extent, so as to make it difficult for it to
change its course. So long as the Brahmapootra was only forming an
inland delta im the depressed country, the Megna had no hold upon
ig; but when it came to flow in what was practically an aqueduct,
along the top of an embankment of its own making, it was rendered
powerless, and the struggle was soon over. Had it not been for the
upheaved tract already alluded to, it would, of course, have sidled
away westward, and so have avoided the contest with the Sylhet
rivers; but that being impossible, we find it retracing its steps nearly
seventy miles northwards, and finding a new channel for itself above
Dewangunge in the bed of the Jennai.

3. Eastern Gap in the Seaward Face of the Delia.—Before leaving
this branch of the subject, it may be well to allude to another
geographical fact, which I believe to have been in a great measure
the result of this diversion of the Brahmapootra into the Sylhet
Jheels. It is the great gap or gulf that exists to the eastward of
the Gangetic half of the delta.

From the Hoogly to the Horringotta the seaward faee of the
Sunderbuns is tolerably level and fixed; at all events, it has under-
gone no sensible change within any period to which our knowledge
extends ; and, so far as can be ascertained, it shows no tendency to
go forward. In that portion of the delta, however, allotted to the
Brahmapootra a great deal of work has yet to be done; everything
there is sa new, and in such a constant state of change, that, even
in that chmate, vegetation has not been able to settle upon the
islands, and these are continually moving and changing their places.
A great deal has been done to fil up the gap since the Brahma-
pootra last changed its course, in the beginning of the present cen-
tury ; but we want a new survey to be quite sure to what extent
this has gone. If I am correct in my view, that the gap is mainly
the result of the straining of the waters of the Brahmapootra
through the Sylhet Jheels, and their consequently reaching the Bay
of Bengal deprived of all their silt, it follows that the process of
filling up will now be comparatively rapid, and that the eastern face
of the delta will assume before long the same fixed character which

1863.] FERGUSSON——DELTA OF THE GANGES. 33a

now marks that of the western portion, and which is due—as will
be afterwards explained—to the joint action of the tidal and fluvia-
tile forces which meet at that point.

4. Change in the Bed of the Brahmapootra.—It would have been
extremely instructive if the progress of the struggle between the
Megna and the Brahmapootra had been carefully watched and re-
corded; all we now know is, that when Major Rennell surveyed
these rivers in 1785, neither he nor any of his assistants had any
idea that the Brahmapootra had not always flowed, and would not
always continue to do so, in the channel in which he then found it.
We now know that, though a considerable body of water may flow
that way in the rains, yet during nine months in the year a creek,
or rather chain of ponds, 100 or 200 feet wide, and everywhere
fordable, represents the river that a little more than half a century
before flowed through that country in seven-mile reaches, and with
a breadth of more than a mile and a half even in the dry season.

It is unfortunate that Buchanan Hamilton* did not visit this
country when surveying the neighbouring districts in 1807-10, as
the change must then have set in; and his greater knowledge of the
language and of the customs of the natives would have led him to
remark upon the anomaly of the smaller stream (the Megna) giving
its name to the Brahmapootra, from their junction at Sonerampore
to the sea, proving that the bed belonged to the smaller river, and
that it had been invaded by the larger; and proving also—for this
class of evidence is very cogent in these regions—that the invasion
had taken place after the country had been sufficiently inhabited
and settled to have the names of its rivers fixed on the bases they
now maintain. So far as we can judge from appearances, this could
hardly have occurred very long ago.

When the survey now in progress is completed, it will not be
very difficult to estimate this epoch approximately. ‘The first thing
to be ascertained is, of course, the quantity of silt brought down by
the Brahmapootra; then to estimate the area of the Syihet Jheels
filled up by the great delta formed in them by the waters of the
Brahmapootra, checking this with the area of the delta at the
mouth of the Megna, which remains to be filled in; and, with a few
borings, all this ought not to be very difficult. Im the meantime, it
certainly is to be regretted, in an economic point of view, that the
combined Sylhet rivers prevailed in this struggle. They cannot fill up
their own swamps, because they possess no silt; and they shut out
the only river that is capable of doing it for them. Now, however,
every year must make their condition worse; for, as the delta extends,
the land between them and the sea, below Dacca, must rise, and they
consequently must deepen, and their water spread, until the whole pro-
vince may become asubmerged peat-factory, from which fate nothing
can save it but inviting back the river they have just expelled.

5. Opening of the R. Jennai.—The first river the Brahmapootra met
which could afford it a means of escape was, as just mentioned, the

* His surveys, in a mutilated form, were published in 3 vols. 8vo, by Mont-
gomery Martin, in 1838.

d34 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. l,

Jennai. Having no earlier maps than those of Rennell, it is impos-
sible to be certain what the condition of this river was before he
surveyed it. He found it flowing due north and south, in one-mile
oscillations, with a breadth of between 400 and 500 yards, and
flowing so regularly that I cannot help suspecting that it was then
avery young river; if I may be allowed to guess, I should say not
more than twenty years old. In fact, it seems to have been the first
product of the struggle between the Megna and the Brahmapootra,
and did not exist till the waters of the latter river had been dammed
back so as to flow in this direction.

When Buchanan Hamilton visited this country in 1810, he merely
remarked that the Brahmapootra threatened to “‘ carry away all the
vicinity of Dewangunge” (which it has since done), “‘ and perhaps to
force its way through the Konnai (Jennai) into the heart of Natore.”’*

It was not, however, till ten years later that it had increased to
such an extent as to affect the Jessore rivers; and it was not till
about the year 1830 that any reliable information was obtained
regarding it. About that time a party of engineer officers was sent
to connect Assam with the Great Trigonometrical Survey then in
progress in Bengal. They carried a series of triangles up the bed of
that river; and it was at the same time attempted to navigate it with
steamboats. Nothing, however, was published until the river was
laid down on a map of Bengal which I constructed,in conjunction with
the late Mr. Tassin, on a scale of eight miles to one inch, in the year
1836. At that time it was flowing through Natore with an oscilla-
tion of nearly seven miles, and has continued to do so ever since ; for
though in its oscillations it sweeps away hundreds of miles of land
every year, it is only very lately that it has shown any restlessness,
or any tendency to leave its present direction, and whether it will
be successful or not in so doing still remains to be seen. In the
meanwhile the river is nearly where it is shown on the map; but,
as it was there in 1850-53, it certainly is not there now, as it
never is exactly in the same place for two successive years, being
young and active, and roaming through a new and unconsolidated
country. It may also be mentioned that the city of Serajgunge—
the largest and most important mart in that part of the country—is
somewhere in that neighbourhood now, but not where marked on
the map, of course, as it is annually obliged to accommodate itself to
the vagaries of the stream, and change its locality. It may be ten
miles further up the stream, or ten miles further down, or five miles
further east or west; but it is somewhere thereabout; and that is
* all the information geographers can hope for in a country where
land can only be classed with floating capital.

6. Jessore Group of Rivers.—The first result of this invasion of
the Gangetic territory by the Brahmapootra was, that it should
seek to re-enact the part which had just been performed on the other
side of the Madoopore Jungle and should threaten to shut up the
Ganges, and send it back through its own distributaries. It was so
nearly successful that, in 1838, the Great Ganges was fordable at

* Martin, vol. i. p. 396.

1863. | FERGUSSON—DELTA OF THE GANGES. 339

several places above the junction. As the Brahmapootra has an
oscillation of seven or eight miles, while the Ganges has only one of
five miles at that place, and as even that is gradually diminishing,
it must have been successful if the Ganges had been able to find
-another outlet. This, however, was not so easy, the whole of the
country to the southward and westward having been traversed
repeatedly by powerful rivers, and the country consequently well
raised and consolidated.

The Chandna was the first river it met above the junction, from
which it could look for relief. ‘This river, however, was old, its
oscillation short, and its banks high and consolidated. But, even if
it could have been opened, its natural outlet to the eastward, the
Coomar, was older still, and less likely to give way; from a two-
or three-mile oscillation, which can still easily be traced, it had
sunk to one averaging half a mile or less. No water runs through
it in the dry weather, and during the imundation the flow is so
sluggish that all the silt it receives is spread on-its own banks ;
consequently it has raised its district higher than any of the sur-
rounding country. ;

Proceeding up the stream, the next river was the Goraie. This
was more tractable ; it was not originally a distributary, but a local
stream, draining some jheels—it was consequently only at its head
that its banks were at all stiff or consolidated; lower down the land
was low, and the river divided into several branches, each of which
could be opened out separately. Even its upper reaches were so tract-
able, that, from a width of 600 feet, at which it stood in 1828, it has
increased to 1908, which is now the least width at the lowest season.
The next river upwards was the Upper Coomar. It has not been
opened to the same extent for the reasons just stated; but, as the
pressure the Ganges could bring to bear upon it was infinitely greater
than could be effected by the Chandna on its lower division, it has
been opened and increased from 330 to 792 feet, and both these rivers
are still increasing.

When these three came together above Baboocally, there were
several courses open to them; the most natural one—for the Coomar
at least—would have been to have opened the Novo Gunga. Though
called new, this, however, was the next oldest stream of the district,
after the Coomar. Its oscillation is only half a mile, and its banks
are consolidated and thickly inhabited; and though, no doubt, some
of its reaches might have been lengthened, still if, at any one place,
two or three oscillations are so stiff that they cannot be extended,
they govern the whole; and as there are several such in this river,
its increase was hopeless.

The Barassya looked more favourable, and a part of its bed was
actually appropriated and widened; but there were two oscillations
opposite Muddenderry Factory which were in such stiff soil that they
could not be extended, and, though the river has been somewhat
widened and deepened, it remains now practically the same as when
Rennell surveyed it.

To any one unacquainted with the habits of rivers, it will imme-

336 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ apeett;

diately suggest itself that the easiest escape from these difficulties
would have been to break into that long low range of jheels behind
Mahmudpore, and so get to the sea without difficulty. As I have,
however, tried to explain above, water resists water better than
land. It broke several times into the low land, but was on every
occasion repelled, being forced to deposit its silt so as to make a
barrier against its own incursions.

The only remaining course, and the one that eventually was
adopted, was to seize on a small khal, or creek, called the Ellan
Khalee, and widen it for the purpose. This was not difficult, as
the land was low and friable, no great river having come that way
in recent times.

In Rennell’s time the creek was so insignificant that it is not
mentioned in his maps, and even in 1818-20 it was so small that it
could be easily leaped on horseback ; when I first knew it in 1830-83
it was sweeping through the country with two-mile oscillations, as
regular as if they had been drawn by hand. It was nearly 800 yards
wide, and deeper in proportion than the older rivers. It was, in fact,
the only river that all the year round was open for steam-navigation
between Calcutta and the upper provinces. After being rejoined by
the Novo Gunga and Barassya, it increases its reaches to three miles,
and carries this oscillation to the sea—certainly the largest and finest
of the delta-rivers after the great Poddah* or Megna.

Since I surveyed it in 1833 it has been getting straitened in its
bed, and it evidently has been embanking itself too rapidly. Its
reaches have lost their beautiful regularity and have become con-
torted; and one of them has stretched about two miles to the
eastward, so as to cut off the Muddenderry reaches. If it has
accomplished this—which I believe it has—it may be able to open
out the lower part of the Barassya River, and get into the low country
behind; and then, perhaps, joining some of the old branches of the
Ganges which existed i in Rennell’s time, so get to the sea.

If this should be accomplished, the Goraie and the Upper Coomar,
with the Chandna, will practically become the great outlets of the
Ganges, and the whole of the eastern half of the delta will then be
abandoned to the Brahmapootra. This will certainly be the case if
the Ganges’ waters find a sufficient outlet in this direction; and the
chances are so equally balanced that the struggle is extremely inter-
esting at the present time.

7. Natore Group of Rivers.—The Ganges at Jaffiergunge, united
with the Natore rivers at Oorasagur, is so nearly a match for the
Brahmapootra, that the latter river is attempting to escape the conflict
by cutting off the angle at Attree, and joining the Dallaserrai through
the Elamjanee River. To do this effectually, however, it must open

* Poddah, or Padma (the Lotus), is the stream, running nearly east and west,
by which the Bhagaruttee, or true Ganges, above Bauleah at some recent time
connected itself with the Brahmapootra somewhere above Jafliergunge. The
tradition of this junction taking place is quite distinct in the minds of the
natives inhabiting its banks, who do not consequently look on the Poddah as a

sacred stream. Still it must have taken place before the diversion of the Assan
river into Sylhet.

1863. | FERGUSSON—DELTA OF THE GANGES. 337

out some eighty miles of tolerably settled watercourses; and this
would occupy some twenty years, even if it succeeded eventually.
Our knowledge of the country is still too imperfect to enable us to
predict the result with certainty. Whether it can accomplish this or
not depends more on the success of the Goraie and the Jessore rivers
in finding an outlet for the waters of the Ganges, than on the resist-
ance of the eastern country. I may, however, be allowed to remark,
in passing, that it will be a great advantage to the delta if the
Brahmapootra does maintain its present course, and continues to act
as a barraye to the waters of the Ganges. ‘There is a great deal of
land to the westward that would be improved by being raised, while
it would be an immense benefit to the internal navigation if the
Kishnaghur rivers could again be opened, and these objects can only
be attained by the persistence of the eastern rivers in their endea-
vour to confine the western to their own territory.

If the Brahmapootra is able to maintain its present position at
Jaffiergunge, another effect will be, that by continually damming
back the waters of the Oorasagur, it will force the Natore rivers to
deposit their silt, and to fill up the very low country through which
theyrun. A good deal has already been done in this direction since
Rennell’s survey; and if the action continues much longer, they
must abandon the struggle with the Brahmapootra, and seek an
outlet somewhere between Bauleah and Surdah, some eighty miles
further up the stream of the Ganges.

It follows from all this that, if the Brahmapootra continues in its

present bed, it will almost certainly close the eastern outlet of the
Ganges. At present it is kept open by a rather curious process,
which it may be worth while to describe.
_ As before mentioned, the principal means by which the Megna
defeated the Brahmapootra was by being first in the battle-field ; and
though the Brahmapootra is slower than the Megna, it 1s quicker
than the Ganges, owing to the length of course of the latter river,
and its depending more on the melting of snow than on rain.

The consequence of this is that, for the first month of the
inundation, the water in the Ganges above Jaffiergunge almost flows
backwards, and the Echamuttee at Pubna flows into the Ganges
instead of out of it; and, during this season, the deposit in its bed is
very considerable. But, during the last month of the rains, when the
waters of the Brahmapootra have nearly run off, the immense body of
water spread over the vast plains of Hindostan rushes into the par-
tially deserted bed of the Brahmapootra, which then acts as a waste-
water reservoir, and with a force that, to a great extent, clears out
the deposit of the earlier months, and so restores the equilibrium.

This has been so entirely the case of late years that the Ganges
has straightened its course very considerably below the head of the
Jellinghy. ‘The first result of this was to cut off a great six-mile
bend on the left bank just above Pubna. This took place some
thirty years ago. Within the last two years it has cut off the next
bend on the right bank, leaving the Koostee Station of the Eastern
Bengal Railway some two or three miles below the head of the

338 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Aprsk,

Goraie, instead of two miles above it on the Ganges as it originally
was, and was designed to be ; and if this sudden rapid rush at the
end of the rains can be maintained, it probably will suffice to keep
the river open, and so maintain the present status.

It will be easy to perceive how this effect takes place, if we bear in
mind that the fall of the country between Pubna and Jaffiergunge
(thirty-six miles) is only about seven feet; and if all the waters
were supplied by one river, that would be their slope; but if, at any
moment, the waters of the Brahmapootra should be seven feet lower
than those of the Ganges, the slope will be doubled; and if ten feet,
the scour must be tremendous; and it 1s believed that this was the
difference when the last bend was cut off.

8. Kishnaghur Group of Rivers.—After the Jessore rivers just de-
seribed, the only other great group of distributaries of the Ganges is
that known as the Kishnaghur rivers, and consists of the Bhagaruttee,
Jellinghy, and Matabangah, which, uniting above Sooksaghur, form
the Hoogly.

Of these the oldest is the first-named. Indeed, if we consult
either native traditions or internal evidence, it is the Ganges itself,
and bears the same sacred name here as it does at its source; the
name Ganges, which is applied to the intermediate portion, merely
means Gunga or Gonga—the river “ par excellence.”

Whether we look at it from a geological or an historical point of
view, there can be little doubt that the original river, after passing
Rajmahal, would naturally run southward, parallel, or nearly so, to
the course of the Brahmapootra at that time, the distance between the
two being probably under ninety miles. The intermediate space
would then have been fully occupied by the Coosy, Mahanuddee,
Atree, Teesta, and other Himalayan torrents, all of which were pro-
bably at that time tributaries to the Brahmapootra ; though, in con-
sequence of the extension of the delta, they have most of them
seceded to the Ganges.

It is probable that the Bhagaruttee River, or true Ganges, always
flowed very nearly in the direction it now does, the extension of
the delta on the left being about sufficient to counterbalance the
repulsive action of the More, Adjie, Damooda, and Roopnarain, on
its right bank. There is, indeed, no improbability in supposing that
the original state of things may be, to a great extent, restored before
long. All the silt of the two great rivers has been employed for a
considerable time in raising the eastern half of the delta, and as that
rises it throws the waters westward; and though we can hardly con-
template the Great Ganges flowing again past Moorshedabad, there
is every reason to suppose that the body of water flowing through
the Kishnaghur rivers will largely and steadily increase.

It is not very easy to ascertain now which were the earliest as-
sistants of the Bhagaruttee in distributing the waters of the Ganges ;
but, of those which have left any traces, three may be mentioned as
the best known. The first of these was the Coomar, mentioned be-
fore, and running E.S.E. nearly parallel to the bed occupied by the
Ganges fifty years ago; the Boyrub, running south-east; and the

1863. | FERGUSSON——DELTA OF THE GANGES. 339

Echamuttee, taking an intermediate course between the last-named
and the Hoogly, whose course is due north and south. As mentioned
above, the lower part of the first-named river was cut off by the
Chandna, and it then dried. The upper half long remained mofibund,
but was revived by the late invasion of the Brahmapootra. The
second was extinguished, probably some 300 or 400 years ago, by
the Jellinghy, which, when the slope of the delta towards the east
became less, turned its waters from the south-east to south by west,
and with them joined the Bhagaruttee at Nuddea, the Nyadwipa
of olden times—a new island when the neighbourhood was a sea,
or at least a tidal swamp. The third was nearly meeting a like fate
from the Matabungah, which, appropriating a part of the bed of
the Coomar, and then a part of the Echamuttee, opened out the
Choornee nullah of Rennell, and joining the Hoogly above Sooksa-
ghur, it promises, if not checked, to play an important part in the
fluviatile history of the delta.

The cause of the recent increase of the Matabungah is, of course,
the action of the Brahmapootra on the lower Ganges, and its inabi-
lity to open up the Coomar suddenly, or the Echamuttee, which is
an old and thoroughly settled river, with high consolidated banks
and very short oscillations. Its success, however, will mainly depend
on whether it can so open out the Hoogly as to admit of its taking off
the extra supply of water it may bring down. Whatever the ulti-
mate result may be, it began vigorously. At Sooksaghur there was a
noble country-house, built by Warren Hastings, about a mile from the
banks of the Hoogly. When I first knew it in 1830, half the avenue
of noble trees, which led from the river to the house, was gone;
when I last saw it, some eight years afterwards, the river was close
at hand. Since then, house, stables, garden, and village are all
gone, and the river was on the point of breaking through the
narrow neck of high land that remained, and pouring itself into
some weak-banked nullahs in the low lands beyond; and,.if it had
succeeded, the Hoogly would have deserted Calcutta. At this junc-
ture the Eastern Bengal Railway Company intervened. They were
carrying their works along the ridge, and they have, for the moment
at least, stopped the oscillation in this direction. If they are able
to do so in future, it will remain to be seen whether the Matabangah
has the power to open out the reaches of the Hoogly so as to take
off the water; but this doubt. The river is old, its banks are high
and much built upon, and great sums of money would be spent in
groins and embankments to stop its encroachments. These may be
successful ; in which case it must open up the Echamuttee, or break
through somewhere and get behind Calcutta. This might not be a
_ serious misfortune for that city; indeed, the Hoogly becoming a
mere tidal estuary like those of the Sunderbuns, without any silt-
bearing streams flowing into it, would be an advantage, were it
not that lower down there are two rivers, the Damooda and the
Roopnarain, which would probably, during the rains, be able to shut
it up if there was not a very heavy counterbalancing pressure from
the Kishnaghur rivers to keep it open.

340 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. { Apr,

Not very long ago, if we may trust tradition, the Damooda joined
the Hoogly at Satgong, above Hoogly; and even in Rennell’s time
the old bed was open, and is marked in his maps; but it was bent
back, and was evidently, in his time, losing its gripe on that stream.
It has now, like the Sylhet rivers, been bent south, and, like the
Megna, les in wait further down, prepared, in conjunction with the
Roopnarain, to retaliate if any accident or moment of weakness
should come over its old antagonist, the Hoogly.

According to the natives, this great change took place only in
1757-1762 *, when the Damooda burst into what had been the old
channel of the Bhagaruttee and joined the Hoogly—the new name
of the new stream—close to the mouth of the Roopnarain, which the
natives persist in asserting is an old mouth of the Ganges; and they
are probably right, though Major Rennell, in his Atlas, takes the
trouble of denying it.

If the time when this great change is said to have taken place be
even approximatively true, it affords a mucb more satisfactory ex-
planation of any change that may have taken place in the navi-
gability of the Hoogly than can be derived from any silting-up of
the Kishnaghur rivers, which seem to have remained unaltered at
least since Tavernier travelled in India in 1666, when these rivers
seem to have been pretty much in the state they now are. But if
the land is rising rapidly in the eastern half, especially about Jaf-
fiergunge, which there seems no reason to doubt, while there has
been no change of level in recent times in the western half, it follows,
almost as a certainty, that the western rivers must go on gradually
but steadily increasing in volume, and with them the quantity of
water flowing through the Hoogly.

On the whole, therefore, it seems fortunate for Calcutta that the
Hoogly did not break through at Sooksaghur; and this circum-
stance will be a benefit to a large portion of the delta if it forces
either the Echamuttee or the Boyrub again to open its oscillations. As
mentioned above, both these rivers were cut off by the Jellinghy and
Matabangah when this part of the delta had been so-raised that the
inclination was rather to the west than the east or south. When
the town of Jessore was built on the Boyrub, some 350 years ago, it
is said that it was situated on the sea-shore, though this probably
only means that the country to the southward of it was a tidal
swamp, which, so far as we can judge, was the condition of a great
portion of the delta at that period, though the seaward face of the
Sunderbuns was probably the same as it now is.

It must have been immediately after this that the Kishnaghur
rivers cut across the Boyrub, and deprived it of its supply of Ganges
water ; for at a distance of about six miles below the town of Jessore
it ceases to be a “depositing” river. Up to that point its banks
are high and firm, its oscillations quick, and it has all the appear-
ance of an active river. For twenty-five miles from that point it
runs to Culna, and beyond it, as straight as a canal, through an
immense tract of jheel-land. It has had no silt to form banks, or

* Capt. Sherwell’s Report on the Rivers of the Ganges, 1858.

1863. | FERGUSSON

DELTA OF THE GANGES. 341

to raise the country, for nearly forty miles in length and some
twenty to thirty in breadth; while, as the more active rivers on
either hand have raised theirs, this remains an immense half-inha-
bited tract, which is yearly getting relatively lower, and will become
absolutely uninhabitable unless some active silt-bearing river turns
in that direction. Whether it will be from the westward or the
eastward that the succour will come remains to be seen. My im-
pression is that it will be in the latter direction. Already the Ellan-
khally has sent the Chittra in a south-westerly direction across the
Boyrub at Kulna; and it has done a great deal of good in raising the
depressed country. This stream is not marked in Rennell’s maps.
When I knew it, it was narrow and crooked, but deep and navigable.
It has now one-mile oscillations, with a width of about 1200 feet,
and is increasing. Its only defect is, that it strikes the Jheel-
country too low. What is wanted is that the Ellankhally should
send off a branch a few miles below the junction of the Novo Gunga,
which would enter the heart of the swamps. If it does not find an
opening to the eastward, across the Barassya (which, as mentioned
above, it is now seeking), it will probably turn in this direction, as
it affords an opening which, though not so promising, is yet pro-
bably more easily accessible than the other.

9. Changes in the Course of the R. Teesta.—Before leaving the
rivers of the Delta, there is one that exhibits phenomena of so dif-
ferent a class that it may be well worth while noticing them, in
order fully to understand the subject.

The largest tributary to the delta-streams, east of the ae is the
Teesta. It rises in the Sikkim Mountains not far from Darjeeling ;
and when surveyed by Major Rennell, it took a course due south
_ after passing Julpigoree, joimed the Attree, and, after flowing past
Dinajepoor, joined the Natore rivers, and thence, passing through the
Oorasagur, joined the Ganges at Jaffiergunge. In the year 1787,
either one or two years after Major Rennell’s survey was completed,
an unusual flood occurred; the river brought down from the hills a
sufficient quantity of sticks and stones to throw a dam across its
junction with the Attree, and, taking a south-east course, it joined
the Brahmapootra above Dewangunge.

The curious part of the matter is that, on looking into Rennell’s
original MS. surveys, a chain of ponds is marked in this direction
as ‘* the old bed of the Teesta,” too insignificant to be marked in his
Atlas; but at their junction with the Brahmapootra he does mark
“ Teesta Creek.’’? To those who know how permanent the names of
rivers are, this is proof positive that the river once before flowed
in this direction; but, unfortunately, we have no knowledge when
it deserted this bed and became a confluent of the Attree. Since the
separation, however, it has shown no tendency to go back, but runs
steadily in the direction it took seventy-six years ago, and in which
it now flows with an oscillation of two miles, and a width, even in the
dry weather, of some 2000 feet.

One thing, however, may be remarked, namely, that it certainly
was not any change in the leyel or the course of the Brahmapootra

VOL. XIX.—PART I. 2A

342 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 1,

which induced the change. Julpigoree, where the alteration took
place, is 200 feet above the level of the river at its mouth, and it
flows for the first forty or fifty miles with a fall of 3 feet per mile ; for
a like distance further on the fall is 2 feet, and the slope gradually
sinks to 6 inches, or it may be less; but nowhere is it a depositing
river or, consequently, influenced by back-waters ; and it therefore
appears to have been merely an accident which caused the change,
though being so, it is as likely to go back any day as to remain in
its present position.

10. Retrocession of the Junctions of tributary Streams with main
Rivers.—There still remains one class of phenomena to which I must
direct attention before concluding, namely, the shifting upwards of
all the mouths of the tributaries of the Ganges along the main
stream. ‘This is, perhaps, the most generally interesting of the
alterations that are taking place, not only from the magnitude of the
changes it superinduces, but because of its forming the best chrono-
metric scale for estimating the extension of the delta and the recent
sequence of events.

Although I am not aware that they have been anywhere alluded
to before, the causes that lead to the changes appear to be tolerably
obvious when pointed out.

In order, however, to make myself perfectly understood, let me
first refer to what I said about secular elevation in an early part of
this paper, and then assume two hypothetical cases, which I trust
will make the matter quite clear.

First let me assume hypothetically that the Ganges, from Allahabad
to Rajmahal, was a perfectly horizontal canal or arm of the sea, run-
ning due east and west. It is evident that the slope formed by the
rivers bringing down detritus from the hills on the north and south
would dip north and south—but their plains would equally be hori-
zontal in a direction east and west—and consequently that all the

Figs. 3-6.—Diagrams illustrating the Junctions of tributary Streams
with Main Rivers.

=

i (

| ewintniii, *>

MAME it A yf Gp }

\ } | WT Wate Vig fl
ifthe SG ZS hi. [ ==

RANI IO NN

AEA

FERGUSSON——DELTA OF THE GANGES.

Fig. 4.

343

242

344 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [aspraahs

tributary streams would join the assumed Ganges-canal at right
angles, as shown in the diagram, fig. 3.

For the second hypothesis, let me assume that the sea, or canal,
extended from somewhere below Rajmahal to the Himalayas, due
north and south, and that the dip of the plain was west and east,
say from Cawnpore or Fyzabad to this canal or sea, as shown in
fig. 4. It is evident that all the streams, on issuing from the
hills, would tend to turn eastward, and to run parallel to the Ganges.
Neither of these, of course, truly represents the facts of the case.
The valley or the basin of the Ganges, like that of almost all rivers,
is compounded of these two plains, varying in slope according to
circumstances ; and the course of the tributaries is along the diagonal
or mean of these two intersecting plains.

Thus, if we assume that when the sea was at Rajmahal the
slopes of the two plains were about equal, as shown in fig. 5, all
the tributaries would join the main stream at about an angle of
45°; but the extension of the delta has now raised the land about
this place to nearly 80 feet above the sea-level. This has been
equal to tilting back the valley of the Ganges to that extent, without
materially affecting the slopes of the lateral plains, as they are
shorter, and start from much higher fixed points at the foot of these
hills. The consequence is, that the angle of 45° is always tending
to increase, and must eventually reach 90°, or nearly so, in all cases.

There are only slight indications in Bengal of the state of affairs
represented in fig. 4, but it can be traced in parts. The upper
part of the valley of the Ganges, from Allahabad to the mouth of
the Gogra, is in the state represented in fig. 5, with a tendency
rather towards that shown in fig. 4. The lower partis fast assuming
the form represented in fig. 3. But there is still a fourth form which
the rivers must all ultimately assume, and which more resembles
fig. 4 than any of the other diagrams. It is this: as soon as the
slope of the principal stream has been so reduced by the elevation
or extension of the delta, or other causes, that it becomes a deposit-
ing river, it will then so raise the level of its plain above the sur-
rounding country that the tributaries cannot flow directly into it.

The form they will then take is shown in fig. 6: having been re-
duced to joing the main river at right angles, as in fig. 3, they will
be turned at right angles on reaching the edge of its plain, and,
flowing parallel to it, join it at some point lower down, where the
tributary may have acquired sufficient elevation to force its way
into the bed of the great river.

We have already examples of this in the way the Soorma was
deflected by the Brahmapootra, the Damooda by the Hoogly, the
Attree by the Poddah, and all the minor South Behar streams by
the Ganges. The Coosy too is fast assuming this shape, and even-
tually it will become the normal condition of all the tributaries of
the Ganges.

The first river to feel the effect of the tilting backward of the
plane of the Ganges, by the elevation of the land at Rajmahal, was
the Coosy, as the nearest to the delta. The consequence is, that

1863. ] FERGUSSON—DELTA OF THE GANGES. 345

when Rennell surveyed Purneah, he saw, and recorded in his memoir
in the ‘ Philosophical Transactions’ *, as well as in his Atlas, that
the Coosy had at no distant date flowed past the station at Purneah,
and joined the Ganges forty-five miles further down than its present
junction. Buchanan Hamilton not only confirms this, but adds :—
“This tradition is not only supported by the above-mentioned
appearance, but by the opinion of the Pundits, or natives of learn-
ing, who inhabit its banks. These, indeed, go still further, and
allege that in times of remote antiquity the Coosy passed south-east
by where Tajpore now is situated, and thence towards the east till
it joined the Brahmapootra, having no connexion with the Ganges ; ”
and he adds, “this opinion seems highly probable” +. Indeed, an
attentive study of the successive changes that have taken place
renders this almost certain; and it is probable that the Oorasagur
is the mouth by which the combined waters of the Coosy, the
Mahanuddee, and the Attree were originally discharged into the
Assam river.

Were it possible, it would be extremely interesting to know
when this was the case. We may certainly assert that it was before
the Madoopore jungle was upheaved—and when, consequently, the
course of the Brahmapootra was very nearly what it now is—and also
at a time when the tide, or at least very low land, extended to
Pubna or thereabouts ; and that this should have occurred within the
very limited range of the traditions of Lower Bengal induces me to sup-
pose that the beginning of the Christian era is the highest antiquity
that can be ascribed to such a state of things. Itmay be much later.

The present course of the Coosy is so nearly perpendicular to that
of the Ganges, that its direct Junction can hardly travel more than a
mile or two further up stream. The first result of any further rise
in the level of the Ganges will be that of decreasing the radii of its
curves, making it more winding, and converting it into a depositing
stream, which it hardly is at present

The rising of the deltaic plain has already produced another effect
since Rennell’s survey was made, the middle, or the belly, of the
river having travelled westward some four or five miles throughout
the greater part of its course; and it shows a great tendency to go
further in this direction—in fact, to emulate the example of its old
confluent, the Mahanuddee, which forms a curve extending thirty-
five miles to the westward of the straight line in which we may
reasonably suppose it reached the Ganges at no very distant date.

As just mentioned, its junction with the Ganges tends to assume
the rectangular form explained in fig. 6; and though its main
course is steadily travelling westward, its mouth may travel east-
ward; and, before many years are over, it probably will again join
the Ganges as low down as it did when its main stream flowed past
the station of Purneah.

The principal river of the Tirhoot district is the Bogmutty, which
presents exactly the same phenomena as those last described. It
has an old bed to the eastward, much more perpendicular to the

* Vol, Ixxi. p. a7, + Martin, vol. ii. p. 15.

346 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 1,

course of the Ganges than that it now occupies. It has now been
deflected so far westward that it joins the old bed of the Gunduck,
and, in our careless nomenclature, actually gives its name to the
lower part of that stream, and in Rennell’s maps is so called at its
junction with the Ganges opposite Monghyr.

The next river to feel the effect of these changes was the Gun-
duck. In this instance the evidence is as clear as could be desired.
A river marked on our maps as the Little Gunduck—sometimes,
but very improperly, as just mentioned, called the Bogmutty, from
the name of its principal tributary—joins the Ganges opposite Mon-
ghyr; and there can be little or no doubt that it was what it is
styled in the maps of the recent Survey, the Boor Gunduck, or old bed
of that river.

Judging from the height of its banks and that of the land in its
neighbourhood, and the extreme sinuosity of its course, this old
river must long ago have ceased to flow with any vigour. A date
might possibly be found for the time when this was the principal
river; but, with the information at present available, all we can
say is that it was so at a time when the country was sufficiently
inhabited for the nomenclature of the rivers to be fixed.

At the earliest period to which anything like authentic history
reaches, this river seems to have been distant from its present
channel about twenty-two miles to the north of its present mouth,
near Bakhra, or the site of the famous city of Vaisali, celebrated as
the place where the second convocation of the Buddhists was held,
300 years before Christ, and to have joined the Ganges some thirty-
three miles further down than at present. It is now so nearly per-
pendicular, that it will probably be a long time before it travels
much farther westward.

Proceeding upwards, the next river of any importance we meet is
the Soane. Here, fortunately, we have more precise information.
Arrian, Strabo, and Pliny—or rather Megasthenes—tell us that
Palibothra, the great capital of this country, was situated at the
junction of the Erranaboas and the Ganges. Recent antiquarian
discoveries have left no doubt that Patna—‘ Palibothra”— is
the city designated, and that the Hyranya Bahu—the Golden-
armed, or, popularly, the Sona, or Golden—is the river; and,
fortunately, an old branch of the Soane can still be traced, from
a spot about twelve miles up the stream to near the west end
of the present city. In Rennell’s time the Soane joined the Ganges
at Moneah, twenty-two miles further west, by a single mouth.
Since his survey it has formed a delta, and the upper mouth is
the more important; so that, practically, it may be said to have
receded four miles since that time. If in eighty years it has pro-
gressed so much, in 2000 it ought to have gone back 110 miles,
instead of only twenty-five or twenty-six; the probability con-
sequently is, that the delta was not then sufficiently extended or
raised to affect rivers so far up the stream ; indeed, it may have been
1000 or more years after the fact was notified to us that the eleva-
tion of the delta was first felt so high up as Patna; and, if so, we

1863. | FERGUSSON—DELTA OF THE GANGES. 347

may expect that the retrocession will now go on at a rapidly in-
creasing rate. Whether our railway-works and bridge may be able
to prevent this or not remains to be seen. If they do so, it can
only be at an enormous annual expenditure for embanking and
repairs. In fact, had the engineers been aware of this physical
fact, they would probably have placed their bridge very much
further up the stream than they have done. But be this as it may,
it will be extremely interesting to watch now the progress of the
stream ; and having two surveys, separated by an interval of eighty
years, and the old indications of the Greek geographers, we may
from these data obtain a tolerable index by which, to measure the
progress of the delta seawards, or its progressive elevation above the
sea-level at Rajmahal.

The next stream that ought to be affected is the Sarjoo, or Gogra.
It does not, however, seem to have been affected at all; indeed, at
first sight, it seems to have been moved downwards since Rennell’s
survey. This arises, however, only from the Ganges having cut off
a sharp bend at this point of its course, and the river Gogra flowing
through the arm thus left unoccupied. It does not appear probable,
however, that it can remain much longer uninfluenced by these
changes; but, until it is so,it may be taken as the fixed point beyond
which the extension of the delta has not in recent times affected the
slope of the bed of the Ganges.

The only indication I have been able to obtain of the Gogra,
or Ghagra, having travelled westward, in historical times, is the fol-
lowing :—

There is an old bed of an old river which leaves the present
Gunduck at a point somewhere between Bakhra and Lalgunge, and
joins the Ganges opposite Bar. This branch, I have just stated, was:
probably an old bed of the Gunduck ; but it still bears the name of
Ghagra; and those who know how permanent Indian names are will
hardly hesitate to believe that it may have been an old channel of that
river. The evidence cannot be considered as conclusive, however, as
I have been unable to trace the course of that river across Sarun.
Nothing can be more probable than that, when the Gunduck joined
the Ganges opposite Monghyr, the Ghagra should have joined oppo-
site Bar; or that the Gunduck should have cut across that stream
at Bakhra and occupied its lower portion, just as the Bogmutty has
cut into the old Gunduck and occupied its lower portion ; and, lastly,
that the new Gunduck should have broken through and sought an
independent opening into the parent stream. The Bogmutty will
certainly do this one day; at present it is too small and weak a stream
to act with the energy of the Coosy or Gunduck, but it must even-
tually come to this.

The next move must be that the Ghagra will seek a junction with
the Tonse, and join the Ganges either through its bed or further
west. Jam not aware, however, that any tendency in that direc-
tion has yet been observed.

348 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 4,

§ III. Mistorical Evidence of Changes in the Delta of the Ganges.

Having now run through all the principal phenomena to which I
wished to call attention, describing them from a topographical point
of view, allow me to recapitulate, as briefly as I can, the his-
torical events connected with them, in order that their approximate
dates may be judged of; for as all the events to which I have
alluded appear to me to have occurred within historical times, and
after the rivers had received their names from the Aryan races
inhabiting their banks, we may, without difficulty, connect history
with topography in this instance at least.

With the first-dawn of history or tradition, about 3000 years B.c.,
we find the immigrating Aryan Hindoos traversing the Punjaub, and
settling, so far as India is concerned, exclusively in the tract of
country between the Sutledge and the Jumna. Their rivers were
the Sareswati, the Caggar, and the Markandya, which must then
have been far more important streams than they are now. Whether
their decay arose from neglect of cultivation, after breaking up the
soil, or from their raising their beds so as to spill towards the
Jumna, or from what other cause, is by no means clear. The last-
specified, however, is the most probable. The bed of the Sareswati,
at a distance of twenty-four miles from the Jumna, is thirty feet
higher than that river. The Caggar, at a distance of fifty miles, is
ten feet higher than the last; and the country gradually slopes
upwards till it reaches a height of fifty feet, close to the Sutledge,
whose waters at Loodiana are at the same level as those of the
Jumna at Kurnal*.

This tract, though not quite a desert now, is nearlyso. Its rivers
are insignificant streams, and lose themselves in the desert; and
Thaneswara and Samana, the old classical cities of Arya-Varuta, are
now nearly deserted.

The next capitals of this race were Delhi, on the extreme
northern spur of a range of hills on the nght bank of the Jumna,
and Muttra, about eighty miles further down, but still on the
elevated right bank. The first cities really in the plain were
Hastinapora, on the Ganges, about fifty miles from the hills, and
Ayodya, on the Gogra, at about sixty miles from the Himalayas,
the last occupying the same position with reference to the valley of
the Ganges that Sudya does to Assam; and it seems to have been
one of India’s most important cities between 2000 and 1000 years B.c.
About the last-named date it appears to have been superseded by
Cannouge, on the Ganges, this time 120 miles from the hills, being
the farthest advance into the plains before the Christian era.
Allahabad and Benares next rose into importance.

In the fifth or sixth century before Christ, when we become
tolerably familiar with the geography of India, from the events of
Buddha’s life, we find, in the south, Rajagriha on the hills, and Gya
close by, the most important cities of the central portion of the

* These levels are taken from a survey by Lieut. (now Col.) Baker, Journ,
Asiat. Soc. Bengal, vol: ix. p. 688.

1863. | FERGUSSON—DELTA OF THE GANGES. 349

Gangetic plain ; these were superseded about three centuries later, or
in Alexander’s time, by Palibothra, or Patna, which was the most
important city of India at the time of Alexander’s conquests*.
On the north of the valley we first find Janakpore, in the Terai,
between the Bogmutty and the Coosy, figuring as the capital of
Bengal at the time when Ayodya was practically the capital of
India; then Sravasti, Kapilavasti, and Kucinagara, all nestling under
the hills close to the Terai, and the remains of ruined cities of this
epoch within its now pestiferous limits,—showing that from the
greater steepness of the slope, or some such local cause, this was then
the most habitable part of the valley of the lower Ganges.

It is not till six or ten centuries after our era that we find any
more important cities eastward of Patna; but, about the last-named
period, Gour, opposite Rajmahal, became the capital of Bengal, to be
superseded by Dacca, founded in 1604, and Moorshedabad, which
only rose into importance in 1704.

For a century after 1634, when our ships were permitted to enter
the Ganges, Satgong or Hoogly was the port of Bengal, and continued
to be so till superseded by Calcutta.

The ships of those earliest days were no doubt much smaller than
those afterwards introduced; but no sea-going vessel could well now
get so far up the river. And it may also be remarked that when
Admiral Watson attacked Chandernagore in 1757, he took up to
that city what were then called line-of-battle ships, vessels of
60 and 64 guns, which, whatever their tonnage may have been,
would with difficulty reach Calcutta now without the aid of steam.

It would be tedious, as it would be out of place here, to attempt to
explain the data on which these historical conclusions rest, and
pedantic to assert that they are more than approximate inductions
from imperfect data. But I may state, generally, that long local
study has left the conviction strongly impressed on my mind, that
3000 years B.c. the only practically habitable part of the alluvial
plains of the province of Bengal was the portion between the
Sutledge and the Jumna; that even 1000 years later it was only
here and there, on the banks of some minor streams, that the country
was in a state to support a large population, and to possess con-
siderable cities; that nearly up to the Christian era it was only on
the southern hills, or at the foot of the Himalayas (what is now the
Terai), that cities could be placed, because the central parts of the
plain eastward of the Gogra were still unfit for human habitation ;
that it was not till 1000 years afterwards that the plain of the
Ganges was sufficiently desiccated to admit of such a city as Gour
rising to importance, so far from the hills; and not till the Maho-
metan conquest in the 14th century that the Delta, properly so
called, became fit for extensive occupation.

So far as can be judged from the rapid rate at which changes have
taken place, and the immense quantity of land which has been

* The circumstance of four of the largest rivers in India—the Gogra, the Gun-
duck, the Soane, and the Ganges—meeting at one spot has so raised the country
in the neighbourhood of Patna, that it must early have been a habitable tract.

350 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [-ApEsl;

redeemed from jungle and swamps, during the last century, there
seems nothing to contradict this theory of the very modern origin of
the present configuration of the valley of the Ganges.

It is not, of course, meant to be asserted that the valley of the
Ganges was filled up, geologically speaking, within that period, but
only that it became fit for man’s occupation within the limits of the
historical period, as hundreds of square miles of the Delta have
become since Rennell’s survey was made.

The greater part of the valley of Assam still remains—what the
plains of Bengal may be conceived to have been 2000 or 3000 years
ago—uninhabitable swamps, with occasional spots where cities have
existed or do now stand. But if the principles enunciated above
are to be depended upon, the recent changes in the course of the
Brahmapootra ought rapidly to affect the level of the land in that
valley; and it cannot possibly require a thousand, or half that
number of years, before the swamps opposite Gealparah and Goa-
huttee become as dry and as habitable as the plains of Purneah in
Tirhoot.

§ IV. Increase of the Delta seaward.

1. Silt held in suspension in Ganges’ Water.—It will have been
observed that, in the previous part of this paper, I have said
nothing about the quantity of silt contained in the water of the
rivers I have been describing, nor attempted to calculate its in-
fluence either in extending the delta seaward, or in raising it
upwards. I have refrained from alluding to this simply because
I know of no data on which any reliance can be placed.

To base any calculation on this agent, the experiments ought
to be continued for, at the very least, one whole year, on some one
at least of the larger rivers. But this has not yet been done; and,
even if it were done for the Ganges, it must be nearly useless unless
we had the same knowledge as regards the Brahmapootra, which I
believe to be an infinitely more important stream in this respect than
the Ganges itself. And we ought also to know what is brought down
by the Mahanuddee, and the group of Natore streams debouching
through the Oorasagur.

The latter rivers run through so low a country that they probably
deposit most of their silt en route; but the Mahanuddee and its tri-
butaries are swift, and strongly embanked. The Sylhet rivers may
probably be disregarded; they never possess much silt, and what
little they have they deposit at home, so they contribute little or
nothing to the delta. Supposing, however, all this were ascertained
for every river just as it enters the delta, another very important
question arises—How much is deposited on the plains of the delta,
and how much carried to sea? During the cold weather, when the
rivers are low, almost all their silt will be carried to sea; but then
the quantity of water is small, and that little comparatively clear.
At the height of the inundation, when the river is overflowing its
banks, at least one-half is deposited inland. As the rivers fall, the
greater part will again be carried away; but as the force of the

1863. | FERGUSSON——DELTA OF THE GANGES. 351

current slackens, there is a great tendency for rivers to deposit their
mud in their own beds, and to heal the wounds that have been made
in their banks; so that even during that period it is doubtful if more
than half is carried off. For instance, careful simultaneous experi-
ments were made, two years ago, as to the quantity of solid particles
held in suspension in the waters of the Matabangah,—first, at leaving
the Ganges, when it was found to be 1 in 294 parts, while nearly
at its junction with the Hoogly the quantity was only 1 in 884,
proving that two-thirds had been deposited en route in that short
distance *.

Sometimes an acre or two of a bank will fall in in a single night,
- and, consequently, the stream will be unusually turbid for the next
twenty-four hours; but, in such an abnormal instance, one-half
at least probably never leaves the local stream, but is deposited again
a few miles further down; and, in fact, every stream and every
locality has its peculiar regimen in this respect, and until they are
more carefully examined than they have hitherto been, it will be
safer to look to such indications as history affords us, and to our
charts. These last show that little or no change or extension
seawards has taken place, during the last 100 years, between the
Hoogly and the Horringotta, or about halfway across the seaward
face of the delta. But the eastern half is in a state of rapid change,
haying remained behind, I believe, principally in consequence of the
absorption of the Brahmapootra’s silt by the Sylhet Jheels; but
probably in little more than a century or two from this time the gap
may be repaired, and the Sunderbuns bounded by a nearly straight
line east and west.

As regards the elevation of the delta, by far the safest test is the
progress of the junction of the tributary streams, such as the Soane
and Gogra. Ifthe former be carefully surveyed from time to time, and
the retrocession of the tributaries carefully noted, we shall gather far
more satisfactory evidence of the gradual elevation of the delta than
can be obtained by dipping tumblers from the sides of ‘ Budgerows,’
which operation has hitherto been supposed to be sufficient to gauge
the growth of continents.

2. Swatch of “ No Ground.” —There is still one other phenomenon
which it is necessary to allude to, in order to understand the
present or prospective condition of the seaward face of the delta
of Bengal. This is the existence of a great depression, or hole, in
the middle of the Bay of Bengal, known in the charts as the
“Swatch of No Ground.” Its exact position is shown on the map
accompanying this paper (Plate XIJ.), and its sides are so steep and
well defined that it affords mariners the best possible sea-mark—the
lead suddenly dropping, especially on its western face, from 5 and 10
to 200 and even 300 fathoms, with “no ground.”

' It seems quite impossible to ascribe this sinking to volcanic

action, inasmuch as we know that no such violent conyulsion has

taken place in Lower Bengal, during the last 200 years, as could

have caused such a chasm; and it is not conceivable that so large
* «The Ganges and the Hoogly,’ by F. Prestage. Calcutta, 1861.

aoe PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 1,

and so sharply defined a depression could have existed in so muddy a
sea for even a fraction of that time without being obliterated. or
smoothed over, unless there was some tidal or fluviatile action
always at work tending to keep it open; nor does it appear difficult
to explain where this action is.

If we turn to the authorized chart of the mouths of the Hoogly, we
find the following description of the action of the tides in that side of
the delta. ‘The tides in the channels have a rotary movement
with the sun, first quarter-flood W.N.W., round by N. to the last
quarter E.N.E., to first quarter-ebb E.S.E., round by 8S. to the last
quarter W.S.W.”

The same description applies to those on the other side, with the
difference that the larger portion of the tidal wave comes from the
eastward—following the course of the sun. The circle there is
considerably larger, as shown in the two black circles on the map.
The action is, in fact, strictly analogous to that of the phenomenon
known as the “ Bore,” which exists, to a greater or less extent, in all
funnel-shaped tidal estuaries. The flood-tide, coming up the con-
tracting bay from the southward, is accelerated on the shelving
shore on either hand, and reaching the face of the delta at its
eastern and western extremities before it touches the centre, this
rotary motion ensues. The consequence seems to be that the two
circular tides, meeting somewhere in the centre of the bay, must do
one of two things—either they must throw up a bar or spit between
them, or they must scoop out a depression. ‘The first would be the
action of two rivers, the velocity of whose currents was diminished or
stopped by contact with the ocean. The latter seems the probable
action of two tides whose motion is continuous and uniform.

It is quite reasonable to assume that the action of these tides might
not have sufficient force to scoop out such a canal as this, if they
found the delta perfectly formed and uniform across the whole head
of the bay; but, as the tides certainly existed before the delta had
been formed by the deposit of the silt of the rivers, there is no reason
for doubting that their daily action is quite sufficient to sweep out
and keep clear any channel which may be necessary for the efflux of
these waters; and such, I feel convinced, is the true explanation of
the phenomenon. It must also be borne in mind that there is every
reason to suppose that the action of these tides has been constant
and uniform ever since the Bay of Bengal took its present shape,
and, consequently, it is probable that there may have always existed
a bar or spit on the neutral line between the oceanic and river
forces, somewhere not far from where the Sunderbuns now are.
If this were the case, the deltaic plains would then have been, as
hinted above, a great lagoon or inland sea—a circumstance which
would tend very considerably to accelerate the deposition of mud in
them, and thus to account for the rapidity of some of the changes,
which might otherwise seem strange.

As the case now stands, the western tidal wave has had sufficient
strength to sweep out the Balasore Roads, and to keep open the estuary
of the Hoogly, known as Saugur Roads. Thence turning eastward

1863. | FERGUSSON—DELTA OF THE GANGES. 353

towards the Swatch, it seems to have sufficient force to fix the
seaward limit of the western Sunderbuns as certainly as the current
that passes eastward has fixed the seaward boundary of the Delta of
the Nile.

The eastern half of the delta is by no means so fixed in its
regimen, principally, I am convinced, owing to the cause pointed
out in a previous part of this paper—in consequence of the
Brahmapootra being diverted into the Sylhet Jheels, in which its
waters were filtered, and its consequently bringing no silt seaward.
We learn, however, from Lloyd’s survey, made in 1836, that great
progress had been made in filling up the gap since the beginning of
the century; and if we had a new survey now, we might prophesy
approximately how long it would be before the eastern face of the
delta would assume a form as fixed as the western half.

The true base of the delta to seaward is the neutral ground
between the 5- and 20-fathom lines, which there is no reason
to suppose has altered, or will alter, in any time of which we can
take cognizance; for, the whole of the silt brought down by the ebb
being swept away to the depths of the ocean through the Swatch,
there is no reason to suppose that any sufficient portion of it is
brought back by the flood to alter so marked a boundary in any
appreciable degree.

Inland there is another neutral line parallel to this, in the tract of
high land extending from Calcutta to Bakirgunge, and when the
delta is complete it will reach Seetacond; this marks the boundary
where the tidal forces are stopped by the river’s action, and where,
consequently, a certain deposit takes place. Behind this inland
barrier there still exists an immense tract of jheel-country, in the
districts of Jessore and Fureedpore; but, judging from the extra-
ordinary changes which have taken place since Rennell’s survey
was made, there seems no reason to doubt that, in the course of
another century, if the rivers are left alone, there will be very little
jheel-country left in the western half of the delta; and the task of
the Ganges will then be completed, with the exception of a little
smoothing and filling here and there. But it will take several
centuries before the Brahmapootra will have rendered its domains,
especially in Assam and Sylhet, as habitable and as fertile as the
whole of the valley of the Ganges is, even at the present day.

§ V. AppEnpIx.

The following Table, though constructed on the best available
data, can only be regarded as an approximation to the truth, no
surveys having been undertaken with reference to the objects in
view; and though certain levels may be absolutely correct, they
do not give either the average height of the land or of the water, or
they give that only at exceptional periods.

The first two are from Col. Cautley’s survey for the Ganges-
canal; the next three from that for the East Indian Railway,
and may be depended upon except as regards the correct representa-

304 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 22,

tion of the true level of the mean high water or of the land at the
places mentioned. The remaining levels are from the survey for
the Eastern Bengal Railway, and may be depended upon within
fractional quantities, both as regards accuracy and levels of water.

The whole is based on the assumption that the highest level of
the floods represents the highest level of the land, and that this
datum at Calcutta is 27 feet above the Howrah Dock Sill.

Height, Wtrone Slope

in feet. | direct. | per mile.
burda 7c. WOR ee 974 miles. | inches.
Cann ponents 203A Fe 402 350 1S
Allahabad): 2252952008 ae 269 122 13:
Patna Moneahwy. 2st 161 200 6°5
Rapmabal: ea A, asa etal 68 185 6°
Calentia 2. 7h Rian Bee 0 168 4-8
Kooshibeaia: 1:1 iru. Sn OR, 27 100 32
Serajruneers:. wad 30 54 8

| Dacca and Naraingunge.... 4 76 4+]

This last would make the level of high water and of the land at
Goahuttee about 100 feet, at a distance of 350 feet from the sea,
which accords very tolerably with that of 70 feet given by Schla-
gintweit for the low-water-level above mean sea-level.

Aprit 22, 1863.

Nicholas Kendall, Esq., M.P., Member of the Royal Commission
of Mines, Pelyn, Cornwall; Major F. J. Rickard, Inspector-General
of Mines in the Argentine Republic, 214 Hanover Square, W. ;
and Charles Easton Spooner, Esq., Bron-y-Garth, Port Madoc,
North Wales, were elected Fellows.

M. A. Favre, Professor of Geology in the Academy of Geneva;
Franz Ritter von Hauer, k.-k. Bergrath, and of the Imperial Geo-
logical Institute of Vienna; M. Hébert, Professor of Geology to the
Faculty of Sciences at Paris; M. E. Beyrich, Professor of Geology
in the University of Berlin; and Dr. F. Sandberger, Professor of
Mineralogy at Carlsruhe, were elected Foreign Correspondents.

The following communications were read :—

1. On the Gxuiss and other Azorc Rocks, and on the superjacent Pa mo-
zo1c Formations, of Bavarta and Bonemia. By Sir Ropericx I.
Morcuison, K.C.B., D.C.L., LL.D., F.R.S., F.G.S8., &e.

Introduction.—In my last journey to Bohemia, I had no sooner
reached Darmstadt than I was gratified to find that, in two of the most

1863. ] MURCHISON—BAVARIA AND BOHEMIA. 300

recently published geological maps of Germany, M. Ludwig had
marked the Palaozoic subdivisions as Silurian, Devonian, Carboni-
ferous, and Permian*.

Thus, in travelling to the baths of Marienbad, I perceived that on
the western flank of the crystalline rocks of Eastern Bohemia and
the Erzgebirge the author had thus named and delineated the three
oldest of these groups in the tract around Hof, where, when I first
explored it, “‘ grauwacke” only was applied to the whole region by
German authorities.

It was, indeed, in the year 1839 that Professor Sedgwick and
myself began to make the subdivision, by pointing out the existence
of both Devonian and Carboniferous limestones near Hof. In sub-
sequent years, with the good maps of Naumann, I tracked Silurian
rocks, with Graptolites, as separated from Devonian limestones, ex-
tending from the Frankenwald into the Thiringerwald, where certain
meagre representatives of the Upper Carboniferous rocks are sur-
mounted by a full Permian series.

Proceeding from Eisenach on the north-west, where the great
Paleozoic promontory of the Thiiringerwald terminates in a point,
we see, in advancing to the south-east, that these Palaeozoic rocks
gradually expand, until, in the latitude of Hof, they occupy a great
width, and are succeeded on the south-east by the inferior azoic
and crystalline rocks of the Fichtelgebirge and the broad tracts of
eastern Bohemia.

To the south-east of Hof, M. Giimbel, of Munich, has recently
made a most important discovery. In schists overlying primary
clay-slate, and underlying Silurian rocks with Graptolites, he found
a peculiar fossiliferous band, the Trilobites of which, having been
transmitted to M. Barrande, were determined by his authority to be
Conocephalh, Olen, and Ellipsocephali, associated with Cystidec, Orthis,
Diseina, and Pugiunculus. Hence it was clear that M. Giimbel had
discovered in Bavaria an equivalent of the Primordial zone of the
Silurian series, of which M. Barrande had been the discoverer in his
Silurian basin of Prague. We thus learn that the Silurian rocks of
Bavaria, however less rich in fossils in their central and upper
members than those of the Bohemian basin of Prague, have the same
Trilobite-bearing base as the latter.

Having myself passed over the tract occupied by the older rocks
which separate those two Paleozoic tracts, 1 became very desirous of
obtaining from M. Giimbel some account of the exact order, as well
as of the dimensions, of those inferior rocks on which the Palzozoic
rocks repose. As he has been so kind as to send me a sketch-map
of all the region (fig. 1), as well as a transverse section (figs. 2 & 3),
showing the succession from the Carboniferous Limestone of Hof,
down to the gneiss and granite of the Fichtelgebirge near Selb, I

* See Ludwig’s ‘ Deutschland,’ 1860, and ‘ Deutschland und das Alpen-
Gebiet,’ and compare them with yon Dechen’s Geological Map of Germany,
published in 1838, in which the vast tracts now so subdivided were, as re-
gards the three lower formations, as well as the inferior clay-slate, all grouped
under one colour and with the name of ‘ Grauwacke.’

350 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 22,

Fig. 1.—Geological Sketch-map of a Part of Bavaria and Bohenua
(after Giimbel).

Le LZ

PME Hons 3
WEIDEN~

NEN SENES

‘

. Granite.

} Gneissose series,

4. Mica-schist.

5, Clay-slate.

6. Silurian Primordial Zone.

7. Silurian (except the Primordial Zone).
8. Devonian.

9. Upper Carboniferous.

10. Carboniferous.

11. Rothliegende.

12. Tertiary.

i \ Basalt.
C. Pfahl.

Lard

1863. | MURCHISON—BAVARIA AND BOHEMIA. 357

will presently dilate upon these important contributions, which con-
stitute, in fact, a main part of this communication*.

Gneiss of Bavaria and Bohemia.—One of my great objects in ex-
ploring this region was to satisfy myself, if possible, as to the
existence of a fundamental gneiss of as high antiquity as the Lau-
rentian rocks of Canada, and those of the north-west Highlands
of Scotland, which I had described. For this purpose, besides
traversing the country from Marienbad to Pilsen, and thence to
Prague and Pardowitz on the east, I repassed from Pilsen by Furth
to Regensburg, and afterwards examined the huge masses of gneiss
and granite which form the southern wall of the chain of the
Bohmerwaldgebirge between Passau and Linz, on the banks of the
Danube. I was unable, in my partial examination, to satisfy my-
self that the true gneiss of any one part of this vast crystalline
region overlies another or more ancient gneiss. But M. Giimbel in
Bavaria, and M. Crejci in Bohemia, believe in the existence of an
older and a younger gneiss, As, however, I am not aware that an
order of superposition has anywhere been seen, I am the more dis-
posed to consider all the gneissose rocks which underlie the micaceous
schists and primary clay-slate as belonging to one great fundamental
group, though eventually these rocks may be separated by proofs
worked out by local observers.

In order to convey to me his own ideas on this subject, M. Giimbel
has kindly transmitted to me a sketch-map (fig. 1) as condensed from
his long and laborious surveys, executed upon maps of a very large
seale. Dividing the gneiss into older and younger (2 and 3 of the
map), he distinguishes the first as a highly granitoid and reddish
rock, like the gneiss of the Erzgebirge, and containing 75 per cent.
of silex, and as being both intermixed with and penetrated by
granite. The younger or grey group of this gneiss contains courses
of hornblende, slaty greenstone, syenite, granulite, and serpentine.
The elder of these gneissose groups is roughly estimated by M. Giim-
bel to have a thickness of about 50,000 French feet, and the younger
group to be about 35,000 French feet thick; so that, as a whole,
the gneiss of Bavaria and Bohemia, according to this author, has a
maximum thickness of not less than 90,000 English feet!

Unable, as I have said, to see any order of superposition between
these two varieties of gneiss, I afterwards found that the same
variety of gneiss changed its direction so greatly in its range through
different tracts, that no inference respecting the age of the deposit
could be drawn from the strike of the strata.

This is, indeed, clearly demonstrated by M. Giimbel’s map (fig. 1),
by which it is seen that both the older and younger gneiss of that
author assume in some tracts the same strike, 7. e. E.S.E. to W.N.W.,
while in others they both change to a direction perpendicular or rect-
angular to the above, or from S.W. and W.S.W. to N.E. and E.N.E.

* The detailed labours of M. Giimbel are not to be judged of by this little
sketch-map. He has, in fact, so closely examined the various rocks of granite
and gneiss and all the superjacent rocks, as to have laid them down on the huge
cadastral map of Bohemia which is called the “‘ Feuer Cadaster.”

VOL. XIX.—DPART I. 28

358 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 22,

Thus, on the eastern flank of the Silurian basin of Prague, M.
Giimbel’s younger member of the gneiss, after conforming, with a
north-easterly strike, to the superjacent clay-slate and Silurian rocks,
folds round by devious bends until it reaches the southern end of
the mountainous wooded region called the Bohmerwaldgebirge.
There, where the gneiss-rocks are associated with vast masses of
granite, the longer axes of which are directed from W.S.W. to
E.N.E., both the older and younger gneiss have a coincident strike,
and they both range at a right angle to the dominant direction of
the strata in those parts of the region where they flank the fossiii-
ferous Silurian rocks.

I examined in some detail the gneiss-strata on the banks of the
Danube, between Linz and Passau, which form the southern fringe
of the Bohmerwaldgebirge; and, judging from their strike, which
diverged from that of all those beds of gneiss with which I was
acquainted to the S.E. of Prague, I thought that they might repre-
sent the older gneiss. Again, judging from their very siliceous
character, and led by the analogy of their structure and their having
the same direction as the older gneiss of the West Highlands of
Scotland, I at first inferred that they were probably inferior to other
gneiss-rocks lying to the N.E., as well as to those near Furth.

In these rocks of the Danube, whether at Passau or Linz, I saw no
trace of micaceous schists or serpentines, or any of those associations
which M. Giimbel assigns to the upper gneiss. On the contrary, I
found the grey gneiss, particularly at Linz, to be so eminently quartz-
ose and siliceous, that the fine white layers of quartz and felspar con-
stituted the dominant feature, as contrasted with the dark layers of
black mica. Such opinions, however, were necessarily modified by
the information kindly offered to me by M. Giimbel, and as laid down
in his little sketch-map. Thus, to the N.W. of Cham, the older
gneiss of that author, first ranging to the N.W., then bends to the
N.E., and is followed by the younger gneiss. ‘The latter, folding
round large masses of granite, after several contortions, passes away
with a normal north-easterly strike, as it extends to the south of
Marienbad and Karlsbad.

Again, as M. Giimbel shows in his map, the gneiss which he
believes to be the younger is that which ranges by Passau, and
occupies the gorges of the Danube—the very rock which I had sup-
posed to be of older date. Now, as he marks these, his younger
rocks, as dipping to the N.E., so as to seem to pass under his newer
beds, he was naturally struck with the anomaly. He supposes,
indeed, that this anomaly may be accounted for by a grand inversion
similar to the numerous cases of overthrow in the Alps, which he, as
well as others, has described. But, from what I saw, I cannot as
yet coincide with him in this view, inasmuch as the grand buttresses
of gneiss and granite which occupy the banks of the Danube between
Passau and Linz, and which are presumed by him to be the younger
gneiss, occupy a very low country, with no mountain-chain nor
igneous rock to the S8.E. or at the back of them, by which we might
account for their upheaval, and yet they all incline rapidly to the N.

1863. ] MURCHISON—BAVARIA AND BOHEMIA. 309.

and N.K., and seem fairly to pass under the other gneiss, My im-
pression, therefore, is that, on the Danube, the masses of gneiss are
in their normal position, and form simply one of the lower members
of the great gneissic series of Bohemia, the diversified mineral struc-
ture of which requires no detailed description by me.

M. Giimbel shows that a remarkable band of quartz-rock, seven-
teen German miles in length, called the “ Pfahl” (C, fig. 1), is asso-
ciated with his lower gneiss. But, again, this rock, as well as the
gneiss to which it 1s subordinate, strikes from E.S.E. to W.N.W.,
and is perfectly parallel to the associated gneiss of the Danube.

I am the more disposed to view all the gneissose rocks of Bohemia
and Bavaria as belonging to one great series, by examining M. Gim-
bel’s sketch-map, by which it appears that, where his older gneiss
folds round and strikes to the north, there are signs of great distor-
tion of the strike where the strata meet the southern end of the
granitic masses of the Fichtelgebirge. There, both his varieties of
gneiss bend round with very devious strikes, but each more or less
conforming to the granitic nucleus. It appears to me, therefore, that
the older and newer gneiss of this region form, as before said, one
great series only, and are not to be distinguished, like the fundamental
or Laurentian gneiss and the younger or micaceous gneiss of the
Highlands of Scotland, by a total unconformity, and by being sepa-
rated from each other by a great intervening deposit, as is the case in
Scotland. In point of fact, the so-called younger gneiss of Scotland
is simply altered Silurian, whilst mm Bohemia and Bavaria the one
gneiss is followed by another gneiss without any separating deposit.

In Bohemia and Bavaria we have, as before shown, many proofs
that the age of the old slaty and crystalline rocks cannot be deter-
mined by any partial examination of their strike ; for in one tract we
find the very same rocks ranging N.W. to S.E., and in another
trending from N.E. to 8.W.

In viewing these gneiss-rocks for the present as one great series,
I do so with some hesitation, and with every respect for the labours
of M. Giimbel, who has with infinite pains followed these crystalline
rocks into all their sinuosities, and may have better reason than my-
self for distinguishing the lower or, what he calls, the Bavarian gneiss
from that named by him Hercynian gneiss. I must also here re-
mark, that if all the true gneissic rocks of Bavaria be united, they
may well, from their colossal dimensions, stand in the place of the
Laurentian gneiss of Canada and of thenorth-west of Scotland. The
clear evidence which exists of the interpolation of a vast thickness
of sedimentary formations in which no fossils have been found, be-
tween the great gneissose series and the lowest Silurian rock, is a
good reason for believing that the gneiss of Bohemia and Bavaria is
truly the representative of the Laurentian or fundamental gneiss.

General ascending order of the Rocks.—A clear illustration of the
inference previously arrived at as regards the fundamental gneiss is
afforded, indeed, by the regular ascending series of rocks from the
gneiss of the Fichtelgebirge at Selb to Hof in Bavaria, as drawn by
M. Giimbel in the annexed instructive sections. One of these sec-

232

}ROLOGICAL SOCIETY. [Apr. 22,

yy
vy

PROCEEDINGS OF THI

360

Fig. 2.—Section from the Labyrinth-Berg, near Hof, to Selb (from 7 to 8 miles).

N.W. 28 : S.E.
et 3 & | a
be s ws} 2 |>| Ss
£3 345 ao Sate 3 a S 5 e
Bie Seas & 38 2 E e 3 3 3
a Re a etal ; eM g Be Be
ee bee b | 12: | | fs
3 w ° TZ. aS Eee 7) y We - VT) WGI yy, Vv Y ey
; eS De 1 Se
fed a k lm l n! (a) p q
See Fig. 3.
Fig. 3.—Detailed Section from the Laubyrinth-Berg to the Watch-tower.
Labyrinth-Berg, Limestone- Road from Hof to ' Road from Hof Watch-tower
near Hof. quarry. Hartmanreuth. Leimitz. to Gattendorf, E. of Hof.
N.W. ve ; S.E.
: ae
as / LM | ( G (| =
i g h g fe OR: b
eet, Fig. 2. a Fig. 2 (continued). Figs. 2 & 3 (continued).
. f et. , : : °
RGnoiueey <> a. Moe te 8000 i Se ieee ie ae breccia, Ae: f. Siliceous slate and lydite, full of feet.
r. Mica-schiss . . . . . . . 6,000 I eae ee | Graptolites . . . - - . 270
q. Chlorite-schist with quartz . . 3,000 Figs. 2 & 3. | é. Primordial ZONE. > ahh ease ay 60| &
p. Primary clay-slate. . . . . 9,000] 4. Diabase, tuff, and breccia. | d. Blackish-grey laminated clay- 5
1. Silurian Primordial zone. . . 50 | hk. Cypridina-limestone ... . 250 \ slate and lydite ... - ao a
o,2.Silurian . . ... . . . . 5,000] g. Greyish-whiteclay-slate, alterna- | S| ¢. Black crystalline limestone . . 180] :
m,n. Deyoulany sa ae &- 0000 ting with lydite, the upper- 4 | 3. Grey, red, and yellow clay-slate,
m. Mountain-limestone, with many most portion being the Ne- P Ee micaceous and talcose above . 950
species of Productus . . . 70 reites- and Pentamerus-beds, 3 | a. Chlorite-, hornblende-, and dio-
i @arboniferous . .9. . =. » 000 more than... « sane 0,000 rite-slate.

1863. ] MURCHISON—BAVARIA AND BOHEMIA. 361

tions, fig. 2, exhibits, in the space of about 7 or 8 miles, the
following ascending order of strata, arranged in conformable super-
position :—

Gneiss (s) resting against granite (¢), and, in this spot, near Selb,
having a superficial width of 3000 metres only, or about 10,000
English feet, though in Bohemia this thickness, as before
stated, is enormously increased. These strata of gneiss pass
upwards into

Mica-slate (7°), occupying a surface of about 20,000 feet wide, and
all at very high angles of inclination. These beds, after one
or two undulations, plunge at an angle of 45° under

Chloritic, quartzose, concretionary masses (q), which form the
natural base of the vast thickness of the great mudstone
series to which the Germans assign the name of Urthon-
Schiefer (p), and which, with the underlying chloritic beds, has
here (to the 8.E. of Rehau) a thickness of 36,000 French
feet.

It is this grand and massive accumulation of primary clay-slate
(in which no fossils have yet been found, and to which M. Giimbel
assigns, in other tracts, a thickness of about 80,000 English feet)
which, with the underlying and more metamorphosed portions of it,
may be viewed as the German equivalent of the Cambrian rocks of
North Wales, as laid down in the maps executed by my predecessor
Sir Henry De la Beche and his associates. In some places this great
series of the “roches azoiques” of Barrande is a micaceous grey-
wacke, in others it contains quartzose and even pebbly beds, and is
often charged with lead-veins in quartzose matrices. In traversing
the wide tract around the town of Mies* in Bohemia, which is
occupied by this Thon-Schiefer, I was so much struck with its re-
semblance to those ordinary Silurian mudstones, or “rotch” of
South Wales, which have been affected by an imperfect cleavage,
that I could not avoid the reflection that, if fossils are ever to be
found in the strata which underlie the Primordial Silurian zone of
Barrande, this is a tract singularly favourable for an endeavour to
find them; for I can assert that much of this Urthon-Schiefer is
less altered or crystalline than many Silurian rocks of younger
age, which are charged with fossils}. Not wishing, however, to
dogmatize on this point, or to adhere blindly to my title-page of
‘Siluria,’ in calling attention to what I still consider to be un-
assailed, “the oldest fossiliferous rocks and their foundations,” I
simply invite all those who sustain theories against facts, hitherto
uncontradicted, to travel into the region now described, and many
others to which I could refer them, and try to discover fossils in
these quasi unaltered primary strata of mudstone. If they succeed,

* This tract was described, in 1791, by Lindacher (see Barrande, Systéme
Silurien du Centre de la Bohéme, vol. i. p. 10).

+ On this head see a valuable memoir by Dr. Bigsby, “‘ On the Organic Con-
tents of the Older Metamorphic Rocks,” Kdin. New Phil. Journ., April 1863.
The author, citing well-known authorities, refers to sixty-four cases where or-
ganic remains have been observed in altered Paleozoic rocks of different countries.

362 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 22,

and detect recognizable fossils, why then my datum-line as to the
first appearance of invertebrate animals will of course be lowered,
and I shall bow, as I have always hitherto done, to paleontological
facts.

But to return to the ascending section of M.Giimbel. The summit
of the primary clay-slate, here reddish and chloritic, passes up into
quartzites, about 300 feet thick (2), containing Fucoids ; these are fol-
lowed by black siliceous roofing-slate (lydianstone or lydite), in which
fossils of the Primordial zone (1) occur, and among which M. Barrande
has detected the genera before mentioned. According to M. Bar-
rande, who examined them when I was at Prague, they consist of
Conocephali and Oleni, and also some species of Lingula, Orthis,
Discina, Pugiunculus, and fragments of Cystidew.

In answer to a recent letter from myself, M. Barrande writes as
follows :—‘ This fauna (from the environs of Hof) presents evidently
Primordial characters by the predominance and the forms of its
Trilobites, which are accompanied by a small number only of the
usual Lower Silurian genera, 7. e. Lingula and Discina, the Pteropod
Pugiunculus, and a Cystidean.

‘‘The Trilobites predominate, indeed, over the other fossils, both
in the number of species and in the relative quantity of individuals.
I recognized eight to ten species of Conocephalus and Olenus, alk
new, as well as another type which also seemed to me to be new.
With these Primordial Trilobites are also associated two or three
forms which everywhere characterize the Second Silurian fauna
(Llandeilo and Caradoc), 2. e. Calymene and Cheirurus.

«<The coexistence of these different types 1s evident, since I found
them im the same piece of rock not larger than my hand.

«‘ The occurrence of the genus Olenus, which is entirely absent in
Bohemia, and the appearances which the species of it present,
indicate that the fauna of the environs of Hof has more relation to
the English and northern zone than to the central zone of Europe.
There was, therefore, (of old) a gneissic barrier, more or less elevated,
between Bohemia and Bavaria, such as that which we now see.

“T was drawing up an interesting parallel between these two
Paleozoic basins ; but just as I was about to complete it, I was obliged
to quit Prague; and since then I have been absorbed in very dif-
ferent occupations.

“You will observe that the partial coexistence of the Primordial
and Second faunas on the frontier of Bohemia comes in very a pro-
pos to aid us in the conception of the partial coexistence of the
Second and Third faunas in Bohemia, or, in other words, of my
‘Colonies.’ ”

May I not add to this important notice of M. Barrande, that this
discovery near Hof links together, in a remarkable manner, the
lowest to the next succeeding member of the Silurian, and that this
band forms the natural base of that first great Trilobite-bearmg |
series, below which no recognizable Crustacean has yet ever been
found ? This Primordial zone is followed upwards by black siliceous
schists, 10,000 feet thick, all symmetrically and compactly arranged

1863. ] MURCHISON—BAVARIA AND BOHEMIA. 363

conformably to the slates below and to the beds above, and which,
being loaded with Graptolites, are unquestionably Silurian (0).

The Graptolite-bearing schists are next surmounted, also in perfect
conformity, by a micaceous, glossy, waved, and uneven-bedded sili-
ceous clay-slate, representing the Nereites-flags of the Thiringer-
wald. These strata, standing for a portion of the Devonian rocks (n),
and occupying a thickness of about 15,000 feet, are surmounted by
the concretionary Cypridina-limestone (7), so well known near Saal-
feld and other places in the Thiringerwald. This is the Upper
Devonian, or Clymenia-limestone, of Minster, which is characterized
by the Plants described by Richter and Unger*.

Ascending from the Cypridinz- and plant-bed, M. Gumbel assigns
a thickness of about 14,000 or 15,000 feet to the conformably
overlying schists, clay-slate, and grauwacke (1), which, containing the
Calamites transitionis and other plants of the Lower Carboniferous
group, pass regularly upwards into a zone of limestone (m) about
220 feet thick. This limestone is charged with numerous Producti,
of species well known in the Mountain-lmestone of Britain and
France, several of which were collected by Professor Sedgwick and
myself in the year 1839. This true carboniferous limestone, which
is intercalated in a great expansion of schistose ‘ grauwacke,’ was
shown by my associate and myself to have been elevated with and to
be parallel to the underlying Devonian rocks, and to be quite uncon-
formable to the horizontal, upper Coal-formations of Bohemia.

This last-mentioned great break in the geological succession
occurs in France as well as in Germany, and will be again alluded
to in the sequel.

In the remainder, or north-western part of M. Giumbel’s section,
which bringsus up to the town of Hof, we see a good example of
the dislocation and inversion to which the strata have been subjected
where they have been affected by various igneous rocks.

Here, in the detailed section across the country from the Laby-
rinth Hill, near Hof, by the village of Leimitz, to the hill of the
Watch-tower, east of Hof, as drawn by M. Giimbel (fig. 3), all the
strata are inverted. The crystalline chloritic and hornblendic rocks
(a) of the Watch-tower overlie parts of yellow, red, and grey mica-
ceous clay-slate dipping tothe S.E., and, after passing over a de-
pression occupied by alluvium, other beds of grey clay-slate, with
lydianstone and slate, lie upon black granular dolomite- limestone
(c), nearly 200 feet thick, which lies on a considerable thickness of
lydianstone and clay-slate (d). It was in the next band (e) where
M. Giimbel first found those fossils which M. Barrande pronounced
as belonging to the Primordial Silurian fauna, mingled with some
forms indicating a transition into the Second Silurian fauna of that

* See ‘Siluria,’ 2nd edit. p. 408. These plants are very peculiar; and, accord-
ing to Unger, besides forms intermediate between Ferns and Equisetace, others
seem to be the primitive forms of Cycads and Conifers. In the environs of Saal-
feld there is a most perfect and gradual transition from the Devonian Plant-beds
into the overlying strata charged with Lower Carboniferous Plants of entirely
different forms.

364 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 22,

author, or what I call the Lower Llandeilo series. This Primordial
zone is overlain by dark flinty slate and lydianstone (f), full of
Graptolites ; and in the Eichelberg these again underlie glossy clay-
slates of greenish-grey colour (g), with Nereites and Tentaculites,
Finally, the true Devonian limestones (h) (the concretionary Cy-
pridina-limestones, so well seen in the environs of Saalfeld, 7.¢. the
Clymenia-limestone of Miinster, or this younger formation) under-
he all the older Silurian series.

With this highly-inverted region around Hof I was already
acquainted in previous years. In fact, I had abandoned all idea of
eliciting the order of superposition, and of assigning to the beds their
proper places in the succession by the fossils they respectively con-
tained. My associates may therefore well imagine what great value I
attach to the investigations of M.Giimbel, who has so effectually cleared
away the remainder of the obscurity in which this tract was shrouded,
and has given to the fossiliferous deposits such clear base-lines.

The Silurian Rocks of Bohemia.—Having now described the re-
gular ascending succession of the Paleozoic rocks of Bavaria, in the
environs of Hof, as well as their inversion, let us traverse the great
region of crystalline rocks which separates them from that cele-
brated Silurian basin of Bohemia, so well described by M. Barrande
in his truly classical work.

I have already alluded to the wide extension of the so-called Ur-
thon-Schiefer, or primary clay-slate, which subtends this basin on
the west; and M. Barrande has, indeed, clearly shown how in other
parts, particularly near Przibram, the fossiliferous primary zone is
equally supported by unfossiliferous schists and grauwacke, and his
still older “‘ roches azoiques.”’

Knowing that the Austrian Surveyors had prepared, and were
about to issue, their geological maps of this region, the eastern parts
of which only I had several times visited, in company with my
friend M. Barrande, I naturally felt a great desire to see how the
lower members of his series were related to the still older rocks on
the western flank of the basin—a tract which [had never seen. I
also knew that from this western side a new railroad had been cut,
which, in proceeding from Pilsen to Prague, laid open several of
the Silurian rocks. In sending to me the new Austrian maps at
Marienbad, M. Haidinger also stated that he had requested M. Li-
pold, who had coloured the sheets in question, to meet me at Pilsen.
I had, indeed, previously made the acquaintance in London of a very
intelligent Bohemian naturalist and paleontologist, Dr. Anton Fritsch,
the Curator of the Natural History Museum at Prague, who attended
the recent International Exhibition in London, and this gentleman
(M. Barrande being then absent from Prague) agreed to meet me
at Pilsen, accompanied by M. Lipold, the Austrian Surveyor.

Aware that the subject of the “ Colonies ”’ had been so criticised
as to cause my eminent friend to bring out replies in defence of his
views, I explicitly told the gentlemen who accompanied me in my
rapid journey from Pilsen to Prague, that the subject of the ‘ Colo-
nies”’ could form no part of my observations, stating truly that,

1863. | MURCHISON—BAVARIA AND BOHEMIA. 365

from want of time, I had no power to sift the question at issue,
and I therefore resolved not to examine any one of the sections of
M. Lipold or of M. Crejci, which had been brought forward in anta-
gonism to M. Barrande. My main object, I stated, was to see how
the lower part only of the great deposit of grauwacke-slate, in parts
alum-slate, in parts flinty-slate, which overlies the Thon-Schiefer,
exhibits here and there only the Primordial fossils discovered by Bar-
rande, and how from that Primordial zone the transition into the
overlying schists, with fossils of Llandeilo age, was to be best seen.

And here I must do M. Lipold and Dr. Fritsch the justice to say,

that, far from undervaluing the original and masterly labours of M.
Barrande, they had adopted all his formations, as base-lines, though
they had assigned local names to subformations, as synonyms of his
alphabetic classification. Thus, his lowest fossiliferous or Primordial
zone of C was their Przibram beds, and so on with all the overlying
divisions. As such, indeed, they appear in the accompanying map
of the Austrian Survey, and with their references to the stages of
Barrande.
. I must also here state, that, before I left London, Mr. Salter had
come to the conclusion, from Bohemian fossils which he had ex-
amined, that the zone D’ of Barrande, or the next division above the
Primordial (C), was a true equivalent of the Llandeilo beds. Again,
from a comparison of their fossils, M. Barrande had previously
properly compared other overlying beds of his great group D with
my Caradoc sandstone. In his great work he had, however, simply
divided, as I did in my first classification, the Silurian system into
upper and lower.

In elaborating the British fossils of what was formerly called
Upper Caradoc, and particularly through the labours of Mr. Salter, it
was found, however, that an intermediate group ought to be esta-
blished, which I called Llandovery rocks, the lower member of which
had strong affinities with the Caradoc formation, whilst the upper
member was as clearly connected by its fossils with the Welsh strata.

To the possible intercalation of the Llandovery rocks in the Bo-
hemian series of Barrande I will presently advert.

I now beg to call attention to the Austrian Geological Map of the
Silurian basin of Bohemia, and of the subtending and overlying rocks,
by the Imperial Surveyors, which my old friend M. Haidinger, the
Director of that Survey, has transmitted to me. He has obligingly
attended to my request, and has had all the strata coloured on the
same principle which regulates the colouring of the Silurian rocks in
the British Survey. The only deviations from the base-colours of
dull and brighter grey and purple are where the Loess covers certain
lower tracts, or where the Upper Coal-strata are represented, as they
range unconformably over the Silurian rocks. .

In directing attention to the table of colours accompanying this
elaborate map, I must say that much closer analyses and compa-
risons of paleontologists will be required before the subordinate
parts of the Bohemian series can be placed in such exact correlation
with our British local details as is here given. In fact, I do not

366 PROCEEDINGS OF THE GEOLOGICAL socrery. [Apr. 22,

believe that a much closer analogy between the Silurian series of
Bohemia and Britain can be set up than that which M. Barrande has
established by a very good general identification of his rocks with my
Upper and Lower Silurians. And although, as before said, I think
that, in Bohemia, the Llandeilo zone can be distinguished from the
Caradoc zone, it will be impracticable so to define other details as to
say that any one bed of the Bohemian series is the equivalent of
one of our British Lower Silurian subformations.

Again, in the Upper Silurian rocks, though the limestones or
upper portion of the ‘ EK’ of Barrande are clearly identifiable with the
Wenlock limestone, it does not follow that the shale beneath it
is equal to the Wenlock shale, merely because the mineral character
of the two rocks and the order of superposition agree. Judging
from the organic remains, M. Barrande may, I think, possibly be
induced to form a new group, and unite this shale with his D’, or
next underlying bed, and thus represent our Llandovery rocks.

On this point I am disposed to be guided by the opinion of Mr.
Salter, who has taken great interest in the question of the Colonies ;
and he thus wrote, in June 1860, to Sir Charles Lyell :—* I regard at
present the Colonies, with the beds called Lower Silurian over them,
and the base of Etage E (Graptolite-bearing schists and trappean
beds), as equivalent to the Llandovery rocks, under an aspect different
from that which they present in Scandinavia and Britain.” This
view, which Mr. Salter still maintains, he strengthens by assuring
me that the fauna of the Colonies consists chiefly of about 65
species (Barrande), of which 5 are peculiar, 2 are common to D*, or
Caradoc and Wenlock, and 58 are Wenlock forms.*

In the uppermost Silurian rocks a few Ludlow types only are
mixed with many forms quite peculiar. It is therefore impracticable
to define the Bohemian subdivisions into Lower Ludlow, Aymestry
Limestone, Upper Ludlow, and Passage-beds, as attempted in the

* On this head Mr. Salter has furnished me with the range of certain striking
Bohemian genera and species, as they occur in Britain :—
BOHEMIA. BRITAIN.
_ {Cheirurus insignis . . . . . Very like the Wenlock C. bimucronatus,

2 but long known as a species in the Ca-
mA radoc of Bohemia.
)Cyphaspis . . . . . « « « The genus in England—Wenlock.
gj jlichas . . . . . «. « « « The genus in England—Wenlock.
Spherexochus mirus. . . . . Lower Silurian to Upper Silurian.
Orthoceras origmale. . . . . Upper Silurian.
, 7 species.
Cyrtoceras . . . . . . ~ « Genus in England—Upper Silurian.
Terebratula obovata. . . . . Upper Silurian.
reticularisP . . . . ~ Lower Llandovery to Upper Silurian.
Spirifer togatus . . . . . . Species not yet recognized.
Leptena euglypha . . . . . Lower Llandovery to Upper Silurian.
Cardiola, 4 species.
interrupta . . . . « + Lower Silurian ? to Upper Silurian.
Favosites Gothlandica . . . . Lower Silurian to Upper Silurian.
Graptolithus priodon . . . . Lower and Upper Silurian.
Nilsson...) 4 . . .. Lower Silurian.

Beek ig. sam aete AON: x Lower'Silurian,

1863. | MURCHISON

BAVARIA AND BOHEMIA, 367

new Austrian map, and we must be content in the meantime with
those broad divisions of Lower and Upper Silurian into which M.
Barrande divided them, with the possible establishment of a Middle
Silurian; whilst we can certainly affirm that our Lingula-flags,
Llandeilo, Caradoc, and Wenlock formations are paleontologically well
represented, with a full equivalent in time, by some fossils of the
Ludlow rocks.

The total absence of Devonian rocks in the environs of Prague
shows how very different a development of Paleozoic life took place on
this the south-eastern side of the old crystalline rocks from that
which occurred at a short distance on their north-western flank, nearer
Hof, where, as already noted, the Silurian rocks, though infinitely
less rich in fossils and containing no limestones, have still a vast
formation of clay-slate and a clear Primordial zone. From that
horizon, however, upwards, we have a marked difference. Instead
of the rich Lower and Upper Silurian, with their numerous lime-
stones and abundance of fossils, as seen in Bohemia, the system
above the Primordial zone in Bavaria is simply represented by grau-
wacke schists with Graptolites, which pass upwards into true Devo-
nian rocks with many fossils. The latter again are there surmounted
conformably, as previously shown, by Carboniferous limestones with
many Producti. There are no Upper Carboniferous strata in that
neighbourhood. In Bohemia, on the contrary, with a very full
Silurian series, there is no Devonian nor Lower Carboniferous rock,
whilst there is an abundant Upper Carboniferous deposit with coal,
the sandstones and shales of which rest quite transgressively upon
different members of the Silurian system. The differences in the
fauna and flora of the Lower and Upper Carboniferous formations,
and between which there is ‘such a manifest break throughout
Germany and France, have been ably pointed out in Saxony by
Dr. Geinitz.

Our President, Professor Ramsay, in his recent Anniversary Ad-
dress, opened out a highly interesting and important inquiry, and has
clearly shown that in britain there have been ten breaks or disloca-
tions in the older Paleozoic times. Let this inquiry be followed in
other countries. From my expefience I am led to believe that the
breaks he has enumerated as common to Britain are essentially local,
and are rarely to be paralleled even in the adjacent continent of
Europe, where the solutions of continuity are often of very different
age from those common to our land.

Thus, I have long known that the great disseverance between
Lower and Upper Carboniferous, so strongly marked all over Ger-
many and France, has apparently no existence in Britain, whilst, as
shown in the preceding consecutive section of M. Giimbel, there still
exists in Bavaria an unbroken and conformable ascending order,
from the older stratified rocks, through the Silurian and Devonian,
up into the Lower Carboniferous—a striking contrast to the Silurian
derangements in Wales, as cited by Professor Ramsay.

In the endeavour to grapple with such great questions as the
amount of time which may have occurred whilst the breaks and

368 PROCEEDINGS OF THE GEOLOGICAL society. [ Apr. 22,

overlaps of the various formations were in course of production, as
broached by Professor Ramsay, it seems to me to be still more import-
ant to draw special attention to the gradual transitions or passages
between two formations, or, in other words, from the quiet burial-
grounds of one epoch of life into those of another. For if, through
the patient accumulation of well-compared data, derived from differ-
ent and distant regions, we can ultimately succeed in showing that,
though the geological record is locally broken, yet all such gaps
in one country can be filled up by putting together the local
sequences in other and numerous tracts, we shall be in a much
fitter condition to reason upon the hypothesis suggested by Mr.
Charles Darwin, as to the probability of finding, in those enormous
deposits of former ages (which could indeed only have been formed
in very long periods), any forms of life which link on one group of
animals to another. As a stratigraphical geologist, who has con-
vinced himself that the particular break of one region is often well
filled up by the unbroken sequences of strata in another, I will only
observe, that I am acquainted with many examples of such true
physical transitions from one formation into another, in which
there is not a trace of disturbance. Thus, in addition to the ex-
amples given by M. Giimbel, I would refer to the tract near Saalfeld,
where the Upper Devonian, with its very peculiar Plants, is gradu-
ally linked on to the Lower Carboniferous, containing very different
plants.

Again, in those well-known quiet transitional deposits which
occur in Britain between the great natural divisions, the Silurian
and the Devonian *, and again between the latter and the Carbo-
niferous, it is an undoubted fact that, in ascending from the lower
to the higher beds, we ever find different genera and species of ani-
mals. On the other hand, we have never foundin such united strata
an animal representing a link between two great divisions of the
animal kingdom. Yet, if such links, which have not yet been found
in existing nature, are to be detected in the ancient crusts of the
earth, it is in such transitional unbroken bands as these that they
must be specially sought for; and as they have been very sedulously
examined without affording a tracé of the requisite evidence, I con-
tend that the geological record yields no support whatever to the
transmutation-theory, if that theory be restricted to the examination
of true natural species, and be not based on those varieties which
man has educed by his own efforts and perseverance.

2. Notice of a Section at Mocxrrer. By R. Lienrzopy, Esq.
{Communicated by J. W. Salter, Esq., F.G.S.]

A REMARKABLE section having been recently noticed in the Aymestry
Limestone at Mocktree, near Leintwardine, it may be interesting to
record a few particulars in reference to it.

* See Silurian System, 1839 (passim), Siluria, 2nd edit. p. 149 e¢ seg., and
Memoirs published in the Quarterly Journal of the Geological Society.

1863. | LIGHTBODY——-AYMESTRY LIMESTONE, 369

The section in question is in the upper quarry of Aymestry Lime-
stone, on the north side of the turnpike-road from Ludlow, and
about 12? mile from Leintwardine, on the right-hand side on enter-
ing the quarry. The rock has been cut down about thirty feet in
a perpendicular face through the Aymestry Limestone, where it
yields a few examples of Pentamerus Knightw ; the upper beds con-
sisting of what has hitherto been considered to be Upper Ludlow
rock, but which I shall presently endeavour to show ought to be
classed with the Aymestry Limestone. This upper part is composed
of thin beds, chiefly argillaceo-arenaceous, with interposed occa-
sional calcareous bands. The argillaceous limestone in the lower two-
thirds of the section (1) contains Pentamerus Knightii and Atrypa
reticularis, though not abundantly, and exhibits the characteristic
lines of honeycomb-structure peculiar to the Aymestry Limestone.
In the upper part of this rock may be seen a hollow, some ten or
twelve yards in diameter at the top, but rounded at the bottom, and
four to five feet deep; it appears to have been a channel cut through
the honeycombed beds by the action of water. This has been
again filled in with thin arenaceo-argillaceous beds (3), which are de-
posited at the bottom of it, in an inverted are, quite unconformable
to the beds on which they rest, but corresponding to the hollow of
the trough. This bent character gradually disappears, until, at some
little distance above the edges of the trough, the beds again dip
conformably, or nearly so, to the honeycombed beds, and in straight
lines, at a moderate angle towards the south-east, These beds are
here from three to four yards thick.

Section in the Aymestry Limestone at Mocktree.

1. Aymestry Limestone. 2. Fault. 3. Starfish-bed.

There appears to be an oblique fault (2), dipping south, a little to
the left of the trough, but which has been covered by the thin beds.
These thin beds, which fill the trough, though not quite so hard,
correspond very much with the Lower Ludlow beds in the Church-
Hill quarry, where the Starfish are so abundant, and contain, to-
gether with other fossils—such as Lingula lata, Ceratiocaris (two
species), Pterygotus punctatus, Entomis tuberosa, Calymene Blumen-
bachii, and Encrinurus punctatus,—one or two species of Starfish,
but only very rarely, and very indifferently preserved.

370 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 22,

To Mr. Alfred Marston, of Ludlow, is due the credit of making
the discovery of Starfish here; and he has also found them in a
similar bed, three feet thick, in a quarry about a quarter of a mile
north of this one, on the west side of the old road to Leintwardine,
but having this peculiarity—that it lies conformably on a bed full
of Pentamerus Knightii, at least nine feet thick, and is covered by
another Pentamerus-bed eighteen inches thick, so that it is unques-
tionably enveloped in the Aymestry Limestone. This neighbour-
hood is traversed by many faults, and it has been suggested that
the occurrence of these Lower Ludlow beds above the Aymestry
Limestone may be due to them and the falling over or reversal of
the beds; but in the last-mentioned case, certainly, this would not
explain the phenomena, inasmuch as the limestone-beds overlie, as
well as underlie, these beds containing Lower Ludlow fossils. In
the first-mentioned section, too, the circumstances are very peculiar;
for there is, apparently, evidence of the action of water, either sub-
aérial or, possibly, an ocean-current, which has cut through the
consolidated (but possibly not then indurated) beds of the Aymestry
Limestone previous to the cessation of the animal life of the Lower
Ludlow period ; so that, when circumstances again admitted of it, a
deposit took place, nearly similar in nature and contents to that of
the Lower Ludlow. Does it not bear some comparison with M.
Barrande’s “‘ Colonies,” only reversed in position ?

I now come to the question of classification of the beds overlying
the Aymestry Limestone. It is well known that, at the time when the
maps of the Geological Survey relating to the Ludlow district were
coloured, there was comparatively less weight than at present
attached to the paleontology of the Silurian strata in the discrimi-
nation of the beds, which was determined more by their lithological
character. We may fairly assume, I think, that the Whitcliff at
Ludlow was considered the typical section of the Upper Ludlow
rock, running downwards as it does from the Downton Sandstone,
and the Bone-bed, in apparently unbroken sequence. The surveyor
at that time, looking at the nearly identical dips of the beds there,
their lithological character, and structure of bedding,—and, more-
over, finding certain fossils, such as Chonetes lata, Rhynchonella
nucula, Goniophora cymbeformis, and Orthonota amygdalina, in both
the upper and the lower beds, very naturally believed that they were
all part of the same group, and undisturbed. A little closer exami-
nation, however, would have shown the existence of two faults, by
which a large portion of the middle of the cliff is thrown up, until
the beds originally at the bottom of it now form the capping, though
the dip is but slightly altered. Again, a closer examination of the
fossils would have shown that though some of the fossils pervade
the whole series of beds, yet that portion between the faults also con-
tains a number of other species, which I believe are never found in
the true Upper Ludlow, and others, abundantly, which are very rare
in those beds, while all belong specially to the so-called Aymestry
Limestone and the Lower Ludlow. Among the fossils belonging
to the lower formation, but found on Whitchff, I may mention

1863. | LIGHTBODY—AYMESTRY LIMESTONE. 371

Strophomena depressa, S. filosa, and Atrypa reticularis, all abun-
dantly ; Acroculia Halotis, Lingula striata, Proétus Stokesii, Eneri-
nurus punctatus, EH. variolaris, and Lichas Bucklandi. Besides
these fossils, however, the character of the rock, if closely examined,
testifies to the same effect, as it is much more calcareous than the
true Upper Ludlow beds ever are, and shows the honeycombed
structure in the joints along the bedding. This is shown also by the
whiteness left, on the central parts of the cliff, by the trickling of
water, which has given it the name of White Cliff.

The consequence of this oversight has been that the admixture of
Aymestry Limestone fossils (most of which run through the Lower
Ludlow) with the Upper Ludlow list has rendered it impossible,
where the thick calcareous beds do not intervene (as is the case
towards the west), to discriminate between the Upper Ludlow and
the Lower Ludlow, and they are consequently coloured the same on
the maps.

When we consider that all through the strata, from the top of
the Aymestry Limestone, there is a constant intercalation of cal-
eareous beds, to the bottom of the Lower Ludlow, of which the
Aymestry Limestone is only an exaggeration arising from the casual
occurrence of large beds of shells or corals in certain places,—if we
further consider the identity of a large proportion of the fossils of
the Aymestry Limestone with those of the Lower Ludlow, parti-
cularly when we find such local fossils as the Lower Ludlow Star-
fish in beds above the whole thickness of the Aymestry workable
limestone,—if we consider the impossibility of fixing upon the point
where the one formation ends and the other begins,—and, lastly,
that the Aymestry or thick limestone does not exist through large
tracts of Ludlow rocks, but only where certain fossils are very abun-
dant,—would it not seem better to discontinue the name Aymestry
Limestone as a division altogether, and to call all the beds between
the Upper Ludlow and the Wenlock simply Lower Ludlow, though
still colouring the thick calcareous beds as before ?

DONATIONS

TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From January 1st to March 31st, 1863.

I. TRANSACTIONS AND JOURNALS.

Presented by the respective Societies and Editors.

American Journal of Science and Arts. Second Series. Vol. xxxiv.
No. 102. November 1862. From Prof. B. Silliman, For. Mem. GS.

A. Winchell.—Saliferous Rocks and Salt-springs of Michigan, 307.

W. Gibbs.—Researches on the Platinum Metals, 341.

O. D. Allen.—On Cesium and Rubidium, 367.

C. Rominger.—Calamopore from the Gravel-deposits near Ann Ar-
bour, Michigan, 589.

G. J. Brush.—Triphyline at Norwich, Massachusetts, 402.

Spectrum-analysis, 403; Thallium, 409.

J. P. Lesley. —Appalachian region of Southern Virginia, 413.

J. W. Dawson.—t'ootprints of Limulus compared with the Protich-
nites of the Potsdam Sandstone, 416.

Thirty-second Meeting of the British Association, 432.

Dana’s ‘ Manual of Geology,’ noticed, 444.

. Vol. xxxv. No. 103. January 1863. From Prof.
Be sie For. Mem. GS.

A. Winchell.—Identification of the Cattskill Red Sandstone Group
with the Chemung, 61.

C. Rominger.—True nature of Pleurodictyum problematicum, 82.
D. M. Balch.—Tellurbismuth from Dahlonega, 99.

poe and Torrey.—Variety of Galena with octahedral cleavage, 126.
The Archeopteryx, 129.

J. W. Kirkby.—Species common to Carboniferous and Permian strata,
133.

Art-Union of London, Report for 1862.

DONATIONS. 373
Assurance Magazine. Vol. x. Part 6. No.50. January 1863.
Atheneum Journal. Nos. 1836-1848.

Notices of Meetings of Scientific Societies, &c.

R. Mallet.—The Harthquake-wave, 52.

J. E. Wood’s ‘Geological observations in South Australia,’ noticed,
82.

Dana’s ‘ Manual of Geology,’ noticed, 152.

Crocodile in the Red Sandstone, 155.

C. Lyell’s ‘Geological Evidences of the Antiquity of Man,’ noticed,
219.

T. H. Huxley’s ‘Evidence as to Man’s place in Nature,’ noticed, 287.

W. B. Carpenter’s and W. K, Parker and T, R. Jones’s ‘ Foraminifera,’
noticed, 417.

Batavia. Natuurkundig Tijdschrift voor Nederlandsch Indic. Deel
a. 1861.

S. Bleekrode.—Eenige woorden over de Bruinkool van Borneo, 29.

P. J. Maier.—Mineraalwater der bron Prajan, 46.

A. Pruijs van der Hoeven.— Mededeeling aangaande Mineralewaters
in de Redjang, 69.

Nagel.— Wit en zwart goudhoudend zand uit de rivier Sepoetih en
Cardamomum of Rapoerlaga uit de Lampongsche distrikten, 110.

J. L. Warnas.—T wee zandsoorten uit de rivier Sepoetih, 220.

P. J. Maier.—Mineraalwater van Manindjoe, 221.

Berlin. Zeitschrift der deutschen geol. Gesellschaft. Band xiv.
Hefte 2 & 3. February—July 1862.

Proceedings, 236-241, 533-540. Letters, 247-251, 541-550.
ee ee Datereachung des Alaunsteines und des Liwigites,
53.
eee eammsnsetzung von Magnesiaglimmer und Hornblende,
65.
H. Karsten.—Geognostische Beschaffenheit der Gebirge von Caracas,
282 (plate).
H. Eck.—Kalkstein des oberschlesischen Muschelkalks, 288.
H. Fischer.—Ueber den Pechstein und Perlstein, 312.
F. yon Richthofen.—Ueber einen Ausflug in Java, 327.
» Nummulitenformation auf Japan und den Philippinen, 357.
—. Ueber Siam und die hinterindische Halbinsel, 361.
G.vom Rath.—Geoenostisch-mineralogische Beobachtungen im Quell-
gebiete des Rheins, 369 (4 plates).
H. R. Goppert.—Ueber die in der Geschiebeformation vorkommen-
den versteinten Holzer, 551.
——. Neuere Untersuchungen iiber die Stigmaria ficoides, Brong.,
555.
C. Rammelsberg.—Ueber den letzten Ausbruch des Vesuvs vom 8
December 1861, 567.
F, Romer.—Ueber die Diluvial-Geschiebe, 575.
Pies Die Nachweisung des Keupers in Oberschlesien und Polen,
38.
G. vom Rath.—Skizzen aus dem vulkanischen Gebiete des Nieder-
rheins, 655 (plate).
Roth.— Quantitative mineralogische Zusammensetzung der krystalli-
nischen Silikatgesteine, 675,
VOL, XIX,— PART I. 2¢

374

DONATIONS.

Bologna. Nuovi Annali delle Scienze Naturali. From Dr. Bianconi.
Vol. i. (imperfect). 1838.

D. Santagata.—Sulla montagna Bolognese, 48.

G. Bertolinii—Un legno fossile delle nostre gessaie, 76.
Sgarzi.—Materia concreta delle acque della Porretta, 161.
Procaccini Ricci.—Filliti Sinigalliesi, 190 (2 plates).
Bianconi.—Sulle filliti, 345 (7 plates).

Proceedings of the Academy of Sciences of Bologna, 108, 260, 409.
Reviews, &c., 81, 1382, 281, 457.

—. s: Volo ne, 1833:

vow
.

V. Procaccini Ricci.—Sulle filliti Sinigalliesi, 15 (2 plates).

D. Santagata.—Osservazioni geologiche sulle Rocce serpentinose del
Bolognese, 81, 266 (2 plates).

F. Facchini.—Considerazioni geologico-botaniche sopra la Valle di
Fassa e di Fiemme, 241.

G. Bianconi.—Fenomeni geologici operati dal gas idrogene, 422.

Proceedings of the Academy of Sciences of Bologna, 37, 385, 448.

Reviews, &c., 80, 222, 318.

Vol. ii. 1840.

G. Bianconi.—Sui fenomeni geologici operati dal gas idrogene, 60,
115, 200, 241, 349, 421.

D, Santagata.—Serpentini del Bolognese, 81, 190.

V. Procaccini Ricci.—Corpi organici fossili da Monte Conaro di An-
cona, 337.

Proceedings of the Academy of Sciences of Bologna, 129, 215, 288,
372, 456.

Reviews, &c., 73, 153, 233, 318, 395, 401.

Vol. iv. 1840.

G. Bianconi.—Sui fenomeni geologici operati dal gas idrogene, 110,
165, 278.

V. Procaccini Ricci.—Vegetabili fossili delle colline Sinigagliesi, 127.

Agassiz.—Enumerazione dei pesci fossili d’Italia, 244, 325.

Catullo.—Lettera d’argomento geognostico, 267.

Proceedings of the Academy of Sciences of Bologna, 136, 303, 435.

Reviews, &c., 58, 81, 237, 253, 535.

Vol. v. 1841.

V. Procaccini Ricci.—Sul colore delle filliti Sinigagliesi, 265.

Proceedings of the Academy of Sciences of Bologna, 35, 124, 279,
339, 423.

Reviews, &c., 16, 78, 136, 306, 391, 439.

Vol.vi. 1841.

T. Catullo.—Lettera ad Signor Conte Salina di argomento geologico,
1G.
——. Nota intorno gli Echinidi della creta e del terreno terziario
delle provincie Venete, 176.
Sulle caverne di Costoza, 241.
Proceedings of the Academy of Sciences of Bologna, 61, 188, 212,
285, 353, 443.
Reviews, &c., 71, 126, 161, 318, 346, 422

DONATIONS. 375

Bologna. Nuovi Annali delle Scienze Naturali. Vol. vu. 1842.

G. Mamiani.—Cristalli di solfuro di piombo rinvenuti in vicinanza
di Cagli, 161.

V. Procaccini Ricci—Sui prodotti organici fossili di una parte del
Piceno, &c., 179.

G. Mamiani.—Sulla galena di Porta-Cagliesi, 281.

-——. Terreno di trasporto nella collina della Tomba presso Pesaro,
402.

V. Procaccini Ricci —Entomoliti delle gessaje Sinigagliesi, 448.

—* Proceedings of the Academy of Sciences of Bologna, 56, 152, 285, 426.
Reviews, &c., 44, 116, 168, 805, 399, 428.

Vol. vii. 1842.

G. Mamiani.—Terreno di trasporto nella collina Pesarese la Tomba,

L. Pilla.—Passegeiata geologica ad Arqua, 335.

G. Giulj.—Saggio di statistica mineralogica della Toscana, 5, 401.
Proceedings of the Academy of Sciences of Bologna, 34, 177, 300, 321.
Reviews, Notices, &c.

Vol. ix. 1843.

G. Giulj.—Statistica mineralogica della Toscana, 160, 885,

——. Sulle Breccie a cemento di ferro oligisto, 456.

G. Mamiani.—Addizione alla nota sul terreno di trasporto nella col-
lina della Tomba, 443.

Proceedings of the Academy of Sciences of Bologna, 46, 188, 417.

Reviews, Notices, &c.

—. ——. Vol.x. 1843.

G. Giulj.—Statistica mineralogica della Toscana, 47, 145, 278.

G. Sennoner.—Gita negli apennini di Piacenza, 259, 392.

G. Mamiani, della Rovere.—Vedute geognostiche sul distretto Pesa-
rese, 369.

Proceedings of the Academy of Sciences of Bologna, 80, 302.

Reviews, Notices, &c.

Caen. Bulletin de la Société Linnéenne de Normandie. Vol. vii.
Année 1861-62.

Eugéne Deslongchamps.—Formation des nodules caleaires renfermés
dans les argiles du lias supérieur de Curcy et autres localités, 231.

——. Etudes critiques sur des brachiopodes nouveaux ou peu con-
nus, 248 (8 plates).

Notes pour servir @ la géologie du Calvados, 304 (plate).

Moriére.—Empreintes de poissons des mines de Littry, 327.

Géologie d’Arromanches, 332.

——. Institut des Provinces de France. Congrés des Délégués des
Societés Savantes. Ouverture de la Session de 1863.

Calcutta. Journal of the Asiatic Society of Bengal. New Series.
No. 113. 1862, No. 4.

Canadian Journal. New Series. No. 33. May 1861.

EK. J. Chapman.—Drift-deposits of Western Canada, 221.

S. Fleming.—Davenport Gravel-drift, 247.

kK. Billings.—Devonian Fossils of Canada West, 253.
2c2

376 DONATIONS,

Canadian Journal. New Series. No. 33 (continued).

J. F. Smith.— New Species of Zriarthrus from the Utica Slate of
Whitby, Canada West, 275.

J. Hall.—Primordial Fauna and Point Levi Fossils, 284.

J. De Cew.—Geology of the Townships of Windham and Middleton,
County of Norfolk, 295.

——= se NO, 42, Noveniver tous.

——, . No. 43. February 1863.

E. J. Chapman.—Minerals and Geology of Canada; part iv., 17.
A. C. Ramsay.—Origin of Lakes, 86. :

Chemical Society. Journal. Second Series. Vol. i. Nos. 1-3.
January—March 1863.

A. H. Church.—Processes of Rock-formation now in action, 30.
——. Analysis of Red Chalk, 79.

Cherbourg, Mémoires de la Société Impériale des Sciences Naturelles
de. Vol. viii. 1861.

Daubrée.—Nature des actions métamorphiques, 52.
Bonissent.—LHssai géologique sur le département de la Manche, 57.

Christiania. Forhandlinger i Videnskabs-Selskabet i Christiania,
Aar 1861. 1862.

Kjerulf.—Om Prof. J. Esmark’s Stilling til Glacialtheorierne, 67.

Samme.—Om Labradoritfelspath fra Noritformationen paa Hitero,
177.

T. Dahll.—Om Runeskriften yed Framvaren, 247.

——. Om de fossile Hvalbeen paa ydre Flekkero ved Christiansand,
249,

Colliery Guardian. Vol. v. Nos. 105-117.

Notices of Meetings of Scientific Societies, &c.

R, Hunt.—Mines, Minerals, and Miners of the United Kingdom, 6,
28.

Ventilation of Mines, 25.

J. Goodwin.—Longwall system of getting Coals versus Pillar-and-
Stall system, 26.

Goniometer for Mine-dialling, 29.

M. Fryar.—Kstablishment of Colliery-works, 45.

peeee Smyth.—Lectures on Mining, 47, 68, 87, 107, 126, 146, 165,

6, 206.

H. Mackworth.—Ventilation of Mines, 65.

Ventilation of Mines, 85.

Scotch Granite, 95.

EK. Hull.—The formation of Coal, 105, 125,

J. Napier.—Mineral Veins, 108.

D. T. Ansted.—Tertiary Bituminous Coal in Transylvania, 125.

Coal-pits and their Dangers, 129,

G. Smith’s ‘Cassiterides,’ noticed, 147.

Coal and Salt of Michigan, 148,

J. Tennant.—Lime and Limestones, 185.

Mineral and Metallurgical Products of Italy, 185, 205.

H. Johnson.—Application of Geology to Mining, 228,

DONATIONS. StL

Critic. Vol. xxv. Nos, 632-634, January-March 1863.

Notices of Meetings of Scientific Societies, &c.
C. Lyell’s ‘ Antiquity of Man,’ noticed, 264.

Darmstadt. Notizblatt des Vereins fiir Erdkunde, &e. Folge 3.
Hefti. Nos. 9-12. 1862.
R. Ludwig.—Die Steinkohlenformation zwischen Prag und Pilsen
129, 174, 181.

Geneva. Mémoires de la Société de Physique et d'Histoire Naturelle
de Genéve. Vol. xvi. Part 2.

Geologist. Vol. vi. Nos. 61-64. January—April 1863.

Notices of Meetings of Scientific Societies, &c.

S. J. Mackie.—A€éronauts of the Solenhofen Age, 1 (plate).

C. C. Blake.—Didymodon Vauclusianum, 8.

W. Pengelly.—Age of the Dartmoor Granites, 11.

J. D. La Touche and J. W. Salter.—Formation of Limestone-bands,
20.

C. C. Blake.—Horses in the New World, 24 (plate).

R. C. Clarke.—Analysis of the Red Chalk of Hunstanton, 29.

Correspondence, 29, 92, 134.

Proceedings of Geological Societies, 31.

Notes and Queries, 35, 64, 105, 154.

Reviews, 37, 70, 119, 156.

S. J. Mackie.—Turtle-remains in the Stonesfield Slate, 41.

H. Mitchell.— Gilyptolepis in the Dura Den Sandstone, 43.

C. C. Blake.—Celts from Chiriqui, 44.

G. N. Smith.—Flint Implements in the Oyle Cave, Tenby, 47.

C. J. A. Meyer.—Age of the Blackdown Greensand, 50 (plate).

C. C. Blake.—Elephas Texianus, 56.

G. V. Du Noyer.—Bituminous Coal of the Arigna District, Counties
Roscommon and Leitrim, 81 (2 plates).

S. J. Mackie.—Parallel Roads of Glen Roy, 121 (plate).

C. C. Blake.—New Fish-jaws from the Gault at Folkestone, 133.

Institution of Civil Engineers. Abstracts. Session 1862-63, Nos.
5, 7-10, 12, 13.
J. C. Clutterbuck.—The Perennial and Flood-waters of the Upper
Thames. i
——. Minutes of Proceedings. Session 1860-61. Vol. xx.
J. Murray.—The North Sea, 314 (2 plates).

Intellectual Observer. Nos. 12-15. January—April 1863.

Notices of Meetings of Scientific Societies, &c.
H. Woodward.—The flying Lizards of the Secondary Rocks, 445.
Eosaurus Acadianus and Anthracosaurus Russelli, 226,

Linnean Society. Journal of Proceedings. Vol. vii. No. 25.

Liverpool Gallery of Inventions and Science. Second Annual Report
of the Committee, and Proceedings of the Aggregate Meeting of
the Five Societies, held on the 31st October, 1862. 1862.

378 DONATIONS.

Liverpool, Transactions of the Historic Society of Lancashire and
Cheshire. New Series. Vol. ii. Session 1861-62.

J. Newton.—Origin and History of the Human Race, 95 (2 plates).
J. Whitaker and T. T. Wilkinson.—Burnley Coal-field, 113.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xxiv. No. 164. Supplement.

R. P. Greg.—Meteorites in the British Museum, &c., 534.

Vol. xxv. Nos. 165-168. January—April 1863.

N.S. Maskelyne and V. y. Lang.—Mineralogical Notes, 39 (2 plates).

J. Ball.—Formation of Alpine Valleys and Alpine Lakes, 81.

D. Forbes.—Composition of some Chilian Minerals, 103.

R. Mallet.—Earthquake-experiments made at Holyhead, 146.

D. Brewster.—Pressure-cavities ini Topaz, Beryl, and Diamond, and
their bearing on Geological Theories, 174.

8. V. Wood.—Purbeck and Wealden Deposits of England and France,
268 (map).

Tschermak.—Pseudomorphs in the Imperial Museum of Vienna, 328,

Haidinger.—Pseudomorph of Mica after Cordierite, 324.

London Review. Vol. vi. Nos. 131-143.

Notices of Meetings of Scientific Societies, &e.
R. Mallet’s ‘Neapolitan Earthquake of 1857,’ noticed, 200.
Lyell’s ‘Antiquity of Man,’ noticed, 336.

Longman’s Monthly List. January 1, 1863.
Longman’s Notes on Books. Vol. ii. No. 32. February 28, 1863.

Manchester Geological Society. Transactions. Vol. in. 1862.

EK. W. Binney.—Down Holland Moss, 9.

EE. Hull.—Geological Maps of Lancashire, 23. :

J. Dickinson.—Cause of the Explosion at the Hetton Colliery, 39.

J. Taylor.—Geology of Castleton, 73.

E. W. Binney.—The late Mr. Elias Hall, 92.

——. Drift-deposits found about Llandudno, 97.

—.. Sgillaria and its roots, 110.

J. Taylor.—Pleistocene deposits on the Stockport and Woodley
Railway, 147.

J. Goodwin.—Ventilation of Mines, 154, 202.

A. Knowles.—Bank Top and Hagside Pits, and the proving ef Faults,
190.

J. Atkinson.—Gases met with in Coal-mines, 218.

J. Taylor.—Geology of the Railway between Hyde and Marple, 296.

J. Bradbury.—North Staffordshire Coal-field, 304,

EK. W. Binney.—Excursion to Todmorden, 325.

——. Geology of Manchester and its Neighbourhood, 350,

Vol. iv. Nos. 2-5. Session 1862-63.

Excursion to Halifax, Hipperholme, Lightcliffe, and Low Moor, 16.

J. Goodwin.—Long-wall versus Pillar-and-Stall System of getting
Coals, 28.

J. S. Bland.—Carboniferous Rocks of Shap and Crosby Ravensworth,
44

J. Taylor.—Cambrian Strata of the Isle of Man, 70.

DONATIONS. 379

Manchester Geological Society. Transactions. Vol. iv. Nos. 2-5
(continued),
T. Farrimond.—Edmond’s Main Colliery Explosion, 85.
T..T. Wilkinson.—Drift-deposits néar Burnley, 108.
Geinitz.—Dyas or Permian Formation in England, 120.

Manchester Literary and Philosophical Society. Proceedings. Ses-
sion 1862-63. No. 6.

EK. W. Binney.—Position of the Rothliegende, 35.
K. Hull.—Age of the New South Wales Coal-field, 38.

Mechanics’ Magazine. New Series. Vol.ix. Nos. 210-222.

Notices of Meetings of Scientific Societies, &c.
Howden and Thresh’s Safety-lamp, 43.

Safety-lamps for Mines, 51.

G. C. Wallich’s ‘North-Atlantic Sea-bed,’ noticed, 67.
Prevention of Accidents in Mines, 68.

California and Gold, 169.

Californian Mining in 1861, 199.

Melbourne. Transactions of the Royal Society of Victoria. Vol. v.
1860.
W. B. Clarke.—Prof. M‘Coy’s “New Teniopteris” from the Coal-
bearing Rocks of Cape Patterson, 89, 209.
EF. M‘Coy.—Defence of his “ New Teniopteris” from the Coal-bearing
Rocks of Cape Patterson, 96, 215.

Mining and Smelting Magazine. Vol. iii. Nos. 13-15. January—
March 1863.

Notices of Meetings of Scientific Societies, &c.

Abstracts and Reviews, 20, 89, 148.

Notes and Memoranda, 37, 106, 165.

D. T. Ansted.—Tertiary Bituminous Coal in Transylvania, and the
Brown Coals of the Danube, 65.

The St. Ives and Selant Tin-mining District, Cornwall, 138.

Montreal. Canadian Naturalist and Geologist. Vol. vi. No. 6.
December 1861.
J. W. Dawson.—Recent Discoveries of Gold in Nova Scotia, 417.
L. Saemann.—Unity of Geological Phenomena in the Solar System,
444,
R. I. Murchison.—New Geological Map of Scotland, 464.
J. Hall.— Receptaculites, 465.

Vol. vu. No.6. December 1862.

J. Hall. New Crustacean from the Potsdam Sandstone, 443.

T. Macfarlane.—Contributions to the History of the Acton Copper
Mine, 447.

J. Dana’s ‘Manual of Geology,’ noticed, 474.

Moscow. Bulletin de la Société Impériale des Naturalistes de Mos-
cou. Vol. xxxiv. Premiére Partie. Nos.1 &2. 1861.
H. Trautschold.—Recherches géologiques aux environs de Moscou,
64 (5 plates).
R. Hermann.—Ueber das Dianium, 156.

380 DONATIONS,

Moscow. Bulletin de la Société Impériale des Naturalistes de Mos-
cou. Vol. xxxiv. Premicre Partie. Nos. 1 & 2 (continued).

G. v. Jager—Die Sumpfschildkrote (Emys Europea) in fossilem

Zustande, 190. . :
N. B. de Marny.—Die relative Lage der Steinkohlen in Central-Russ-
land, 295.

J. Lewakowski.—Terrains tertiaire et quaternaire dans les Gouver-
nements de Kherson, d’Ekathérinoslaw, &c., 463.

A. v. Nordmann.—Zur Palaontologie Siidrusslands, 577 (2 plates).

R. Hermann.—Zusammensetzung der Kaukasischen Mineralquellen
in verschiedenen Perioden, 587.

Vol. xxxiv. Seconde Partie. No.3. 1861.

H. Trautschold.—Recherches géologiques aux environs de Moscou,
267 (plate).

—. Die Kreide-Ablagerungen im Gouvernement Moskau, 432
(plate).

E. eat a Griinsand in der Umgegend von Moskwa, 278.

R. Ludwig.— Die in der Umgebung von Lithwinsk in den Kalkstei-
nen der Steinkohlenformation vorkommenden Korallen- und Bryo-
zoen-Sticke, 579.

Munich. Sitzungsberichte der konigl. bayer. Akad. der Wissenschaf-
ten. Jahrgang 1862, Bandi. Heft 4.

—. —. Jahrgang 1862, Band u. Hefte 1 & 2.

Neuchatel. Bulletin de la Société des Sciences Naturelles de Neu-
chatel. Vol. vi. Prem. Cahier. 1862.

E. Desor.—De l’orographie des Alpes, 147 (plate).

New Zealand Government Gazette. Vol.ix. No. 18.
J. Haast.—Geology of the Province of Canterbury, 121.

Offenbach-am-Main. Dritter Bericht des Offenbacher Vereins fiir
Naturkunde. 1862.

Paris. Académie des Sciences. Comptes Rendus. 1862, Premier
Semestre. Vol. liv.

Dumont.—Faux de Paris et de Lyon, 1084.

Distribution de ]’eau dans les villes, 1182.

Poggiale et Lambert.—Analyse chimique de l’eau du puits artésien
de Passy, 1062.

A. le Play.—Origine de la chaux qui se trouve dans les plantes cul-
tivées sur les terrains primitifs du Limousin, Rapport par M. Du-
mas, 304, .

Dehérain.—Composition de quelques terres arables, 122.

Palmieri—Phénomeénes électriques dans la fumée du Vésuve pendant
Véruption du 8 Décembre 1861, 284.

Marcel de Serres.—Mines de peroxyde de fer ou limonite de l’Hérault,
1189,

De Villeneuve-Flayose.—Structure du globe terrestre, 200, 362,

Cordier.—Origine des roches de dolomie, 293.

Lecoq.—Alternance des assises calcaires et des basaltes dans le bas-
sin de la Limagne d’Auvergne, 1099,

DONATIONS. 381

Paris. Académie des Sciences. Comptes Rendus. Vol. liv. (con-
tinued).

Pissis—Produits de la vulcanicité correspondant aux différentes
époques géologiques, 192, 1185. é ;
Hébert.—Dépots tertiaires marins et lacustres des environs de Provins

(Seine-et-Marne), 513. ;

Leymerie.—Découverte de l’étage aptien aux environs d’Orthez,
683.

De Quatrefages.—Structure artificielle des buttes de Saint-Michel-
en-Lherm, 816.

Riviére.—Buttes coquilliéres de Saint-Michel-en-Lherm, 1065, 1131,

Aucapitaine.—Ile de l’Etang de Diane (Corse), 1114.

Sterry Hunt.—Chimie du globe, 11990.

Engelhardt.—Observations sur les glaces de fond; rapport sur ce tra=
vail par M. de Senarmont, 897.

Dufour.—Densité de la glace, 1079.

Léchalas.—Mouvement des eaux dans la partie maritime des fleuves,
analyse par M. Combes, 593.

Dru.—Ecoulement de l’eau dans les puits artesiens, 668.

Muller.—Nouvelle méthode de traitement direct des minerais de zine,
4017.

H. Sainte-Claire Deville et H. Debray.—Métallurgie du platine, 1189.

H. Sainte-Claire Deville.—Production artificielle de la levyne, 324.

Fournet.—Arséniate de cuivre plombifére de Diou, 1096.

Pisani.—Pseudomorphose de pyroxéne du lac Inférieur, 51.

Rastolite de Monroe (Etat de New York), 621, 686.

Phipson.—Sombrérite (nouveau minéral provenant de Vile de Som-
brero, petites Antilles), 1129.

Marcel de Serres.—Sulfate de baryte hydraté des eaux minérales de
La Malou, 764.

Dumas.—Formation du limon du Nil et la constitution des lacs a
natron, d’aprés les observations de M. Méhédin et les analyses de
M. Willm, 1220.

Daubrée.—Echantillon d’or natif cristallisé de Californie, 578.

Valenciennes.—Le bras d’un Plésiosaure de l’argile de Kimmeridge,
au pied du cap de la Héve, 628.

——. Une machoire inférieure de Dauphin fossile envoyée par M.
Thore, 788.

Gervais.—Les ossements d’un trés-grand Lophiodon trouvé a Bra-
connac, prés Lautrec, 820.

Examen d’un ornitholithe d’Armissan, 895.

Gaudry.—Résultats des fouilles exécutées en Gréce sous les auspices
de Académie: Oiseaux et Reptiles, 502.

Les Singes fossiles de Gréce, 1112.

Pidancet et Chopard.—Un saurien gigantesque, le Dimodosaurus
Poligmensis de marnes irisées de Poligny (Jura), 1259.

Scipion Gras.—L’insuffisance des preuves tirées du gisement de silex
travaillés de Saint-Acheul pour faire admettre l’existence de
Vhomme pendant la période quaternaire, 1126.

Despine.—Découverte d’habitations lacustres dans le lac du Bourget,
1160.

Marcel de Serres.—Présence du sulfate de plomb dans les mines de
sulfure de plomb de Kef-oum-Theboul, en Algérie, 743.

Gaudin.—Ktablissement de puits artésiens d’un grand diamétre, 445,

De Commines de Marsilly.—Les chances de succés que présente le
forage de puits artésiens 4 Amiens et dans le département de la
Somme, 849,

382 DONATIONS.

Paris. Académie des Sciences. Comptes Rendus. Vol. liv. (con-
tinued).

Prost.—Trépidations du sol & Nice pendant l’éruption du Vésuve,
511, 1198.

Palmieri.—Secousses de tremblement de terre ressenties & l’observa-
poe du Vésuve pendant les mois de décembre 1861 et janvier 1862,

8.

Schmidt.—Grand tremblement de terre qui a eu lieu en Gréce le 26
décembre 1861, 669.

Perrey.—Léger tremblement de terre ressenti 4 Dijon, et dans les
départements voisins le 17 avril 1862, 923.

Ch. Sainte-Claire Deville—Phénoménes éruptifs de l’Italie méridio-
nale, 99, 241, 328, 473, 528.

Maugeto-Pacnomings consécutifs de la derniére éruption du Vésuyve,
926.

Meyer et d’Eichtal.—Tumuli des anciens habitants de la Sibérie:
analyse par M. Rayer, 559.

—. 1 ——. ——. Vol.lv. Nos. 12-26. 1862.
—. ——. —. Vol.lvi. Nos. 1-4. 1863.
——. Annales des Mines. 6™¢ Série. Vol. u. Liv. 4,5. 1862.

Domeyko.—Amalgames natifs trouvés au Chili, 123.

A. Bernard.—Exécution des terrassements de la ligne de Busigny a
Somain, 273 (6 plates).

Descloizeaux.—Action de la chaleur sur quelques propriétés optiques
de plusieurs corps cristallisés, 327.

. Forme cristalline et les propriétés optiques de la tephroite,

339.

Bulletin de la Société Géologique de France. 2™¢ Série.
Vol. xviii. feuill. 46-68. 1862.

J. Barrande.—Assentiment du professeur J. Hall, et nouveaux docu-
ments au sujet de la faune primordiale d’Amérique, 721.

J. Marcou.—Liste additionnelle des fossiles du terrain taconique de
PAmérique du Nord, 746.

Gosselet.—Sur la découverte de fossiles siluriens 4 Gembloux, 752.

J. Barrande.—Existence de la faune seconde silurienne en Belgique,
fol.

H. Lecoq.—Sur la carte géologique du Puy-de-Dome, 762.

Zienkowicz.—Sur le forage d’un puits artésien & Mestre, prés de
Venise, 775.

De Hauslab.—Comparaison géographique, orographique et géologique
de la surface terrestre avec celle de la partie visible de la lune, 778.

Th. Ebray.—Stratigraphie de la craie moyenne de la vallée du Cher
et de la vallée de l’Indre, 789.

G. de Mortillet.—Origine des sources sulfureuses de la Savoie, 802.

H. Le Hon.—Terrains tertiaires de Bruxelles, 804 (plate).

E. Dumortier.—Coup d’ceil sur l’oolithe inférieure du Var, 839.

G. de Mortillet.—Terrains du versant italien des Alpes, comparés a
ceux du versant frangais, 849.

P. Dalimier.—Sur les terrains primaires des environs de Falaise
(Calvados), 907.

D’Omalius d’Halloy.—Sur une nouvelle édition de ’Abrégé de géo-
logie, 917.

DONATIONS. 383

Paris. Bulletin de la Société Géologique de France. 2™¢ Série.
Vol. xviii. feuill. 46-68 (continued).

J. Barrande.—Réponse a M. d’Omalius, au sujet des fossiles siluriens
de la Belgique, 923.

A. Favre.—Sur la présence en Savoie de la ligne anticlinale de la
mollasse qui traverse la Suisse et une partie de la Baviére, 928.
Ed. Jannettaz.—Observation de quelques feuilles dans les marnes du
gypse des buttes Chaumont, 932.

A. de Quatrefages.—Sur V’origine artificielle des amas de coquilles
connus sous le nom de Saint-Michel-en-Lherm (Vendée), 933
(plate).

Ba Pictte-—La partie inférieure du terrain crétacé dans l’Aisne et
dans la région occidentale des Ardennes, 946.

Th. Davidson.—Brachiopodes fossiles des iles Britanniques, 950,

Paul Gervais.—Sur le dépét lacustre d’Armissan (Aude), 969.

J. Cornuel.—Essai sur les rapports qui existent entre le grés vert
inférieur du pays de Bray et celui du 8.-E. et du N.-O. du bassin
anglo-frangais, 975.

L. Saemann et A. Guyerdet.—Expériences sur la formation du sul-
fate de magnésie (epsomite) aux environs de Saint-Jean-de-Mau-
rienne (Savoie), 995.

co et Th. Ebray.—Carte géologique du département de la Niévre,

001.

Deshayes.—Sur la Monographie des céphalopodes de la craie supé-
rieure du duché de Limbourg, par M. de Binkhorst, 1002.

J. Barrande.—Sur l’ouvrage de M. Geinitz, intitulé: ‘Dyas,’ 1003.

Albert Gaudry.—Sur le Singe fossile de Gréce, 1022.

L. Saemann.—Observations sur Belemnites quadratus, 1025 (plate).

Th. Ebray.—Sur la minette du Morvan, 1029.

G. Guiscardi.—Sur le Spherulites Tenoreana, 1031.

Tournouér.—Note stratigraphique et paléontologique sur les faluns
du département de la Gironde, 1035 (plate).

——. Congrés Archéologique de France. Session xxviii.

Parthenon. Vol. u. Nos. 36-48.
Notices of Meetings of Scientific Societies, &c.
R. Mallet’s ‘Great Neapolitan Earthquake of 1857, &c.,’ noticed, 18.
C. Lyell’s ‘Geological Evidences of the Antiquity of Man,’ noticed,
194, 233.
PH: "Huxley’s ‘Man’s place in Nature,’ noticed, 261.
Dana’s ‘ Manual of Geology,’ noticed, 369.

Philadelphia. Proceedings of the American Philosophical Society.
Vol. ix. Nos. 67 & 68. January—December 1862.

Lesley.—The Coal-formation of the Alleghany Mountains, 30.
Section of the Coal-measures at Sydney, C. B., 92.

Photographic Journal. Nos. 129-131. January-March 1863.

s

Quarterly Journal of Microscopical Science. New Series. No. 9.
January 1863.

Reader. Nos. 1-18.

Notices of Meetings of Scientific Societies, &e.
Science during the past year, 19. -

384 DONATIONS,

Reader. Nos. 1-13 (continued).

J. D. Dana’s ‘Manual of Geology,’ noticed, 45.
C. Lyell’s ‘ Antiquity of Man,’ noticed, 185, 211.
Inundation of the Nile, 221.

Royal College of Physicians. List of Fellows, &c., for 1862.

Royal Dublin Society. Journal. Nos. 26-28. July 1862 to
January 1863.
A. Leith Adams.—Fossiliferous Caves of Malta, 11 (2 plates).

Royal Geographical Society. Proceedings. Vol. vii. No.1. 1863.
J. Kent.—Physical geography of Australia, 42.

Royal Horticultural Society. Proceedings. Vol.u. No. 12. De-
cember 1862.

—. ——. Vol.ii. Nos. 1-4. January-April 1863.

Royal Institution of Great Britain. List of Members, Officers, &c.,
for 1861. 1862.

——. Notices of the Proceedings. Part 12. 1861-62.

W. Hopkins.—The Theories of the Motion of Glaciers, 410.
T. H. Huxley.—Fossil Remains of Man, 420.
W. W. Smyth.—Coal, 510.

Royal Society. List of Fellows. December 1862.

—. Philosophical Transactions. Vol. cli. Part 3, for 1861.
1862.
R. Mallet.—Transit-velocity of Earthquake-waves, 655 (4 plates).

—, Vol. clu. 1862.
R. Owen.—The Dicynodont Reptiha, and Rhynchosaurus, 455 (7
plates).
——. Proceedings. Vol. xu. Nos. 53 & 54.

R. Owen.—Archeopteryx macrurus, 272.
T. H. Huxley.—New specimen of Glyptodon, 316.

Sculptor’s Journal. Nos. 1-3. January-March 1863.
Society of Arts. Journal. Index to vols. 1x. 1863.

Vol. x1. No. 528-540.

Notices of Meetings of Scientific Societies, &e.
Mr. Hunt’s paper on Mines, 124, 138, 152.

———
e

Tyneside Naturalists’ Field-club. Vol. v. Part 4. 1863.

W. Featherstonhaugh.—Geological Features of the Parish of Ed-
mondbyers, 310,

DONATIONS. 385

Vienna. Sitzungsberichte der kais. Akademie der Wissenschaften.
Math.-Nat. Classe. Vol. xlv. Erste Abtheilung. Hefte 3-5.
March—May 1862.

C. W. Giimbel.—Die Dachsteinbivalve (Megalodon triqueter) und ihre
alpinen Verwandten, 325 (7 plates).

Von Zepharovich.—Ueber die Krystallformen des Epidot, 381
(plate).

BT Fousimit 431 (7 plates).

Kner.—Die fossile Fische Oesterreichs, 485 (2 plates).

Von Zepharovich.—Krystallformen des unterschwefligsauren Kalkes,
499 (3 plates).

1862.

W. Haidinger.—Der Meteorsteinfall im Gorukpur-Districte in Ober-
Bengalen, am 12 Mai 1861, 665.

——. Das Eisen yon Kurrukpur nicht meteorischen Ursprungs, 672.

——. Stannern: ein zweiter Meteorstein, 790 (plate).

; : . Vol. xlvi. Zweite Abtheilung. Hefte1 & 2.
June and July 1862.

A. Boué.—Entdeckung einiger Leithakalk-Petrefacten in den ober-
sten Schichten der Kalkdolomit-Breccien Gainfahrns, 41.
W. Haidinger.—Das Meteoreisen von Sarepta, 286 (6 plates).

Vol.xlv. Zweite Abtheilung. Heft 5 May

ee

II, PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 38rd Series. Vol. xi.
Nos. 61-64. January—April 1863.

J. B. Jukes’s ‘Student’s Manual of Geology,’ noticed, 51.

E. Hull’s ‘ Coal-fields of Great Britain,’ noticed, 53.

R. Walker.—Fossil fishes of Dura Den, 93 (plate).

W. H. Baily.—Coal-measure Crustacea, 107 (plate).

R. Owen.—Archeopteryx macrurus, 122.

T. H. Huxley.—New species of Glyptodon, 123.

J. Leidy.—Pliocene Fossil Fauna of the Niobrara River, in Nebraska,
148.

J. E. Woods’s ‘Geological Observations in South Australia,’ noticed,
294,

Bronn und Leonhard’s Neues Jahrbuch fiir Min., Geog., Geol., und
Petrefaktenkunde. Jahrgang 1862, Hefte 6-8.

B. v. Cotta.—Ueber Gesteine und deren Entstehung, 641.

F, Scharffi—Der kohlensaure Kalk: I[J. Rhomboéder und Scale-
noéder, 684 (3 plates).

F, J. und T. Wurtemberger.—Verzeichniss von fossilen Pflanzen-
Resten aus den Tertiir-Gebilden des Klettgaues, 719.

C. W. C. Fuchs.—Der Granit des Harzes und seine Nebengesteine,
769, 929 (plate).

H: a Bronn.—Das Blatt einer Dattel-Palme aus Mollasse-Mergel,
860.

A. Streng.—Ueber den Gabbro und den sogenannten Schillerfels des
Harzes. Zweite Abtheilung: Gabbro, 933.

Letters; Notices of Books, Minerals, Geology, Fossils.

386 DONATIONS.

Edinburgh New Philosophical Journal. New Series. Nos. 33 & 34.
Vol. xvii. Nos. 1 & 2. January and April 1863.
C. Daubeny.—Recent Eruption of Vesuvius, in December 1861, 1.
R. Edmonds.—Buried Church in the Sands of Gwithian in Cornwall,

14,

J. A. Smith.—Meteoric Iron found in the village of Newstead, Rox-
burghshire, 67.

M. Thomson.—Analysis of Meteorite described by Dr. Smith, 69.

H. Worms’s ‘ Earth and its Mechanism,’ noticed, 104.

Montgomerie.—Glaciers in Turkistan, 157.

W. Theobald.—Celts from Bundelkund, 158.

A. Leith Adams.—Paleontology of Malta, 161.

J. J. Bigsby.—Organic Contents of the Older Metamorphic Rocks,

7k

W. Lauder Lindsay.—Geology of Otago, 280.

R. B. Watson.—Geology of Liineberg, Hanover, 305.

A. Taylor.—Bituminous Shales of Linlithgowshire and Edinburgh-
shire, 312.

Remains of Vertebrate Animals provided with Feathers in a deposit
of Jurassic Age, 326.

Leonhard und Geinitz’s Neues Jahrbuch fiir Mineralogie, Geologie,
und Paliontologie. Jahrgang 1863. Heft 1.

C. F. Naumann.—Ueber die Miinchberger Gneiss-Bildung, 1.

B. v. Cotta.—Alter der granitischen Gesteine von Predazzo und yon
Monzon in Tyrol, 16 (plate).

H. Vogelsang.—Zur Theorie der Gang-Bildungen, 30.

Letters; Notices of Books, Minerals, Geology, Fossils.

LInstitut. Te Section. 30° Année. Nos. 1508-1520.
——, II° Section. 28° Année. Nos. 323 & 325.

Natural History Review. Vol.i. 1861.
J. Lubbock.—The Kjokkenmoddings, 489 (plate).

——. Vol.u. 1862.

J. Lubbock.—Lake-habitations of Switzerland, 26.
E. Lartet.—Co-existence of Man with the Great Fossil Mammals, 53.

J. Lubbock.—Antiquity of Man, 244 (plate).
——. Vol.ii. No.9. January 1863.

J. Lubbock.—North-American Archeology, 1.
H. Falconer.—LElephas Columbi, 45 (2 plates).

Paleontographica, herausgegeben von H. von Meyer. Band x.
Lief. 5. January 1863.
H. v. Meyer.—Der Schiidel des Belodon aus dem Stubensandstein
des oberen Keupers, 227 (5 plates).
—— Supplement-Band. Lief. 2, 3. December 1862.
A. Hellmann.—Die Petrefacten Thiiringens, 11 (9 plates).

DONATIONS. 387

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.

Aldis, C. J. B. General Report on the Sanitary Condition of the
Belgrave sub-district, parish of St.{George, Hanover Square, and
on the qualities of the waters used therein. 2nd edition. 1857.
From W. Whitaker, Esq., F.GS.

Annales Hydrographiques, recueil d’avis, instructions, documents et
mémoires relatifs 4 ’Hydrographie et a la Navigation. 2° tri-
mestre de 1862. 1862.

——. 3° trimestre de 1862. 1862.

——. Vol. xxi. Année 1862 (Index). 1862. From the Dépét de
la Marine.

Annuaire des Marées des Cotes de France pour l’an 1864, par M.
Gaussin et M. E. Ploix. 1862. From the Dépét de la Marine.

Anon. Unity of System. No. 2.

Archiac, A. d’. Histoire des Progrés de la Géologie de 1834 4 1859.
Tome Huitiéme. Formation triasique. 1860.

Baily, W. H. Remarks on some Coal-measure Crustacea belonging
to the genus Belinurus, Konig. With descriptions of two new
species from Queen’s County, Ireland. 1863.

Bathoe, C. Observations on Professor Tyndall’s paper on the
“Conformation of the Alps.” 1862.

Bianconi, G. G. Alcune ricerche sui Capreoli delle Cucurbitacee.
1855.

Del Calore prodotto per l’attrito fra fluidi e solidi in rapporto
colle sorgenti termali e cogli aeroliti. 1862.

. Dello Apyorms maximus menzionato da Marco Polo e da Fra
Mauro. 1862.

Descrizione delle Forme Cristalline di Zolfo delle Miniere del
Cesenate. 1861.

Se il mare abbia in tempi antichi oceupato le pianure ed 1
colli d’Italia, di Grecia, dell’ Asia Minore ec. e del terreno marino
detto marna bleu subapennina. 1844.

Storia naturale dei terreni ardenti, dei vulcani fangosi, delle
sorgenti infiammabili, dei pozzi idropirici, e di altri fenomeni geo-
logici operati dal gas idrogene e della origine di esso gas. 1840.

Sul sistema vascolare delle foglie considerato come carattere
distintivo per la determinazione delle filliti. 1838.

388 DONATIONS.

Blanford, H. F. Memoirs of the Geological Survey of India. Vol.
iv. Part i. On the Cretaceous and other Rocks of the South
Arcot and Trichinopoly Districts, Madras. 1862. From Dr. T.
Oldham, F.GS.

Capello, De B. Guide pour l’usage des cartes des vents et des cou-
rants du Golfe de Guinée. Traduit du Portugais par MM. West
et A. le Gras. 1862. From the Dépét de la Marine.

Catalogue Annuel de la Librairie Francaise publie, par C. Reinwald.
Cinquiéme année, 1862. 1863. From M. C. Reinwald.

Catalogue of the Maps and Plans and other Publications of the
Ordnance Survey of England and Wales to 31st December 1862.
1862. From the Secretary of State for War.

Scotland. 1863. From the Secretary of State for War.
Ireland. 1862. From the Secretary of State for War.

Catalogue. Repertorio Italiano per la storia naturale. Repertorium
Italicum complectens Zoologiam, Mineralogiam, Geologiam, et
Paleontologiam, cura J. J. Bianconi. Anno 1854, Voli. 1854.
From Prof. G. G. Biancon.

Dana, J. D. Manual of Geology: treating of the principles of the
science with special reference to American geological history.
1863.

——. On the Higher Subdivisions in the Classification of Mammals,
1863.

Daubeny, C. Remarks on the Recent Eruption of Vesuvius in
December 1861. 1863.

Dawson, J. W. Zoological Classification ; or Coelenterata and Pro-
tozoa versus Radiata. 1863.

Desmoulins. Renseignements Hydrographiques et Statistiques sur
la cote de Syrie. 1862. From the Dépéot de la Marine.

Desormeaux, et P. Gervais. Description d’un Foetus Humain Mon-
strueux devant former un genre 4 part sous le nom de Pseudacé-
phale, 1860. From M. Paul Gervais.

Du Noyer, G. V. On the Bituminous Coal of the Arigna District,
counties of Roscommon and Leitrim. 1863.

Emmons, KE. Natural History of New York. Vol. v. Agriculture
of New York, comprising an account of the classification, compo-
sition, and distribution of the soils and rocks, &c. 1854. From
the Legislature of the State of New York.

Favre, A. Explication de la Carte Géologique des parties de la
Savoie, du Piémont et de la Suisse yoisines du Mont Blane. 1862.

DONATIONS. 389
Gastaldi, B. Nuovi cenni sug oggetti di alta antichita trovati nelle
Torbiere e nelle Marniere dell’ Italia. 1862.

Gervais, P. Additions aux recherches sur les Mammiféres Fossiles
de ’ Amérique méridionale. 1856.

——. De la comparaison des membres chez les animaux vertébrés.
1853.

Description de lV Aphelosaurus Lutevensis, saurien fossile des
schistes permiens de Lodeéve.

Description de quelques ossements fossiles de Phoques et de
Cétacés.

——. Documents Zoologiques pour servir 4 la monographie des
Cheiroptéres Sud-Ameéricains.

Liste des Ouvrages et Mémoires de Zoologie et d’Anatomie
Comparée publiés par M. Paul Gervais. 1852.

——. Notice sur les travaux de Paléontologie publiés par M. Paul
Gervais. 1857.

——. Notice sur les travaux de Zoologie, d’Anatomie comparée et
de Paléontologie publiés par M. Paul Gervais. 1861.

——, Notice sur M. Marcel de Serres.

Recherches sur les Mammiféres Fossiles de ’ Amérique Méri-
dionale.

Sur différentes espéces de Vertébrés Fossiles observées pour
la plupart dans le midi de la France.

——. Sur les debris fossiles de Mastodonte et d’Elephas Africanus
découverts en Algérie.

——. Sur quelques Entozoaires Teenioides et Hydatides.

——. Sur quelques points de la Morphologie générale des animaux.

Sur une nouvelle espece d’Hipparion découverte auprés de
Perpignan.

Grant, R. E. Swiney Lectures on Geology. Syllabus of a course
of twelve lectures on Palzozoology, or the Natural History of
Extinct Animals. 1855. From W. Whitaker, Esq., F.G.S.

Haast, J. Anniversary Address delivered at the Philosophical In-
stitute of Canterbury, New Zealand.

Hall, J. Natural History of New York. Part 6. Paleontology:
Vol. ii., containing descriptions and figures of the organic remains
of the Lower Helderberg Group and the Oriskany Sandstone.
1855-59. Text and plates. 1859.

VOL, XIX,—PART I, 2D

390 DONATIONS. .

Hartmann, C. Handworterbuch der Mineralogie, Berg-, Hutten-
und Salz-Werkskunde, nebst der franzésischen Synonymie und
einem franzdsischen Register. 2 vols. 1825. From Sir C. Lyell,
V.E.GS.

Hartung, G. Betrachtungen iiber Erhebungskrater altere und neuere
Eruptionmassen, nebst einer Schilderung der geologischen Verhalt-
nisse der Insel Gran Canaria. 1862. From Sir C. Lyell, V.P.G.S.

Hiortdahl, T. og M. Irgens. Geologiske undersogelser 1 Bergens
Omegn. 1862.

Horsburgh, J. Instructions Nautiques. II° Partie. Traduction de
MM. le Prédour, Darondeau, et Reille. 3° édition, revue sur la
septiéme édition anglaise, par Ch. Pigeard. 1862. From the
Dépot de la Marine.

Hunt, E. B. On the Origin, Growth, Substructure, and Chronology
of the Florida Reef. 1863.

Hunt, J. Introductory Address on the Study of Anthropology,
delivered before the Anthropological Society of London, February
24th, 1863. 1863. From C. Carter Blake, Esq., F.GS.

Hunt, R. On the Mines, Minerals, and Miners of the United
Kingdom. 1862. From Prof. J. Tennant, P.GS.

Kerhallet, C. P. de. Manuel de la Navigation dans la mer des
Antilles et dans le Golfe du Mexique. Premiére Partie. 2™°
édition. 1862. From the Dépéot de la Marine.

kKjerulf, T. Beskrivelse over Jordbunden i Ringeriget. 1862.
——. Ueber das Friktions-Phinomen. 1860.

Zusammenstellung der bisherigen Ergebnisse der geologis-
chen Untersuchung Norwegens. 1862.

Kner, R., und F. Steindachner. Neue Beitrige zur Kenntniss der
fossilen Fische Oesterreichs. 1863.

Koninck, L. de. De Vinfluence de la Chimie sur les progrés de l’In-
dustrie. 1863,

Krettmayr, J. Erstes Verzeichniss der Gypsabgiisse. 1862.

Langle, F.de. Campagne de la Cordeliére, études sur l’océan Indien.
1862. From the Dépét de la Marine.

Lesley, J. P. Section of Coal-measures at Sydney, Cape Breton
Coast. 1862.

Lubbock, J. North-American Archeology. (Review). 1863.

Lyell, C. The Geological Evidences of the Antiquity of Man, with
remarks on theories of the origin of species by variation. 1863.

DONATIONS. 391

Magnetical and Meteorological Observations made at the Government
Observatory, Bombay, in the year 1860, under the superintendence
of Lieut. E. F. T. Fergusson and Lieut. P. W. Mitcheson. 1861.
From the Secretary of State for India.

Mouchez, E. Nouveau Manuel de la Navigation dans le Rio de la
Plata. 1862. From the Dépét de la Marine.

Murchison, R. I., and A. Geikie. First sketch of a new geological
map of Scotland, with explanatory notes. 1861.

Oldham, T., and J. Morris. Memoirs of the Geological Survey of
India. Paleontologica Indica. II. The Fossil Flora of the Raj-
mahal Series, Rajmahal Hills, Bengal. Parts 1, 2, and 3. 1862.
From Dr. T. Oldham, F.G.S., Director of the Geological Survey of
India.

O'Riley, H. <A brief notice of the Tenasserim Provinces, in relation
to their commercial and political importance. 1862.

Otter, H. C., et M. W. Stanton. Instructions Nautiques sur le
Sound de Harris et le petit Minch. Traduit de l’Anglais par A.
le Gras. 1862. From the Dépot de la Marine.

Poey, A. ‘Table Chronologique de quatre cents Cyclones qui ont
sévi dans les Indes Occidentales et dans l’Océan Atlantique Nord,
pendant un intervalle de 362 années (depuis 1493 jusqu’en 1855).
1862. From the Dépot de la Marine.

Rapport sur les travaux de la Faculté des Sciences de Montpellier
pendant l’année scolaire 1861-62. 1862. From M. Paul Gervais.

Recherches Chronométriques. VI° Cahier. 1862. From the Dépét
de la Marine.

Reinecke. Description Hydrographique des cétes septentrionales de
la Russie. Deuxiéme Partie. Céte de la Laponie. Traduction
du russe par H. de la Planche. 1862. From the Dépét de la
Marine.

Report. Annual Report of the Geological Survey of India, and of
the Museum of Geology. For the year 1861-62. 1862. From
Dr. T. Oldham, F.G.S., Director.

Fifteenth Annual Report of the Regents of the University of
the State of New York, on the Condition of the State Cabinet of
Natural History, and the Historical and Antiquarian Collections
annexed thereto. 1862. From the Regents of the University of
the State of New York.

——. Forty-fourth Annual Report of the Trustees of the New
York State Library. 1862. From the Trustees of the New York
State Library.

International Exhibition, 1862. Class XXXI. By A.
Tylor, Esq., F.G.S. 1862. From A. Tylor, Esq., F.GS.
2D 2

392 DONATIONS,

Report of the chief Gold-commissioner for the Province of Nova
Scotia, for the year 1862. 1863. From the Rev. D. Honeyman,
F.GS.

Sandberger, F. Die Conchylien des Mainzer Tertiirbeckens.
Schlussheft. Text: Bogen 35-59. 1863.

Sars, M. Beskrivelse over Lophogaster typicus en meerkveerdig Form
af de Lavere tifoddeve Krebsdyr. 1862.

Saussure, H. de. Coup d’ceil sur ’Hydrologie du Mexique, princi-
palement de la partie orientale, accompagné de quelques observa-
tions sur la nature physique de ce pays. 1862. From Sir C.
Lyell, V.P.GS.

Nécrologie de M. Louis Necker. 1861. From Sir C. Lyell,
V 2P GES:

Sharswood, W. Catalogue of the Localities of the Mineralogical
species Allanite. 1861.

——. Catalogue of the Minerals containing Cerium. 1861.

Stoppan, A. Supplément a l’Essai sur les Conditions générales des
Couches & Avicula contorta. 1863.

Studer, B, Geschichte der physischen Geographie der Schweiz.
1863,

——. Observations Géologiques dans les Alpes du Lac de Thoune.
1862.

Switzerland. Societé Helvétique des Sciences Naturelles. Matéri-
aux pour la Carte Géologique de la Suisse. Premiére Livraison :
Geognostische Skizze des Kantons Basel, von Dr. Alb. Muller.
1862. From Prof. B. Studer, For. Mem. GS.

Turgan. La foudre filature de coton de M. Pouyer-Quertier. (Ex-
trait des Grandes Usines de France). 1863.

Les Grandes Usines de France. Boulangerie Centrale de
Vassistance publique de la Seine. 1863.

Zittel, K. A, Die obere Nummulitenformation in Ungarn. 1863.

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

May 6, 1863.

William Whitaker Collins, Esq., M.I.C.E., 15 Buckingham Street,
Adelphi; Charles Carter Blake, Esq., Honorary Secretary of the
Anthropological Society, 1 Mabledon Place, W.C.; and John Martin,
Esq., Cambridge House, Portsmouth, and Keydell, Shorndean, Hants,
were elected Fellows.

M. F.-J. Pictet, Professor of Zoology and Comparative Anatomy
in the Academy of Geneva; Signor Q. Sella, Member of the Italian
Parliament, Turin; Herr Credner, Koniglicher Bergmeister of
Gotha; Dr. J. J. Kaup, Conservator of the Museum of Darmstadt ;
Signor G. Meneghini, Professor of Paleontology in the University of
Pisa ; Signor B. Gastaldi, of Turin; and M. A. Morlot, of Berne,
were elected Foreign Correspondents.

The following communications were read :—

1. On the Bricx-prr at Lexpen, near CoucHesteR. By the Rev.
O. Fisuer, M.A., F.G.S. With Nores on the CoLEorrera; by
T. V. Woxtaston, Esq., M.A., F.L.S.

Description of the Strata.—The Brick-pit at Lexden is situated on a

plateau upon the south side of the valley of the Colne, about a mile

west of Colchester. The table-land around Colchester, elevated some-

what more than a hundred feet above the level of the sea, upon the
VOL. XIX.—PART I. 25

394 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

south side of the Colne, consists of thick beds of gravel and sand resting
upon London Clay. This gravel is for the most part well rolled, and
its stratification is very regular. Its upper and lower portions are
stony, while the middle consists principally of false-bedded strata of
sand. Fine sections are exposed by the drainage-works now going
on at the new cavalry-barracks at Colchester, and in pits in the
suburbs. The lowest bed, resting on the London Clay, is a coarse
gravel, well seen at Wivenhoe ballast-pit.

I believe this extensive bed of gravel to be the old gravel which
elsewhere underlies the Boulder-clay. It crops out towards the
southern part of Essex, ranging from Danbury, where it attains
a considerable elevation, by Tiptree Heath to Colchester. It is seen
near the railway-station at Hadleigh in Suffolk, and in the same
county forms an extensive heath near Dunwich.

There is an excavation in the lower portion of this gravel, in the
corner of Lexden Brick-pit, close to the kiln, where the following
section is exposed :—

Section in the Brick-pit at Lewden.

ft. in.

L.. Gravelly sand, about. Sa sicol ere Te, 0
9 oon te dltchend oped alt ds PTAs EAE Ops GA Aa ae 20 0
* | Loamy sand with dark staims ............ O65

3. Coarse gravel with water, not pierced.

The latter is doubtless the lowest member of the deposit, resting
upon the London Clay.

The newer deposits of the Brick-field appear to rest upon a shelf of
the London Clay, and to abut against the old gravel above described.
The clay which, under the local name of “ Strong Clay,” is dug at the
north-west corner of the field seems to be the London Clay (a in
section, p. 395). There it has been excavated to the depth of about
12 feet; and at the lowest point ever reached pyrites are said to
have been found, and to have been pronounced by the late Mr. J.
Brown of Stanway to be “ petrified wood,” like that found at Walton-
on-the-Naze, where such remains are found in the London Clay.
There is a septarium to be seen in the river-bed just below. I have
not been so fortunate as to see this part of the pit in work.

Upon this clay lies a bed of gravel (6), largely dug in those
parts of the field from which the superincumbent brick-earth has
been extracted. It is very different in character from the older
gravel above described, although its materials seem to have been for
the most part derived from the more ancient deposit. In the course
of its re-formation much of the sand has been removed, and a certain
proportion of clay incorporated instead, which renders the cementing
material more ‘“‘ binding.” This gravel also contains a few large,
slightly rolled flints; one which I saw must have weighed twenty-
five pounds. These flints were probably derived from the Boulder-
clay. The thickness of this gravel is about 7 feet; but there are
other layers of clay and gravel, beneath the one which is worked,
which have not been proved.

1863.) ' FISHER—LEXDEN BRICK-PIT. 395

Occupying a trough about 30 feet wide
River Colne. in this gravel, and running parallel with the
southern boundary, where the newer strata
abut upon the older gravel, is found a deposit
of fine grey clay passing into carbonaceous
clay with rootlets, and resting upon it a bed
of peat (e), In the central and thickest part
the peat measures about afoot in depth, and
the grey clay 3 feet. The clay extends
north and south beyond the edges of the
peat, and both are planed off above to one
general surface. A thin seam of whitish
gravel and yellow clay, and, above that, about
a foot of whitish clay, cover these deposits,
and pass upwards into the main bed of brown
brick-earth (d) hereafter to be described.

As far as Paleontology is concerned, the
interest of the locality is confined to this re-
markable trough, which has formed a perfect
cemetery for the pachyderms of the period.
Elephas primigenius is found abundantly,
associated with Rhinoceros leptorhinus, of
which latter animal some fine jaws were ob-
tained here by Mr. Brown, who placed them
in the British Museum. Their bones lie upon
the surface of the clay immediately beneath
the peat, while their condition shows that
they have been affected by contact with it.

_The peat itself contains an amazing number
of fragments of Beetles in a remarkable state
of preservation. I collected as many speci-
mens as I could find in the portion of peat
that had been dug out during the past win-
ter, and submitted them to the inspection of
my friend Mr. Wollaston, and I have ap-
pended his highly interesting description of
them to this paper.

The peat has almost thinned out at the
point which the excavations have reached
towards the east; but what remains of it
seems unaltered in character, as if it were
the remaining portion of a thicker mass, of
which the upper part has been removed by
denudation.

In digging the brick-earth, the workmen
are now stopped at the south end of the pit
by a bank of sandy gravel (¢), with a slope of
about 30°. This I concluded to be a talus of

A the ancient bank of the valley ; and accord-

4 ingly, upon digging into it, I found that its

2E2

g on carbonaceous clay.
, 0. Probable old Gravel.

é. Peat restin

1,2

Section through the Brick-pit at Leaden.
(1,2, 3).

c. Talus of old Gravel

d. Brick-earth.

y.
6. Post-pliocene Gravel.

a. London Cla

45 ft. above the valley.

396 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

materials were identical in substance and colour with those of the old
glacial gravel, but that it was wholly unstratified; whereas that gravel,
when 7n situ, is notably bedded. I had, therefore, a pit dug following
the face of this talus until stopped by watcr. I found that the base-
ment gravel of the newer deposits runs underneath the talus, while a
sandy layer resting upon it, but markedly distinct, has the end of the
talus intercalated with it. All the beds above this rest against the
face of the talus, and have their ends slightly bent upwards against it.
A few pebbles le upon the face of the talus, as if they had rolled down
it while the upper beds which abut upon it were being deposited.

Passing upwards from the denuded surface of the peat, we next
meet with a deposit of sandy brown briek-earth (d), about 9 feet
thick. It differs entirely from all the beds below it, and was evi-
dently deposited by a comparatively quiet action against the face of
the old talus, which is wholly undisturbed by it, while its lines of
stratification bend upwards where they abut upon it. In this brick-
earth are a few very thin beds of pebbles. There are also, as already
noticed, a few pebbles where it jois the talus. In the former
position was found a singular red stone, which seems to have been
baked in fire*. In character the brick-earth seems like a silt
derived from the weathered surface of London Clay, abundant in the
neighbourhood. A similar bed of brick-earth oceurs in some pits
near the Colchester railway-station, where it is nearly 20 feet
thick. I have obtained from it the teeth of Deer.

The next deposit in ascending order is the eapping of soil, or
“heading,” passing upwards into the vegetable mould. Of this deposit
I believe less is known than of almost any other, while its import-
ance as containing the records of the latest geological changes ex-
eeeds perhaps that of many of the older strata. In the present
locality there seems to be sufficient evidence that it is a drift. Its
line of junction with the brick-earth is, as usnal, extremely irregular ;
and its lower portion is here, as elsewhere, studded with small sub-
angular flints. Small flints occur only sparingly in the brick-earth
on which it rests. There is at present to be seen, intercalated in
the deposit, a thin wedge-shaped drift of sandy gravel, evidently
washed down from the old gravel forming the hillside above. At
the brick-pit near the Colchester station this drift in patches has
almost the character of a gravel, while the brick-earth on which it
rests is nearly devoid of pebbles. It seems impossible that the one
can have been derived by any subaérial action from the other.

There is also at Lexden a section of a natural bank, beneath which
the surface of the brick-earth is seen to follow the form of the super-
ficial surface, with this overlying drift wrapping round it.

Mode of Formation of the Strata. —In endeavouring to understand
the causes which have led to the phenomena just described, I have
been much assisted by noticing the present condition of the locality,
and have httle doubt that the state of things during the period when
the Elephant lived here was only an older edition of the present.

* Deposited in the Society’s Museum. Mr. Prestwich has indicated Lexden as
a probable locality for “ Flint Implements,” Phil. Trans. 1860, part 2, p. 308.

1863. | FISHER—-LEXDEN BRICK~PIT. 397

At present the River Colne meanders through flat meadow-land,
whose surface it is raising by the deposit of inundation-mud, so that
old trees are becoming buried over their butts. The bed of the river
reveals a layer of coarse gravel asthe subsoil. On the right bank and
a little above the Brick-pit, a short cliff has been excavated in the
valley-side, where the course of the stream makes its most southern
elbow. A talus has been formed in the curve of the cliff, and is co-
vered with vegetation. A mere inspection of the place shows that. the
area in which the Brick-pit is situated is simply a similar curve in the
boundary of the more ancient river-valley, where an elbow of the
stream which then occupied it may have encroached upon the valley-
side,—the bed of gravel which forms the base of the Post-pliocene
deposits being the former equivalent of the gravel now to be seen
40 feet lower in the present bed of the stream, while the old talus
answers to the present one. But the points of similarity do not cease
here; for along the base of the present cliff are some small springs
issuing from the junction of the old gravel and the London Clay,which,
trickling down the face of the bank, have been received in a deep hole,
and have formed a thick bed of peat with a soft quaggy surface. A
short time ago a horse got mired here, and would have perished but
for timely aid. Itis obvious that the ancient bed of peat was formed
in a similar manner by springs issuing from the same junction of the
old gravel and London Clay, which yields water abundantly through-
out the pit; and that the Elephants got mired and perished there,
as the horse would have done without rescue the other day. This
explains why so many individuals have left their remains in so small
a space, and also accounts for the bones. of the feet of an Elephant
being found in juxtaposition in the clay at the base of the peat *.

I am doubtful whether the modern cliff is the result of an under-
mining action of the stream. Such cliffs are very noticeable when
they occur, but are rare in the sides of valleys among soft strata ;
and when they are met with, they usually present springs at their
bases. I believe their formation to be due to the erosive action of
the springs, aided by the slipping away of peat as it becomes gra-
dually too heavy to remain where it was formed; and the ordinary
proximity of an elbow of the stream to such cliffs seems to be an
effect rather than a cause. Nevertheless such a rule need not be
general, and there appears to be evidence, in the gravel underlying
the talus, that the torrential action which brought it there had at
least its share in causing the ancient cliff in the valley-side.

Both the ancient and the recent deposits of peat contain much sand
and gravel on the side nearest to the bank. This may have been
brought here on the feet of birds or other animals, or by stones rolling
and sand being blown down from the bank above. Both peats seem
to have had the effect of discharging all ferruginous colour from the
gravel immediately beneath them, by rendering the colouring material
soluble through the evolution of carbonic acid. The pebbles of flint
in actual contact with the peat are stained black. The ancient peat

* These bones are now in the Museum of Practical Geology, in Jermyn Street,
London.

398 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

seems to have been formed entirely by succulent plants, and to con-
tain no wood, whilst the modern peat is full of sticks and boughs.

I have expressed an opinion in a former paper* that the valleys in
this neighbourhood are not due to causes such as we now see in ope-
ration, but have been excavated and re-excavated by a powerful and
comparatively transient action. Isee, then, in the gravel at the base
of the Brick-field the débris of a former period of denudation, during
which the current swept in an eddy against the hillside forming
the ancient cliff, and deposited gravel against its base. This action
would leave a hole at a short distance from the bank, such as every
angler knows to exist in the elbow of a stream. When the force of
the current abated, that hole would become partially filled with mud,
and afterwards with a rank growth of marsh-plants, which were con-
tinually kept moist and converted into peat by the springs that rose
close by. Here the Phytophagous Insects disported themselves, and
here the Elephants were lured to their destruction.

We now come to the consideration of the brick-earth which covers
the peat. I have stated that the surface of the peat seems to have
been denuded. The denudation has not, however, been of large
amount, but has merely produced channels which appear to run
parallel with the old bank, and are filled with clay. In places there
is a thin bed of shingle above the peat. The denudation may have
been caused by the shifting of the river-course, causing the water to
flow at some period or other over the peat; and the brick-earth
may be nothing more than the silt deposited by the stream in periods
of flood.

It is also possible that the brick-earth may be an estuarine de-
posit, for its height above the sea cannot exceed 60 feet ; the tide
now reaches to within less than two miles of the spot. Such a rise
in the sea-level would be nothing remarkable in the Post-pliocene
period, during which, as is well known, there was in many parts a
subsidence of the land to the depth of about 40 feet f.

Organic Remains.—The facts as yet observed at Lexden do not
add to the evidence now relied upon for the association of Man with
extinct Mammalia. Mr. Prestwich has indicated the locality as one
in which Flint Implements are likely to be found, but they have not
yet been observed. There is, however, a bed of gravel still lower
than that which is dug; and it is very probable that, if Flint Imple-
ments do occur in the pit, that is their position.

When I submitted the Insect-remains to Mr. Wollaston for his
examination, I requested him particularly to give me his opinion as
to the climate which they appeared to indicate; and also to notice
especially whether they agreed specifically with the Coleoptera at
present inhabiting Britain. In reply he writes:—“One thing
I feel pretty certain about, namely, that none of those few species,
the portions of which I have yet examined, are specifically identical
with any of the existing British forms, unless, indeed, it be No. 14,

* Quart. Journ. Geol. Soc. vol. xvu. p. 1.
+ Smith’s ‘ Newer Pliocene Geology,’ p.19.
+ Sce the specimens, which are in the Society’s Muscum.

1863. | FISHER—LEXDEN BRICK-PIT. 399

which may possibly belong to an ordinary Coccinella. Generically
perhaps some of them may be, though at least two, unless I am
much mistaken, cannot be referred to any genus now inhabiting the
British Isles. I say two; but I believe that, even of the few I have
seen, the number is greater. Without more data it would be scarcely
safe to speculate much as to the climate which such species would
indicate. But so far as I am able to judge, if there were any differ-
ence from that which now obtains, I should be inclined to suppose it
to have been warmer, and not the reverse. Thus Cossyphus (and I
can scarcely be mistaken as to that Insect) does not now occur in Eng-
land at all, indeed not even I believe in Central Europe, but in Medi-
terranean latitudes. The existence, in abundance, of a large metallic
Curculio, or anything else so gorgeously cyaneous as to have trans-
mitted even a respectable tint to our times, is certainly more sug-
gestive of a warm climate than of a cold one. I do not think there
can be much doubt that a warmer temperature than what at present
obtains is indicated by these few forms; though at the same time I
am well aware that it is possible to be mistaken as to this, because
some of the Alpine (and therefore Boreal) species assume the brilliant
metallic hues and somewhat large size of insects of more southern
latitudes. Still I do not believe such to be the explanation in the
present case, but exactly the reverse; more particularly if I am not
mistaken in the genus Cossyphus, which I imagine will hardly be
met with now-a-days north of the Pyrenees.”

Mr. Wollaston’s opinion seems, at any rate, to lead to the conclusion
that there was a higher summer-temperature than we now have in
England; and if, as is generally believed, our Island was at that
period annexed to the Continent, such a circumstance, together with
more rigorous winters, would be natural. But the facts, as inter-
preted by him, seem to suggest that the cosmical cooling of the
glacial age had passed away *.

Mr. Wollaston’s opinion as to the diversity of the Lexden Insects
from recent British species is singularly in contrast to the statement
that the Insects of the Forest-bed of Norfolk, and also those of Mun-
desley, are of recent British species. A change of climate from the
already cold preglacial era to a warmer summer-temperature might
cause the introduction of more southern types, and might account
for the insect-forms of the Forest-bed coming nearer to those of the
present day. But this would not explain the case of Mundesley,
where the deposit is supposed to be of the same age as that of Hoxne,
and probably of Lexden. However, I may be permitted to remark
that, apart from Mr. Wollaston’s high authority in any question of
this kind, it must be remembered that it is much safer for an ento-
mologist to pronounce that a portion of an Insect is unlike anything

* Captain Godwin-Austen’s account of the former extension of Glaciers in
the Himalaya (if that extension was contemporary with our Glacial Period)
seems to prove that the phenomenon was general, at least in the northern hemi-
sphere. See Report of the British Association Meeting at Cambridge, 1862,
Transactions of the Sections, p. 67. Dr. Hooker’s observation that the cedars

of Lebanon grow on old moraines confirms this view ; see Tyndall’s ‘ Heat con-
sidered as a mode of motion,’ p. 191.

400 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

with which he is acquainted, than, from the fragmentary remains of
a geological deposit, to pronounce definitely upon the species to which
those fragments may have belonged.

Note on the Rematns of Corzoprrera from the Prat of LEXDEN
Bricx-pit. By T. V. Wottaston, Esq., M.A., F.L.S.

Although each specimen of peat is one mass, apparently, of or-
ganic matter, I have been unable to detect much of an entomological
kind, except elytra. In one specimen*, No. 4, there is part of a
prothorax, and the scutellum is traceable; but the insect is much
covered, and I cannot be sure that its margins are sufficiently flat-
tened for it to be regarded as a Cassida. Also in another case,
No. 5 (perhaps the most interesting and significant of the whole), a
prothorax of such an unmistakeable nature is exposed, that I feel
almost sure it can be nothing but the heteromerous genus Cossyphus.

The enclosed memorandum will show you that I am satisfied that
there are certainly eleven well-defined species,—probably many
more; but the fragments of the rest are too small and unsatisfactory
to dogmatize upon. I can discern no limbs, though the other por-
tions come out very clean and decipherable by brushing them over
with benzine collas y.

But how to generalize satisfactorily from such fragments I cannot
say ; for elytra are the most unsatisfactory parts of Insects for deter-
mining their affinities. A few points perhaps may be ventured upon.

Imprimis, with the exception of two species, Nos. 6 and 7, both
apparently scarce, and which may be Carabideous (though I will not
be positive of this), all the remainder seem to be Phytophagous ; and
as one or two of these, for instance No. 3, seem to have been ex-
tremely abundant, this fact is the more significant. The Chrysome-
lide, Curculionide, and Cassidide, I suspect, embrace the pre-
vailing forms. Bright metallic tints seem to have been the prevail-
ing ones, such as one finds in many of the marsh-insects of our own
times; and there is no evidence of anything very extraordinary
either in size or structure {; though I do not think that any, unless
it be one or two, could be referred to actual species now existing in
England. If any of the species had been fossorial, I imagine that
their strongly developed corneous anterior legs, which are often
wide and externally dentate, could not fail to have been preserved.

Description of the Fragments of Coleoptera.

1. A small, short, and rounded elytron, with a strong outer rim,
uneven, and almost without sculpture, though coarsely coriaceous
under a high power: perhaps a Cassida, or more probably a muti-
lated Coccinella.

2. A larger and extremely wrinkled elytron, most densely and

* The specimens are in the Museum of the Geological Society.

+ The same difficulty m identifying limbs occurs among the fossil Insects of
the Purbeck beds.—O. F.

{ I have reason to think, from the report of the intelligent manager of the pit
Mr. Steward, that much larger Insects occur than any that I have seen.—O. F.

1863. ] SORBY—MICA-SCHIST. 401

minutely punctulated all over, but not striated: possibly one of the
Chrysomelide (such as Orein).

3. A large uneven elytron, of a bright cyaneous blue, deeply
punctate-striated, and coarsely wrinkled transversely : possibly, from
its colour, a Chrysomela, though more probably, from its sculpture,
a large metallic Curculio; apparently a common species.

4, Elytron, scutellum, and prothorax, all partly visible. Elytra
gibbous, shining, sparingly punctured, but not striated, of the same
breadth at the base as the prothorax, but divided from it by a sharp
narrow suture; scutellum very minute and triangular; prothorax
more opaque, most closely and minutely alutaceous, with a longitu-
dinal depression on either side at its base: a small and rounded
Insect, like a very minute Cassida.

5. A prothorax very evident, with an extremely broad, flattened,
and perhaps tubercled margin. The Insect is clearly elongate-oblong
and flat, though more convex and carinated down its central region :
either Cossyphus or Cassida; I think decidedly the former.

6. A large, bright, and more flattened elytron, finely, but simply,
or at the utmost subcrenately striated; with the interstices most
minutely and sparingly punctured, and a little wrinkled. I think
Carabideous ; possibly a Zicenus (or an allied genus).

7. A large, uneven, but rather flattened elytron, distinctly cre-
nate-striated, and with the interstices most closely “and coarsely
rugulose transversely, but not punctulated. Probably Carabideous.

8. A long, rather narrow, and bright elytron, with the striz
excessively deep, sulciform, and impunctate; the interstices almost
unsculptured, though most minutely alutaceous under a high power.
Apparently a rather large Insect. Possibly one of the Buprestide.

9. A bright cyaneous elytron, coarsely seriate-punctate, the punc-
tures large and remote, and with the interstices minutely rugulose :
most likely a Chrysomela.

10. A small portion of an elytron, most coarsely, regularly, and
thickly tubercled or shagreened, but apparently without any other
sculpture.

11. A large convex and polished elytron, most densely, regularly,
and minutely punctulated all over, but without any other sculpture:
I believe a Water-beetle. |

12. Possibly the fractured underside of No. 11.—T. V. W.

2. On the OrternaL Nature and Sussequent ALTERATION of
Mica-scuist. By H. C. Sorsy, Esq., F.R.S., F.G.S.

THAT micaceous schists were originally deposited as sand and mud,
and that their present mineralogical and mechanical structure is due
to subsequent metamorphic action, may appear to some geologists so
thoroughly established as to make further proof needless. Since, how-
ever, some geologists in our own country and on the Continent have,
within the last few years, argued that the bands of varying mineral
character do not represent original stratification, but were due to
causes similar to those which have produced thin-bedded and almost

402 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

laminar trachytes, or to some little-understood force of polarity, it
appears to me far from superfluous to describe certain facts very
completely establishing the sedimentary and metamorphic origin of
the schistose rocks of the localities mentioned in the sequel. That
the mere repetition of layers of different mineral character is of
itself no absolute proof of sedimentary formation is sufficiently
apparent from what is often seen in well-known igneous rocks ; but
mica-schist sometimes possesses other peculiarities, to which I beg
to call attention.

In very many stratified rocks the ripple-marks are extremely
characteristic of deposition under the influence of a current ; but, if
these were found in bent and contorted schists, it would, I think,
be rash to base any important conclusion on them, since mere
mechanical bendings might so readily mislead an observer. There
is, however, a structure generated when ripples are formed whilst
material is being deposited and permanently accumulated, which
has such well-defined peculiarities that it appears to me almost
impossible to confound it with any structure produced by other
means. I here allude to what, in the various papers I have pub-
lished on the subject*, I have called “ ripple-drift,” the most im-
portant characters of which will be better understood from the fol-
lowing drawing :—

Fig. 1.—Thin bed of “Ripple-drift” in unaltered sandstone (nat. size).

Frequently there are quite horizontal beds below and above
(ab, cd), and between are beds inclined to them at an angle ade,
which are themselves made up of smaller beds or stratula dipping in
the opposite direction, namely from 6 towards c. Such bands often
occur in the green slates of Langdale in Westmoreland, the cleavage
cutting them at a considerable angle; and when the slates are
ground smooth and slightly varnished, the peculiar structure may

* Edin. New Phil. Journ., new ser. vols. iii. p. 112, iv. p. 317, v. p. 275,
vil. p. 226; ‘Geologist,’ 1859, p. 187.

1868. | SORBY—MICA-SCHIST. 403

generally be seen very distinctly. The existence of this “ ripple-
drift” appears to me to prove most conclusively the sedimentary
origin of the rock in which it occurs. Its various peculiarities are
so characteristic that it could not, I think, be confounded with any
structure known in any unstratified rock; and therefore, since I
find that it is by no means rare in the mica-schist of the Highlands
of Scotland, I contend that it is a most convincing proof of the
material having been originally deposited from water, whilst other
facts prove quite as conclusively that the present schistose condition
was produced by subsequent crystallization. That these conclusions
are also borne out by the relations of the rocks on a large scale is
shown in the interesting paper by Murchison and Geikie, published in
the Society’s Journal, vol. xvii. p. 232. The localities in which I have
more especially met with this ripple-drift are in the neighbourhood of
Arroquhar and of Aberdeen. Along the coast between the latter
place and Stonehaven I have seen some most excellent examples
with all the characteristic peculiarities, but the rocks are often so
much contorted that very complicated appearances have been pro-
duced. Such structures are also very well seen in a small quarry
between Arroquhar and Tarbat ; and were it not that the most com-
plicated cases gradually pass into others sufficiently simple, one might
sometimes be induced to abandon all hope of a satisfactory explana-
tion. I must here remark that it is often almost impossible to
make out the true structure by examining the rock in its natural
state. It should be ground down to a smooth, flat surface, and
slightly varnished, when the structure is revealed in a most striking
manner. The contortion and compression of the beds have produced
very various and curious results. In some cases the small stratula
have been greatly contorted, whilst the oblique beds have been but
little affected. In others the latter have been much disturbed, and
the stratula forced together, so as to be nearly all parallel; but so
various and complicated are the relations, that possibly I cannot
explain them better than by saying that nearly all the results are
met with that could be produced by bending and squeezing bands of
ripple-drift in all sorts of positions.

Though specimens ground flat and varnished show the general
structure to very great advantage, yet many, more minute par-
ticulars can only be learned by preparing thin transparent sections
for microscopical examination,—some facts being best seen by using
a Wenham’s parabolic condenser, and others by reflected or by
transmitted light, with or without polarizing apparatus. When the
coarser varieties of clay-slate are thus examined, the separate grains
of sand, composed of quartz, felspar, or of compound rocks, can be dis-
tinctly seen; but very commonly no such grains are visible in the
typical varieties of mica-schist. In them the quartz exists as masses
of smaller or larger crystals, not bounded by crystalline planes,
but mutually interfering, so as to give rise to a very different struc-
ture from that of quartzose slates. However, I have lately met with
many specimens of typical mica-schist in which the original grains
of sand may be distinctly seen, even although the rock has been

404 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

ereatly altered and is quite crystallme. In some cases their being
now visible is due to the nature of the surrounding material, which
is so slightly quartzose that their outline is well defined; but in
other cases it 1s due to the character of the quartz of the grains-of
sand being different from that of the quartz subsequently developed
in the rock. Thus it often happens that, whilst the quartz of the
schist itself is clear and transparent, that of the grains of sand con-
tains many fluid-cavities and minute acicular crystals, and is milk-
white or brownish, so that, when seen with a Wenham’s condenser,
each of the grains has a distinct outline, though surrounded by the
clear quartz which has been deposited on them in crystalline con-
tinuity. The grains of felspar-sand are in a similar manner sur-
rounded by quartz, near the junction containing granules due to the
decomposition of the felspar, which occasionally appears to have been
itself metamorphosed into a fine-grained mica-schist. Some of these
facts are scen to great advantage in the sericite slate (a kind of
green mica-schist), which occurs near Wiesbaden in Germany, and
also in the mica-schist of the Highlands of Scotland; and since
I first observed them last autumn, I have been surprised to find
how frequently they may be seen, when carefully looked for. I
scarcely need say that their occurrence in metamorphic rocks is
avery important fact, for they show most clearly that mica-schist
originally contained grains of sand, and that there has been a
subsequent erystallization of quartz throughout the whole rock ;
whilst other facts prove that there was a crystallization of mica,
garnets, felspar, and other minerals, so as to completely alter its
original character, and form what we call a metamorphic schist. It
appears to me that nothing establishes this more conclusively than
the structure of those varieties of mica-schist which possess what I
have described as “ cleavage-foliation” in papers read before the
British Association (Report, Trans. Sects. 1855, p. 96, and 1856, p. 78).
I will especially call attention to a thin microscopical section which
1 have lately prepared of a mica-schist from Muchuls, about ten
miles south of Aberdeen, which contains in itself proof of all the
leading facts connected with metamorphism. It was originally part
of a band of ripple-drift, and therefore the material must have been
deposited from a gentle current of water, but has since been com-
pletely altered into mica-schist with cleavage-foliation. In ripple-
drift in fine-grained sandstones of perfectly unaltered rocks, the
small stratula of sand are separated by layers of argillaceous matter,
and the bands of stratula are also separated by a similar deposit.
These facts readily explain the structure of the ripple-drift in mica-
schist ; for in those parts where in unaltered rocks we find sand or
impure clay, in mica-schist occur bands of quartz or mica, the
sandy parts corresponding to the quartzose, and the argillaceous to
the micaceous. But this is not all; for the stratula have been
greatly disturbed by mechanical forces, have been placed at angles
at which they could not possibly have been deposited, and have been
bent into contortions that show clearly the direction of the pressure,
as will be best understood from the following drawing :—

1863. | SORBY—MICA-SCHIST. 405

Fig. 2.—Contorted “ Ripple-drift” im Mica-schist from Muchuls,
exhibiting “ Cleavage-foliation.” (Magnified 3 diameters.)

a b
ete a Tl i ra ir
\, agnor ni ai! {ir aia if ir AT gal ih ai i") ini ra
ti i gti! il iy il ni Bn wut fy ; it :
aaa ua ag OTN i «al! fll wit i) ( Fr:
“iy me "wn age we oi af jf i ‘a
Hite ; tn BH], if ! { :
yt h h ; if ca i" hE aft ( i!
‘Ny I fl i! i hy av iF ' i" (ta } i { ! i
ty oe eG fee ON a lll
i i jl ie ‘ td ee i 1)
(

f a if ? ‘ia
en sill yi gitinn # i 4 hy
te fe Mtr

ae : 4 sages
(Ce oa My, 17 '

ie if
Fi ity if a Cun

‘
(fice in La ae
ati af i walt { of o ia i
ety vom ‘n, HE: itl at eregeut
7 h

b gt i!
"iy tp Mp y fit of pipe it
(TT CN

Cc

The micaceous parts possess a well-marked cleavage-foliation :
the crystals of black mica do not lie in the line of the stratula (6¢),
nor in that of the compound bands (a b, ¢d), but have one prevailing
direction, as shown in the drawing. Judging from the small con-
tortions, and from the alteration of the inclination of the stratula to
the compound bands, which originally cannot have been more than
30°, but is now often as much as 90°, this direction is perpendicular
to that of the pressure which produced the disturbance, and, no
doubt, developed slaty cleavage in the rock; so that, when subse-
quently metamorphosed, the crystals of mica were formed with their
flat surfaces and cleavage in the plane of the slaty cleavage. In mica-
schist which has been contorted since 1t was metamorphosed and
possesses only stratification-foliation, the crystals of mica le with
their flat surfaces in the plane of deposition of each part of the
ripple-drift, so that it might be argued that they had been mechani-
cally deposited in that position. In the case of the specimen I am
now describing this explanation is, however, quite inadmissible ; for
the crystals of mica could not possibly have derived their present
arrangement from deposition and subsequent mere mechanical dis-
turbance, and must, I contend, have been formed in the midst of the
rock by chemical and crystalline action. Hence this one thin
section does by itself afford most complete proof of original deposi-
tion as a stratified rock, of subsequent compression and the develop-
ment of slaty cleavage, and of the final alteration into a crystalline
schist. As throwing light on this last change, I may here state that
I have recently prepared a thin section of mica-schist from the same
locality as that just described, which, on the whole, is extremely
altered and crystalline. Some parts are solid, clear quartz, and
others a mixture of black, green, and white miéa and of pink
garnets; but mixed up with these highly crystalline portions are
others of much finer grain, which, though not having the structure

406 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | May 6,

of clay-slate, properly so called, are such a very fine-grained mix-
ture of mica and quartz, that to the naked eye a rock of such a
nature might, and perhaps would, be looked upon by many as a
clay-slate—at all events it would be extremely analogous to some
clay-slates slightly altered by contact with granite. These portions
are not small beds interstratified with the very crystalline, but pass
into them irregularly along the plane of bedding, just as if the very
crystalline parts had been formed out of the fine-grained material
which here and there has remained in a comparatively unaltered con-
dition.

From the facts thus briefly described we may, I think, unhesi-
tatingly draw the following general conclusions :—

1. The existence of ripple-drift proves that the material from
which the schists were formed was mechanically deposited from
water.

2. This material originally contained grains of sand, and was
probably a deposit of more or less pure sand and clay.

3. Whatever may have been their original nature, the present
highly crystalline structure of the schists was developed after depo-
sition ; in some cases, indeed, after mechanical movements had pro-
duced complicated contortions and given rise to slaty cleavage.

4, The bands of different minerals represent the planes of original
deposition, rendered very distinct by the alteration of thin strata
(which in unaltered rocks often differ more in chemical composition
than in appearance) into layers of minerals having entirely different
physical characters. :

3. On the Fosstt Corats of the Wust Inpran Istanps.—Part I.
By P. Martin Duncan, M.B. Lond., F.G.S., &e.

[Puates XITI.-XVI.]}

ConTENTs.
A. Preliminary Remarks.
I. Introduction. | II. Geology of Antigua.

B. Enumeration of the Species.

VI. Barbadoes.

II. San Domingo. VIL. Trinidad.
IIT. Jamaica. VIII. Guadaloupe, St. Thomas, and
IV. Montserrat. St. Croix.

V. Barbuda. |

J. Antigua.

C. Description of the Species.
IV. Montserrat.
II. San Domingo. V. Barbuda.
IIT. Jamaica. VI. Barbadoes.
D. General Observations on the Genera and Species.

J. Axtigua. > IV. Barbadoes.

If. San Domingo. V. Guadaloupe, &e.
III. Jamaica. |

E. Conclusion.

I. Antigua.

1863. | DUNCAN—WEST INDIAN CORALS. 407

A. Preliminary Remarks.

. Introduction.—This communication was intended to be a deserip-
tion of the Antiguan Fossil Corals in the Collection of the Geolo-
gical Society ; butit has been found necessary to include a notice of
those from other West Indian Islands, especially from San Domingo,
Montserrat, Jamaica, Barbadoes, Guadaloupe, Barbuda, and Tri-
nidad,

The silicified Corals of Antigua have been well known to the
lapidary for many years, and they were brought under the notice
of this Society by Dr. Nugent in 1819. His description of the
geology of Antigua was accompanied by a beautiful collection of the
rocks and fossils of the island; but although it produced some
correspondence, and Mr. Guilding forwarded specimens in after-
years, no attempt was made to describe or classify the organic re-
mains. Dr. Nugent’s gift included some fossil Shells; and as most
of them were evidently either of recent or very late Tertiary species,
the rest and the Zoantharia were unfortunately determined by some
good authorities to be specifically identical with the forms now ex-
isting in the reefs around the island.

A very superficial examination of the Corals sufficed to prove the
fallacy of this view, and by their careful study it was discovered
that, as a whole, they had not even a West Indian facies. It thus
became necessary to extend the scope of the investigation, and to
endeavour to connect the apparently anomalous distribution of the
fossil Corals in Antigua with the fossil Coral-fauna of islands whose
geology was better known.

The collection of Corals from the limestone and Nivaje shale of
San Domingo, which was examined, in 1850, by Mr. Lonsdale, con-
tains forms the study of which resolved the apparent anomaly, as
those strata are said to be of the Miocene period.

The admirable papers by Messrs. Moore, Morris, Lonsdale, and
Heneken, on the Heneken collection, contain interesting notices of
some of the genera of the fossil Corals of San Domingo ; but Mr. Lons-
dale had not time to devote to their complete study and description ;
the whole of the specimens, therefore, are described in this commu-
nication.

The later Tertiary Corals of Jamaica and San Domingo have also
been examined, and will form the subject of a future communica-
tion ;-but the earlier or mid-tertiary specimens, from the hard in-
clined limestone-beds of Jamaica, which were described years ago
by De la Beche, will be noticed now, as well as the few species in the
Geological Society’s collection from Barbadoes, Barbuda, and Mont-
serrat.

The literature of the fossil Corals of the West Indies is remarkably
scanty; and, excepting the results of the Survey of Trinidad by
Messrs. Wall and Sawkins*, the papers by Sir Henry De la Beche +

* Report on the Geology of Trinidad ; or, Part I. of the West Indian Survey.
By G. P. Wall and J. G. Sawkins. 8vo, London, 1860.

oo on the Geology of Jamaica,” Trans. Geol. Soc. 2nd ser. vol. ii.
p-

408 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

and Mr. Barrett * on Jamaica, and Capt. Nelson’s well-known commu-
nications‘, our exact knowledge of the geology of the islands is equally
limited. Mr. Lonsdale’s brief notice + of the genera of the Nivajé
Corals (admitted by himself to be incomplete), Mr. Etheridge’s short
list of the Trinidad forms §, the notice by MM. Duchassaing and
Michelotti of a few species from St. Thomas, Guadaloupe, and
St. Croix ||, and the scanty collection of descriptions by MM. Milne-
Edwards and Haime®] include the whole of what has been done
amongst these formations, second to none in their interest and great
geologicalimportance. A notice of the species already named will be
added to those now described for the first time. Amongst the many
reasons which might be adduced as explanatory of the neglect of the
Corals of these formations, the unsatisfactory state of the classification
and nomenclature of the Zoantharia stands prominently forward. The
paucity of careful descriptions of recent West Indian Corals has
evidently rendered unsatisfactory and uncertain their comparison
with the forms found in the raised beds; and the condition in which
the fossil and semifossil specimens occur renders their identifica-
tion difficult and, without a careful study of their various forms of
silicification, impossible. Both Mr. Parkinson and Dr. Nugent ex-
perienced this difficulty, and they warned those who might interest
themselves in the description of the Barbadian and Antiguan Corals
that the details of their structure were so altered by the peculiarities
of their fossilization as to render their specific identification difficult ;
they both, however, left the matter as they found it. Messrs. Wall,
Sawkins, and Etheridge bear testimony to these difficulties, and to
the general absence of information about the paleontology of the
West Indies.

In investigating the Antiguan Corals, especially, I found it abso-
lutely necessary to study the various methods of their silicifica-
tion, together with the alterations the specimens had undergone
during the process, before I attempted to define the species. Many
of the determinations of the structural differences depend upon the
correct appreciation of the effects of prefossil wear and tear, and of
the results of mineralization. This part of the subject, with a de-
scription of the West Indian Tertiaries, I have postponed until the
next session, on account of the length of this paper. It is necessary,
however, to introduce at once an abstract of, and a few remarks
on, Dr. Nugent’s “ Description of the Geology of Antigua ” **.

II. Geology of Antigua.—the oldest calcareous formation in Antigua

* “« On some Cretaceous Rocks in the South-Eastern Portion of Jamaica,”
Quart. Journ. Geol. Soc. vol. xvi. p. 324.

t “On the Geology of the Bermudas,” Trans. Geol. Soc. 2nd series, vol. v.
p. 103; “ On the Geology of the Bahamas, and on Coral Formations generally,”
Quart. Journ. Geol. Soe. vol. ix. p. 200.

t “On some Tertiary Deposits in San Domingo, by T. 8. Heneken, Esq. ;
with Notes on the Fossil Shells, by Mr. J. C. Moore; and on the Fossil Corals,
by Mr. W. Lonsdale,” Quart. Journ. Geol. Soc. vol. ix. p. 115.

§ Report on the Geology of Trinidad, w7 c7z.

|| Mem. Acad. Turin, 2nd series, vol. xix. p. 279, 1861.

q Hist. Nat. des Coralliaires. 8vo, Paris, 1857-60.
** Trans. Geol. Soc. Ist series, vol. v. p. 459, 1821.

1863.] DUNCAN——WEST INDIAN CORALS. 409

rests upon a trap-formation about 1400 feet high; it forms hills
which are precipitous tewards the trap, but have a gradual slope in
the opposite direction. It is stratified, and the beds, which dip ata
very considerable angle, consist of clays, limestones, and freestones ;
they are yellow in the last case, and green from the presence of
chlorite in the second. The clays contain crystals of felspar; and
masses of porphyry, lava, greenstone, and amygdaloid are found
throughout the strata generally.

The organic remains consist of Woods, Corals, and Shells, either
silicified and fragmentary or, in the case of some Corals, converted
into chert-like masses. Two formations rest unconformably on the
Inclined Strata, namely, a deep Marl, whose surface is undulating
like our chalk-downs, and which forms the superficial structure of
the greater part of the Island ; and a Chert subordinate to the lowest
part of the Marl. The Chert does not rest conformably on the oldest
formation, is limited in extent, and has evidently suffered from
various wearing causes during the deposition of the Marl. It con-
sists of hard, opaque; white limestone-rock, mixed with portions of
coloured stone, and, from its position and organic remains, appears to
be an old coral-reef fringing the Inclined Strata. The specimens of
Corals occurring in it are siliceous and chert-like in appearance, and
the Woods are like those found in the more ancient strata. It is
characterized by the presence of extraordinary quantities of <‘ Ceri-
thia,”’ which are rarely found in the Marl or in the Inclined Strata*.

The Marl (the third formation), although its surface has suffered
greatly from denudation, reaches, nevertheless, to the height of
nearly 400 feet above the level of the sea, and consists of various
more or less compact limestones, white and yellow marls, and free-
stone, and contains vast quantities of Corals in different conditions
of fossilization. No fossil Wood is found in it, and the little chert
with Cerithia, occasionally met with, has evidently been broken off
the chert-rock and become intermixed. Agates, flints in great va-
riety of form and colour, calcareous concretions, and silicified Shells
and their casts are very common, and three or four kinds of Helix
also. Moreover, there are traces of bitumen. The depth of the
Marl, below the sea-level, is not known; but recent coral-reefs
fringe the low cliffs and outliers.

The specimens in the Collection of the Society are derived from

1. The Inclined Strata, or Conglomerate; 2. The Chert; 3. The
lower, middle, and upper parts of the Marl.

Both the Inclined Strata and the Chert contain extraordinary
quantities of silicified Wood; and their Corals, which are also silici-
fied, are often more or less rolled, and are found as agate mixed
with crystalline quartz, or are turned into opal; they present imper-
fect calicular surfaces, but often consist of siliceous casts. The com-
pound Corals are all of great beauty, and Dr. Nugent identified them
invariably by their small patterns and chert-like appearance.

The Marl contains no Wood, and its Mollusca are not identical with
those of the Chert; and many species of Zoantharia also occur in if
* The so-called “ Cerithia” probably belong to the genus Melania,

VOL. XIX,—PART I, 2F

410 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

in the same state of preservation as the Shells sent over by Dr. Nugent.
Those which I have examined are principally gigantic Astreans,
covered with casts of their calices, and presenting every variety of
fossilization, from perfect universal silicification to imperfect silicifi-
cation of the original hard tissues and filling up of the interstices with
granular carbonate of lime. Theyare less perfectlysilicified than in the
other strata, are usually of a yellow-ochre colour externally, and are
remarkable for their luxuriant growth. Some terrestrial Shells are
found in the Marl, and the Corals, generally, are more or less affected
by the matrix in which they were imbedded. The Inclined Strata
appear to have been Coral-formations of no very great luxuriance ;
and their partial and irregular upheaval by the trap was previous to
the formation of the unconformable Chert, which is in the exaet posi-
tion of a fringing reef. The Chert, as far as can be determined from the
Corals, was formed under external circumstances not very different
from those under which the Inclined Beds were deposited; both
contain fossil Woods in great quantity. The Marl, formed as a reef
around the Inclined Beds during times of considerable variation of
level, quite surrounds the Chert, and is found above, below, and out-
side it. Fragments of the Chert are found in the Marl, which has
also suffered greatly from denudation. There is no Wood in the
latter formation, and the Corals are luxuriant and gigantic. Here
there are evidences of a change in the external circumstances which
affect coral-growth—probably the absenee of the current which
carried down the trees whose fragments, often many feet long, are
found mixed with the Corals of the older beds.

The Corals of the Marl are closely allied to some of those in the
older beds. Here are three consecutive coral-formations, furnish-
ing the support for the growth of existing reefs, and evidently
developed according to the same processes now in action in the sur-
rounding sea.

B. Enumeration of the Species.

I. From ANTIGEUA.

a. ier the Marl.

1a. Astrea crassolamellata, sp. nov. 6. Astrea tentis, sp. nov.

10. ——.,, var. magnetica. Barbadensis**, sp. nov-
le. , var. pulchella. 8. radiata, Lamarck, vay, inter-
1d, —— ——, var. nobilis. media.
12, , Var. minor. 9.— costata, sp. nov.
1f. —— , var. Nugenti. 20. Rhodarzea irregularis, sp. nov. —
lg. —— , var. magnifica. 21a. Alveopora Dedalea, Blainville,
3. —— Antiguensis, sp. nov. var. regularis*.
4, endothecata, sp. nov.f, varr.1,} 22. microscopica, sp. NOV.

2, 3. 23. fenestrata, Danat.

* Common to the Chert and the Marl.
+ Common to St. Domingo and Antigua.
** Common to Barbadoes and Antigua.

1863, ]

DUNCAN—WEST INDIAN CORALS.

41]

b. From the Chert.

2 6. Astrea cellulosa, var. curvata, sp.
nov.

5. megalaxona, sp. nov.
10. Solenastrzea Turonensis, Michelin.
11. Isastreea conferta, sp. nov.
12. turbinata, sp. nov.
13. Stephanoccenia tenuis, sp. nov.{
15. Celoria dens-elephantis, sp. nov.

esi, ea

16, Astroria polygonalis, sp, nov.

1 affinis, sp. nov.

18. Antiguensis, sp. nov.

19. Astroceenia ornata, Hdwards &
Haime.

21 a. Alveopora Dedalea, Blainville,
var. regularis *§._

, Var. minor.

e. From the Inchned Beds, or the Conglomerate.

2a. Astrea cellulosa, sp. nov.
13. Stephanoccenia tenuis, sp. nov.t

14, Meandrina, sp.

II. From tue Nivase SHALE, SUPERFICIAL LIMESTONE, PosTRERO AND
EspERANZA SHALES OF San Domineo.

1, Brachycyathus Henekeni, sp. nov.
2. Placocyathus Barretti, sp. nov.||,
varr. 1, 2.
3. Trochocyathus cornucopia, Hd-
wards & Haime.
4, Placotrochus Lonsdalei, sp. nov.
5, Flabellum dubium, sp. nov.
6. » Sp. Nov.
7. Thysanus corbicula, gen. et sp. nov.
8. Barysmilia intermedia, sp. nov.
9. Dichoccenia tuberosa, sp. nov.
10. Stephanoccenia dendroidea, Hd-
wards & Haime.
11. Phyllocenia sculpta, Hdwards &
Haime, var. tegula.
12. limbata, sp. nov.

13. Montlivaltia ponderosa, Edwards &
Haime.

14. Meeandrina filograna, Lamarck.

15. Astrea (Heliastraea, .Edwards) en-
dothecatat, sp. nov.

(Heliastreea, Edwards) cylin-
drica, sp. nov.

17. Siderastreea crenulata, Blainville,
var. Antillarum.

18. Cyphastrezea costata, sp. nov.9]

19a. Stylophora affinis, sp. nov.

198. , Var. minor.

20. Agaricia agaricites, Lamarck.

21. undata, Lamarck, var.

22. Alveopora fenestrata, Danat.

23. Porites Collegniana, Michelin.

16.

IT]. From tar JAmartca TerttAry LIMESTONES.

1. Placocyathus Barretti, sp. nov.||

2. Placotrochus alveolus, sp. nov.

3. Thysanus excentricus, sp. nov.

4, Astroceenia decaphylla, Edwards &
Haime.

5. Siderastreea grandis, sp. nov.

6. Cyphastrzea costata, sp. nov.§

ITV. Montserrat,

1. Astrea Antillarum, sp. nov.

7. Montlivaltia ponderosa ||, Edwards
& Haime.
8. Astreinz dendroide.
9. Alveopora Dedalea, Blainville,
var. regularis §.
10. Porites, sp.

V. Barsupa.

1. Cyphastrzea costata§], sp. nov.

VI. Barsanpozs.

1. Astrea Barbadensis**, sp. nov.
2. Oculina, sp.

3. Madrepora, sp.

¢{ Common to the Conglomerate and the Chert.

§ Common to Jamaica and Antigua.

|| Common to San Domingo and Jamaica.

*| Common to San Domingo, Jamaica, and Barbuda.

N

** Common to Barbadoes and Antigua.

282

412 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

VII. Friniap (Etheridge) *.

1. Turbinolia, two species. 4. Orbicella coronata, Dana.

2. Astrzea (Orbicella,Dana)Argus,iam.| 9. stelligera, Dana.

3. radiata, Lam. 6. —— Pleiades, Dana.

VIIL. Guapaxovurs, St. THomas, Sr. Crorx.

}. Cyathina Guadalupensis, Edwards& | 5. Parasmilia nutans, Duchassaing &
Haime. Michelotti.

2. Paterocyathus Guadalupensis, Du- | 6. Montlivaltia ponderosa, Edwards
chassaing & Michelotti. & Haime.

8. Trochosmilia Laurenti, Duchassaing | 7. Solenastreea Ellisii?, Duchassaing
& Michelotti. & Michelotti.

4, gracilis, Duchassaing & Miche- | 8. Favosites Dietzi, (St. Croix,) Du-
lotti. chassaing & Michelotti.

€. Description of the Species.
I, Antiava.

1, AsrRaiA CRASSOLAMELLATA, spec. nov.} Pl. XIII. figs. 1-7.

General Description.—A group of forms from the Marl presents the
following structural characteristics :— Corallum very massive and
large, with an irregular upper surface, which is convex in some
parts, almost flat in others, and more or less largely gibbous in all ;
intercalicular groove very decided. Corallites usually very large, and
never very small, Wall very delicate and indistinct; coste small;
columella large. Septa variable in cyclical arrangement, the larger
excessively developed at the wall and lmear within. Endotheca
abundant, but not in excess, vesicular. Exotheca not well developed,
but decided and plentiful. Calices invariably found as casts: impres-
sions prove them to have been shallow. Ccenenchyma well developed.

These characters, common to many forms, are more or less varied
in intensity in different specimens. The septal number varies in in-
dividuals of the same corallum, in one series of forms to a remark-
able extent, although the corallites thus differing are nearly equal
in diameter, and are nearly, if not quite, as advanced in deve-
lopment. In other forms it is fixed to four cyeles in six systems ;

* The fossil Corals from the newer Parian Formation of Trinidad were de-
scribed under the above names, by Mr. Etheridge, in Wall & Sawkins’s ‘ Geology
of Trinidad.’ They were all greatly altered by fossilization.

t The genus Astrea of Lamarck contained forms subsequently referred to
Siderastrea by Blainville, as well as those included in the genus Astrea by
Milne-Edwards & Haime in their earlier contributions to the Académie des
Sciences Naturelles, and in the ‘‘Introduction to the Classification of the Zoan-
tharia,”’ prefixed to their ‘ British Fossil Corals,’ published by the Palzontogra~
phical Society. In the ‘ Histoire Naturelle des Coralliaires ’ by Milne-Edwards
& Haime (1857), their genus Astrea appears as Heliastrea, and Blainville’s genus
Siderastrea as Astrea. I have retained the nomenclature recognized amongst
British paleontologists, feeling assured that MM. Milne-Edwards & Haime have
so influenced the successful study of Corals by their earlier works that their
original generic terms will remain in use. Also, instead of their new application
of the generic term Caryophyllia to Cyathina, I retain the latter as they originally
gave it.

1863.] DUNCAN-——WEST INDIAN CORALS. 413

whilst in some there are three cyclesin some systems, and only twe
in others, the corallum being large.

The form which I consider typical of the species has four perfect
eycles in six systems; but in some corallites the rudimentary sixth
and seventh orders of a fifth cycle exist. The specific character-
istics—the thick and great development of the septal laminz at their
wall-end, and the more or less linear, but entire, condition of their
internal parts—are seen in all these forms, in the primary, secondary,
and tertiary septa, according to the relative septal arrangements.
In some corallites with a low septal number, the primary septa alone
are thus characterized; and as the higher cycles are seen, so the
secondary and tertiary septa become enlarged and resemble the
primary. ‘The septa of the higher orders are either linear through-
out or slightly enlarged at the wall ; and as they approach the tertiary
or quaternary, as the case may be, they are seen to become more
equal to them in size. In examining these forms allowance must
be made for their fossil condition; and attention must be given, in
examining transverse sections of corallites, that they are quite at
right angles to the corallite, for any obliquity will, of course, dimi-
nish the peculiar spear-shape or mace-shape of the septa, and render
them more like a paddle, or a leaf with the stalk attached.

The tendency of the higher orders of septa to become linear
throughout, or to be less decidedly large at one end and thin else-
where—that i is, more or less uniformly thick, but in a less degree
than is usual at the wall,—is seen throughout the species; and in
a gigantic variety, where the fully developed corallites have twelve
or fourteen septa in every system, the whole of the septa are less
decidedly thick at the wall, and are either more or less so throughout,
or present the usual form of the septa in a modified degree.

This species is found throughout the great Marl-formation, and
presents every variety of siliceous fossilization, from that character-
ized by silicification of the sclerenchyma and infiltration of the inter-
spaces : by granular carbonate of lime, to that where all is siliceous and
capable of polish. Destructive silicification almost invariably exists
in a greater or less degree; and as the sections preserved were made,
as a rule, for ornament or amusement, I have seldom seen accu-
rately transverse and longitudinal views of the corallites.

All the specimens, with the specific peculiarities mentioned, may be
ranged in seven groups: that which contains the detailed characters in
their greatest intensity, generally, may be considered the typical form.

a, ASTRHA CRASSOLAMELLATA, typical form. Pl. XIII. figs. 1 a—le.

Corallum large, irregularly convex above. Corallites tall, large,
crowded here and there, but not so much so higher up or at the sur-
face. Calices circular, but more or less elliptical when on an irre-
gularity of the surface ; very large, and separated from each other by
well-marked, furrow-shaped, polygonal tracts; tracts marked by
costal elevations and by granules*. Calices crateriform, not much

* As none of the specimens exhibit perfect calices, many of these characters
have, of necessity, been taken from casts,

414 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

elevated above the surface. Wall thin, and rendered insignificant by
the great development of the septa at the margin. Fossa not deep.
Coste numerous, and, considering the diameter of the septa at the
wall, very small; they project but little, and are, as a rule, alter-
nately large and small, not dentate, and often incline one to the other
at their free edge. The larger coste present regular enlargements

Analysis of the Species.

ly tercalicul Diameter of
i peerety Ss Banta: Vyeles, corallites.
a. Astrea crassolamellata (type).| well marked very 4, in some 5| #-4 inch
b, —— ——, var. magnetica ...| well marked aioe ‘s Inch
at wall : eae
C. ——, var. pulchella ... variable | 4-3 inch
less
d, —— ——, var. nobilis ...... well very largeat} variable | variable
marked wall :
é. —— ——, var. Minor......... very small, va-
thick 2and 3 riable
f— , var. Nugenti ...... less marked | | at wall
gs —— ——, Var. magnifica ... well marked | less thick 4-6 4 inch
and more 1 inch and
linear more

where the cross-tissue (dissepiments) of the exotheca joins them :
when there are more than four cycles of septa, the smaller coste
are irregular as regards their appearance and development. Colu-
mella large, of lax lamine, parietal ; it does not project much at the
bottom of the fossa, and occupies a large space in the corallite. Septa
numerous, generally characterized by great enlargement at the wall,
and linear appearance in the rest of their course, the higher orders
being nearly linear at the wall also. The number of cycles varies
with the stage of development of the corallite.

In young corallites there are six systems of three cycles. As
growth proceeds, the other orders of the fourth and sometimes of
the fifth cycle are gradually added. Some systems are defective in
certain orders, while others possess them. The largest corallites
have four perfect cycles, and a fifth in two or three systems; the
ninth order being usually wanting. It is difficult, in the larger
corallites, to distinguish the systems on account of the resemblance
of the primary, secondary, and tertiary septa to each other.

The primary septa are very thick externally, but delicate and linear
elsewhere ; the linear part joins the rest suddenly, like the staff of a
big-headed spear; at the junction the thick corners of the enlarge-
ment give off a lateral spine, like a piece of endotheca; near the
costal end of the septa there are delicate lateral_spines. The space
between the sets of lateral spines is more or less square. The
secondary septa are very like the primary.

When there are more orders in the system than five, that 1s, when
there are six, seven, eight, and nine, the tertiary septa equal the pri-
mary and secondary, the blunt end terminating in the linear portion
a little nearer the wall, When there are four cycles, the tertiary

1863. } DUNCAN—WEST INDIAN CORALS, 415

septa are smaller than the primary and secondary; and when there
are only three cycles, as in young corallites, the tertiary septa are
linear throughout. The quaternary septa are linear and very slightly
developed; when there are more septa than those of the fourth cycle,
the quaternary resemble small tertiary septa. The remaining septa
are very small and linear, and reach a very little way from the wall ;
they are apt to curve tewards the septa nearest them. In examining
the shape of the septa in this and in all the allied forms, particular
attention must be paid that the section is quite transverse, as any
obliquity will more or less alter the shape of the larger end.

As regards the endotheca, the dissepiments are frequent and deli-
eate, and not very much developed. The exotheca is tolerably well
developed, but not in proportion to the size of the corallites. Its dis-
sepiments form square cells. The free surface between the cost and
ealices has afew granules. Increase by extra-calicular gemmation.

Marl-fermation of Antigua. Coll. Geol. Soc.

Measurements ——Diameter of the calices in six specimens ? inch, in
seven others £inch, and in some from 3 to 7 inch. The elliptical
calices (situated on the sides of the corallum) are about 1,4, inch in
longest diameter. The greatest thickness of the septa at the wall
is 54, inch. Columella + inch in diameter.

No recent specimens of this species have as yet been found,
and its alliances are with Astrea Lifolensis, Edwards and Haime*,
and Astrea Guettardi, Edwards and Haime+. The latter species
includes also the Astrea nebilis, Edwards and Haime; it has
a polygonal furrow around the calices, shallow fossz, septa exces-
sively thick at the wall, and indistinct walls. It has also smaller
corallites than the type of the new species, but larger than some of
the varieties ; butits costz being strong, very close, and alternately
very thick and thin, constitutes a specific distinction.

A specimen of Astrea Infolensis (Jurassic) in the British Museum
has stronger resemblances to the West Indian ferms than has A.
Guettardi (Miccene). The general form of the fourth variety
(var. nobilis) differs much from that of A. Lifolensis, although there
is a great resemblance in their details. The coste furnish, how-
ever, a specific difference ; still the alliance is extremely close.

b. Var. Maenetica. Pl. XIII. figs. 4a, 4d.

A magnificent Astrean, resembling the typical form, but having no
more than four cycles of septa. The septa are very marked, very
large at the wall, and resemble the printed radii on a mariner’s
compass-card. Coenenchyma greatly developed. The diameter of
the corallites is from 4 to 4 inch, being very variable.

Marl-formation of Antigua. Coll. Geol. Soc.

c. Var. PULCHELLA.

Corallum large, convex, irregular in superficial outline. Corallites
tall, varying in diameter on account of the mode of growth, rather
crowded at the surface, circular in transverse section, with abundant
ccenenchyma. Coste wide apart. Calices rather crowded, and the

* Polyp. Foss, des Terr. Paleoz., 1851, p. 98. + Op. cit. p. 97.

416 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

intercalicular furrow not so distinct as in the typical form of the
species. Diameter from } to 3 inch. Septa large at the margim,
more or less thin elsewhere; in six systems with a very irregular
septal distribution. In young corallites there are two cycles, and
a third in two systems (eight large septa). In larger corallites
there are three cycles in four systems, and two in the rest (ten
large septa). In the largest there are three cycles in all systems but
one (eleven large septa). In some large corallites a fourth cycle
evidently existed near the calicular margin.

In some specimens the marginal enlargement of the septa is ren-
dered less distinct by rather thick and not very linear septal deve-
lopment internally. The corallum is too large to admit of all the
corallites being badly developed, except those with four cycles; and
the expression of its septal number must be three cycles, the third
being occasionally wanting in some systems, and four cyeles being
the extreme range. The variability in the septal number is very
characteristic of this variety. The exothecal dissepiments are abun-
dant, and bifurcate here and there.

Marl-formation of Antigua. Coll. Geol. Soc.

d. Var. wostis. Pl. XIU. figs. 2a, 2 6.

Corallum large, irregularly convex, and gibbous above. Corallites
distinct, circular in transverse section, varying in size; ccenenchyma
well developed. Septa very large at the wall, linear within, number
of large-headed septa remarkable; primary, secondary, and tertiary
septa often equally large. Calices varying in size. Septal number
from three to four cycles. This form is between the varieties mag-
netica and pulchella. Coll. Geol. Soe.

e. Var. Minor. Pl. XIII. fig. 6.

Corallites tall, slender, crowded, distinct ; walls circular, not thick.
Calices circular, somewhat variable in size ; the largest is =3, inch in
diameter. The larger septa are spear-shaped, the smaller linear ; they
are in six systems of two cycles ; rarely three cycles in two systems in
some corallites. Primary septa much larger than the secondary, but
nearly equalling them when there is a third cycle. Columella large.

The alternate large and small, spear-shaped and linear septa are
very well seen in this form. The same details as in this form are
found in several specimens with larger corallites.

Marl-formation of Antigua. Coll. Geol. Soc., and Mr. W. W.
Jones’s Coll.

j-- Nar. Noeunti.., Fl, XT. fie. 5,

The specimen upon which this variety is founded has no calices,
but the transverse views of the corallites are very distinct.

Corallites 4 inch in diameter, not crowded. Septa in six systems,
two cycles in four systems and three in the other two. The tertiary
orders are small, and often join the secondary near the columella. The
primary septa are square and large at the wall, and not very linear, but
staff-shaped within; their width at the margin is =. inch. The
Secondary septa are very much smaller and thinner than the pri-
mary, but nearly as large when the tertiary orders are present.

1863. ] . DUNCAN— WEST INDIAN CORALS. 417

Coste wide apart. Exothecal cells scalariform, wider than high ;
from =1, to ;1, inch high, and =. inch long. Endotheca abundant.

This form has squarer-headed septa, longer exothecal cells, costae
wider apart, and a lower septal number than many of the forms of
the species; and differs from the forms with three more or less in-
complete septal cycles in the greater thickness of the inner part of
the septal laminee, the broad exothecal cells, and in the disposition of
the tertiary septa to join the secondary.

From the lithological character of the specimen thus described
(Coll. Geol. Soc.), it is either from the Chert-formation of Antigua or
from the lower part of the Marl.

g. Var. maenirica. Pl. XIII. fig. 3.

In the smaller corallites of this variety the spear-shaped septa are
seen ; but in the larger, where there are from twelve to fourteen
septa in a system, the primary, secondary, and tertiary orders are
nearly equal in size. They have lost the extreme relative thickness
between their extremities, and, although still very thin at the
columella, they are not greatly developed at the wall. In some
corallites the septa, in transverse view, are not straight, but form
curving radii*; and in all, the relation which the septa bear to the
interseptal spaces and to the wall is very much exaggerated.

Corallites circular in transverse section; they vary much in dia-
meter, and are now and then crowded, but generally have much
coenenchyma between them. The diameters of five corallites are
as follows :—2 inch, 2 inch, 1 inch, 1,4 inch, } inch. Walls very
indistinct. Coste small, and appearing to be appended to all the
septa. Exotheca is present, and connects the coste. Septa nume-
rous, especially in large corallites, where the cycles, which are small
and rudimentary in the lesser, become well developed. In the small-
est corallites there are six systems of four cycles, the fourth and
eighth orders being very small. In medium-sized corallites there
are six systems, four cycles in five systems, and in the sixth there
are the rudimentary sixth, seventh, and eighth orders. ‘The first,
second, and third orders are nearly equal in size. In the largest
there are six systems, and from twelve to fourteen septa in every
system. Lateral teeth exist on all the primary septa at the place of
greatest width. The higher orders in every system are very linear.
Endotheca abundant, but not in excess. Columella large, well de-
veloped, and spongy. Ccenenchyma formed of cells produced by the
coste and the exothecal dissepiments.

This is the largest form of compound Astreean yet described, and
when in mass must present a very striking appearance ; unfortu-
nately no calices have been discovered as yet. Reproduction by ~
extra-calicular budding.

Marl-formation of Antigua. Coll. Geol. Soc., Mus. Pract. Geol.,
and British Museum.

2a. AsTRHA CELLULOSA, spec. nov., typical form. Pl. XIII. fig. 10.
Corallum tall, and, judging from the disposition of the corallites,

* See a specimen in the Mus. Pract. Geol. Lond.

418 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [May 6,

subplane above. Corallites very numerous, tall, slender, crowded, but
distinct ; usually cylindrical, but sometimes more or less prismatic
from mutual pressure; varying in size. The transverse section of
the corallites is generally circular, now and then deformed. Septa
crowded, linear; the primary are the largest, but often the second-
ary are nearly as large. The primary septa are of nearly the same
thickness at the wall and throughout. There are six systems of
four cycles; in imperfectly developed systems the fourth cycle is
wanting, but the persistence of this cycle throughout all the systems
is very generally decided. The fourth and fifth orders are very
small, and when there are only three cycles, the third order is small ;
the septa are generally straight. Columella small and slightly de-
veloped. The wall appears to be stout. Coste attached to every
septum, subequal, and not very greatly developed. Endotheca
vesicular, greatly developed. There are often four dissepiments di-
viding each interseptal space. Exotheca cellular and highly deve-
loped; exothecal cells small, more rectangular and larger than the
endothecal cells. The reproduction is by extra-calicular gemmation ;
the smallest buds visible have three perfect cycles of septa.

From the Conglomerate of Antigua. Coll. Geol. Soc.

Dimensions.—Height of corallum several inches, Diameter of
corallites from 1-2 lines.

The minute details of the structure of this Coral have disappeared ;
but the brilliant porcellanous silica which fills up the interseptal
loculi and the exothecal cells is so easily distinguished from the dull
colourless remains of the septa, dissepiments, and walls, that the
characters described are easily seen in the specimens. In some
parts of the specimens the sclerenchyma is whitish grey, and the
interspaces are filled with dark homogeneous silica, just reversing
the arrangement generally observed.

The intimate relation between this form and one from a later
formation (the Chert) is very interesting. The latter (var. curvata)
has the teeth on the septa preserved ; and the septa of the third order
eurve towards those of the second near the columella. It has all
the other structural peculiarities of the older form, and is clearly a
variety ; for here and there, amongst the numerous individuals of
the masses from the Inclined Strata, the septa of the third order are
now and then seen to curve towards those of the second.

26. Var. CURVATA.

Corallites slender, long, close, sometimes compressed ; circular in
transverse section, except when compressed. Walls thin and de-
-licate. Coste delicate, unequal, narrow at the base, tapering ex-
ternally. Septa well developed, in six systems of four complete
cycles. The primary septa are large, toothed on either side, not
larger at any one point than at another. The secondary septa are
smaller than the primary, and have a tooth near the columella. The
tertiary are smaller than the secondary, vary much in size, often
extend nearly up to the columella, and curve there towards the
latter; they have lateral teeth, and a larger tooth at the end; or

1863. ] DUNCAN—WEST INDIAN CORALS. 419

they reach only halfway, being either straight or curved. The
quaternary septa have wedge-shaped bases and spike-like prolonga-
tions, extend one-quarter the distance to the columella, and some-
times curve towards the tertiary. Columella lax and parietal. En-
dotheca greatly developed, subdividing the septal loculi by trans-
verse bars. Exotheca distinct, cells small.

Dimensions.—Diameter of the corallites 4 inch; a bud 1 line in
diameter has three cycles.

Chert-formation of Antigua. Coll.Geol. Soc. As a rule, this va-
riety is curiously fossilized.

3. AsTRHA ANTIGUENSIS, spec. noy. Pl. XIII. fig. 8.

Corallum large, turbinate, convex and gibbous above, with a very
small base. Corallites long, close, rather crowded, but distinct and
radiating from the narrow base. ‘Walls well developed, moderately
_ thick. Coste moderately developed, projecting more than the width
of their base; they are plain where seen superficially, very nearly
equal, and are not spined or toothed. In some corallites the fourth
cycle of cost is wanting, but not in those that are fully developed.
Calices circular, slightly raised, appearing as truncated cones, some-
times compressed (at the side of the corallum they are distorted),
unequal in size; margin thin. Fossa not deep, but variable. Colu-
mella well developed, projecting at the bottom of the fossa; its com-
ponent tissue is laminar and folded, and it is rounded above.
Septa straight, very slightly exsert, delicate throughout, not larger
at any point decidedly ; but the largest are more delicate midway
between the walls and the columella; they are arranged in six
systems of four cycles. The primary and secondary septa are
equal ; the tertiary a little smaller; those of the fourth order are very
small, and barely developed in some calices, but they exist in all.
The primary and secondary septa have a tooth near the columella.
Endotheca tolerably developed. Exotheca well developed, forming
large and small cells, both square, though often divided by dissepi-
ments. Reproduction by extra-calicular gemmation. There is no
epitheca.

Dimensions.—Height of corallum several inches; diameter of calices
from a little less than 3 lines to 4; thickness of septa 4, inch. The
dimensions of the elliptical calices are—length 34 lines, breadth 24
lines, depth of fossa $line. LExothecal cells from } to d line. The
lateral calices are very irregular, and the younger corallites have
three cycles of septa.

Fossilization.—Calices, as a rule, not filled up. Sclerenchyma
light-brown in colour, opaque, and siliceous, the central portions of
the corallum evidently consisting of dark homogeneous flint, the
sclerenchyma having been destroyed in the process of silicification.

From the Marl-formation of Antigua. Coll. Geol. Soe.

4, ASTRHA ENDOTHECATA, spec. noy.*, var. 1. Pl. XIV. fig. 9.
Corallum tall, without radiating corallites, subplane above. Coral-

* See also p. 434, amongst the Corals from San Domingo.

420 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

lites crowded, cylindrical, distinct, very long. Coste subequal, large ;
those ee the fourth order sometimes wanting. Calices circular,
from -3, to 54; inch in diameter. Septa very delicate, very crowded,
nearly linear, granular. Endotheca greatly developed, vesicular,
with from three to four dissepiments between the septa, dividing the
loculi into compartments. The fourth cycle of septa appears often
to reach one of these dissepiments, and to end by touching it. Colu-
mella well developed.

From the lower part of the Marl-formation of Antigua. Coll. Geol.
Soc.

This is a variety characterized by a larger amount of endotheca
and a smaller amount of exotheca than in the typical form.

Var. 2.

A variety with the specific details of the typical form, and in ad-
dition an increased amount of exotheca, whose cells are broader than
high, the dissepiments being well developed.

From the lower part of the Marl-formation of Antigua. Coll. Geol.
Soc.

Var. 3.

A variety with smaller corallites, longer and more crowded deli-
cate septa, with the endotheca greatly developed, the dessepiments
being very stout.

From the calcareous beds in the lower par of the Marl-formation
of Antigua. Coll. Geol. Soc.

5, ASTRHA MEGALAXONA, Spec. nov. Pl. XIII. figs. 12 a, 12d.

Corallum large. Corallites very numerous, crowded, very variable
in breadth, long and slender; they have suffered much from mu-
tual pressure, and although the walls are distinct, yet the coral-
lites are often more or less polygonal; diameter from 4 to 4 inch.
Walls thin. Coste small. Septa very delicate, a little thicker at the
wall than elsewhere, and very thin towards the columella; in six
systems, the cycles varying greatly ; thus, in many corallites there
are two cycles, in others two cycles and a third in one or more
systems. Three perfect cycles are seen in large corallites, and two
additional septa in some (in the whole corallite). The primary septa
have a tooth near the wall; the secondary are a little smaller than
the primary. Columella lax, parietal, occupying a very large space.

The details can be made out in only one corallite, which has
escaped the ruinous but remarkable fossilization that has destroyed
them in most of the specimens. The details have nearly all disap-
peared in the mass, and the interseptal loculi look like blunt, thick
septa. In some specimens the large space occupied by the colu-
mella is filled with silica of a white or of a black colour, giving them

a.very curious appearance.

There are many corallites which appear to have been undergoing
fissiparous growth, but it is evident that extra-calicular gemmation
also occurred. There are few details left for a diagnosis of the spe-
cies. The recent Astrea Pleiades, a Pacific form, is the only known

1863. | DUNCAN—WEST INDIAN CORALS, 421

species with a low septal number and fissiparous growth; it differs
from that just described in its costal arrangement, but is more
closely allied to it than to any other Coral.

From the Chert-formation of Antigua. Coll. Geol. Soc.

6, AsTR#A TENUIS, spec. nov. Pl. XIII. fig. 11.

Corallites close, generally cylindrical, but sometimes deformed by
pressure. Walls slender, distinct. Coste distinct, small, subequal,
well separated, sometimes inclined laterally; edges sharp. Colu-
mella lax, badly developed, formed of trabecule passing from the
ends of the septa. Septa thin, close, slender, a little thicker at the
wall than elsewhere, and a little larger at the columella than in the
middle ; they appear to have had a large tooth near the columella,
and are arranged in six systems, the cycles being very variable.
Unfortunately I have not seen any calices, and fully developed
corallites are also wanting. The following are the arrangements of
the septa in the corallites I have seen:—In one corallite there are
thirty septa, or three cycles, in four systems, a fourth cycle in one
system, and fourth and fifth orders in half a system; in a second
corallite the same ; in a third, with thirty-two septa, there are three
cycles in four systems, and four cycles in the other two. Ina
fourth corallite there are thirty-four septa, or three cycles in three
systems, four cycles in two, and fourth and fifth orders in half a
system. The primary septa are slightly thicker and more toothed
than the secondary ; and the latter are more developed than the
tertiary, which are rudimentary except when there is a fourth cycle,
and then they are as large as the secondary. The fourth and fifth
orders often curve towards the third. Doubtless, in well-developed
corallites, the fourth cycle is perfect in all the systems, being now
and then wanting in the half of certain systems. Endotheca ab-
sorbed during fossilization. Exotheca exists as cells between the
coste.

From the Marl-formation of Antigua. Coll. Geol. Soc. Diameter
of the corallites about 2 lines, a little more or less.

7. AstR#A BAaRBADENSIS*, spec. nov. Pl. XV. figs. 6a, 6b.

This Astreean is found in the Marl-formation of Antigua, greatly
altered by fossilization; the calicular surface is subplane, and the
calices are seen as prominent columnar casts. Coll. Geol. Soc.

8. AsTR#A RADIATA, Lamarck, var. INTERMEDIA.

To this variety I refer certain corals presenting the specific dis-
tinctions of Astrea radiata, but having the third cycle of septa
complete, and a little excess of vesicular endotheca. The specimens
are remarkable for their varieties of fossilization, the presence of
crystalline quartz, as well as homogeneous flint, being common inside
the corallites. The variety forms a link between the great Astreans
of the Miocene of the Antilles and the existing Astrea radiata of
the Caribbean Sea, Astrwa Antillarum being closely allied to it.

* See also the Barbadian Corals, pp. 444 & 445,

422 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. — 6,

From the Upper Parian of Trinidad (Wall & Sawkins’s Coll.), and
the Marl-formation of Antigua. Coll. Geol. Soe.

9. AsTRMA cosTaTa, spec. noy. Pl. XIII. fig. 9.

The specimens of this species which I have examined present
polished longitudinal and transverse sections of corallites, but I have
seen no calices. Corallites long, parallel, sometimes deformed,
generally circular in transverse outline, not crowded, but close, vary-
ing in size. Intercorallite spaces very distinct. Walls thin, not
thicker than the delicate septa. Coste large alternately, both sizes
equally produced; wedge-shaped at the wall, pointed, and often
bent at the free end. Septa all delicate and linear near the columella
and in the middle; at the wall their base is narrower than that of
the coste. They are arranged in six systems, the cycles being very
irregular. In three systems there are three cycles, and in the rest
an incomplete fourth; rarely there are two systems with four com-
plete cycles; the fourth and fifth orders often curve towards the
third order. Lamelle rather cribriform, joining the columella by
oblique processes. Columella lax, small, and formed by dissepiments
from the septa and a central spongy mass. Endotheca very abun-
dant, vesicular, and horizontal, with four or five dissepiments in
inch. Exotheca abundant, nearly equal to the endotheca. Repro-
pores by extra-calicular budding. Diameter of the corallites from

to =& inch.

his species is closely allied to the Astreeans with great endothe-
eal development, and especially to Astrwa vesiculosa, Edwards and.
Haime, from Dax, as well as to A. Antillarum, nob., and A. endothe-
cata, nob.

10. SorenastR#A TuRoNENsIS, Michelin.

Some imperfect specimens of this species from Antigua are con-
tained in the collection of the Geological Society, but they add
nothing to our knowledge of the species.

li. Isasrrma conFEeRTA, spec. nov. Pl. XIV. fig. 2.

Corallites very close, tall, slender, straight, and prismatic; a
transverse section shows me wall - be very thin. The breadth of
the corallites varies from ;3, to 1; inch. Septa very numerous,
linear ; the primary extend to the centre of the corallite, the second-
ary less so, and the others join the larger septa at a very acute angle ;
all are very slender and excessively crowded. There are eighty-two
septa in the larger corallites, sixty in the smaller. The septa of one
corallite do not join those of the next, but end sharply at the wall.
Endotheca plainly exists, linear, appearing, in transverse section, to
divide the interseptal loculi into several cells. The reproduction is
by submarginal budding. The sclerenchyma has been replaced by
dark homogeneous silica, and the interspaces by porcellanous and
opaline silica.

From the Chert-formation of Antigua. Coll. Geol. Soc.

This is a very remarkable form. Unfortunately no calices exist ;

1863. | DUNCAN—WEST INDIAN CORALS. 423

but the transverse yiew of the corallites is excellent. If the speci-
men had been found in Oolitic rocks, it would have passed for a small
variety of [sastreea tenwistriata.

12. IsastRHA TURBINATA, spec. noy. Pl. XIY. figs. la—le.

Corallum 7 inches high, subplane and irregularly convex above,
broad and gibbous at the sides, small and conical at the base, whence
the corallites radiate ; upper surface ridged with the elevated mar-
gins of more or less polygonal, close calices. Corallites very long,
slender, and prismatic, excessively crowded. Walls united, simple
throughout. Calices very numerous, irregularly pentagonal, not
deep, and not packed geometrically. Margins existing as sharp
ridges, not marked by the septa, but faintly ragged; united, crowded,
not deep. Septasmall, not exsert, not arched, but slanting irregularly
downwards and inwards, except the primary, which stand up in the
fossa, and are easily seen; they are laminar, delicate, and crowded,
shghtly toothed near the internal end, ragged above, and granular
on the sides. The primary septa sometimes meet by their inner
ends; the secondary and tertiary are subequal when there are
others. They are disposed in six systems. In fully developed
calices there are four cycles in four systems, and three in the rest ;
in other calices three cycles with an occasional fourth order; the
fourth cycle is very small. Septa straight, not crenulate, but slightly
ragged ; no external spines. Endotheca tolerably developed. From
the condition of the base, which has been rolled, no epitheea can be
seen. Reproduction by submarginal (close to the wall) gemmation.
Diameter of the calices from 2 lines to 34 lines.

From the Chert-formation of Antigua. Coll. Geol. Soe.

Fossilization very like that of Isastrcea oblonga in the British Port-
land Oolite.

The affinities of these two Corals with the Jsastree are not to be
mistaken; and their occurring in the Chert of Antigua, where they are
associated with the Miocene Asétrocenia ornata, is very remarkable.

13. STEPHANOCENIA TENUIS, spec. noy. Pl. XIV. figs. 3a, 36.

Corallites very long, slender, nearly straight, prismatic, and closely
approximated; sometimes less prismatic than cylindrical. Walls
thin. Calices wanting; but there are several polished sections of
the corallites which show a pentagonal or hexagonal outline ; occa-
sionally a circular outline is seen. Columella obscurely preserved,
but well enough to be recognized as styliform. Pali long, distinct,
like prolongations of the septa to the columella; opposed to all the
primary septa, and to the secondary where the third cycle is com-
plete. Septa delicate, straight, very little thicker at the wall than
elsewhere; slightly granular, and not crowded. They are disposed
in three cycles, the third being often wanting in some systems, or in
some half-systems, in imperfectly developed corallites. The primary
and secondary septa are nearly equal when the third cycle is com-
plete; the tertiary do not reach halfway to the columella, and are
straight. Reproduction by marginal budding.

424 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

Dimensions.—Diameter of the corallites from 1 line to 2 lines;
height several inches.

This species of Stephanocenia differs widely from the form from San
Domingo; and its distinct, thin, linear pali distinguish it from all
others. It has no other than a generic affinity with the depicted, but
not described, Stephanocenia tenwisepta of the late M. Haime.

From the Inclined Beds and the Chert of Antigua. Coll. Geol. Soc.

14, Maanprina, sp.

One specimen from the lower formation of Antigua is a semi-
polished silicified fossil, greatly affected by the destructive form of
silicification. A few transverse views of “series” enable me to
classify it with the Meandrine, but it presents structural peculiarities
which remove it from the recent forms and connect it with those
described as fossil. It does not come within the diagnosis of any
species as yet described.

Valleys moderately long, very flexuous, repeatedly branching at
nearly right angles. Columella sublamellar, deficient here and there
for a very slight interval. Septa alternately large and small, the first
extending close to the columella, presenting occasionally a slight
transverse enlargement at the end; all delicate and straight, there
being seven in a length of 1 line. Mural elevations (collines) small
and delicate. Breadth of the valleys =4, inch.

The recent Maandrine have a well-developed spongy columella,
but in the fossil forms that organ has a lamellar structure and is
more or less defective. The breadth of the valleys is, as a rule,
smaller in the fossil than in the recent species.

From the defective state of the fossil above described (Coll. Geol.
Soc.), no specific determination is possible, but its characters relate
to fossil more than to recent forms.

15. Ca@LoriA DENS-ELEPHANTIS, spec. nov. Pl. XIV. fig. 8.

Valleys long, very much disposed to be nearly straight, branching
rarely, and then at an acute angle, parallel, varying greatly in
width. The resemblance of transverse sections to the dental laminze
of Elephas is most remarkable. Length 1 inch; breadth from 2
to 3 lines. A columella is present as a few lamine, occasionally
continuous with the septa. Septa alternately thick and thin, with-
out pali or transverse enlargement, four or five to =}; inch. Endo-
theca abundant and at right angles to the septa. The mural eleva-
tions, so far as can be judged from a section, are small and delicate.

The specimen is an example of the variety of siliceous fossilization
where the interspaces are filled with porcellanous and opaline silica,
the sclerenchyma having lost much of its details and being turned
into homogeneous dark flint.

From the Chert-formation of Antigua. Coll. Geol. Soe.

16. AsTRORIA POLYGONALIS, spec. nov.* Pl. XIV. fig. 6.
Walls bearing a very small proportion to the size of the corallite (in
* In the Hist. Nat. des Corall., by Edwards and Haime, the genus Celoria

1863.) DUNCAN—WEST INDIAN CORALS. 425

transverse section). Calices polygonal, varying in size; many form
short series, but the simple corallite is in excess. Columella very
rudimentary. Septa long, thin, alternately large and small; they
are generally numerous, but in a small corallite they are few, and
resemble those of an Astrwa with a low septal number. A small un-
developed corallite gives six systems, two cycles in some and three
= other systems. Length of each series 9} lines; three septa to

1 inch; the width varies, from the ends of the series being pointed.
Width of the largest corallites not forming series 3 inch, of the
smallest 4 inch. Endotheca abundant and subvesicular.

From the Chert-formation of Antigua. Coll. Geol. Soc.

The lithological character of this specimen is very interesting, the
interspaces being filled with opalescent and opaque-white silica.

17. AsTRORIA AFFINIS, spec. nov.

Corallites crowded. Walls very thin indeed. Transverse section
of corallites polygonal, rarely forming short series. Columella shghtly
but decidedly developed. Septa alternately large and very small,
linear, a little larger externally, with at least four cycles in six
systems. Breadth of the calices 4 lines; five septa tol line. Endo-
theca abundant.

From the Chert-formation of Antigua. Coll. Geol. Soe.

The greater independence of the calices and the rare fissiparity
connect this species very closely with the Astreans. In some parti-
culars it is allied to A. astreiformis (a recent species inhabiting the
Red Sea); but that species has a rudimentary columella, only three
cycles of septa, and smaller corallites. It has greater affinities with
the species of Astroria just described than with any recent form.

18. Astror1A ANTIGUENSIS, spec. Nov.

Corallites not crowded, but close, tall. Walls rather thin. The
transverse section of the corallites is in many cases circular, in others
obscurely polygonal; some present short series, but rarely. Columella
very indistinct. Septa alternately large and small, in six systems of
four cycles, the fourth being occasionally deficient in two systems.
Breadth of the corallites from 2 to 34 lines. Length of the series
6 lines ; five septa to a line. Endotheca abundant.

Fossilization like that of the other Astrorians, and rendering the
details indistinct. It is closely allied to the other species of Astroria
from Antigua.

From the Chert-formation of Antigua. Coll. Geol. Soe.

19. Asrrocania ornata, Edwards & Haime. Pl. XIV. fig. 7.

This well-known Miocene species is found in the Chert-formation
of Antigua. The corallum is massive, in some cases most singularly
altered by fossilization, and presenting most abundant corallites ; the

absorbs Astroria (see vol. ii. p. 412). I have, however, retained the latter as a
distinct genus, as it certainly forms a connective link between the fissiparous
Astree and the Celorie, and a certain number of species group themselves
readily within the terms of its definition.

VOL, XIX.—PART I. 2G

426 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

ealices are a little smaller than in the European form, There is no
specific difference,
Coll, Geol. Soc. and Brit. Mus.

20. RaopAR#A IRREGULARIS, spec. Noy.

Corallum massive and tall. Corallites long, irregularly prismatic,
crowded, distinct ; diameter $ inch. Walls irregularly reticulate,
delicate. Septa in six systems of three cycles; sometimes a fourth
is seen; they are tolerably well developed and sublamellar. Pali
very distinct before the primary and secondary septa. Columella
formed by the junction of the pali.

The specimens are much altered by fossilization, but the struc-
tural details enumerated above are evident enough. ‘The species is
distinguished by the mass of pali and the presence of an incomplete
fourth cycle. There are no recent West Indian species of this genus,
those known being either Chinese or from New Holland; the fossil
form is from Dax (Miocene).

From the Marl-formation of Antigua. Coll. Geol. Soe.

21a, AtveoporA Dmpatms, Blainville, var. rEeuLARIS. Pl. XIV.
figs. 4a—4c¢.

Corallites prismatic, in all cases radiating from a small base, and
lobed above. Walls very regularly perforated and thin. Calices
a little smaller than the transverse sections of the corallites, rather
deformed, polygonal; 4 line in diameter. Septa spiculiform, and
forming a false columella by their junction with some slight cellular
trabecule.

From the Chert- and Marl-formations of Antigua. Coll. Geol. Soc.

216. Var. MINOR.
A small variety from the Chert of Antigua. Coll. Geol. Soc.

22, ALVEOPORA MICROSCOPICA, Spec. nov. Pl. XIV. fig. 5.

Corallites barely 54, inch in diameter, prismatic and hexagonal,
tall. Walls with reticulations, rendered less regular and equal than
in the above species by the rather wavy track of the large longitu-
dinal sclerenchymatous threads and by their irregular thickness.
Septa small, less spiniform than in other species; usually twelve in

number.
.From the Marl-formation of Antigua. Coll. Geol. Soc,

23. ALVEOPORA FENESTRATA, Dana.
In fronds. From the Marl-formation of Antigua. Coll. Geol. Soe.

II. San Domrneo.

1. Bracuycyataus HENnEKENI, spec. nov. Pl. XV. fig. 1.

The numerous small simple Corals considered to belong to this
Species are all young, and in examining them allowance must be
made for the rapid growth which takes place in their breadth after
a certain height has been attained. Corallum simple, straight, with

1863.] DUNCAN—WEST INDIAN CORALS. 427

a small circular base, conical below, cylindrical above, with a slight
enlargement below the calicular margin: no trace of adherence,
Coste distinct, very slightly prominent, blunt; those of the primary:
and secondary septa are visible to the base, being most preminent at
the calicular margin; at the enlargement they are ragged. The
tertiary coste resemble the primary and secendary when there are
higher orders of septa; but when there are not, they only extend a
little way from the calice, and are small. The fourth and fifth orders
of septa are continuous, with short and very small coste. Wall very
faintly granular. No epitheca nor exotheca. Calice circular ; its mar-
gins and axes are on even planes; fossa shallew. Columella large,
essential, presenting at the free surface numerous small, free, cylin-
drical, papillary elevations, the largest bemmg external, Pali very in-
distinct, and feebly developed. Septa crowded, in six systems of four
eycles; incomplete. Septa of the fourth and fifth orders wanting
in four half-systems; primary and secondary well developed and
equal, thin, and not larger at any part than at another; straight, but
slightly exsert and arched. Lamine marked with a few distinct and
prominent papille. The tertiary septa are larger when the higher
orders of septa are present, and resemble the secondary; but when
these are absent, they are like the fourth and fifth orders—linear,
rarely granular, and often bending laterally.

From the Nivajé shale. Coll. Geol. Soc.

Dimensions.— Height of the largest specimens equal to the breadth;
of the smaller greater than the breadth—from 1} to 7 inch. Itis
evident that, were the septal cycles complete, the breadth would in-
erease still more; and also that the growth of the coral is at first
in excess longitudinally, then transversely. The specimens are very
hard and calcareous.

One specimen with the larger coste more decidedly dentate supe-
riorly must be considered to constitute a variety of this species.

From the Nivajé shale. Coll. Geol. Soe.

The twelve specimens of this species which I examined presented
the above-mentioned structural details, except one, which was con-
sidered a variety. The breadth of the corals in their young stage,
their large papillose columella, and their small pali lead to their |
comparison with Brachycyathus Orbigryanus, Edwards & Haime;
nevertheless there is only a remote affinity. Their small pali and
undecided transverse development must be considered, with the de-
fective fourth cycle, as indicative of immaturity. The new forms
do not fall within any other generic definition, and the varying deve-
lopment of the pali in the Cenocyatht must be remembered before a
great value is placed on this peculiarity. The genus Brachycyathus
has hitherto included only one species, which is closely allied to the
shorter Cyathine. Duchassaing and Michelotti have formed the genus
Paterocyathus to admit a form which differs from Brachycyathus in
being turbinate, and having the upper part of the wall strongly
striated, the pali being in a simple crown. The specimen described*
by them came from the Upper Tertiary beds of Guadaloupe. If the

* Mem. Acad, Turin, 2nd series, 1861, vol. xix. p. 336. ES 5. on 11,
ce

428 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

turbinate shape does not depend upon the incomplete development
of the individual, the necessity for a new genus is evident; but in
the other characters this Paterocyathus Guadalupensis is closely allied
to the genus Brachycyathus. There is no reason for separating the
San Domingo forms from the genus Brachycyathus, but they con-
stitute a group not sufficiently resembling the species B. Orbig-
nyanus* to be placed in close alliance with it.

2. Puacocyatuus Barrerti, spec. nov. Pl. XVI. figs. la—le.

Varel.

A fragment of a simple corallum, with a curved lamellar columella
and with the pali destroyed, probably belongs to the same species as
the Jamaican form, page 437.

From Postrero. Brit. Mus.

Var. 2:

A variety with more rounded ends, less epitheca, and more distinet
coste than seen in the Jamaican form.

From Postrero. Brit. Mus.

3. TrocnocyatHus cornucopia, Edwards & Haime (Turbimolia cor-
nucopia, Michelin),
A specimen of this species from the San-Domingan shale is in the

British Museum, The species is common in the Vienna Basin and
at Tortona.

4, Pracorrocnus LonspaLer, spec. nov. Pl. XY. figs. 2a, 26.

Corallum simple, straight, compressed; surrounded by a delicate
but complete epitheca, through which the rounded, badly developed
coste can be seen. The epitheca is delicate and pellicular for nearly
halfway up the wall, where it presents a slight constriction ; it is
most dense above and below this constriction, and presents no other
folds. Coste numerous, very indistinct, except the two lateral ones,
which have a well-marked crest projecting like the cutwater of a
boat, and at first not following the line of the wall, but being car-
ried outwards and downwards, forming an angle, and then following
the line of the wall. The costae are most prominent at the angle,
and the crests diminish in width towards the basilar mark, and just
above this there is the appearance as if there had been a small spine.
The margins of the crests and the basilar mark form an angle quite
equal to a right angle. The basilar mark is distinct, but small, and
not eroded, though flat. Calice elliptical. The long axis is termi-
nated by the crested coste, and the widest part of the short axis
corresponds to a prominent part of the margin on each side. From
this prominent part the margin gradually slopes to the crested coste.
The plane of the long axis is thus lower than the short. The long
axis 1s exactly twice the length of the short one, excluding the
salient crests. Width of the calice 4} inch; length }inch. Fossa
large and moderately deep. Columella essential, long, free to but a
slight extent, formed of a thin vertical lamina with a rather arched,

* This species is found in the Neocomian (Hautes Alpes),

1863. ] DUNCAN—WEST INDIAN CORALS, 429

not dentate, upper border; it is perfect in a considerable part of
the specimen, and the sides of the lamina are finely granular. Septa
numerous and crowded, in six unequal systems. There are four
cycles in two systems, in two systems five, minus certain orders, and
in the remaining systems the fourth and fifth orders are wanting in
half of each system.

In 2 systems there are 8 septa =16
In 2 9 ” eee b ” =26
In 2 re > a 6, =12

D4 septa.

The primary, secondary, and tertiary septa are very much alike,
and project but little. They are all slightly arched, and rather
stouter nearer the wall than internally. They are faintly granular,
and their orders may be recognized with care. The septa of the
higher orders are very delicate; all correspond to faint coste, and
the primary septa at each extremity correspond with the large coste.
Height + inch.

From the Nivajé shale. Coll. Geol. Soc.

As aspecies of the Turbinolides without pali and with an epitheca,
this specimen might be considered a Flabellum closely allied to F. avi-
cula (Turin, Miocene); but the laminar columella places it in the
genus Placotrochus. Its compressed form, lateral crests, irregular
septal arrangement, small basilar spot, and angular calicular mar-
gins are very distinctive of the species. The basilar spot is not a
concave fracture, but a plane rupture as in Flabellum spinoswm.
The great angle formed by the coste is equally a peculiarity of the
genus Pabellum, and, close as Placotrochus is to that genus (differing
in the important laminar columella), the form from San Domingo con-
nects the two more intimately than the species Placotrochus levis and
Placotrochus Candeanus, both of which are recent, the first from the
Philippines, and the second from the Chinese Seas.

The alar cost and the small base of Placotrochus Lonsdale distin-
guish it from Placotrochus alveolus (Jamaica, Miocene). I have
named this beautiful little form after Mr. Lonsdale, who noticed the
existence of the genus in the Heneken Collection, in his brief sum-
mary of the San-Domingan fossil Corals already noticed.

5. FLABELLUM DUBIUM, spec. nov.

Corallum simple, in the form of a slightly compressed cone,
straight. Epitheca incomplete, pellicular. Base small and conical. A
mark of attachment is visible, there being two fractured appendices on
one side of the base, one of which corresponds to the long axis. Coste
not crested, none larger than the majority. The lines of the cost
at the ends of the long axis form less than a right angle, or about
70°, where they join at the base. Long axis about one-third longer
than the height of the corallum; length 11 inch. Length of the
short axis 1 inch ; its plane is a little higher than that of the long
axis. Calice elliptical ; fossa shallow at the sides, and deepening in
the middle. Septa rather exsert, delicate. Primary, secondary, and

430 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

tertiary septa of the same size. Lamine slender and granular. In
six systems of five cycles. Some septa appear to be united by their
inner extremities. Coste subequal, although the septa are alter-
nately large and small. Height 1 inch.

From the Nivajé shale.

In shape the corallum resembles that of Michelin’s Turbinolha
Japhetii ; but Flabellum dubiwm has not the dense septa of that
species, and is furnished with an epitheca. Flabellum Galapagense
and Flabellum crassum have alliances with it, especially the former.
Although, from the state of its fossilization, the anatomy of the ap-
pendices cannot be made out, still it is clear that there was never
any large mark of erosion. The specimen is shorter in relation to
the length of the long axis of the calice than is the case in F, Gala-
pagense, and the laminar granules are smaller; moreover the ends of
the septa are not very thick.

6. FLABELLUM, sp.

Several casts and portions of a large Flabellum are found in the
blue shale of San Domingo, but the specimens are all too incomplete
for specific determination.

7. THysaNus* corBIcuLA, gen. et spec. nov. Pl. XV. figs. 3a, 36.

Corallum simple, in the shape of an elliptical dish with a rounded
and ovoid base, fringed with granular ribs; apparently it was once
attached, but became free by the rupture of a lateral pedicel, the
erosion resulting from the separation remaining at one extremity.
The base is smooth, and has a central groove. The height is greatest
at the end marked by the erosion; and the base, as it recedes, ap-
proaches more or less the calicular margin. Epitheca imperfect,—
perfect in the lower half, wanting in a circular groove above it, and
again present for a small space above the groove on the portion of
the wall remote from the erosion,—smooth, not echinulate or gra-
nular, raised into slight ridges which are continuous with the coste.
The ridges radiate more or less from the eroded end, and the general
growth of the coral appears to start from this point, although the
elliptical form is perfect. Groove shallow. Erosion circular, rather
deep, ragged at the edges; it is situated above the epitheca, which
bounds its lower half, and is deeply grooved for a short space by it.
Wall hidden by the epitheca and cost; its general outline is more
convex near the erosion than elsewhere. Costee very distinct, exist-
ing as ridges when beneath the epitheca, and as prominent granu-
lated lamin in the rest of their course. The ridges pass in curves
from the part of the base nearest to the eroded end. The costz are
alternately large and small, those corresponding to the rudimentary
septa of the fifth cycle being very slight; but the coste of the other
cycles are very equal. The granulations are very marked, and are
very characteristic ; at regular intervals they swell out the costz,
a granule being developed on each side of the lamin and on the
free surface. These three irregular growths add to the swellings,

* Oicavos, a tassel, See also Thysani from Jamaica, p. 439.

1863.] DUNCAN—WEST INDIAN CORALS. 431

and render the intervals between them delicate and linear. Each
costa consists of alternate granular swellings and linear intervals,
being thus irregularly moniliform. The smaller coste present
smaller granulations. Intercostal dissepiments wanting. Calice
elliptical, margin broad, fossa very deep. Length to breadth as
16 to 10. Length 4 inch and =4,; breadth 4 inch. Depth of fossa
2 lines. Marginal surface on one plane. Septa well developed,
projecting upwards three-quarters of a line, boldly arched above,
ending in coste externally, but arched and irregularly prominent in
the fossa internally. They slope at last to the bottom. All the
septa have more or less a tendency to radiate from the eroded end.
Primary and secondary septa very much alike; the others are un-
equal, according to their orders, but the tertiary are a little smaller
than the secondary. Free septal margin strongly and regularly
granulated; sides of the lamine marked with rows of granulations
with sharp points, each row ending at the septal margin in one of
the swellings. Granulations very distinct on broken septa. No pali,
endotheca, nor synapticule. Septa in six systems of five cycles; in
all ninety-six septa. Columella badly developed, parietal, consisting
of a lax tissue reaching from the septa to those on each side; it is
situated at the bottom of the fossa.

The species under examination is one of the Yurbinolides, as
there are no pali; it is deficient in endotheca, open from the base of
the fossa upwards, and has a dense wall; the epitheca is tolerably
developed. Coming thus under the division of epithecal Turbino-
lides, it is associated with Flabellum, Rhizotrochus, Placotrochus, and
Blastotrochus.

Blastotrochus is distinguished from the other genera by its gem-
miparous reproduction ; it is moreover cylindroid. Placotrochus has
a laminar columella. Flabellum has non-projecting septa, and costae
crested, spined, and covered by epitheca. This last genus only re-
sembles the new form in its species having more or less granular
septa, a parietal and badly developed columella, and a high septal
number. ‘The elliptical calice of Rhizotrochus, as well as the arched
and prominent septa and deep fossa of that genus, are found in the
new form, Allied thus to Flabellum and Rhizotrochus, the genus
Thysanus is distinguished by its lateral erosion, highly granular
cost, incomplete epitheca, grooved base, and elliptical and depressed
shape.

From the Nivajé shale. Coll. Geol. Soe.

8. BARYsMILIA INTERMEDIA, spec. noy. Pl. XV. fig. 4.

Corallum with the trunk irregularly cylindrical, the spot of former
adhesion being smaller than the diameter of the trunk, which has
some undeveloped calices on its surface. Head convex and closely
covered with calices, whose long axis is in no definite direction.
Calices crowded, tolerably elevated above the surface, elliptical and
circular, forming series of not more than three, by fissiparity ; lateral
margin of some calices higher than others. Fossa tolerably deep.
Septa barely exsert, slightly arched inwards, granular on their faces ;

432 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

in six systems of four cycles, generally incomplete in some half-
systems. The primary septa are the largest; the fourth and fifth
orders are very small. Columellarudimentary. Coste very marked,
subplane, alternately large and small, reaching down the trunk; near
the calices they are marked by a series of distant papillary elevations,
with a small and superficial foramen at their apices. Height of
corallum 2 inches; small diameter of calices 2 inch.

This species is closely allied to Bara ysmilia tuberosa, Reuss, from
Gosau, and the genus has not hitherto been noticed out of the Creta-
ceous group.

From the shale at Esperanza, San Domingo. Coll. Geol. Soc.

9. DicHoca@nia TUBEROSA, spec. nov. Pl. XV. figs. 5a, 56.

Corallum tuber-shaped, with a circular or oval eroded base, and a
more or less gibbous surface, covered with a delicate epitheca and
numerous calices. Calices numerous, rather close, decidedly promi-
nent, the lower edge generally longer than the upper. The calices
look generally upwards and outwards; they are either circular and
small or elliptical and larger; in the largest form, series of two or
three are produced in the process of fissiparous reproduction. The
long axes of the calices point in all directions; some small calices
are hidden by the epitheca. Coste well marked on the calice, but
becoming granular and slightly spined on the surface of the Coral: a
shagreen-looking epitheca, which, when broken, shows linear costz
beneath, separates the calices. The costal markings on the epi-
theca are now and then continuous from one ecalice to another, and
from calices to the base. Septa in six systems; four cycles in some
systems, three in others; the fourth orders are often wanting. They
are delicate, a little larger at the wall than elsewhere, and faintly
granular. Columella laminar, parietal, or spongy in different calices.
Pali exist very irregularly ; they are placed very constantly before
the secondary septa, but are often not ae a all. Calicular fossze
tolerably deep. Diameter of the calices =3,, 2, to 2 inch. The Coral
is generally some inches high, and bulky.

No fossil species of this genus have been described, except a doubt-
ful form, to which Milne-Edwards gives a Lower Cretaceous age.

From the Nivajé shale and tufaceous lmestone of San Domingo,
Coll. Geol. Soc. and Brit. Mus.

10. SrePHANOC@HNIA DENDROIDEA, Edwards & Haime, Hist. Nat. des
Polyp. &c., p. 169.

Edwards and Haime give no habitat for this form ; but the ramose
species of Stephanocenia, common in the Miocene of San Domingo,
is evidently the same.

11. Puyriocentra scunpta, Edwards & Haime, var. TEGULA.

Astrea sculpta, Michelin.

A thin, flat, tile-shaped Coral from San Domingo corresponds with
the Astrea sculpta, Michelin (the Phylloceenia sculpta, Kdwards &
Haime), in the majority of its details. The cost are not so decidedly

1863. | | DUNCAN—WEST INDIAN CORALS, 433

granular, the septa less equal, and the calices not quite so elevated
(little as they are) as in the form depicted by Michelin (Zooph. pl. 71.
fig. 3) and described by Edwards and Haime (Recherches, p. 304).
There is not, however, a specific difference between the San-Domingan
form and that from Martigues. It is with doubt that Edwards and
Haime call this a Phyllocenia, and certainly the San-Domingan form
has some very strong Eusmilian features, and one very indecisive
Astrean peculiarity. Diameter of the calices hardly }inch. Height
of the coral from 2 to 2 inch.
From the Nivajé shale. Coll. Geol. Soe.

12, PHYLLOC@NIA LIMBATA, spec. Nov.

Corallum in the shape of Stylina limbata, Edwards & Haime.
Stem large and cylindrical. Corallites numerous, irregularly placed.
Calices separated by much coenenchyma, circular and but slightly
elevated. Coste covering much surface, slightly dentate where they
approach, and turning aside from those of other calices; they are
not continuous, not very prominent, and slightly granular. Septa
not projecting far inwards, lamine granular; their upper margin is
neither incised nor dentate ; In six systems of generally three cycles,
though occasionally of four. Primary septa largest. Columella rudi-
mentary. Endotheca abundant. Diameter of calice, with coste,
1 inch.

° ‘The deficient columella is the only point in which this species
differs from Madrepora limbata, Goldfuss, which has been determined
by Milne-Edwards to be a Stylina.

From the yellow shale of San Domingo. Coll. Geol. Soc.

13. Monrrivatrra ponperosa, Edwards & Haime. Pl. XVI. figs. 6a, 66,

Thecophyllia ponderosa, Edwards & Haime.
Turbinolia Deucalioms, Duchassaing.

From the shales of St. Domingo. Brit. Mus. Guadaloupe and Ja-
maica; also Travancore in Southern India. Coll. Geol. Soc.

The description of this great Coral, whose synonyms have arisen
from the description of defective specimens, is given with the Ja-
maican Corals, p. 441. It is to be noticed that the San-Domingan
specimens are young, but are better preserved than that drawn by
Milne-Edwards in the plates of the ‘ Hist. Nat. des Corall.’ I have
also examined a specimen from Travancore.

14. Mmanprina FILoGRANA, Lamarck.

A figure of this Coral was given by Michelin (Zooph. pl. 14. fig. 7),
and described as a Supracretaceous fossil. Milne-Edwards and
Haime add to the above notice that the specimen is not a fossil. The
species is Hast Indian; and if the Madrepora filograna (Ksper,
Pflanz. t. 1. p. 139, pl. 22, 1791) be received as a Meandrina, there
is proof of a West Indian habitat.

From the San-Domingan shale (Coll. Geol. Soc.) ; recent in the
East Indian and American seas.

434 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

15, AstR#A ENDOTHECATA, spec. nov. Pl. XV. figs. 7a, 7 6.

An Astrean, characterized by large corallites, great development
of the coste and exotheca, as well as of the endotheca, and by the
delicate and numerous septa. Varieties are found in the Lower
Calcareous beds (Marl) of Antigua very closely allied to this form.

Corallum tall, subplane above. Corallites tall, stout, cylindrical ;
a little wavy in their course, slightly enlarged here and there; close,
but not crowded, separated occasionally by buds, which speedily be-
come as large as the parent corallite. Wall well developed, strong.
Calices rather irregular in size, irregular in their mutual distances,
and unequally elevated above the surface; not much elevated,
but still decidedly so, like truncated cones; margin thin ; external
surface of the calices inclined, and marked by the coste and oblique
dissepiments. These dissepiments have often a granular tooth, and,
when broken through, a corresponding dissepiment with a tooth
is seen below. Septa delicate, barely exsert, straight, granular ;
in six systems of four cycles, the higher orders being but slightly
developed. Coste largely developed, those belonging to the fourth
and fifth orders of septa being smaller, and hidden between the
large coste on each side; they have, moreover, a papillary-looking
tooth between each dissepiment. On the calicular surface the costee
are small and slightly dentate. Columella well developed, formed
of lax trabecule. Endotheca greatly developed, close, vesicular,
and separating the interseptal loculi into cells ; it closes the shallow
calicular fossa, leaving afew foramina. Exotheca greatly developed ;
dissepiments stout, inclined forwards and downwards, arched; on
each dissepiment is the tooth of the fourth cycle. No epitheca,
Increase by extracalicular gemmation. Diameter of the calices 2 inch,
of the corallites a little more. Exothecal cells three in =), inch.

This fine Astreean is not to be identified with any known species ;
its endothecal development is extraordinary, and connects it with
the Astreans from Antigua possessing much endotheca. It is worthy
of notice that the European Miocene Astreeans are generally charac-
terized by having much vesicular endotheca,

From the Nivajé shale of San Domingo; varieties in Antigua and
Persia.

16. AsTR#A CYLINDRICA, spec. nov. Pl. XV. fig. 8.

Corallum flat; surface irregular, nearly plane in large specimens ;
marked by prominent truncated cones (ends of corallites), with
very projecting and somewhat irregular coste. Corallites wide
apart, short, from 11 to 24 inches long, cylindrical, more or less
parallel, becoming sensibly smaller close to the calice, projecting
considerably (from 3 to 4 inch) above the common ccenenchyma ;
often twisted inferiorly, and swollen out'‘in certain parts. Walls
very well developed, stouter below than above. Costs forming a
marked structure; very slightly developed at the immediate calicular
margin, they are soon considerably and often irregularly produced in
some corallites, while in others they form thin, well-developed, sub-

1863. ] DUNCAN—-WEST INDIAN CORALS, 435

equal, more or less dentate projections, the small, dentate fourth and
fifth orders being here and there seen as rudimentary coste between
the larger. The tallest corallites have subequal and regular costae,
and the smaller corallites usually have them irregular and produced,
whilst those whose calices reach but a little above the coenenchyma
have their cost produced on its surface. The small and rudi-
mentary cost correspond to septa. Calices as truncated cones with
small blunt apertures, rather wide apart, from 3 to 4 inch high, cir-
cular at the margin, which is rather inverted; itis also much less in
diameter than the corallite with its costee. Fossa shallow in some, and
about as deep as broad in others. Columella lax, parietal, and well
developed. Septa small, unequal, and much smaller than their
cost, barely exsert, rounded at the margin, and there a little larger
than elsewhere; delicate and linear within; in six systems of
usually three cycles, rarely four, occasionally the fourth cycle in half
a system; the primary septa are generally the largest, the higher
- orders are very small, and the fourth and fifth orders often incline to
the tertiary septa. The lamine are delicate, not cribriform, but per-
forated now and then, and join the columella by numerous close,
slightly ascending, oblique dissepiments; they are slightly dentate,
and unequally granulated laterally. Endotheca but little deve-
loped. Exotheca close, abundant, and shelving outwards ; it is very
distinct on some of the produced coste. Epitheca none. Exothecal
dissepiments four or five in 4, inch. Diameter of the calices from
+ to =3, inch. In large specimens, here and there, the coste are
produced to 51, inch.

From the tufaceous limestone of San Domingo. Coll. Geol. Soc.

The smaller specimens of this species consist of a few corallites,
and the larger of tabular masses. The budding is always extra-cali-
cular. The truncated extremities of the cylindrical short corallites,
the small, dentate, rudimentary coste, and the production of the
larger cost distinguish this species. There are some points of re-
semblance to Astrwa cavernosa (recent, Antilles), Astrea Forskelana
(recent and subfossil, Egypt and West Indies), and to Astrea De-
francu (Miocene).

17. SIDERASTRHA CRENULATA, Blainyille, var. ANTIZLLARUM.

An incrusting Coral, very short, with a slightly convex and gib-
bous surface. It resembles Siderastrea crenulata in all particulars,
except in having a less deep calicular fossa, and the crenulations of
the septa most marked near the papillary columella. The septa of
the fourth and fifth orders turn towards and join that between them
at various distances from the columella, and often the fourth orders
appear longer than they really are. Diameter of the calices 4 inch;
depth of fossa =, inch.

Its nearest living species is Siderastrea siderea of the Antilles,
and it is distant from the other American forms.

From the Nivajé shale of San Domingo (Coll. Geol. Soc.). It occurs
also in the Miocene of Europe.

436 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

18, CYPHASTR#A COSTATA, spec. Nov.

This species is found also at Barbuda and Jamaica (see Barbuda,
page 443).

From the Nivajé shale. Coll. Geol. Soc.

19 a. StYLoPHORA AFFINIS, spec. noy. Pl. XVI. fig. 4.

Corallum branched, large; branches nearly cylindrical, leaving
the stem at an acute angle, slightly flattened on one side. The
largest stem is #inch in diameter. Blunt, aborted, branch-like
swellings exist on some of the larger stems. Corallites radiating
from the centre of the stem and branches, separated by about their
own width of dense coenenchyma, which is seen, in the larger speci-
mens, to be very slightly cellular. Walls not distinguishable from
the ccenenchyma in the substance of the mass, but slightly raised
into a very shallow crateriform edge on the surface. Calices cir-
cular, a very little raised as crateriform elevations, very numerous,
disposed irregularly, but very nearly equidistant in some places and
less so in others; margins sharp. Diameter =), inch, rarely larger.
The calicular margin, when well preserved, looks like a little ring
placed on the intercalicular space, and the small styliform columella
renders the appearance very distinct. Intercalicular spaces marked
by’a continuous and ridged line, which, being in the part of the
spaces at the base of the calicular elevations, and being continued
round each calice, is, from its general straightness, formed into irre-
gular polygons. The line is sensibly raised, convex, and now and
then dentated. Between the line and the calicular margin there are
distinct papille, one row at the very marginal edge, the other corre-
sponding to it a little lower down the calicular wall; a third is some-
times seen ; and in places where there is an unusual distance between
the calices, and when the “line” is wanting, the papille are nu-
merous, distinct, and a little smaller. The line and the papille form
a very marked distinction. Between some calices there are faint
elevations. Septa whole, not exsert, but little visible in perfect
calices, but very distinct when the coral is worn. Upper margin
perfect, and concave upwards, the septa appearing festooned to the
columella; they are delicate, very little thicker at the wall than
elsewhere, and join the columella high up near its point. The papille
at the calicular edge extend a little on the wall, and may be con-
sidered as rudimentary septa and coste; if so, there is a second
cycle, and also a third in half of each system. ‘The persistence of
six septa, nearly all of the same size, is very remarkable. Columella
styliform, large and dense in the corallite, and forming a rounded-off
cylinder with a sharpish rounded tip, which is very distinct halfway
down the calice. Calicular fossa shallow, about half as deep as broad.
Endothecal dissepiments stout, transverse, numerous. The walls and
columella do not fill up the lower parts of the corallites. Increase
by extracalicular gemmation.

From the Nivajé shale Coll. Geol. Soe.

196. Var. mrnor.
A portion of a branched Stylophora in a mass of shell- and coral-

1863. | DUNCAN—WEST INDIAN CORALS. 437

breccia from the Nivajé shale differs from the typical form of S.
affinis by haying its calices much wider apart, and consequently by
having moreccenenchyma. It is asmall form; the calices are about
the same size as those of the larger variety, where, however, they
are closer together.

This new species and its variety are closely allied to Stylophora
costulata, Edwards & Haime, from Gaas (Miocene), and less so to
Stylophora raristella (Dax and Turin). In some very large specimens
there are irregular gibbosities, like truncated shoots, from the main
stem; and the Jamaican specimens often present this form of coral-
lum in small branches. The imperfect septal development and de-
fective costal arrangement distinguish the new species from S. costu-
lata, but still the alliance is very close. Apaxt from the form of the
coral, there is much resemblance to Stylophora palmata (recent, Red
Sea). The fossil forms are from La Palarea, Scinde, Biarritz, Dax,
Turin, Vienna, Belforte, and Gaas.

20. Acaricra agaRiciTes, Lamarck.

Three fragments of one specimen are of this species, which now
exists in the American seas. The Coral is known under various
generic synonyms, such as Pavonia, Madrepora, &c. It is remarkable
that dissepiments clearly exist in the interseptal loculi of these speci-
mens, as well as synapticule.

From the Nivajée shale. Coll. Geol. Soc.

21. Agaricia unpata, Lamarck, var.

A fragment imbedded in Nivajé shale, with pieces of one of the
Turbinolides and of a Stylophora. It is more closely identical with
A. undata than with any other form; the slanting calices and the
inferior surface unequally costated are very characteristic of that
species. At the same time the specimen has more septa and closer
‘ collines ” than the typical A. wndata, and it presents many resem-
blances to forms of the genus Mycedia. Both Agaricia and Mycedia
are found in the existing American seas.

From the Nivaje shale. Coll. Geol. Soc.

22. ALVEOPORA- FENESTRATA, Dana.
This fossil is from the Heneken Collection, and coincides with the
description of A. fenestrata by Edwards and Haime (see descriptions

of fossil Alveopore from Antigua and Jamaica, pp. 426 & 442).
From the Nivajé shale. Coll. Geol. Soc.

23. Porrres CortEentana, Michelin.
Occurs in the Nivajé shale in a Coral-breccia. Coll. Geol. Soe.
It is also found in the Vienna Basin (Reuss).

II. Jamaica.

1. Pracocyatuus Barrerri, spec. nov. Pl. XVI. figs. 1 a—le.
Corallum simple, elongated, greatly compressed, the small axis of
the calice being to the large as 100 to 366 ; conical and pedunculated,

438 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

the lower part of the base being curved in the direction of the great
axis ; pedicel very slender. Epitheca well developed, pellicular, and
permitting the costs to be seen ; it is in more or less transverse wavy
ridges, and it ceases two or three lines below,the horizontal calicular
margin. Wall very thick and dense. Coste: the larger are all nearly
equal; the smaller correspond with the rudimentary septa, and are
continued down between the larger, gradually merging into a row of
rounded granules as the epitheca covers them: the larger are to be
traced more or less to the pedicel; they project but little at the cali-
cular margin, and are rounded; where the epitheca commences they
become flatter, and are sparsely granular, the granules being really
dentations in one series; shortly, however, the granular appearance
is lost, and a ridged farm is seen, some of the lateral costee evidently
uniting with others a little above the pedicel; they are close, but
not crowded ; many are parallel, and never crested nor sharply spined.
Calice with its margins a little sinuous, very long, narrow, and a
little curved, the long axis on the same plane as the short. Fossa
deep and narrow. Septa very numerous, barely exsert, rounded at
the wall, and a little thicker there than elsewhere; often a little
curved, extending well inwards. Except the rudimentary septa,
which correspond to the short cost, the septa are subequal, and the
principal are not easily recognized; generally one is large, and the
next smaller; they are rounded above, and are nearly perpendicular
at their inner margin; free margin not incised; lamelle granular.
The granules, which are conical and large, form linear series, which
are directed from below inwards and upwards. Septa in six systems
of at least six cycles. There are forty-three septa to an inch. Colu-
mella essential, lamellar, attached to the septa by trabecule passing
at right angles from it; its surface is very long, and it probably was
sharp; above the free surface there is a deep, linear, calicular fossa.
Pali as delicate rounded lobes, barely to be recognized, attached to
the usual lamine ; the granules of the pali form series parallel to
their circular outline. Endotheca none. Height 13 inch; length of
calice 33 inches; breadth 9 lines; depth of fossa 4 lines, of inter-
septal locul much more.

This interesting simple Coral was discovered in Jamaica by the
late Mr. Barrett, with whose memory I associate it.

Jamaica; varieties in San Domingo. Brit. Mus.

2. PLAcoTROCHUS ALVEOLUS, spec. nov. Pl. XVI. figs. 2a, 2b.

Corallum simple, very long, low, and narrow; trough-shaped,
rounded at the extremities, by one of which it was attached; trans-
verse outline triangular. Wall very thick, stout at the calicular
margin, covered close up to this by a dense epitheca, which shows
traces of the cost tolerably distinctly above, where they are repre-
sented by a series of granules, and less so below, where they are
simple elevations on the wall; all the granules are microscopic.
Sides of the wall more or less wavy. Between the semicircular
margin of the calicular end and the base there is a cireular hole
with irregular and rounded lips—the “erosion.” This lateral

1863. ] DUNCAN—WEST INDIAN CORALS, 439

wound is evidence of a former appendicular attachment. Calice very
long, gutter-shaped, on an even plane; margin very narrow, slightly
elevated at the extremity, and compressed a little here and there.
Septa very numerous, sixty to one inch; primary, secondary, and
tertiary nearly equal; very delicate, rounded above, finely granu-
lated, and barely exsert at the wall; the small septa which extend
well inwards are numerous, and a large septum is succeeded by one
of these, then a middle-sized one follows. Inner margins very de-
licate, rounded, and separated from those opposite by the space which
leads down to the columella. Coste indistinct, parallel. Columella
essential, lamelliform, free, sharp, very long and continuous, joining
the septa (out of sight) by trabecule. Length (fractured specimen)
2 inches 4 lines; breadth 6 lines; height 4 inch.

A Coral of unique shape. It is very different from the other
species of the genus, but its columella and its deficiency of pali and
endotheca prove it to be a form of Placotrochus.

3. THYSANUS EXCENTRIcUS, gen.etspec.noy. Pl. XVI. figs. 3a-3e.

Five specimens of a simple Coral (Nos. 1-5), in the British
Museum, very unusual in shape, and all specifically related, have
the following characters. The description is taken from No. 1, a
young individual.

Corallum simple, resembling in shape a half-folded ovate leaf, the
lobes of whose base are joined, the petiolar junction being still evi-
dent. There are three angles to the corallum:—1. An inferior and
anterior angle which projects forwards and obliquely downwards (the
petiole of a leaf would be attached here). 2. A superior and anterior
angle, which is immediately above the first, and is connected to it
by a linear and concave furrow ; it is situated at the anterior rounded
overlapping margin of the calice, and this margin forms the base of
a triangle, of which the inferior angle is the apex. A lateral view
shows a curve between the calicular end and the pointed inferior angle.
3. A posterior angle is produced by a curved line passing backwards
and downwards from the first angle, which joins the posterior calicular
end, and forms a gutter-like extremity. The line from the first to
the third angle is the base in the ordinary sense ; this base is linear,
and is marked by a rounded shallow keel. There is an erosion or
spot in some specimens, where the corals were once attached, imme-
diately above the first angle. There is a general curve of the re-
ceding lines to the left, and the corallum is gently twisted in that
direction. The width of the corallum in front and above is greater than
at any other part, and it becomes narrower towards the third angle.
The width of the calice is very small in comparison with its length.

Corallum narrow and long, low, and generally triangular, present-
ing the appearance as if the anterior end were the original turbinate
coral, which has since grown posteriorly only. Wall well developed,
imperforate, marked anteriorly by a curved linear furrow and traces
of an erosion—the mark of an appendicular process. Epitheca exists,
very rudimentary, but is visible around the first angle and close to
the erosion, Calice long, narrow, slightly curved, wider in front,

440 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

where it is more rounded than behind, being there sharply oval.
Lateral plane higher than the antero-posterior. Fossa tolerably deep.
Furrow between the free ends of the septa very distinct. Margins
slightly everted, thin, and a little irregular. Coste very numerous,
very regular, faintly yet decidedly prominent, sharply dentate, the
dentations being delicate and numerous. Costal curves very elegant.
The keel between the first and third angles is really a costa, and all
the coste have a relation to it, passing off from it at acute angles, very
much as the veins of some leaves pass off from the midrib. One large
costa is usually followed by a very much smaller one. Septa numerous,
corresponding to the cost, hardly exsert, but the larger are more so
than the smaller. Laminze rounded above and within, not incised,
regularly granular, in series; a little thicker at the wall, but some
are enlarged internally. Size of the septa very irregular ; anteriorly
two large septa join at the wall, and posteriorly all the septa have an
eccentric relation to the centre of the curve formed by the anterior
calicular margin; they do not pass from the wall at right angles.
Apparently there are many systems of four cycles each, and there
are 132 great and small septa. Columella situated very deep in the
coral, parietal and rudimentary. Endotheca and exotheca none.

Dimensions.—Height of corallum between the first and second
angles t inch; length of base between the first and third angles
2 inch; length of calice a little more than 2 inch; breadth of calice
33) inch.

No. 2. An older individual, stouter, and more marked by an
erosion. Calicular fossa deep.

No. 3. A large specimen, more fully developed, but deficient in
its calicular margin. It is taller, but still keeps the peculiar form
of the species. Coste less sharply but well toothed. Mark of
erosion very visible. Septa larger, and the inner paliform enlarge-
ment very evident on many. Septa 140. Columella more deve-
loped.

The specimens 4 & 5 are fragmentary.

These corals resemble a produced Ceratotrochus, if such a varia-
tion in form could occur. The lateral or rather the anterior erosion
is seen in Thysanus corbicula from San Domingo. The absence of
endotheca proves that they are not young buds of such a genus as
Rhipidogyra, and includes them amongst the Turbinolides. The
eccentric distribution of cost and septa is faintly seen in a fossil
from the chalk-marl of Lemburg—Turbinoha galeriformis, Kner (a
Ceratotrochus). The more or less transverse ends of the larger
septa are very peculiar, as is also the existence of a small amount
of epitheca.

The Thysani have, in common, an eccentric arrangement of the
septa and coste, a lateral erosion, a badly developed epitheca, and a
parietal columella.

4, ASTROCHNIA DECAPHYLLA, Edwards & Haime, var.

In the form of a short stunted branch. From the Tertiaries of
Jamaica; Lower Cretaceous of Europe. Brit. Mus.

1863.] -- DUNCAN—WESI INDIAN CORALS, © 441

5, SIDERASTR#A GRANDIs, spec. nov. . Pl. XVI. figs. 5a, 5.

Corallum many inches high ; no calicular surfaces are left. Coral-
lites very tall, slender, crowded, and polygonal. Septa crowded, in
six systems of four cycles ; the fourth and fifth orders curve to the
larger, and the third to the second also; there are three rows of large
granules on the lamin near the wall, also traces of endotheca; the
free edge of the secondary septa is beautifully dentate; transverse,
granular, synapticular processes well developed. Columella tolerably
developed. The height of the corallum and the slender corallites
distinguish the species, Corallites not more than 23 lines broad, and
generally less.

Coll. Brit. Mus.

6. CYPHASTRMA COSTATA, Spec. Nov,

A specimen specifically the same as the forms found fossil at
Barbuda and San Domingo. It presents a great development of the
endotheca; its fossilization is more complete than that of the others.

7. MonvtiivaLtia ponpERosA, Edwards & Haime. Pl. XVI. figs. 6a,

A large, simple, heavy Coral. It is short, plano-convex, and sub-
elliptical. Below the calice it is conico-convex; laterally it is
slightly constricted. It has been free, and there are the remains of
a small tubercle-like pedicel, quite in the centre of the base, towards
which faint coste radiate. Epitheca well developed, thin in some
parts, thicker in others, and here and there not reaching as far as
the top of the wall; it is very generally perforated by circular
foramina, Coste seen more or less distinctly through the epitheca,
but never very well; they are marked by distinct but weak strie,
the epitheca being thickened and ridged between them, and they
are sharply spined, the points often coming through the epitheca,
Calice longer than broad, subelliptical; ends rounded; sides less so,
and in their middle either straight or incurved. Margin not entirely
on the same plane; that of the long axis is a little lower than
that of the transverse. Wall well developed at the margin. Calicular
fossa very shallow, especially if the central elliptical depression be not
considered. The fractured specimen (No. 2) proves the mass which
forms the floor of the central depression to be a flat and dense colu-
mella, formed by tortuous ascending trabecule. It is quite possible
to consider the flat or slightly concave surface of the depression the
floor of the coral, but this is not really the case. The columella is
essential and spongy. Septa very numerous, crowded here and
there ; primary, secondary, and tertiary nearly alike; in six systems of
six cycles, but the higher orders are not developed in all the systems,
The primary septa project upwards from the wall for 2 lines, and the
higher orders do not project much. The lateral (external) projection
is but slight, and the coste project but little from the wall. Septal
margin rounded near the wall, then spined or acutely serrate; it
inclines gradually, and the inner end is usually but little lower than
the outer. Septa thin, often a little curved; their inner end is per-

VOL, XIX,—PART I. 25

442 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [May 6,

pendicular in the largest; their base appears to rest on the colu-
mella, and the upper corner is very angular and free, Lamine
marked by distinct rows of granules, which are less developed in-
ternally and inferiorly. The septa are thicker at the wall than
elsewhere. Endotheca not to be distinguished except in fractured
specimens, but it is well developed. Exotheca represented here and
there by a few dissepiments. Height of corallite 11 inch, length 3}
inches, breadth 23 inches ; length of columella 1 inch 1 line, breadth
4 lines, height 1 inch; height of septal edge above the columella
os lines.

“A younger specimen has the corallum very short, and more con-
vex than the other, also shield-shaped below, and the central pro-
jecting boss, like a pedicel, Epitheca tolerably developed. Calice
less elliptical; sides more curved, and the plane of the short axis
higher than in the larger specimen, Fossa a little deeper. Septa
more acutely and slenderly spined, as well as the coste ; some spines of
the septa are very straight and sharp, all are slender ; in six systems of
five cycles. Columella as in the large specimen, very distinctly sepa-
rated from the wall. Exotheca barely a trace. Length of corallum
1 inch 8 lines, breadth 1 inch 5 lines, height 8 lines without the boss.

The close affinities of the genera Caryophyllia (Lithophyllia)*, Cor-
cophyllia, and Montlivaltia account for the synonyms of this great
simple Coral. If the central fossa had its foundation on the base of
the coral-wall, and if the septa had met internally, as they usually
do in Astreans without columelle, there would have been no dif-
ficulty in classifying the species amongst the Montlivaltiw ; but it is
by no means improbable that a genus will have to be determined
which will admit these simple corals with a columella and an epi-
theca, especially as new forms are presenting themselves daily for
examination, I have noticed a young C, ponderosa amongst some
Miocene fossils from Travancore, and, therefore, it occurs in the Ter-
tiaries of Postrero, San Domingo, and of Jamaica, and also in the
Miocene of Guadaloupe and Travancore.

Coll. Geol. Soc. and Brit. Mus.

8. AstRmINA DENDROIDEA, gen. et spec.?

A dendroid Astrean, multiplying by fissiparity, and forming a
bush-lke mass, but taller than broad; it is much altered by fossiliza-
tion, all the details, except the general shape and the walls, having

been destroyed.
9. AtyEoporA DmpALmA, var, REGULARIS. Pl. XIV. figs. 4a, 40.
From hard white limestone, in the form of casts, as at Antigua.

10. Poxrrss,

Several specimens of casts of a massive Porites from the limestone ;
the details, except the reticulations, are destroyed.

* The term-Caryophyllia has been applied by Edwards and Haime (Hist.
Nat. des Corall.) to the forms previously comprehended under the well-known
generic term Cyathina, and the former Caryophyllians are termed Lithophyllia.
I retain, however, the older and generally recetved nomenclature.

1863. ] DUNCAN—WEST INDIAN CORALS, 443

IV. Montserrat.

1. AstR=A ANTILLARUM, spec. noy.

A specimen in the form of a rolled flint, found with silicified Wood,
has the corallum large, tall, probably resembling in shape that of
the San-Domingan A. eaothecata. Corallites close, unequal in size, but
quite distinct ; the transverse section shows them to be circular in
outline. Septa in six systems of three cycles. The primary and
secondary septa are nearly equal, and reach to the columella; the
tertiary are small and straight; all are slender, wide apart, and very
distinct. Coste tolerably developed, subequal. Walls moderately
developed, by no means strong. Columella small, and occupying a
small space. Endotheca greatly developed, vesicular, and forming
cells between the septa. Exotheca well developed ; large cells broad,
others squarer, with shelving dissepiments. Diameter of the coral-
lites 53, inch.

_ The interspaces are filled with opalescent or porcellanous silica ;
sclerenchyma often destroyed.

Coll. Geol. Soc.

VY. Barsupa.

1. CYPHASTRHA COSTATA, Spec. Nov.

Corallum large, compound, with a large base; very hard. Coral-
lites long, slender, numerous, close, but distinct, except at certain
points; converging from the wide base towards a subplane, slightly
gibbous, and irregular surface. Walls very dense, generally in-
creasing in density and thickness as they become more remote from
the calices; in some places the walls encroach upon the exothecal
space, and the corallites are joined by their walls, a dense structure
being formed. Wherever the walls become thicker, it is at the ex-
pense of the intercorallite space, and not of the interseptal loculi.
Walls thin at the calicular margin. Coste well developed, and
forming with the exotheca a very marked structure; at the calicular
margin they project a little upwards, are a little dentate, and
slightly prominent along the outer slope of the truncated calicular
elevation. They correspond to the septa in number, the primary
and secondary coste being but little larger than the tertiary. They
are not crowded, but have a deep fossa between them, are not con-
tinuous with those of other calices, but are frequently irregularly
projected, and often touch. In longitudinal sections they are crossed
by dissepiments regularly during their whole course; their edge is
not simply linear, but each costa presents a series of wedges placed
one over the other, the thin end of one wedge resting on the thick
end of that below it, the dissepiment intervening. The dissepi-
ments project beyond the costal edge, and render it irregular;
they are absorbed now and then by the development of the walls.
Calices circular, forming low truncated cones; they are well sepa-
rated from each other, and frequently, where four meet, a consider-

able space exists. Calicular edge sharp. Fossavery shallow. Colu-
2H 2

444 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

mella largely developed, consisting of.nearly horizontal trabeculee
from the lace-like septa, and of its special tissue. Tissue spongy,
filling up much of the lower part of the calice, and projecting a little
at the bottom of the shallow fossa. Septa delicate, a little thicker
at the calicular margin than elsewhere, barely projecting; they slant
rapidly downwards and inwards, being slightly dentate. Laminze
perfect and granular at the wall, but perforate and cellular else-
where. In six systems of three cycles. The primary septa are a
little projecting at the margin, arched inwards, then become concave,
and finally reach the columella; the secondary either do not reach
the columella, or do so by the trabecule, and are a little smaller
than the primary; tertiary often barely developed. Endotheca
greatly developed, extending even to the calicular floor; seen, in
longitudinal sections, as faint lines on the septal lamine, curved and
often oblique, and as cross-bars between the septa at very short in-
tervals; near the calice the dissepiments become oblique, and form
complete floors between two septa, or simply join the septal lamine
by cross-bars. Exotheca greatly developed, that between the calices
formed by wide dissepiments, and marked out into checkered spaces
by the coste; in the spaces a little papillary eminence is now and
then seen; lower down and in longitudinal views the dissepiments
are stout, project more than the cost, and form cells generally
higher than broad, but occasionally very broad and less high; they
are nearly on the same plane throughout the corallum. There are
six dissepiments to =, inch. The young buds have not the tertiary
septa. Diameter of the calices from =}, to 1; inch.

The perforate lamine of the septa, the exothecal development,
and the density and compactness of the walls determine the genus.
Only one recent West Indian form has been described, differing
widely, however, from any other species. The Cyphastrwa obiata
from St. Thomas’s has few coste and almost confluent walls. The
other species inhabit the reefs of New Holland, the Fejees, the Sand-
wich Islands, and the Red Sea. There are two Corals doubtfully
referred to Cyphastrea by Milne-EKdwards; they are both from the
Lower Chalk, and were originally noticed by Reuss.

From the hard superficial limestone. Coll. Geol. Soc.

VI. Barpapozs.
1. AstR#A BARBADENSIS, spec. nov. Pl. XV. figs. 6a, 66.

Corallum tall, subplane, with tall and slender corallites, which
are crowded, but distinct. Calices circular, but slightly prominent
and very shallow. Coste well developed, not much produced, ex-
cept the primary, which now and then join those of neighbouring
corallites ; they are slightly spinous and inclined at the surface, and a
little wavy in their longitudinal course, but are distinct and strong at
their base. Primary and secondary coste equal, the primary being
now and then most produced; the tertiary do not vary much in size
from the others, but are less produced. Septa stout, projecting up-
wards considerably from the calicular margin, especially the primary ;

1863. ] ‘ _ DUNCAN—WEST INDIAN CORALS. 445

superior margin irregularly dentate. Each septum corresponds
with a costa, is large at the wall, tolerably thick internally, and
not delicate in any part of its course. Lamine not granular, well
developed, not perforated, joining the columella by delicate processes
which pass upwards and inwards. In six systems of three cycles.
The primary and secondary septa are nearly equal, and reach the
columella; the tertiary reach but a little way inwards, and end in
a sharp edge. Columella parietal, slightly developed. Exotheca
tolerably well developed between the costs; cells nearly square and
very small. Endotheca very scanty. Wall cylindrical, well deve-
loped. Diameter of the calices 1, inch.

The fossilization of this specimen is peculiar; the loculi are not
filled with any mineral, and the sclerenchyma is silicified and very
crisp in its texture.

This species is closely allied to the recent Astrwa annularis
(Pacific ?), but differs in not being convex and subgibbous in shape,
in not having a strong paliform tooth on the septa, and in not pre-
senting delicate walls and horizontal processes from the laminz
to the columella. It is more remote from a common West Indian
form (Astrea stellulata) than it is from A. annularis.

There is no recent Coral which corresponds to this tall, subplane,
simply laminar Astrean.

From the Marl; the specimen was obtained from a well 40 feet
deep. Coll. Geol. Soe,

A cast has also been obtained from the Marl-formation of Antigua.

2. OcuLIna, sp.
A worn specimen; species not to be determined. Coll. Geol. Soc.

3. MApDREPORA, sp.
A rolled specimen. Coll. Geol. Soc.

These last two specimens are too fragmentary for specific determi-
nation, and their original position with regard to the raised reef is
uncertain.

D. General Observations on the Genera and Species.
I. Anrieva.

The absence of simple Corals from the collection from Antigua is
somewhat remarkable, especially when their prevalence in San Do-
mingo and Jamaica is considered. Equally remarkable is the
presence of no less than nine species of Astrea, some of them second
to none in size and development. The large blocks of these Astrea,
the existence of Mwandrine, Alveopore, and a species of Stepha-
nocema, together with a large Rhodarewa, indicate a reef with
‘* Pacific’ rather than West Indian peculiarities.

The predominance of the genus Astrwa is remarkable, and there
is no instance of so many forms being found elsewhere in so small an
area. The majority of the specimens from Antigua are great masses
of Coral covered with casts of the calices, and are for the most

446 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [May 6,

part Astreans. By far the greater number belong to the species
I have named Astrea crassolamellata, from the great thickness
of the outer part of the principal septa. The six varieties and the
typical form of this species form a most interesting group; and
although no specimens have as yet been discovered except in Antigua,
still there are some remarkable specific alliances. I have preferred
terming the several forms described, varieties, for they all have the
closest structural resemblance to each other and to the typical form.
There is generally some variation in the appearance of the indi-
viduals of compound corals; this is not simply the result of imma-
turity or of arrested development, but is to be referred to the causes
which determine individual differences in secondary and tertiary
characters. Some masses of the species Astrea crassolamellata con-
sist of aggregations of corallites which have those individual peculi-
arities and deviations from the type which are to be seen in a few
corallites in the typical specimens; and in the variety pulchella,
which is very polymorphic, the corallites of a large corallum vary
sufficiently in different parts of it to constitute other varieties were
the specimen broken up and its original entirety not understood.

The restriction of Astrea crassolamellata to the Marl-formation
is interesting. The species does not appear to have any close West
Indian affinities, either fossil or recent, and it must be referred to
that part of the Miocene Coral-fauna which, having a much earlier
origin, died out in Tertiary times.

The fossil Corals of the West Indies appear to have relation to
two distinct Coral-faunas, one of which existed during the Oolitic
period, and has also left its traces in the Lower Cretaceous strata,
and another whose first appearance is uncertain, but which attained
its greatest development during the Miocene period, and is now
represented in the Pacific Ocean and its associated seas.

The European fossil Corals related by structural resemblances to
Astrea crassolamellata are Astrea Lifolensis, Middle Oolite, and
Astrea Guettardi, Miocene. A specimen of the first from the Vosges,
in the British Museum, has great resemblance to those of the new
species; and the description of Astrea nobilis, now merged into
Astrea Guettardi by Milne-Edwards and J. Haime, suggests the
existence of several important points of structural affinity between
that species and Astrea crassolamellata.

The species Astrea endothecata, of which there are varieties in
Antigua, is a San-Domingan type; and Astrea Antillarum, from
Montserrat, is closely allied to it.

Astrea cellulosa and its variety with curved septa are very
remarkable forms; they are in many respects miniatures of the
ereat Astrea endothecata, and are found in the older strata. Their
discovery in a formation where fossil Wood, and Testacea not purely
marine, are noticed is interesting; for the presence of fresh or
brackish water is very antagonistic to coral-growth, and especially
as the great Astrawa which they resemble was found in the Marl,
which contains no evidence of such conditions.

Astrea megalaxona increases by fissiparous growth, as well as by

1863. ] DUNCAN-—-WEST INDIAN CORALS, 447

extracalicular gemmation; in this it resembles the recent Astrea
Pleiades; moreover it would appear that one of the varieties of
Astrea crassolamellata does so likewise.

Astrea radiata, var. intermedia, connects the fossil Astrea endothe-
cata with the recent Astrea radiata of the Caribbean Sea; and Astrea
costata has a close affinity with the recent Astrea cavernosa of the
West Indies.

Astrea Barbadensis, which is common to the Marl-formation of
Barbadoes and Antigua, has a close affinity with Astrea annularis
of the Pacific, but differs from all the known recent West Indian
forms,

Astrea Antiguensis is a well-marked species and a very fine form ;
it has many structural affinities with Astrea endothecata, and to a
slight extent with Astrca cavernosa.

There are two species of Jsastrea, one of Astrocenia, and one of
Stephanocenia, at Antigua.

The range of the genus Jsastrea has been difficult to determine,
on account of the state of preservation of some Corals of the genus
Prionastrea, which would appear to be of Miocene age. The Jsas-
tree of the Antiguan beds have a very remote affinity to the
Miocene corals formerly called Prionastrea irregularis, P. diversi-
formis, and P. aranea, but a very close resemblance to the true
Isastree of Tisbury. They are without columelle, and can only
be classified under the genus Jsastre@a ; one species equals Jsastraa
tenuistriata (Inferior Oolite) in the number of its septa, but is a
dwarf, its corallites never measuring more than 53, inch across: the
other has great resemblances, both in its structure and mode of
fossilization, to the Isastrwa oblonga (Portland); it is smaller, how-
ever, and the septal number is never so complete.

Isastrea angulosa, Edwards & Haime (Meestricht), is also closely
allied to the Jsastrea turbinata from Antigua.

The Astrocenia so common in Antigua is found in irregular
masses, which present most curious varieties of silicification. The
form is hardly separable from Astrocenia ornata (Turin, Miocene),
even as a variety, but the typical form is found in small masses.
This variety is only remotely allied to the species of Astrocenia
a Jamaica, which is the A. decaphylla, a European Cretaceous

orm.

The Stephanoceenia tenuis of the oldest beds has not been found in
the Marl ; it has only a generic affinity with the species from the Mio-
cene of San Domingo, and its alliances with all the known forms are
remote; it approaches Stephanocenia formosissima and Stephano-
coma intersepta more closely than it does the Eocene species. The
genus ranges from the Jurassic strata to the recent Coral-formations,
species having been determined from the Oolite at St. Mihiel, from
the Lower Cretaceous strata at Gosau, and from the Eocene; but not
hitherto from the Miocene, though S. intersepta, which is barely sepa-
rable from the Gosau Astrea (Stephanoceenia) formosissima, Sowerby,
is said by Lamarck to exist in the American and South Seas.

The Solenastrea Turonensis of the Faluns appears to be represented

448 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [May 6,

in Antigua: there is some doubt about the accurate determination
of the Antiguan form, on account of its state of preservation ; but,
as far as the structures can be seen, the fossils are specifically the
same.

Species of the genera Astroria and Celoria are found in the Chert,
and are remarkable for the beauty of their silicification, the original
hard tissues being turned into homogeneous black flint, whilst the
interspaces are filled with opalescent silica. These are the first
fossils of the genera which have been noticed; and the species are
remote from Celoria labyrinthiformis, which is said by Dana to
exist round the Bermudas and in the Red Sea.

It is very doubtful whether the species of Celoria and Astroria
(see note attached to the description of the species, p. 424) said to be
of West Indian origin are really so. -Astroria Sinensis is commonly
offered for sale as a West Indian specimen, with other corals de-
cidedly belonging to the East Indian fauna. The Red Sea Astroria
astreeformis, and Astroria stricta from the Straits of Malacca, have
very close structural alliances with the new species from the Chert
of Antigua, one of which (Astroria polygonalis) is a well-marked and
most important species.

The Antiguan species prove how gradual is the passage from a
perfect Astrea to a sinuous Celoria, through the fissiparous Astrac
already mentioned and the various Astrorie.

It will be found difficult to maintain the present genera intact
when the anatomy of these forms is better understood; for in one
specimen there are such variations of thickness of wall, depth of
fossa, and length of series, as seriously interfere with its satisfactory
classification ; and it is most probable that in most specimens, when
they were entire, similar variations existed.

The Alveopore are reef-corals, and although there are species
common to the limestones of Antigua, Jamaica, and San Domingo,
still the genus is no longer West Indian, but Pacific. These are the
first instances of fossil Alveopore.

The large Rhodarea is allied to R. Raulini of the Dax Miocene,
though but slightly; all the recent species are found in the Chinese
and Australian Seas, not in the Caribbean.

There are none of the species of those genera which are so strongly
represented in the present West Indian Seas amongst any of the col-
lections of Antiguan fossil Corals in the British Museum, the Museum
of the Geological Society, or the Museum of Practical Geology. For
example, the following well-known recent West Indian genera are
quite unrepresented :—

Eusmilia. Colpophyllia. Prionastreea. Oculina.
Ctenophyllia. Manicina. Siderastreea. Porites.
Dendrogyra. Diploria. Parastreea. Madrepora.
Lobophyllia. Cladocora. Phyllangia. Millepora.
Symphyllia. Cyphastrea.

There is a Meandrina in the Chert which has very short series,
and is very sinuous, but its details are too deficient to enable me to
determine its specific affinities.

1863. | DUNCAN—WEST INDIAN CORALS. 449

II. San Domrineo.

The genera are very numerous, and include many simple corals.

Astrea, Stephanocenia, Alveopora, and Meandrina are represented
here as well as in Antigua.

The great Astrea endothecata, whose varieties at Antigua have
been noticed, flourished formerly in the coral-reefs of San Domingo ;
it is characterized by the extraordinary development of its endotheca,
and is only second in size to the great Astrea crassolamellata of the
Marl of Antigua. Considering that several forms of Astree at
Montserrat and Antigua are more or less structurally related to
the great Astreean of San Domingo, it is necessary to examine the
Astreans of the European Miocene seas for their alliances, especially
as the Testacea of the Nivajé and Esperanza shales have a mid-
tertiary facies.

It is, then, provisionally that I collect the Astreeans with an un-
usual development of endotheca into a subgenus, as follows :—

Astrea Ellisiana. Dax, Turin, &.
Reussiana. Vienna.

— Raulini. Leognan. Miocene.

Defrancii. Bordeaux and Turin. |

vesiculosa. Dax. i)

cellulosa, et var.

endothecata, var. Antigua.

—— Antiguensis.

— Antillarum. Montserrat.

San Domingo, Miocene.
Miocene ? of Persia*.

— Forskezlana. Red Sea and West Indian Seas, recent; sub-

fossil in Egypt.

— endothecata.

The species are placed according to their affinities.

The range of species closely allied to Astrea exothecata is from
the Miocene of Europe and of the East and West Indies to recent
times, the only existing form being common to the Red Sea and the
Caribbean.

Astrea cylindrica is a very interesting form, as it has not been
found elsewhere than in the Nivajé shale; it resembles somewhat
the recent Astrea cavernosa of the Antilles, and Astrea costata
of the Marl of Antigua; it differs from A. Forskelana in the deve-
lopment of the endotheca and the rather cribriform septa.

Stephanocema is found in a ramose form; its presence in San

Domingo is interesting on account of a species haying been found in
the Chert of Antigua, the geologic age of which is uncertain.
_ Alveopora fenestrata is found fossil; it is now common as a reef-
coral in the South Seas; but although Alveopora Dedalea and its
varieties also occur fossil in Antigua and in Jamaica, still there are
no species of the genus in the present Caribbean Sea.

Barysmilia, which has a species at Le Mans (Greensand), at Gosau,
and also at Uchaux’, is a well-marked genus; the species in the
yellow shale at Esperanza, San Domingo, is clearly intermediate be-
tween the other forms.

* See a specimen in the British Museum. t Edwards and Haime, op. cit

F

450 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

In the yellow shale there is a ramose Coral which, provisionally,
is classed with Phyllocenia. With one exception, its structural
characteristics agree with a very remarkable Coral which has been
referred to many genera, having been called by Goldfuss Madrepora
limbata, by Bronn Oculina limbata, by M‘Coy Gemmastrea limbata,
and by Milne-Edwards Stylina limbata. Our species has no colu-
mella visible ; and although it is notorious that the little sharp colu-
melle of Styline constantly fall out, still I have considered it advisable
to disregard this and to classify the form with Phyllocenia, and to
state the probability that other specimens will determine the presence
or absence of a columella. Another species so closely resembles
Phylloceenia sculpta (Michelin, Zooph. pl. 71. figs. 1 & 3), that it can
only be considered a variety with a tile-shaped corallum. Phyllo-
cenia sculpta is from the Hippurite-limestone of Martigues. There
are no existing forms known, and it is worthy of notice that the San
Domingan species are but very distantly allied to the Eocene and
Miocene species of the genus.

Brachycyathus, known amongst European Corals from the Neoco-
mian, has a species at San Domingo, very remote, however, from B,
Orbignyanus.

Stylophora, a genus closely allied to Astrocenia and to the Oculi-
nidee, is represented by one species in the Blue Shale of San Domingo ;
it 1s more closely allied to the Miocene species from Dax, Gaas, and
Turin than it is to any recent one. The recent Stylophora mirabilis
of the West Indies is a doubtful species, but many live around the
Fejees, East Indies, Seychelles, Zanzibar, and the Cape of Good Hope,
and in the Red Sea.

Siderastrea crenulata, a well-known species from the Gironde
Miocene, has a variety.in the Blue Shale of San-Domingo. There is
a very close resemblance between all the Siderastree, but the recent
West Indian species are clearly more allied to the Miocene forms than
the latter are to the Eocene species.

Flabellum is represented by two species in the Blue Shale, and in
the Limestone there are many examples of impressions which pro-
bably denote a third. F. dubiwm of the Shale resembles in some
points Flabellum Galapagense, Edwards & Haime, from the Miocene
of the Galapagos. There are no recent species in the West Indies,
but they abound to the west of America.

Placotrochus, a genus inhabiting the coral-sea of the Philippines
and China, has a fossil species both in San-Domingo and Jamaica.

Trochocyathus cornucopia, Kdwards & Haime, a species common
to Tortona and the Vienna Miocene, is represented in the San-Do-
mingan Tertiary beds; it is so characteristic a form that it stamps
their age satisfactorily.

The San-Domingan Thysanus corbicula is allied to the Jamaican
Thysam ; but these beautiful corals do not appear to have any very
close recent allies, although they have affinities with Flabellum, Rhi-
zotrochus, and Ceratotrochus.

Dichocenia tuberosa, a common fossil of the Blue Shale, belongs to
a genus doubtfully represented in the French Gres Vert, but well

1863. ] DUNCAN—WEST INDIAN CORALS, 451

known in the present Caribbean Sea and in the Indian Ocean and
Red Sea. Singularly enough, the fossil San-Domingan species is
more closely allied to D. porcata and D. wa of the Indian and Red
Seas than it is to D. Stokesw, D. Cassiopea, and D. pulcherrima of the
sea around Cuba and St. Thomas.

Agaricia agaricites and A. undata are common both ina coral-
breccia in the San-Domingan shales as well as in the West Indian
seas. The genus dates from the Cretaceous period, occurring in
rocks of that age in France; it has a very wide distribution in the
present day, and is found subfossil by the side of the Red Sea.

Cyphastrea costata, found in the Barbuda limestone, occurs also
in San Domingo; a slight variation exists in the wavy course of the
exotheca, but this forms no specific distinction. The genus is dis-
tinguished from Astrea by the imperfect condition and cribriform
appearance of the septa, and the condition of the septa in A. Forske-
lana shows the close relation of that species to the Cyphastrew. The
correlation of growth between certain parts of the sclerenchyma of
compound Astreeans is as yet little understood; but thick septa and
large columelle are usually found associated with thin walls and
slender coste, whilst thin septa, thick walls, and large costs are
common; it is, therefore, quite possible that the thick walls, great
costee, and well-developed endotheca and exotheca may have a signi-
ficance with regard to the cribriform septa. There are recent spe-
cies in the Caribbean and East Indian seas,

III. Jamatca.

There is a general relation between the fossil Corals of Jamaica
and of San Domingo, and several species are common to both islands.
Cyphastreea costata, common to Barbuda and San Domingo, is found
also in the Tertiaries of Jamaica; and Alveopora Dedalea, fossil in
San Domingo and Antigua, but recent in the Pacific, is a common
form in the hard, white Tertiary limestone.

Porites is represented in Jamaica by a fossil species related to the
recent forms in the Caribbean Sea.

The great Montlivaltia ponderosa of the Guadaloupe Miocene is
found in Jamaica and also in San Domingo; moreover Placocyathus
Barrett is a prominent Jamaican form.

A very remarkable Placotrochus with a lateral erosion is peculiar
to this island, and a species of Thysanus also. As in considering the
species from Antigua and San Domingo, Corals were noticed allied
to forms in Secondary European strata, so in Jamaica Astrocenia
decaphylla (the Astrea decaphylla of Michelin, from Gosau and
Corbiéres) is found in an admirable state of preservation.

The new species of Stderastrwa in the British Museum is a tall
and massive form, well worthy of the name “ grandis.”” Doubtless,
as more specimens are obtained, the Corals will determine the age of
the Tertiaries lying upon the Chalk in this island.

452 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

IV. BarBaboes.

The Corals from this island were obtained partly from a well sunk
40 feet in the Coral-marl, and some were picked from the shore.

Astrea Barbadensis is a very distinct species ; it is found fossil also
in the Marl-formation of Antigua, and it is more closely allied to the
recent Astrea annularis of the Pacific than to any recent West In-
dian species. The Oculina and Madrepora are too fragmentary to be
determined specifically ; they would appear to have come from a dense
Coral-breccia.

V. GuaDALoupE, &c.

Paterocyathus is a new genus.

Cyathina is represented by a species like the C. arcuata of Europe ;
there are no recent Cyathine in the West Indies.

A species of Solenastrea and a Meandrina are also found in the
island; and the genus Z’rochosmilia is said to be represented there,
associated with the Paleeozoic Fuvosites.

Montserrat has the Astrwa Antillarum, closely allied to Astrea
endothecata, amongst the beds which contain its silicified Woods; and
from Barbuda there has been, as yet, only one fossil Coral obtained
—a Cyphastrea, which was discovered in a mass of Shells and Corals
under the superficial soil.

It is most unfortunate that the state of fossilization of the Tri-
nidad Upper Parian Corals should have rendered their determination
doubtful. Mr. Etheridge, using Dana’s nomenclature, distinguishes
some fossil Astreeans with recent alliances; a Turbinolia, an essen-
tially Eocene genus, and the Astrea Pleiades, which most probably is
Astrea megalaxona.

E. Conclusion.

It has been noticed that the Testacea sent from Antigua with the
Corals have been stated to belong to the present age. This is correct ;
but there are a few Shells and casts of Shells of an older date.
A Helix, common as a fossil, is not now, according to Dr. Nugent, an
inhabitant of the island; and the extinct Welanie are found in great
abundance with silicified Woods.

Both in Jamaica and in San Domingo there are late Tertiary Shells
and Corals, but it is impossible to bring these facts in antagonism
with those which give a more remote age to the strata whence the
specimens described were obtained.

So with regard to Antigua, Barbuda, and Barbadoes, it is not correct
to give the whole Islands a Pliocene or Postpliocene age because
recent and subfossil Shells are found in them.

As yet, the Testacea have not assisted in determining the geologic
age of the three coral-formations of Antigua; but Mr. C. Moore has
given a Miocene age to the Mollusca from the San-Domingan shales,
whence the Corals here described were derived. The Alabama Eocene
Shells and Corals are distinct from those of the raised Coral-beds of
the West Indian Islands; and it is worthy of remembrance that,

1863.] DUNCAN——WEST INDIAN CORALS. 453

although there are genera and species of Corals in Antigua, San Do-
mingo, and Jamaica belonging to the great European Miocene Coral-
age, still there are a few European Miocene genera of Corals which
are not as yet known to belong to the West Indian Miocene.

The range, in strata, of the genera of Corals is often so great, and
the species of remote formations are so frequently closely allied, that
the Zoantharia form better guides for estimating the external phy-
sical circumstances of the regions in which they existed, than for
determining the age of strata. There are few subjects better
understood than the relation between the presence of certain genera
and species of Coral and certain definite, external, physical condi-
tions. Depth of sea, purity of sea-water, its intense aération, force of
wave, absence of fresh water, the climate and nature of the coast-
line, with all their possible varieties, appear to determine, according
to their mutual reactions, the presence and persistence of species
and genera. Indeed, very slight variations from the general rule of
the external circumstances in a Coral-sea would appear to prevent
the development of certain genera. It is a reasonable induction
that, if a species be found in strata of any age and distant in space,
the two sets of strata were formed under the same external physical
circumstances.

The question of contemporaneity may be fairly considered when
the strata are close together in which identical forms, or those closely
allied, are found. Thus, Stephanocenia formosissima, of Gosau and
Uchaux, is so closely allied to S. entersepta of the present South Seas,
that there is hardly a specific difference. When the latter is broken
from recent Coral-limestone, all that can be said is that the modern
and the ancient Corals existed under the same circumstances of cli-
mate and aqueous distribution.

But when Stephanocenia dendroidea is found fossil at San Domingo,
and a closely allied species at Antigua, and when the short distance
between the formations, and the existence of the equivalents of the
Caribbean and of the older and newer Parian formations throughout
the West Indian Islands are considered, the sameness of external
circumstances may be received as a concurrent testimony of identical
age.

There is nothing anomalous, as would at first appear to be the
ease, in finding species already classified amongst European Creta-
ceous Corals, in West Indian Miocene strata; nor in finding species
of Jurassic Corals closely allied to forms in these Mid-tertiaries.

The European Miocene contains both Jurassic and Lower Creta-
ceous genera, and in some instances the specific relations of the
Corals are very close. Thus, Astrwa Lifolensis is hardly worthy of a
specific distinction from Astrea Guettardi, and the Phyllocenie of
the formation at Corbieres greatly resemble those of Dax and Castel
Gomberto.

The Isastreeans from Antigua, whatever may be the geologic age
of the Chert, are very closely allied to those of the Oolites, and it is
unnecessary to repeat the close resemblance of some and the identity
of other San- Domingan Miocene Corals to European Cretaceous forms,

454 "PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 6,

~ It is somewhat singular that the majority of the genera common
to the earlier Secondary formations and to the Miocene are extinct ;
and that, on examining the Corals common generically to the
Jurassic and the Miocene (the two great Coral-ages), many of these
genera will be distinguished in the Lower Cretaceous horizon.

The determination of the geologic age of the Trap, the Inclined
Conglomerate, the Chert, and the Marl of Antigua can only be sub-
ject to doubt at present; but that these three last strata should be
of the same age as the coral-reefs in the surrounding sea is impos-
sible, inasmuch as the silicified Corals have a greater resemblance to
European fossil forms and to Pacific and East Indian recent forms
than to those of the present Caribbean Sea.

From the consideration of the affinities of the fossil Corals of
Antigua, San Domingo, and Jamaica, all of them possessing forms in
common—species and genera of European Miocene age, and many
now existing in the Pacific and East Indian seas, together with a few
varieties of species peculiar to the present West Indian Ocean,—the
doubtful age of the beds of the first Island may be approximated to
that of those in the others.

The paucity of recent species in these Miocene Coral-beds is very
remarkable. In Antigua there is not one West Indian recent spe-
cies; andin San Domingo the Agaricia agaricites is the only decided
recent form, for the Agaricia undata being in the form of a variety,
and the general absence of the characteristic West Indian genera,
give a foreign look to the Miocene Coral-fauna of that Island.

There are species common to the European and West Indian
Miocene, and several genera appear in the latter for the first time as
Miocene.

The relation of the Lower Cretaceous system underlying the Ter-
tiaries in San Domingo, Jamaica, and Trinidad must be remembered
in reflecting on the apparently misplaced Cretaceous Corals in those
Islands and in Antigua.

There was a vast alteration in the physical geography of the
West Indian seas caused by the gradual upheayal of the former Coral-
reefs and banks, now recognized as the Newer Parian of Trinidad,
the Shales of San Domingo, the Inclined Beds of Jamaica, and the
compound formation of Antigua, previously to which these probably
contemporaneous formations attained far less than their present
magnitude. The area of elevation was a vast region, and the
remains of the flora of the period prove the corresponding depression
to have been great. It appears that this slow and yet immense
physical change terminated the Miocene age in the Caribbean region ;
or, rather, altered the external conditions which were necessary for
the persistence of the species, and produced such new combinations
of those external conditions as were antagonistic to the perpetuatioa
of the old Coral-fauna, but favourable to the development of those
varieties of its species which were the progenitors of the present
peculiar Caribbean types.

If the breaking down of the Arctic barrier-land ended the

1863. ] DUNCAN—WEST INDIAN CORALS. 455

Miocene period of Europe by the production of a great change of
climate and the consequent introduction, by emigration, of forms
with more or less arctic affinities into the European fauna and flora—
if this be held to be a reasonable explanation of the cause of the
difference between the Miocene and Pliocene formations in Europe,
corresponding data exist to connect the end of the Miocene Coral-
fauna of the West Indies with the physical revolution which closed
the Pacific from the Caribbean.

The peculiar Coral-fauna of the Caribbean Sea is strongly repre-
sented in all the superficial deposits of the Islands, and there are no
forms, so far as is yet known, amongst these which have other than
West Indian affinities. Some genera are found which prove that
the causes producing the more or less arctic condition of the European
Pliocene, affected very slightly the climate of the Caribbean Sea also.
But in all the calcareous formations which are coralliferous and are
considerably elevated above the level of the Caribbean Sea, there
is a very limited series of Corals with generic relation to those now
existing and characteristic of the West Indian Coral-fauna, but a
predominance of forms resembling those of the present Coral-seas of
the Pacific, South Sea, and the Indian Ocean*,

The most strongly marked West Indian species are not represented,
even in the raised beds, by allied species; and it can readily be
believed that a great change in the distribution of land and sea
preceded the extinction of the Corals with Pacific affinities.

In the Coral-seas of the South Sea, Pacific and Indian Oceans,
and Red Sea, the external circumstances which are so well known
to influence Coral-life are very different from those which operate
in the restricted West Indian regions.

In the first there is an extraordinary freedom from the effects of
great rivers, such as pour mud and fresh water for leagues into the
pent-up Caribbean Sea: in the great Ocean there are opportunities for
migration of species, but in the case of the Caribbean there are impedi-
ments on all sides: in the Coral-islands of the Pacific the soundings
are soon found to be great; but in the northern part of the Carib-
bean, the great banks, which in their shallow sea somewhat resemble
the shoals to the north of the Malay Archipelago, are rarely affected
by the furious surf and force of wave, which appear to determine
the persistence of several species; on the contrary, peculiar genera
are seen to flourish around Cuba and the Bahamas.

The presence of species of Alveopora, Stylophora, Flabellum,
Placotrochus, Rhodarcea, Astroria, Coloria, &c., in the raised Coral-
formations must refer to a different condition of the physical circum-
stances of the West Indian seas from that now existing, and to those
peculiarities of climate, of sea-depth, purity and force of sea, and of
coast-line, which are noticed in the ocean between Eastern Africa
and America. It is worthy of notice that, at the present time, the
Australian, Pacific, and Indian Ocean Corals differ as a rule in
species and often in genera, that the nearest coral-reef is hundreds

* Mr. J. Carrick Moore asserts that the San-Domingan Shells have a Pacific
facies; see Quart. Journ. Geol. Soc. vol. vi. 1850, p. 43, and vol. ix. 1853, p. 181,

456 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [May 6,

of miles to the west of the Isthmus of Panama, and that the Corals
of the Atlantic are few and far between; yet the existing Coral-
provinces are all represented in the Miocene beds now under con-
sideration.

The genus Flabellum has no species in the Caribbean Sea, but
there are some in the San-Domingan Miocene; they abound in the
Australian, South, and China Seas as recent forms, and a fossil
species has been discovered in the Galapagos Islands; it was named
by Milne-Edwards /. Galapagense, and determined by him to be
derived from a Miocene bed. ‘This fossil has a resemblance to a
new form from the San-Domingan shale; moreover the great Mont-
livaltia of the Jamaican Miocene is found at Travancore. This
carries the subject of a former connexion between the Central
American Sea and the Pacific Ocean, during the life of the Miocene
Corals, a step further ; and the consideration of the extent of the
Newer Parian series, of the relation of the Tertiary formations of
the Isthmus to the central mountain-chain, and of the elevation and
magnitude of the Miocene strata in the Antilles, strengthens the
hypothesis that the Corals of the San-Domingan and Antiguan beds
were washed by the same sea which nourished the progenitors of the
present Pacific forms.

Nothing can be more satisfactory than the determination of the
alliances between the San-Domingan and Antiguan fossil Corals and
those characteristic of the Faluns and of the Viennese, Bordeaux,
Dax, Saucats, and Turin Miocene.

The affinity between the Corals of the European Miocene and the
Pacific recent forms is as decided as that noticed now for the first
time between them and those of the Antilles Miocene.

Doubtless further researches will discover more species common to
the European and American Miocene than have yet been described,
and perhaps some genera also; but, from the study of the forms
now under consideration, it 1s evident that a greater facility for
Coral-migration between the two sides of the Atlantic existed for-
merly than is now the case.

The researches of Prof. E. Forbes and Mr. Godwin-Austen have
led to the belief that, during the Mid-tertiary period, Europe was
very much in the condition of the present Pacific Archipelago ;
Mr. Darwin concurs in this view, and it is reasonable to affirm the
prolongation of the maze of islands across the Atlantic. Prof. Heer
accounts for the specific identity of European and San Domingan
Miocene Plants by a great continent intervening; but such masses
of land are antagonistic to coral-growth, by the production of rivers
of great size; moreover, there are positive proofs of old Coral-reefs
between San-Domingo and the Atlantic... A series of islands, formed
very much like the Antilles, with Coral-reefs around them, extend-
ing from the Mid-pacific across to Europe, would remove Heer’s
difficulty, and account for the relation between the Miocene Corals
of the Old and New World and those of the Galapagos and East
Indian raised beds, as well as the relation between the former and
the recent species of the great seas to the west of America.

[ To face p. 456, vol. xix.

On the Fosstz Corats of the West Inpian Istanps. Parr I.
ApPpeNDIxX. By P. Martin Duncan, M.B., F.G.S.

ERRATA, AND NOTES ON PLATES XIII.—-XVI.

Page 415, line 37, dele a, 4 6,
,, 434, line 1, add 7 ec.
», 442, line 30, for C. ponderosa read M. ponderosa.

Puate XIII.

In Figs. 1 a, 2a, andi, the septa and the original hard parts are white, whilst,
from a difference in their silicification, the corresponding parts are black in
figs. 3, 4, and 6.

In the natural cast, fig. 1 4, the black portions were once occupied by scleren-

chyma; the interstices now alone remain, being filled with a white siliceous
mineral,

Fig. 8. The costz, which are often worn, are generally rather more visible than
those on the side nearest the number.

10. The dark lines are the sclerenchymatous parts more or less thinned
during mineralization, the interstices being white from infiltration.

11. The costz are best seen at the lower margin; the dark spots are spaces
on either side of their extremities. In this specimen the scleren-
chyma is white, and the interspaces black.

12a. The septa and wall are white in this figure, and black in fig. 125.
The natural appearance of the sclerenchyma has been nearly oblite-
rated by the process of silicification.

Puate XIV.

Fig. 9. The appearance of the costz can be determined by reference to Plate XV.
figs. 7a and 7c.

Puate XV.

Fig. 2, The columella should appear as a thin white line extending across the
long axis of the central black space.

6c. The dentations of the septa have been omitted accidentally.

7c. This figure represents the larger cost, the dentate smaller coste, and
the exothecal dissepiments of Astrea endothecata.

The artist has given the general appearance of the specimens, and, in most
instances, the minute characters also, with great exactness; but in the others the
condition of the Corals and their variable colour will account for slight discre-
pancies.—[P, M. D.}

Quart. Journ. Geol. Soc. Vol. XIX PL AUT.

7

gv

INDIAN FOSSIL CORALS.

ee aes Cee ae
i
r
¥
Z -
‘
as
’
t
i
p

: J -
» 4 a
i v
= ”* m lee 0 y -
F ; _ ol lt
y oe
~ yay eee os
©
. * be
yy oe
‘
*
yee
i
. Q oe ’
‘ * pi
= : .
+
Car
b it)
Fs f ¥ mt
; A x
Sar 5 a A
ee - '’ <<
j _* 7 x s MW ‘
Vat ce 1 . . wd
%
P Pe on t »

ee ee eee eS |
we

a

* ~
‘
‘
a
‘

18
BE ha
Sey ero
? ee
re ‘ ,
oo
r ‘a Dae De
y ec
y ‘ * *
:
we
* F
* '
ts
ul Witw.”)
, Sphere
’ a bo
{ if ” way

W.West imp.

Geo.West hth.adnav.

WEST INDIAN FOSSIL CORALS.

f ‘
oon

an
rt oa

Pianeta

\

efile: teed ee ee

he

len? Op

a a e et
a Lome rey

Quart. Journ. Geol. Soc. VoL XIX PI XVI

DoW

Ue.

Keer eitiy

j

re ta aS
pre Oe TP

Coed iy ue he Oe
re eet Z i!

ee OG Vy
e te Cae
by a8

Peak see : er / Ww

OCR lee aN “POF
spaenee x Kistner arora”
vas

3 ey ty, fe
ASABE Midis cle By

Geo. West Tithad nat.

W. West imp.

WEST INDIAN FOSSIL CORALS.

o>

0 I tee I OS — a ee

4

1863.]

DUNCAN—WEST INDIAN CORALS. 457

EXPLANATION OF PLATES XIII.-XVI.,
Illustrative of the Fossil Corals of the West Indies.
Puate XIII.

Fig. 1. Astrea ( Heliastrea, Edwards & Haime) crassolamellata: a, transverse

Fig

Fig.

section of a corallite; 4, natural cast of a calice; c, diagram of the
septal arrangement.

2. —— ——,, var. nobilis: a, transverse section of a corallite; 4, dia-
gram of the septa.
3. — , Var. magnifica; transverse section of a corallite.
4, —— , Var. magnetica; transverse section of a corallite.
5. —— , var. Nugenti; transverse section of a corallite.
—— , Var. minor; transverse section of a corallite.
7. The primary septa of the various forms.
8. Astrea (Heliastrea, Edwards & Haime) Antiguensis; the calice, mag-
nified 3 a diameter.
9. ——( ) costata ; transverse section of a corallite, magnified 3 dia-
meters.
10. ( ) cellulosa ; transverse section of a corallite, magnified 6
diameters.
11. ——( ) tenuis; transverse section of a corallite, magnified 3 dia-
meters.
12. (——) megalaxona: a, transverse section of part of a corallite,

ad.

oom

OD ob C9 poe

“ magnified 4 diameters ; 3, transverse section of a cast of a corallite,
magnified 3 diameters.

Puate XIV.
Isastrea turbinata: a, transverse section of a corallite; 4, ealice; c,
longitudinal section of a corallite; all magnified 2 diameters.
conferta; transverse section of a corallite, magnified 4 dia-
meters.

. Stephanocenia tenuis: a, part of corallum; 4, transverse section of

corallite ; both magnified 5 diameters.

. Alveopora Dedalea, var. regularis: a, transverse section of corallites ;

&, longitudinal view; c, same view of a cast; all magnified 6 dia-
meters.
microscopica ; transverse section, magnified 15 diameters.

. Astroria polygonalis; transverse section of a cast, magnified 2 dia-

meters.

. Astrocenia ornata; transverse section of part of a corallum, to illus-

trate the thinning of the larger septa and the absorption of the
smaller during silicification, magnified 10 diameters.

. Celoria dens-elephantis; transvetse section of the cast of a corallite,

magnified 2 diameters.

. Astrea (Heliastrea, Edwards & Haime) endothecata, var. 1; transe

verse section of a corallite, magnified 24 diameters.
Puiate XV,

. Brachycyathus Henekeni; calice, magnified 4 diameters.
. Placotrochus Lonsdalei: a, lateral view of a corallite; 4, calice; both

magnified 4 diameters.

. Thysanus corbicula: a, lateral view of a corallite; 4, calice; both

magnified 24 diameters.

. Barysmilia intermedia; corallum.

Dichocenia tuberosa; b, corallum, of the natural size; a, calice, mag-
nified 3 diameters.

. Astrea (Heliastrea, Edwards & Haime) Barbadensis: a, lateral view

of corallum, magnified 3 a diameter ; 4, calice, magnified 3 diame-
ters; c, two septal laminez, magnified 4 diameters.

( ) endothecata: a, lateral view of a corallite; 4, calice.

. —( ) cylindrica: lateral view of part of the corallum.

VOL. XIX.—PART I. ay

458 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [May 20,

Puate XVI,

Fig. 1. Placocyathus Barretti (part of a corallite): a, lateral view; 5, calice
(both diminished 2ths) ; c, the columella and one of the pali, mag-
nified 2 diameters.

2. Placotrochus alveolus: a, part of a calice, of the natural size ; 4, cross-
section, magnified 2 diameters,

3. Thysanus excentricus: a, calice; 6, lateral view of a corallite (both of
the natural size); c, costa, magnified 2 diameters.

4. Stylophora affinis; calice, magnified 10 diameters.

5. Siderastrea (Astrea, Edwards & Haime) grandis: a, longitudinal view
of the septa; 4, transverse section of corallites; both magnified
43 diameters.

6. Monitlivaltia ponderosa: a, a young corallum, of the natural size; 4,

calice, of the natural size.

May 20, 1863,

Sir Charles Tilston Bright, C.E., 12 Upper Hyde Park Gardens ;
James Dees, Esq., C.E., Whitehaven; E. C. Hartsincke Day, Esq.,
Charmouth; W. Dickinson, Esq., M.A., Croydon; Robert Francis
Hodgson, Esq., 126 Marine Parade, Brighton; the Rev. Charles
Kingsley, M.A., F.L.S., Rector of Eversley, Hants, and Professor
of Modern History in the University of Cambridge ; Edward Coulson
Musson, Esq., B.A., Martyr Worthy, near Winchester; Thomas
Glazebrook Rylands, Esq., F.L.S., Heath House, Warrington; and
John Scott, Esq., 3 Chester Place, Hyde Park, were elected Fellows.

The following communications were read :—

1. Furraer OxssEervations on the Devontan Puants of Marne, Gaspk,
and New Yorr. By J. W. Dawson, LL.D., F.RS., F.GS.,
Principal of M‘Gill University, Montreal.

[Puates XVII.-XIX.]

ConTENTS.

I. Introduction. ‘ III. Gaspé, Canada.
II. Perry, Maine. TV. New York.
V. Conclusion.

§ I. Introduction.

Since the preparation of my paper “On the Devonian Flora of
North-eastern America,” published last year*, I have been enabled to
explore more thoroughly than heretofore the plant-bearing beds at
Perry, in Maine; and Mr. R, Bell, of the Geological Survey of Canada,
has collected some interesting specimens from the Gaspé sand-
stones, which have been kindly placed in my hands by Sir W. E.
Logan for determination. Some important facts have also been as-
certained respecting the distribution of the Devonian rocks of the
State of New York, which give to several of the Plants from that
region a somewhat older geological position than that assigned to

* Quart. Journ. Geol. Soe. vol. xviii. p. 296.

1863. } iy DAWSON—DEVONIAN PLANTS. | 459

them in my former paper. These supplementary facts I now pro-
pose shortly to state. :

SII. Perry, Maine.

With respect to the geological relations of the rocks at this place,

I have little to add to the descriptions of Professor Hitchcock, re-
ferred to in my former paper. The beds at Pigeon Hill and its
vicinity, referred by him to the Upper Silurian, consist of hard, grey
and reddish shale and sandstone, overlain by trappean or trap-ash
beds, and traversed by trap-dykes. They are somewhat, but very
unequally, hatdened and altered, and are inclined at high angles,
with prevailing dips to the north-east. They contain abundance of
Lingule, and of small Lamellibranchiate Shells which have been
referred to the genus Modiolopsis. Mr. Billings regards the Lingula
as an undescribed species, and it appears to differ from that found at
St. John. I think it quite possible, however, that these beds at
Perry may be the equivalents of the St. John slates; and from their
relation to other beds at Pembroke which contain fossils of Lower
Helderberg age, and identical in many species with my “ Arisaig
group ”’ in Nova Scotia, I cannot doubt that they are of Upper Silu-
rian date, unless indeed,they may be Lower Devonian.
. Upon these beds repose,in an unconformable manner, the Devonian
red conglomerates. In their lower part they contain thick beds of
coarse breccia, containing angular fragments of the harder members
of the underlying series, sometimes 3 feet in length. These beds
are well seen at the mouth of the Little River of Perry, near Point
Pleasant. Above these are red conglomerates, with rounded pebbles
of quartzite, syenite, and other hard rocks. The pebbles are of mo-
derate size; and there are interstratified beds of bright red sand-
stone, with green spots and stains, and occasional thin grey layers.
The thickness of these beds exposed on the south side of Little River
is about 1300 feet. They are probably the equivalents of the upper
part of the St. John series and the Upper Red Sandstones of Gaspé ;
and it is worthy of note, as suggesting a caution to explorers of those
regions, that these rocks strikingly resemble in their mineral cha-
racter the Lower Carboniferous red sandstones and conglomerates
of some parts of Nova Scotia and New Brunswick, and also the pro-
bably Mesozoic “‘ New Red Sandstones” of these provinces.

The fossil Plants occur most abundantly in a layer of grey sand-
stone, about 2 feet thick, and apparently of small horizontal ex-
tent, in the upper part of the red conglomerate. This little bed is
filled with fragments of Plants, and probably occupies a spot where
a stream running from neighbouring land emptied itself into the
sea. It is rather a portion of the red sandstone bleached by the
deoxidizing and solvent action of the vegetable matter, than a distinct
bed; and the same remark applies to the numerous grey spots and
thin layers in other parts of the series. A very pretty illustration
of this occurs in a bright-red, fine-grained sandstone farther up the
Little River, in which Mr. Jethro Brown, of Perry, has found fronds
of Cyclopteris Jacksoni, and branches of Psilophyton, which have im-

212

460 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

printed themselves in light-greenish stains on the red stone. The
Plants have been drifted, and are for the most part in fragments, the
smaller and more delicate of which occur in the upper part of the
bed, and those of larger size in its lower part. Above and below
the Plant-bearing bed are red sandstones, passing into the usual
red conglomerate. Though there are abundant exposures of the red
sandstone and conglomerate on the coast of Perry, I could not learn
that fossils have been found in any other locality than those above-
mentioned, so that their occurrence must be considered rare. In
the underlying Upper Silurian Series I could find no Plants, except
some obscure fragments of slender stems.

With the assistance of Mr. Brown, I was enabled to obtain a num-
ber of specimens from the original Plant-bearing bed, the actual
exposure of which we indeed worked out. The more important of
these I shall now notice in detail.

1, ConrFERovs woop (DapoxyLon ET APOROXYLON).

Among the most abundant fossils at Perry are fragments of stems
and roots, and strips of bark, belonging to two or more species of
coniferous trees. They are pyritized, so that their structures can be
made out only as opaque objects, or after treatment with nitric acid.
In the specimens formerly collected, I was able to observe only a porous
woody tissue (Aporowylon). Some of my present specimens, how-
ever, show three or four rows of dises on the cell-walls, and are not
distinguishable from Dadoaylon Ouangondianum of St. John, though
they are not in a sufficiently good state of preservation to admit of
satisfactory comparison. Some of the flattened stems show marks of
lateral branches or cones at rare intervals (Pl. XVIII. fig. 20); others
are long, slender, and tortuous, and were probably roots (Pl. XVII.
fig. 5).

Among the specimens collected by Mr. Brown is one with a porous
tissue, in the form of a flattened stem or branch, 2 inches in diame-
ter, and with a pith half an inch in diameter (not of the Sternbergia-
type). The structure of thewood closely resembles that of Aporoxylon
primigemum, Unger.

2. Sr1gMARIA PUSILLA, spec. noy. PI. XVII. fig. 3.

Allied to 8. exigua, but with larger and more distant scars, not in
depressed areoles.

A few fragments of the bark of this species were found scattered
over the surface of a slab at Perry. It is of the same slender type
as Stigmaria exigua, of the Chemung group of New York, but is
sufficiently different to warrant the belief that it was the root of a
distinct species of Sigillaria.

3. CyYPERITES.

Two kinds of leaves, resembling those of Sigillaria, occur at Perry.

They are a line or less in breadth and 3 inches or more in length,

and have respectively two and four well-marked ribs. Though
no trunks of Sigillaria have been found, I regard these leaves and

1863.]- DAWSON—DEVONIAN PLANTS, 461

the Stigmaria above described as evidence of the existence of two
_ species of that genus.

4, ANARTHROCANNA PERRyANA, spec. nov. Pl. XVIII. fig. 21.

Stem cylindrical, swelling shghtly at the nodes ; ribs flattened, about
fourteen in the circumference of a stem three-fourths of an inch in
diameter ; ribs at the nodes apparently continuous with the decur-
rent verticillate (2?) petioles or branchlets.

This curious stem at first sight resembles a Calamites; but it has
no distinct articulation, and the ribs appear to separate from the
_stem and to pass into the decurrent and probably verticillate branch-
lets or petioles, which are given off at an acute angle, and bear traces
of slender leaves, which are, however, too imperfect for description.
The plant corresponds sufficiently, I think, with the characters of
Geppert’s genus Anarthrocanna to be included in it. It was pro-
bably allied to Calamites or Asterophyllites; and possibly the species
next mentioned may be the fruit of this Plant, though I have not seen
them in connexion.

ie 5. CaRPoLirHEs spicarus, spec. nov. Pl, XVII. fig. 15.

Carpels or spore-cases: oval, about a line in length, apparently with
_ a thick outer coat; densely placed on a thick rachis.

' This is evidently a spike of fructification, and may be allied to
Trigonocarpum racemesum, described in my former paper. It more
nearly resembles the fructification of Annularia and Sphenophyllum

- than any other fossil fruits known to me. Its parts are too indis-
tinct to admit of minute description, and the two-ranked appear-
ance of the seeds or fruits is probably deceptive, as there are indica-
tions that the specimen is a cylindrical spike flattened.

/ 6. Lycopoprres Ricwarpsont, spec. nov. Pl. XVII: figs. 1 & 2.
Stem slender, tortuous, dichotomous ; barren branches with short erect
or recurved leaves, apparently in two ranks ; fertile branches lateral,
one-sided, in the form of sessile strobiles. These strobiles are the
Lepidostrobus Richardsoni of my former papers.

Under the name quoted in the above description, I described in a
former paper* a very singular specimen collected at Perry by Mr.
Richardson, and which, though at first sight it resembled a pinnate
leaf, I believed to be a cone of the nature of Lepidostrobus. More per-
fect specimens confirm this view, and show that these cones were
sessile on one side of aslender and probably creeping stem, termina-
ting in dichotomous branches having short, stout, slightly recurved
leaves, apparently in two rows. The generic name of Lepidostrobus
being no longer applicable, I propose to place the Plant in Lycopodites,
a genus no doubt at present somewhat unsettled, but in which this
Plant, at least, fairly deserves a place.

X 7. Pstmopnyton.

Fragments referable to this genus are very abundant at Perry,
‘ *. Canadian Naturalist, vol. vi. p. 174.

462 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

but all in a very imperfect state. I believe that I can recognize re-
presentatives of the three species which I have named respectively
P. princeps, P. elegans, and P. glabrum, but cannot be quite certain of
this. Here, as elsewhere, I should have been ready to refer these
Plants to the convenient category of Fucoids, but for my eae Oe
of their forms and structures obtained in Gaspé.

8. LepropHi@um RHomBICUM, Dawson. Pl. XVIII. fig. 19.

Additional specimens of this Plant have enabled me to ascertain
that its branches bifurcated regularly, in the manner of Lepidoden-
dron, and tapered somewhat rapidly; that its leaves were long,
parallel-sided, and one-nerved ; and that it produced strobile-like °
bodies with narrow-pointed, closely appressed scales borne on the
sides of the branches. I have attempted to give a restoration of the
Plant, from several specimens in my possession, in Pl. XVIII. fig. 19.
The other characters of the genus, and the points in which it differs
from Leprdodendron and Ulodendron, are stated in my former paper.

9. LycoropirEes comosus, spec. noy. Pl. XVII. fig. 14.

Stem short, not observed to branch, densely covered with long filiform
leaves.

This little Plant, of which several specimens, all equally diminu-
tive, were found, somewhat resembles Selaginites Erdmann of Ger-
mar, but is smaller and differently proportioned.

10. Corpaires (PycHNoPHYLLUM) FLEXvosus,spec.noy. Pl. XVII. fig. 9.

Leaves lanceolate, acuminate, broad at the base; nerves numerous,
parallel, somewhat sinuous and uneven.

A number of more or less perfect specimens of this leaf were found.
It has the general appearance of the leaves of Cordaites; but less
distinct venation, and apparently less rigidity than the other species.
I place it in this genus merely provisionally, as its true affinities are,
of course, quite uncertain.

11. Cyctoprerts Jackson3, Dawson. Pl. XIX. fig. 26.

This is by far the most abundant species at Perry, and a large
number of specimens were obtained. One of these shows that the
full-grown frond was a foot in length, with a strong woody rugose
petiole a quarter of an inch thick at the base. Some of these petioles
in a pyritized state show traces of scalariform vessels. Old stipes
deprived of their leaves very closely resemble the Rhachiopteris
pinnata of the Marcellus shale of New York, though not quite so
large, and perhaps more rugose. Among the numerous scattered
pinne of this species there are some of much smaller size than the
others, which may possibly indicate a distinct species; but, for the
present, Iam rather disposed to regard them as merely a variety.
(See Pl. XIX. fig. 26, c.)

T also found a few detached pinnules, which I believe to belong
to Cyclopteris Halliana, of the Chemung group of New York. I have
attempted to represent the characteristic forms of the ordinary varie-

1863.] ° DAWSON—=DEVONIAN PLANTS, 463.

ties of C. Jacksoni and of C. Halliana in Pl. XIX. figs. 26 & 28. I
may add here that the stipe of Cyclopterts Jacksoni has a few leaves
between the pinnules of the upper part, but is less leafy than that
_ of C. Halleana.

12. Cyctopreris RogErsi, spec. nov. Pl. XVII. figs. 17, 18; and
pte de, Subd. S12. 2 f.
Habit of growth resembling that of Cyclopteris Jacksoni, but the pin-

nules are more elongated and almost cuneate m form, also less
densely placed, and with veins more nearly parallel. Stipe stout,
woody, furrowed longitudinally, and marked with strong transverse
‘bars or punctures.

This Fern is less abundant than C. Jacksoni, from which the points

above mentioned appear sufficient to distinguish it. Its stipe is
marked in the manner of Rhachiopteris punctata of the Chemung
group of New York, and of C. Roemeriana, Geeppert, from the
Upper Devonian of Europe; of the latter species the present may
be regarded as the American representative. I have endeavoured,
from the small fragments collected, to give characteristic repre-
sentations of the appearance of the species. It was probably about
the same size as C. Jacksoni, but with its stipe not leafy, and its
pinne and pinnules less densely placed.
_ It would seem that the remarkable group of pinnate Cyclopterides,
to which this species belongs, was characteristic of the Upper De-
vonian throughout North America and Europe. I dedicate the pre-
sent member of it to Prof. W. B. Rogers, who has done much to
direct attention te the deposits of Perry, and has kindly permitted
me to use the specimens in his collection.

13. CycLorreris Brownt1, Dawson. Pl. XVII. fig. 6.

This fine species, described in my former paper from a mere frag-
ment of a frond, I am now able to figure in its full dimensions, from
a fine specimen in the collection of Prof. Rogers of Boston ; several
others, nearly as perfect, were found by Mr. Brown and myself last
summer. It has a large simple frond, flabellate in form and divided
toward the edges, which are sometimes slightly reflected, as if they
had borne marginal fructification. It belongs to the group of sim-
ple-leaved Cyclopterides, like C. orbicularis, Brongn., of the Coal-
measures, or C. digitata and C. Huttoni of the Oolite. It very
closely resembles a beautiful leaf from the Ponent (Upper Devonian)
of Pennsylvania, figured, but not named, by Prof. H. D. Rogers in
his Report on the Geology of that State (vol. i. pt.2. pl. 22). This
resemblance did not appear from my imperfect specimen of last year ;
but I can’scarcely now doubt that Prof. Rogers’s Plant is the same,
or very closely allied. The leaf from Pennsylvania was compared
by Prof. Balfour, to whom it was submitted by Prof. Rogers, with
that of Salisburyia adzantifolia, to which it unquestionably bears a
strong resemblance; and it may admit of doubt whether it is really
a Fern or a coniferous leaf. In the absence of fructification it may
be impossible to decide this question ; but the form and texture of

464 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [May 20,

the leaf appear to me more those of a Fern, possibly allied to Adian-
tum or Lindsea.

14. SpHENopTeRIs REcURVA, spec.nov. Pl. XVII. figs. 7 & 8.

Leaflets small, cuneate, terminating the divisions of a dichotomous
winged petiole.

This Plant is represented by small and obscure fragments on the
Perry sandstone. Its venation is not preserved; and it may be a
small Cyclopteris with terminal pinnules, like my C. Acadica, from
the Lower Coal-formation of Nova Scotia.

15, TRIcHOMANITES FILICULA, spec. nov. Pl. XVII. figs. 12 & 13.
Pinnules slender, attached to long petioles, and bifurcating into slender
ports.

This species approaches 7’. Beinertit and 7. adnascens, and there
are indications that, like the latter, it may have been parasitic on
petioles or branches of other Plants. Numerous specimens occur at
Perry, but all are small and somewhat obscure.

16. Fruices 1ncert sEpis. Pl, XVII. figs, 10 & 16.

Among the Plants collected by Mr. Brown are two somewhat ob-
scure examples of the frond or pinnule represented in Pl. XVII.
fig. 10. It is of a linear form, with crenations or teeth on the mar-
gins. The midrib is delicate ; the nerves, which are rather indistinct,
appear to be netted near ‘the midrib in the manner of Glossopteris,
Brongn. ; but they are distinct toward the margin, where there are,
in the sinuses of the teeth, dark spots, which are probably remains of
fructification. These evidences of marginal fructification remove the
Plant entirely from Glossopteris; and I am not aware of any other
genus of fossil Ferns in which it could be placed. It may have been
allied to such recent genera as Lonchitis or Hypolepis. The speci-
mens are, however, so imperfect and obscure, that I content myself
in the meantime with representing what I can make out of their
form and venation, trusting that they may at some future time be
named from more perfect examples.

The frond or pinnule shown in Pl. XVII. fig. 16 represents another
uncertain species. Itis cuneiform in shape and broad at the base in
all the specimens that I have seen. It has not been found attached
toa stem or petiole. Its venation is less coarse than that of Cyclopteris
Brown, and much coarser than that of C. Rogersi or C. Jacksont.
It approaches also more nearly to parallelism, and*seems less forked.
This leaf would go into the genus Noeggerathia of some authors, and
may be a distinct species; but I am by no means certain that it is
not a young state or marginal division of Cyclopteris Brownn, and
hence refrain, for the present, from naming it.

17. CARPOLITHES LUNATUS, spec. nov. Pl. XVII. fig. 11.
Base rounded regularly, apex broadly truncate and mucronate ;
nucleus surrounded by a narrow margin.
This species is described from a single specimen, which, however,
appears sufficiently well characterized.

1863. ] ; DAWSON—DEVONIAN PLANTS. 465

\/ 18. CarpotirHes? stireva, spec. nov. Pl. XVII. fig. 4.

Elongate, smooth, flattened, sides slightly sinuate ; two inches or less
in length ; a quarter of an inch or less in breadth.

These objects are too thick and carbonaceous to have been fronds
or leaves, and too regular in form to be fragments of stems. . They
may, howeyer, have been swollen extremities of roots.

§ IT. Gaspé, Canada.

The Plants collected at Gaspé by Mr. Bell, last summer, consist.
principally of Psilophyton princeps in all states of preservation,
still further illustrating the predominance of that species in the
Gaspé sandstones, many parts of which were then, for the first time,
explored by Mr. Bell. In addition to the facts previously known re-
specting this Plant, the specimens now obtained illustrate the internal
structure of its creeping rhizomes, previously found only flattened or
as casts. Mr. Bell has also added to the Gaspé flora Leptophleum
rhombicum, previously found only at Perry, and Didymophyllum re-
niforme, a Plant of the Middle Devonian of New York, thus con-
necting by new links the contemporary floras of these distant loca-
lities. His collection also contains two new and curious species of
fossil wood, and several fragments possibly indicating new species,
but at present of ambiguous character. The more important of these

discoveries I indicate under the following heads.

“1. Pstropnyrox princers, Dawson (rhizomata). Pl. XVIII. fig. 22.

Sir W. S. Logan had obtained from the marine limestones at the
base of the Gaspé sandstones, constituting the lowest members of
the Devonian Series, if they are not Upper Silurian, a few flattened
stems, which in my paper on the Devonian Plants of Gaspé* I
referred with doubt to Psilophyton. Mr. Bell has collected many
additional specimens, some of them perfectly flattened, and which,
but for obscure remains of the surface-markings, might readily be
mistaken for Algew; others retain more or less perfectly their cylin-
drical form. The latter are all rhizomata, usually about half an
inch in diameter, and retain the structures of the outer bark and
internal axis in a calcified state, the cell-walls being changed into
coaly matter. The outer bark is seen under the microscope to con-
sist of cellular tissue, dense toward the surface, and more lax within,
as seen in a transverse section ; while in the longitudinal section the
outer portion is found to consist of cells elongated in the manner of
bast-tissue, and the inner of ordinary parenchymatous cells. The
thick inner bark, which was probably of lax cellular tissue, has disap-
peared. The slender cylindrical axis consists of woody fibres exter-
nally, and of scalariform vessels within; it has a vacant space of
very small size in the centre, which may represent a pith, but is
perhaps merely a result of decay and shrinking, which have caused
the vascular bundle to separate from the woody sheath, and the
fibres of the latter to separate in such a manner as to present very

* Quart, Journ. Geol. Soc. vol, xy.

466 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

different aspects in different parts of the axis of the same rhizome.
This structure, it may be observed, corresponds perfectly with that
of the aérial stem of the same Plant, illustrated in my paper on the
Devonian Plants of Gaspé, the differences being merely those which
might have been anticipated from the greater size of the rhizome,
and its probably subaquatic or subterranean character. I have en-
deavoured, in Pl. XVIII. figs. 22a to 22g, to represent the structures
above described, which, with what was previously known, almost
complete our knowledge of this interesting Plant.

-. It is further interesting to observe that Psilophyton princeps has
now been found to extend from the very bottom of the Devonian
series to its upper members, and throughout every part of Eastern
America in which land-plants have been found in these beds. That -
it has not been recognized in Europe I attribute to its want of de-
cided external characters, when in an imperfect state of preservation,
having caused it to be mistaken for Algze, roots, &c. Similar views
might have prevailed here, but for the vast profusion of these Plants
found in situ in Gaspé, and the admirable preservation both of their
external markings and internal structure.

2. NEMATOXYLON CRASSUM, gen. et spec. nov. Pl. XIX. fig. 24.

Fragments of wood with a smooth thin bark, and a tissue wholly com-
posed of elongated cylindrical cells with irregular pores or markings.
No pith, medullary rays, nor rings of growth.

The specimens to which the above description refers are fragments,

the largest of which may have been 2 inches long, an inch wide,
and half an inch thick. They present under a magnifying-glass a
fibrous appearance (as if made up of thin threads or wires), from which
I have taken the name of the genus. They are calcified, and when
sliced show their structures very perfectly. Under the microscope
they at first sight remind the observer of the structure of Prototax-
ites ; but the cells are of one-third greater diameter than in P. Logani,
and are destitute of its peculiar markings, and there are no rings of
growth or medullary rays. The wood-cells are of great length, some-
what tortuous, loosely aggregated, and much thickened. by ligneous
deposit, which appears to be traversed by many narrow tortuous
lines or pores. The whole stem seems to be perfectly homogeneous,
and the only other structure observed was a faint and doubtful trace
of the existence of parenchymatous cells in some of the spaces be-
tween the fibres. The figures show a longitudinal and cross section,
magnified, and a few detached cells or woody fibres still more highly
magnified.
_ With respect to the affinities of this tissue, I can give no opinion.
It may have been that of a Plant whose stem, destitute of true vessels
and composed of woody fibres imbedded singly in cellular tissue, bore
the same relation to that of an Endogen which Prototazites bears to
an ordinary Exogen. On the other hand, it has a sufficiently strong
resemblance to the fibrous outer bark of some Stgillarie to render
it possible that it may have belonged to a Plant of this character, of
which the axis and inner bark have perished.

eo

1863.) . . DAWSON——DEVONIAN PLANTS. 467

3. NEMATOXYLON TENUE, spec. nov. Pl. XVIII. fig. 23.

Slender stems with thick coaly bark, and woody fibres of much smaller
diameter than in the last species, and marked with minute dots.

The stems of this species are small, not exceeding half an inch in
diameter, but are distinctly surrounded by a thick, shining, coaly bark.
The wood is calcified, and appears to be perfectly homogeneous, and
composed of the tissue represented in Pl. XVIII. figs. 23 a to 23 ¢, the
last two of which are drawn to the same scale as fig. 246, to show
the different dimensions of the cells. It may be doubted if this
species has any real affinity with the last, but they correspond in their
negative characters, and both appear to indicate the existence of cer-
tain woody Plants of singularly simple and homogeneous structure.
Many of the small carbonized fragments scattered over the surfaces
of the Gaspé sandstones belong to the present species, and were no-
ticed in my former paper on the Plants of Gaspé as aporous tissues
of uncertain nature,

4, INCERT SEDIS,

Among Mr. Bell’s specimens are many fragments of quite uncer-
tain character. One of these is a stem thickly studded with minute
irregularly placed points or tubercles, and having a finely striated
surface (Pl. XIX. fig. 25). Itresembles the “branching root” figured
by Mr. Salter from the Devonian of Stromness. Another is a stem
with interrupted ridges, in the manner of Rhachiopteris striata from
the Devonian of New York, fig. 31. It may be the stipe of a Fern.
Another (fig. 29) is a very slender stem marked with minute raised
scales or rudimentary leaves, and possibly a Lycopodites of the type
of Z. Milleri, Salter. To these I have added, from my own collection, a
little Stigmarioid Plant, fig. 31, which, if really a Stigmaria, is the
most diminutive of the genus; but it may admit of doubt whether
it is not an imperfectly preserved Lepidodendroid Plant.

5, Atem. Pl. XIX. figs. 32 & 33.

In Mr. Bell’s collection are numerous specimens, apparently of
Sea-weeds, resembling the Cauda-galli Fucoid of the Devonian rocks
of New York. They appear to include two distinct forms. One of
these (fig. 32) consists of cylindrical and dichotomous filaments, and
may be referred to the provisional genus Chondrites. It appears to
be the first or fibrous form of Fucoides Cauda-galli mentioned
by Vanuxem (Report, p. 128, fig.30). The other (fig. 33) is a con-
tinuous frond, and shows indications of having been thickened or
folded at the convex margin. It might be placed in the genus Zo-—
narites, and is probably identical with Vanuxem’s second or conti-
nuous form, for which he proposes the name Fucoides velum. Both
occasionally appear as if looped or attached at both extremities, as
was the case in Vanuxem’s specimens. The first-mentioned species,
or variety, is found in beds believed to be Upper Silurian, and which
contain obscure remains of Land-plants, at Aune a la Barbe in the

468 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

Baie de Chaleurs. The second is also from rocks at Gaspé*, supposed
to be Upper Silurian, but below those containing Land-plants.

SIV. New York.

In my paper of last year several species were referred to the
Cattskill group, being so labelled in the collection of the Geological
Survey of New York. Prof. Hall has, however, communicated to
me, and published in the ‘ Canadian Naturalist,’ observations recently
made by Mr. Way and others, and confirmed by his own examina-
tions, of sections and fossils, which show that the rocks from which
these Plants were obtained really belong to the underlying Portage
and Chemung groups. This brings the distribution of the Devonian
Plants of New York more nearly into harmony with that observed
at Gaspé and elsewhere, and leaves the Cattskill group, as now re-
stricted, destitute of that evidence of connexion with the underlying
beds which these Plants seemed to afford.

I desire to change the name Pecopteris (Alethopteris) decurrens,
of my last paper, into P. discrepanst,—a species from the Coal of
Pennsylvania having been described by Lesquereux under the
former name.

§ V. Conclusion.

The present paper raises the number of species obtained from the
Devonian rocks of Eastern America to about eighty-two, but does not
in any respect invalidate the general conclusions stated in my former
paper. Of the whole number of species, only two can with certainty
be referred to the Lower Devonian, and these also occur higher in
the series. Twenty-one are found in the Middle Devonian, and of
these nine or ten ascend to the Upper Devonian, which has afforded
about sixty-eight species; and of these probably ten are known in
the Carboniferous System. It must be observed, however, that the
precise age of the beds at Perry and St. John is uncertain, and that
they are referred to the Upper Devonian principally on the evidence
of their fossil Plants,—the stratigraphical evidence being sufficient
merely to prove their Precarboniferous date.

EXPLANATION OF PLATES XVII.-XIX.
Puate XVII.

Figs. 1 & 2. Portions of pinne of Lycopodites Richardsoni; (2a) leaves
enlarged.
3. Stigmaria pusilla.
4, Carpolithes? siliqua.

* Prof. Hall informs me that he has ascertained the ordinary Fucoides Cauda-
galli of New York to be fragments of spiral forms, which he proposes to describe,
under a new generic name, in a forthcoming Report of the Regents of the Uni-
versity of New York. It is possible that the Gaspé fucoids above noticed may
also have been spiral in their growth.

+ This correction has already been made in the list of errata occurring in
vol. xviii. of the Society’s Journal, and published, together with the title-page
and index of that volume, with No. 73 of the Journal.—Ebir.

I

XV

ol XIX. PL

V

+

L Soc

G1 S10)

1

i

Journ

zi
Lu

Quar

‘W.West imp.

JWD. del. G. West hth.

DEVONIAN PLANTS, N.E.AMERICA.

‘
}
;
y
{
.
4
ae
|
‘

W.West imp.

Aa DSTA TELE SS OAS ON ERA

nm

a ee nance. |

omens. =
Re pe es ae

Quart. Journ. Geol. Soc. Vol XIX Pl. XVII.

JWOD. del. G:Westlith.

DEVONIAN PLANTS, N.E. AMERICA.

ee ee

ee

Quart. Journ. Geol. Soc. Vol XIX Pl. XDC

Siem r ieee oe ee ein. dcr,

DEVONIAN PLANTS, NE.AMERICA.

JWD.del. G:West. th

4 Jaen . . i ‘se od im
: . Reet alsa te ae 5
| = VN we ee ; oe o

yf Sia re,
' my ay Ly rts
Te Y q ; of
7 i

eee

1863.]

“ DAWSON—CARBONIFEROUS REPTILES. —~ 469

Figs. 5. Fragment of root of Conifer.
6. Portion of pinna of Cyclopteris Brownii; (6 a) stipe of C. Jacksont.
7 & 8. Sphenopteris recurva.
9. Cordaites flecuosus.
10. Pinna of a Fern, not named; (10a) portion magnified.
11. Carpolithes lunatus.
12 & 13. Trichomanites filicula.

14,

Lycopodites comosus; (14 a) portion magnified.

15. Carpolithes spicatus.

16. Fern, not named.

17. Pinna of Cyclopteris Rogersi.
18. Stipe of Cyclopteris Rogersi.

Fig. 19.

Puate XVIII.
Leptophleum rhombicum, restored; (19 a) leaf.

20. Fragment of bark of Conifer.

21.
22.

Fig. 24.

3l.

Anarthrocanna Perryana.

Rhizoma of Psilophyton princeps ; (22 a) cross section of the same,
showing the axis and bark; (22) portion of cross section magni-
fied, showing remains of the bark (3, of inner bark e, of the woody
sheath of the axis y, of the scalariform centre of the axis d; (22 c)
cross section of the tissue of the axis, magnified 100 diameters ;
(22 d) longitudinal section of the tissue of the axis; (22) cross
section of the outer bark ; (22 f) longitudinal section of the axis of
the aérial stem for comparison with e; (224) cross section of the
axis of another specimen, magnified as in c.

. Portion of the stem of Nematoxylon tenue ; (23 a) cross section slightly

enlarged ; (23 5) longitudinal section ; (23 ¢) transverse section,
magnified 200 diameters.

Puate XIX.

Longitudinal section of the stem of Nematoxylon crassum, magnified
100 diameters; (24a) cross section; (246) transverse section of
a few cells, magnified 200 diameters.

. Stem with tubercles; (25 a) magnified.
. Pinna of Cyclopteris Jacksoni; (26a) separate pinnule; (264) dia-

gram of venation ; (26c) small variety.

. Pinna of Cyclopteris Rogersi; (27 a) separate pinnule; (27 3) dia-

gram of venation.

. Pinna of Cyclopteris Halliana; (28 a) separate pinnule ; (28 4) dia-

gram of venation.

. Lycopodites.
. Stem with ridges.

Stigmaria ?; (31 a) areole magnified.

. Fucoides (Chondrites) Cauda-galli (reduced),
. Fucoides (Zonarites) velum (reduced).

2. Notice of a New Spxcres of DenpRERPETON, and of thé DERMAL
Coverines of certain CaRBONIFEROUS Reprites. By J. W. Dawson,

LL.D.,

F.R.S., F.G.S., Principal of M‘Gill University, Montreal.

Tue following notes relate to new facts ascertained in the course of
a re-examination of the remains of Reptiles from the Coal-formation
of Nova Scotia, made in the preparation of a résumé of the cha-
racters of these creatures, which is in course of publication. I
desire now to communicate these facts to the Geological Society, as

they are

connected with, and supplementary to, the descriptions

published at various times in its Journal.

470 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

§ I. Dendrerpeton Owent, spec. nov.

Among the Reptilian remains found in erect trees at the SouthJog-
gins, there have occurred several portions of skeletons, which, from
their sculptured cranial bones, plicated teeth, and the forms of their
scales and limb-bones, I have referred to the genus Dendrerpeton,
but to individuals of much smaller size than the full-grown specimens
of Dendrerpeton Acadianum. It did not occur to me to suppose that
they were specifically distinct from the larger individuals until I
observed that bones of this kind contained in the collections sent by
me to the Geological Society, or represented in the figures drawn
for me by Mr. Smith, were referred by Professor Owen, in his pub-
lished notes on these specimens and drawings *, to the genus Hylono-
mus, or at least mentioned as probably of that genus. Asthe admission
of these into Hylonomus implied a very different range of characters
from those which I had attributed to that genus, and, indeed, left
little distinction between it and Dendrerpeton, I have been induced
carefully to re-examine all the specimens in my collection, with the
view of determining whether they, in any respect, occupied an in-
termediate place between the genera in question. The result has
been to convince-me that there is no generic affinity between these
specimens and Hylonomus, but to establish a probability that there
was a second species of Dendrerpeton in the Coal-measures of Nova
Scotia, differing from D. Acadianum in the following particulars :—
(1) ats much smaller size; (2) its longer and hooked teeth; (3) the
greater corrugation of the dentine of the intermaaillary teeth; (4) the
proportions of the skull, which seems to have been shorter and
broader, with the orbits larger and more oblique. On the other
hand, it differs from all the species of Hylonomus in the following
respects :—(1) the corrugated character of the teeth, which are
always simple in Hylonomus; (2) the presence of an inner row of
large teeth, which do not occur in Hylonomus; (3) the sculptured
surface of the cranial bones, always smooth or faintly puncto-striate
in Hylonomus ; (4) the form of the vertebre and scales, and the
short and stout limbs. In all these respects it resembles Dendrer-
peton Acadianum, and in some of them is more remote from Hylo~
nomus than that species.

On the grounds thus stated, I refer this creature, without doubt,
to the genus Dendrerpeton, and regard it as probably a distinct spe-
cies. I may add, in confirmation of the distinctness of Dendrerpeton »
Oweni, that I have recently found a specimen showing the jaw and
teeth of a small individual of D. Acadianum, corresponding in their
forms with those of the latter species, though the size is that of the
former.

I refer to the present species the bones figured in Prof. Owen’s
paper in the Quarterly Journal of the Geological Society, vol. xviii.
Plate X. figs. 3 & 4, and Plate IX. fig. 4. The maxillary bone in
Plate IX. fig. 15 belongs to D. Acadianum, having the form of teeth
and the bony sculpture of that species.

* Quart. Journ. Geol. Soc. vol. xviii, p. 242, 1862, ©

1863.] .. DAWSON—CARBONIFEROUS REPTILES. ~ 471.

§ IL. Remains of Skin and Horny Scales.

‘In some of my earliest explorations of the reptile-bearing stumps
of the Joggins, I observed on some of the surfaces patches of a
shining black substance, which, on minute examination, proved to
be the remains of cuticle, with horny scales and other appendages.
The fragments were preserved ; but I found it impossible to determine
with certainty to which of the species, whose bones occur with them,
they belonged, or even to ascertain the precise relations of the
several fragments to each other. I therefore merely mentioned them
in general terms, and stated my belief that they must have belonged
to the species of Hylonomus*. More recently other specimens have
been obtained, and I have undertaken the detailed examination of
the whole. I shall now endeavour to describe the principal frag-

ments, and afterwards to consider the probability of their having be-
longed to certain of the Reptiles entombed with them.

1. One of my specimens is a flattened portion of cuticle, 27 inches
in length, and 13 inch in ayerage breadth. The greater part of the
surface, though wrinkled, is smooth and shining to the naked eye;
but under the microscope it shows minute pits or pores, and in places
indistinct imbricated scales. A limited portion of the upper and, I
suppose, anterior part is covered with imbricated scales, visible to
the naked eye, and which are thin and quite free at the lower edges,
though apparently attached to the skin by the whole breadth of the
base. Most of them show a small spot, or pore, near the anterior
edge, and smaller points, or subordinate scales, on their surfaces. In
contact with the upper part of this specimen there are many frag-
ments of the skull of Dendrerpeton Owenc.

2. In another portion of cuticle, similarly marked, the form of
the posterior part of the animal appears to be preserved, and also a
mark representing the point of attachment of the hind leg, near to
which, and also along the dorsal ridge, the skin is covered with
much smaller scales. The lower or abdominal side shows only a
slightly pitted or porous surface. A notch in the lower or abdominal
surface may perhaps represent the anus; and, immediately in ad-
vance of this, the removal of a part of the outer surface showed an
interior membrane marked with rows of small pits or depressions.
This was found in close proximity to a mass of bones of Dendrer-
peton Oweni mixed with some of Hylonomus Lyelli, and is repre-
sented in pl. 1, fig. 5, of my work already referred to.

3. A third portion of cuticle, procured from a different trunk,
presents precisely the features of that above described, but is flat-
tened, and has on its surface a number of vertebre and detached
bones of Hylonomus Wymani. These, however, lie on its outer sur-
face, and the dimensions of this species would seem to be too small
to suit so large a surface of skin.

4, Another well-preserved fragment, less than 2 inches in.
length, presents a very different aspect from those just described.

* Quart. Journ. Geol. Soe. vol. xvi. p. 277.

472 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

Its general surface is covered with small imbricated scales, not
essentially different from those already mentioned, but these are
associated with other appendages. On either side of what seems to
have been the middle line of the back, covered with small scales,
there is a series of flat horny processes, which probably formed a
double spinous crest. Outside these there are two elongated tufts of
densely grouped, slender, bristle-like processes ; exteriorly to which,
there is, on each side, a row of flat, horny, transversely wrinkled
plates. Near them was a short row of conical, truncated, horny
tubercles. Sections of all these appendages show that they were
horny and attached to the skin. This specimen will be figured, with
enlarged views of its appendages, and a section of one of the thicker
scales, in the work already mentioned.

5. Another fragment may have belonged to a different species
from either of the preceding. It is about an inch in length, and
rather less in breadth, and is covered with very small imbricated
scales. It is crossed by six or seven obscure ridges, which, both at
the lower margin and along a middle line, project in points covered
with larger scales; and a row of large scales with round pores connects
these points along the lower edge. If, as seems likely, this fragment
represents the side of the trunk or tail, it would perhaps indicate a
division of the subcutaneous muscles by a mesial line, as in Fishes
and Newts. A separate fragment has a larger lobe or point, of the
same structure as those above described.

6. A few separate fragments show appendages which may have
been connected with some of the larger portions of integument above
described. Two of these detached fragments show pointed and pro-
bably membranous appendages, marked on each side with rows of
scales not overlapping, and each with a pore in its centre. The
manner in which they are folded and bent shows that they must
have been soft, except at the tips, which were probably horny.
They are arranged in series, as if originally attached to the sides of
the body of an animal of a somewhat elongated form. Another and
very small fragment shows a sort of scale, perhaps abdominal, marked
with transverse slightly furrowed ridges. Another and much larger
portion of cuticle has a beautiful covering of imbricated scales, fringed
at the lower margin with larger scales.

The whole of these specimens are chemically in the condition of
highly bituminous coal, affording an example of the production of
that substance from animal membrane and horny matter. They
present the appearance of jet, and burn with much flame and a
bituminous and ammoniacal odour. It is remarkable that in no
case do the portions of cuticle contain the skeleton of the animal to
which they belonged. This may be accounted for by supposing that
the skins were ruptured in decay, and allowed the bones to fall out;
or possibly they may in some cases have been cast while the animals
were alive. Their preservation implies that the mass in which they
were imbedded was wet and impervious to air, as must have ordinarily
been the case in these deep pits in damp soil.

1863.] DAWSON—CARBONIFEROUS REPTILES. 473

- Six species of Reptiles or Batrachians have left their bones in the
repositories containing these remains of cuticle. Of these, Dendrer-
peton Acadianum was an animal too large to permit us to suppose
that the integuments in question belonged to it. Hylonomus acie-
dentatus and Hylerpeton Dawson are each represented by a single
specimen only, and these do not occur on the same surfaces with the
remains of cuticle. Three species remain; and each of these is

represented by several individuals, whose remains occur near to the

fragments of cuticle, and whose size renders it possible that they
may have been its owners. Of these species Dendrerpeton Owens
seems to have the best claim to the specimens described above as
Nos. 1 and 2, and probably also to No. 3. The specimens described as
Nos. 4 and 5 would then probably belong to Hylonomus Wyman and
H. Lyelli, the larger portion noticed as No. 4 to the trunk of the
latter, and that noticed as No. 5 to the trunk of the former. The
pointed appendages, referred to as No.6, are not attached to any of the
larger fragments; but their size and associations render it likely that
they belonged to Hylonomus Lyell, and possibly to H. aciedentatus.

I have ventured, in the work above mentioned, to give rough
restorations of the dermal coverings of these animals, according to
what I regard as the mest probable arrangement of the parts; but
such attempts must be regarded as merely provisional, and to be
corrected by future discoveries. I may add that I have no means
of determining the arrangement of the bony scales which these Rep-
tiles, or some of them, also possessed. These bony scales present,
under the microscope, a structure peculiarly similar to that of the
bones of Dendrerpeton and Hylonomus. They do not appear to be
attached to any of the portions of cuticle, and it is most probable
that they were placed on the head, neck, or abdomen, or perhaps
generally over the lower surface of the body,

I have already expressed my belief that the species of Hylonomus
may have Lacertian affinities ; and I think their dermal coverings lend
some countenance to this view. We may, however, suppose them to
have been either true Reptiles having certain Batrachian tendencies,
or Batrachians presenting some structural points now limited to true
Reptiles; or, lastly, we may suppose that the specimens entombed
in the erect Srgillarie may be the young of species of Reptiles too
large and vigorous, when adult, to be entrapped in such pitfalls.

I would, however, observe that, in the case of Hylonomus, the
smooth cranial bones, the simple teeth, the long curved ribs, the
well-developed limbs, and the cutaneous appendages must absolutely
prevent this genus from entering either the Order Ganocephala or
the Order Labyrinthodontia, as defined by Owen. If they should
prove to be really Batrachian, a new Order must be constituted for
their reception, and its definition will present many points of coin-
cidence with those of the characters of the humbler tribes of Lizards.

I propose, in the memoir already referred to, to figure and describe
all the characteristic bones of these creatures in my possession, with
the view of enabling naturalists to form more definite opinions on
these points.

yOL, XIX.—PART I, 2k

474 PROCEEDINGS OF THE GHOLOGICAL SOCIETY. [May 20,

3. On the Upper Oxp Rep SanpstonE and Upper Deyontran Rooks.
By J. W. Sarrer, Esq., F.G.8., A.L.S.

ConrTENTS.
1. Introduction, 5. South Treland.
2. South Pembrokeshire. | 6. Foreign Equivalents.
3. North Devonshire. 7. General Conclusions.
4. Somersetshire, Gloucestershire, and 8. Appendix.
Shropshire.

§ 1. Introduction.

T was engaged for three summer months in 1854, and again for a
short time last year, in examining carefully the lower beds of the
Mountain Limestone and the uppermost beds of the Old Red Sand-
stone, with a view to establish, if possible, the correlation between the
Upper Old Red and the corresponding portion of the Devonian series
—a relation which has been called in question by good observers.

The memoir of Sedgwick and Murchison* was, indeed, a full state-
ment of the identification of the Old Red Sandstone, as a mass, with
the Devonian ; a comparison first suggested by Lonsdale from a con-
sideration of the fossil evidence, and ably supported by Godwin-Austen
from his Rhenish explorations, though afterwards called in question
by him, The identification is repeated in the later edition of ‘Siluria.’
Yet, over the North-European districts, there is a singular deficiency
of proof of the superposition of the Devonian to the Upper Silurian
rocks, and more especially of the gradual passage, at any one point,
of the Old Red Sandstone into rocks of the Devonian type.

It has been argued, and with reason, by Sharpeyt that in Belgium
Old Red Sandstone of the ordinary type waderlies the whole of the
Devonian rocks with marine fossils. The opposite case occurs in the
red conglomerates of the Catskill group in America, which themselves
overlie the Devonian. But it has been much overlooked that, in the
latter country, the whole Devonian mass, distinguished by its fossils,
is Clearly superposed on Upper Silurian rocks; while it has been by
no means certain what part of our great Old Red Sandstone group
is represented by the red conglomerates either of America or of Bel-
gium. Nor has it been decisively shown that the Old Red Sandstone
passes conformably into the strata above or below it; all that could
be said with certainty was this—that the Devonian rocks contain
fossils of a newer type than the Silurian and overlie them, and that .
the Old Red Sandstone holds some intermediate place between the
Silurian and the Carboniferous rocks.

In this state of the question, the positive identification of any one
part of the Old Red series with any one portion of the Devonian
became of paramount consequence ; since, if we could know the true
succession of the Old Red beds as accurately as that of the Devonian
rocks has been already traced, we might be able to prove or disprove
the correlation of the two series. I have tried to do this, and have,
I hope, succeeded.

* “On the Devonian Rocks of the Rhenish Provinces,” Trans. Geol. Soc. 2nd

ser. vol. v. pp. 633 &c.
t+ Quart. Journ. Geol. Soe. vol. ix. p. 18.

1863. ] . SALTER—-UPPER OLD RED SANDSTONE. 475

' In the measured sections given by Sir H. De Ja Beche in the
‘Memoirs of the Geological Survey’*, those of East and West Pem-
brokeshire show a clear succession from the Upper Old Red Sand-
stone to the Carboniferous Shales. The most complete of these sec-
tions are those from Caldy Island and Skrinkle Hayen, Tenby,
where the whole mass of the Mountain Limestone is underlain by
shales and limestones, and these again by the upper beds of the Old
Red Sandstone, in unbroken succession. About 150 feet of the latter
formation is given in detail. Twenty miles to the west another sec-
tion, different in detail, but in the main similar, is exhibited in
the wild coast-line of West Angle Bay, Pembrokeshiret. The dis-
erepancies, and agreements too, between the different parts of these
sections are very striking. J examined them all, and then, crossing
_ the Bristol Channel, took up the corresponding sections on the Barn-
staple river and the coast at Croyde Bay. A single fossil in the
collections made by Prof. Phillips in West Pembrokeshire gave me
the hope of identifying the lowest beds of the limestone-shale with
the uppermost Devonian beds, nor was I at all disappointed.

The detailed examinations are written, and wait for publication
in the Memoirs of the Geological Survey. I will here confine myself
to general statements, somewhat different from those made, on my
evidence, in the Anniversary Address of the President of the Geological
Society in 1855. In that year I visited the South of Ireland, and, in
company with Mr. Jukes, saw ample confirmation of the succession
observed in the North Devon and Pembroke sections. The results
obtained are correctly stated in ‘ Siluria,’ 2nd ed., pp. 299, 300. In
Mr. Hamilton’s Address I had, however, ventured prematurely to
identify the Lower Limestone-shales of Pembrokeshire with the
Pilton group (uppermost Devonian) of North Devon; and this in
the teeth of paleontological evidence which was fully stated, and
which ought to have weighed more heavily with me. So exactly
similar, however, are the two sections physically, and so exactly does
the fauna of one represent the fauna of the other, that I allowed
myself to believe that two sets of species, closely allied but actually
different, had lived at one and the same time on either side of a
barrier so narrow as the width of the Bristol Channel!

This idea, which was backed by the strong conviction and pub-
lished opinion of Sir H. De la Beche, was in accordance too with the
doctrine of marine provinces lately advocated by Prof. Edward
Forbes, and there is no wonder that I embraced it.

In the meantime I was enabled to see, in 1857, the Cornish sec-
tion, and was satisfied that the Upper Devonian group in Britain
was divisible into two seriest. And I had in Ireland seen the up-
permost of these in its true place—beneath the Limestone-shale—
and forming, or resting immediately on, the uppermost portion of

* Vol. i. pp. 61, 108, 111, &e.

+ These sections are unrivalled for extent and completeness. The vertical
beds exposed to the coast-waves are worn by them in a manner to clear them of
all detritus, and exhibit the whole series in a remarkably distinct manner.

t ‘Siluria,’ 2nd ed. p. 300.

2K 2

476 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

the Old Red Sandstone. These two formations, when Yon Dechen’s
Map of the Rhenish Provinces was published, were found to be
parallel to the two highest divisions of the Devonian system on the
Continent.

I may now proceed to a few details.

§ 2. South Pembrokeshire.

The best section, sheltered from the south-west winds, and acces-
sible in part at all tides, is on the eastern side of Caldy Island. The
Upper Old Red marls and sandstones, forming the southern horn of
Drinkim Bay, end upwards in yellow conglomerates, and are covered
by 400 feet of shale and limestone in a most variable series. At the
very base are beds of shale with ordinary Carboniferous fossils, such
as occur among the alternating shales and calcareous beds beneath
the mass (nearly 2000 feet) of the Carboniferous Limestone, and in
the base of that rock itself.

The Old Red Sandstone, therefore, at this locality is abruptly
distinct from the overlying beds, in colour, substance, and more
especially in its destitution of fossils.

On the eastern side of the island, where the shales are best seen,
I found the upper portion of the Old Red for some distance much
softer than the beds below, almost destitute of cornstone, and chiefly
consisting of sands and marls of bright colours, mixed with beds of
pale conglomerate, which last is persistent through the island, form-
ing reefs on either side, and stretching away far into South Pem-
brokeshire. This band of pale conglomerates is a good horizon; by
taking advantage of it I was able to compare, bed by bed, the va-
riable series of sandstones and marls below; and on the west side
of the island, about 50 feet down in the Old Red series, to my great
astonishment, a bed of Serpule occurred, in masses, like the S. filo-
grana. I believe the species to be new, and call it Serpula advena
(see figure, p. 496).

Crossing by boat to Skrinkle Bay, of which De la Beche and
Ramsay have given detailed sections, the same beds are visible, even
to minute details. It is needless therefore to describe the separate
sections. Nearly every bed of calcareous shale, nodular or flat-bedded
limestone, cherty sandstone, and oolitic limestone (whieh is very
common) can be traced in the three sections. There is a special
group of oolite-beds and grit near the base, a band of oolitie lime-
stone two-thirds up, and between the two a remarkable series of
thin cherty sandstone-bands, permeated thickly by the burrows of
worms. All of these subgroups are recognizable on the east and west
of Caldy Island, at Skrinkle Bay, and, as will be seen afterwards, to
the extreme point of Pembrokeshire.

These sections are all accessible by paths down the cliff, or better
still by boat from Tenby.

At Skrinkle the upper 133 feet of Old Red Sandstone rests on
some white sandstones, which are conspicuous at Caldy. The upper
37 feet of Old Red is, however, lost by an oblique fault, and this
should be borne in mind in comparing the sections.

1863. ] SALTER—UPPER OLD RED SANDSTONE, 477

The shale-series is remarkable for the quantity of broken and
rolled Fish-remains. Psammodus or Helodus, Cladodus, and, more
rarely, Orodus seem to be the chief cartilaginous Fish, with scales of
Paleoniscus in plenty. Black rounded masses, which I cannot but
regard as coprolitic, but in which my friend Mr. R. Smith can find
no phosphates, contain bones of Fish, with Shells of Orthoceras, Nu-
cula, Cytheropsis, &e. Sometimes rounded masses of this kind seem
to have no organisms included in them. All are blackened. Again,
rounded masses of the ordinary colour of the shale occur, enclosing
Cytheropsis in myriads. Perhaps the whole may be water-worn, as
Sir Henry De la Beche suggested* in the case of the very similar
Bristol bone-beds. I do not know how to explain the blackening
of the included Shells on that view of the case.

The number and size of the Worm-burrows, often 3 inches broad and
many feet in length, form, perhaps, one of the most striking features
in the Lower Limestone-shales. They are present, of small size but
in great numbers, in the group of cherty rocks before mentioned, and
which can be traced, about 70 or 80 feet from the base, throughout
the whole of South Pembrokeshire. The action of the Worms bring-
ing clayey matter into sandy beds, and vice versd, gives great tough-
ness to the rocks, and they resist the sea-action well.

Twenty miles to the westward the small bay of West Angle opens
at the mouth of Milford Haven, and here a sharp faulted synclinal,
in the middle of the bay, permits the whole section to be twice seen
in the promontories and reefs on either side of the bay. The sec-
tion has changed considerably from what is exhibited on the eastern
coast, and nearly 150 feet more shales are added to the upper part.
In these shales a very perfect cleavage is established, fully justifying
the term “ Carboniferous slate” applied to this formation in Ireland
by Sir R. Griffith f.

Sundry other changes are observable when this section is com-
pared with that on the opposite sea-border. The Fish-beds are indeed
present, the bands of oolite and grit agree remarkably in the lower
part of the section, but the thick bands of limestone are replaced by
nodular beds, which indicate a deficiency in the supply of lime.
Again, there is a difference of importance near the base, inasmuch |
as the nodular limestone-bands there contain a vast quantity of a
peculiar Bivalve, for which, as I cannot find a name, I have proposed
the term Curtonotus (see Appendix, p. 494). It occurs in red lme-
stone and grit, to the exclusion of all other fossils, in the bottom
bands on the south side of the bay.

The yellow conglomerates have disappeared, but yellow and brown
sandstone has taken their place; and there is a further remarkable
change in the upper part of the Old Red Sandstone, to which I will
direct particular attention.

* Mem. Geol, Surv. vol. i. p. 124.

+ The upper part of the Skrinkle section measures 135 feet, that of Angle
322 feet. The conditions under which the beds were deposited were greatly
different.

+ It is, however, the Lower Limestone-shale of Dr. Smith, as seen at Bristol
and the Mendips.

478 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20;

I may observe, that the section north and south of the bay is an
unequal one, so far as the Upper Old Red is concerned, though mar-
vellously exact in the overlying beds. On the northern horn of the
bay the stacks and cliffs show a great many bands of conglomerate ;
on the south side scarcely any, the distance being barely a mile.
Northward, the Old Red Sandstone is red sandstone and marl nearly
to the top, intermixed only with a few subcalcareous bands and grey
sandstone; but on the south side each of these interealations becomes
magnified, so to speak. The limestones are thicker and more fre-
quent, and are crowded with fossils; the grey shales thicken out to
the exclusion of the red marls; grey sandstone is abundant; and the
result is that, out of 120 feet, there is not above 25 feet of red shale
in the upper portion of the Old Red Sandstone at this point. Then
follow red, green, and grey beds, in the usual fashion, all the way
to Freshwater *.

By this remarkable change in the mineral character we are pre-
pared for a considerable change in the conditions of life. The soli-
tary Serpula in the cliffs of Caldy had already indicated the neigh-
bourhood of marine life. I found scattered specimens of the same
Serpula here, about 70 feet below the top; but with it were a
number of other forms, familiar to me only in North Devon, namely,
Avicula Damnonensis, in abundance; Cucullea trapezium?; Rhyn-
chonella laticosta; Bellerophon, three species, one identical with the
B. bisulcatus of North Devon; with numerous undescribed forms of
Pleurotomaria, Nucula, Sanguinolites, Modiola, Awinus, and Discina.
In beds of shale associated with these are numerous linear Plants
(observed first by Sir H. De la Beche), but not determinable; they
extend their range into the underlying Old Red?f.

§ 3. North Devonshire.

This change in the mineral character, accompanied by the intro-
duction of a marine fauna, conducts us somewhat less abruptly than
would otherwise be the case to the calcareous and slaty sediments on
the opposite coast of Devonshire. The red tint is, indeed, not wholly
lost in North Deyon, but is confined to narrow belts of the Devonian
. rocks.

I crossed from Combe Martin and Ilfracombe to Barnstaple, in
_ more than one direction, and could find no red colour at all. A
purple tint, however, stains the belt of slate-rocks (Morte Slates of
Sedgwick and Murchison) which intervenes between the grey Middle
Devonian slates of Ilfracombe and the Upper Devonian of Barn-
staple and its neighbourhood. Itis of these last that I must now say
a little, the «‘ Marwood beds” of the above authors being the upper-
most strata of their Devonian system ; and these, in their grey sand- —

* It is worth while noting that the Old Red Sandstone at Freshwater, where
it overlies the Silurian rocks, commences with a conglomerate of Silurian peb-
bles. We have, indeed, plenty of evidence that there is not in Pembrokeshire a
continuous section from the Silurian to the Old Red Sandstone; and in all pro-
bability none but the upper division of the latter formation is present.

t Mem. Geol. Surv. vol. i. p. 107.

1863.] SALTER—-UPPER OLD RED SANDSTONE. 479

stones, calcareous layers, and argillaceous shales, are only (on a
much larger scale) the limestene, shale, and sandstone we have left
in South Pembrokeshire.

Neglecting then the purple Morte slates, which, being destitute
of fossils, cannot yet be safely paralleled with any special division of
the Old Red*, I may, however, say that they pass up by insensible
gradations and loss of colour inte the Marwood series.

In ascending order we have :—
1. Purple slates and sandstones of Morte Bay.
2. A band of pale, nearly white slate, with a few Bivalves.
3. A thick series of greenish-grey grits, with bands of Cu-
cullea and Avicula Damnoniensis, in abundance, and with much
olive shale, in which a new Lingula occurs abundantly.
4, An alternating series of calcareous sandstone, grey shales with
thin nodular bands of limestone, and grey cleaved slate full of
fossils, and many hundred feet thick. Avicula Damnoniensis and
Lthynchonella laticosta, with numerous Lamellibranchiata, occur in
the lower part; and Strophatosia caperata with Spirifer Barumensis
throughout.

The series No. 4 is the upper part of the “ Pilton group” of
Phillips; and its aspect in the grand coast-section of Baggy Point
and Croyde Bay is exactly like that assumed by the Carboniferous
Slates of Pembrokeshire, as they lie, in the section befere noticed,
upon the fossiliferous beds of the Upper Old Red.

So like are the two sections, and so exactly does the succession
appear to correspond, that my faith in fossil-evidence gave way, in
1854, before this apparent identity. The grey sandstone and inter-
vening Plant-beds of Baggy are so like those of West Angle (on a
larger scale), and the overlying calcareous and shaly series so like

Marwood Beds.

Fig. 1.—Generalized Section in Pembrokeshire and North Ireland.

Upper Old Red Carboniferous Slate ha Carboniferous
CI REDE (4? &5). Limestone (6).

Fig. 2.—Generalized Section in Devonshire and South Ireland.

Carboniferous
Limestone (6).

(, 2) Upper Devonian [Marwood (3) and Pilton Group (4)]- oe
ate (5).

the bottom part of the Carboniferous Slate of Angle—having a very
sunilar set of fossils and a few even identical,—that an older geologist

_ * Professor Jukes admits, as I do, these reddish-purple slates to be the equi-
valents of the Old Red of the South of Ireland, and in the same mineral condition.

480 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

than myself must be forgiven for having identified them. Sir H.
De la Beche was decided in his opinion of their being equivalents*.
This view, however, is, I think, erroneous. The Upper Pilton group
(No. 4) in the main represents a series unknown in Pembrokeshire
(compare figs. 1 & 2), or only represented by beds a few feet thick at
the base of the true Carboniferous slate, while its lower portion and
the whole of the Marwood group (No. 3) are certainly equivalent to
the capping of the Old Red Sandstone. I hope I shall have the full
concurrence of the Irish geologists in this last view; Mr. Jukes did
all he could to persuade me, in South Ireland, of the intercalation
of group 4. I could not, however, disbelieve the North Devon sec-
tion, but I had misinterpreted it.

I will now give a few of the chief fossil types, and glance at the
necessary conclusions. The band of pale slate at its base is an ex-
cellent landmark for following the broken outline of the Marwood
beds, from Baggy Point, where they are best exhibited, to eight or
ten miles east of Barnstaple. The whole country is cut up by north
and south faults, and by oblique faults not laid down on any of our
maps, but they do not confuse the sequence much.

Either at Baggy Point, Braunton, Marwood, or Sloly quarries
(the last locality being best known), the Marwood beds contain the
following species :—

In the calcareous sandstones (often a brown limestone), Cucullea
trapezium and its varieties, C. Hardingii, Ctenodonta (Pullastra) anti-
qua, Avicula Damnoniensis, Edmondia, Sanguinolites, Axinus, Mya-
cites, Modiola, and Orthonota of large and small undescribed species.
Spirifer Vernewliu and S. laminosus? occur very rarely. The latter
is a Carboniferous species, as also is Rhynchonella pleurodon, which
is also met with in this bed, together with species of Natica, Platy-
schisma, Macrocheilus, Pleuwrotomaria, and Orthoceras with lateral
siphon, chiefly, if not all, of undescribed species. Two species of
Bellerophon are very common, one of them being either B. bisulcatus,
Reemer, or closely allied to it.

In the greenish shales, or silty beds, are found Bornia ( Calamites)
transitionis, Goeppert, and Lepidodendron (Knorria) dichotomum,
Haughton, and its roots. Lingula Molay, sp. nov., is abundant,
and Orthonota, or Myacites, rare. Discina also occurs, and Worm-
burrows are exceedingly abundant.

Above these sandstone-beds and olive shales commences the cal-
careous and argillaceous Pilton group. It is chiefly grey slate and
finely laminated calcareous sandstone; but thin actual limestone-
bands, oolitic in parts, are frequent in it. Towards the bottom the
shale-beds are rich in Bivalves, both Lamellibranchs and Brachio-
pods. Of the characteristic shells Avicula Damnoniensis is the
most abundant species; Strophalosia (Lepteena) caperata occurs of
large size, and is associated with Spirifer disjunctus, Sow., S. Ba-
rumensis, Sow., Productus prelongus, Sow. (P. Christiant), Orthis in-

* Mem. Geol. Surv. pp. 133, 140, &e.

t Named after the Rev. F. Mules, of Muddiford, Barnstaple. Specimens are
in the Museum of Practical Geology.

1863. | SALTER—UPPER OLD RED SANDSTONE. 481

terlineata, Sow., and Phacops latifrons, Bronn. But with them are
present species of the new genus Curtonotus, of Ctenodonta, Modiola,
Chonetes (small species), Bellerophon, and Aviculopecten (two or
three species); also Encrinites of the genera Actinocrinus, Poterio-
crinus, and Rhodocrinus, all abundant.

There are also black nodules, which contain phosphates dissemi-
nated in the shale along certain lines, and they are, I believe, drop-
pings of Fish. They exactly resemble those in the very similar
slate-series of Angle. There are crowds of Encrinites, not, so far as
I can make out, of the same species, but exceedingly like those of
the Angle Bay section.

There are Orthoceras and Nucula, a small spiral Huomphalus,
smooth and black, and a minute Loxonema,—all of which closely
represent analogous forms in the West Angle series. And there are
the occasional pebble-beds (layers of flat shale-pebbles mixed with
black nodules of various sizes), and the shells above mentioned,
with Curtonotus, long meandering sand-lines, drifted patches with
Shells in them, Annelide-burrows, &c., all as at Angle.

Some of the species at Baggy Point are identical with those at Angle.
I do not know how to distinguish the Rhynchonella from R. pleurodon.
I find it exceedingly difficult sometimes to decide if the Spirifer
be S. disjunctus or one of the varieties of S. attenuatus, &c. But
these doubtful cases (and there are not many of them) are overruled
by the fact that the characteristic Shells are all of the Devonian type.
The catalogue given (p. 480) scarcely contains a Carboniferous form ;
on the contrary, the peculiar species are abundant throughout.

As this is both the most complete and most accessible section, I
will here say of it that the dip continues southwards, though with
several minor faults and flexures, to Croyde Bay (where there is
-good accommodation for the geologist), and here the highest beds of
the series are still full of Phacops latifrons; while the Chonetes and
other shells, such as Athyris concentrica, are common. Spirifer lami-
nosus, a Carboniferous fossil, occurs here among them, but rarely.

The section on the south side of Croyde Bay is only a repetition
of that on the north, and the cliffs along the coast to Saunton show
only the same fossil forms.

Exactly similar sectiqns are obtainable along the Ilfracombe road
from Braunton, along the course of the Knowlwater to Marwood,
and again from Barnstaple. On this last section a few notes may
suffice. I had the advantage here of the great local knowledge of
the Rev. F. Mules, who has produced a MS. map of the range of
the several subdivisions of the rocks of North Devon. It gives the
general course of these formations with accuracy, from Morte Bay to
Exmoor, beyond which the Marwood beds have not yet been traced.
I did not myself go quite so far east.

The road-section from Muddiford to Barnstaple shows a perfect
sequence from the purple slates, through the white band, to a well-
developed Marwood group. The great quarries at Sloly are those
best known as containing the Lepidodendra, Calamites, and other
Plant-fragments first described by Professor Sedgwick. I have the

482 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

measurements of all the beds, and I find that Lingula oceurs in great
quantities in the olive shales, while the calcareous sandstones are full
of Cucullea, Bellerophon, Orthoceras, &e. The whole must have been
accumulated in a very shallow sea.

Thence southward, undulating beds of slate with many sandstone-
bands contain all the fossils of the Pilton group. Top Orchard
quarry, near Pilton, is a favourite locality. In beds below this, and
very near the base of the group, I found a single specimen of Cur-
tonotus, which is somewhat important, inasmuch as this genus, both
in Pembrokeshire and in South Ireland, belongs only to the beds which
underlie the true Carboniferous slate. Spirifer disjunctus, Productus
Christiant, i.e. prelongus, Avicula subradiata, and Athyris concen-
trica are still the common fossils.

But nearer Barnstaple these Pilton beds begin to trough small
patches of a barren softer slate, which is only seen well developed
south of Pilton, and occupying the lower ground east and west of
Barnstaple. Another anticlinal roll throws in a trough of it about
Ashford and Heanton Punchardon, and it is fossiliferous on Ashford
Strand. South of the river it may be seen along the course of the
railway, skirting the marshy ground, and there is a good section of
it at the railway- station.

It is extremely difficult to say precisely where the Pilton group
ends and this group of shales begins; but the absence of sandstone-
bands and the presence of only Carboniferous species show suffi-
ciently the reality of the change. Strophalosia caperata, var. mem-
branacea, is occasionally present, but not the ordinary variety. It
is associated with Spirifer laminosus, S. cuspidatus, Streptorhynchus
crenistria, Chonetes Hardrensis, Athyris Roissy, Bellerophon decus-
satus, Productus costatus, P. Martin, Orthis Michelin, Venus paral-
lela, Phillips, Spirtfer ovalis (small), S. bisulcatus, Phillipsia semini-
fera, and many others. But these are enough to show that we have
-passed from the sandy Pilton group to the true Carboniferous Slate.
The Encrinites are exceedingly common: but those stems I have
been able to compare with Pilton species are not identical, while all
the peculiar Pilton species are quite absent. Yet the general aspect
of the Encrinites, Fenestella, striated Spirifert, Chonetes, &c., is so
much that of the Pilton group just underlying, that it was only by
great good fortune I made out the troughs of this newer formation,
lying among the contorted beds of the Pilton group.

South of Barnstaple we are indeed fairly in the Carboniferous
series. Along the course of the Fremington Pill I found, in 1854,
‘shaly beds overlying these, still with Mountain-limestone fossils.
The Productus Cora, or rather P. Scotica*, as it ought to be called, is
a fossil not yet detected even so low as the Limestone-shale. But
how far upward the Mountain-limestone extends until it is capped
by the Millstone-grit of Coddon Hill it would be out of my province
to discuss here. It is more to the purpose to mention briefly the

* Sowerby’s type-specimens of P. Scotica are identical with the shell D’Orbigny
afterwards called P. Cora, and M‘Coy P, corrugata.

1863.] SALTER—UPPER OLD RED SANDSTONE. 483

result of a short visit to the southern side of the culm-trough, in the
autumn of 1857. The Torquay section was briefly examined, and
its correspondence with that of the Spirifer-sandstone group of the
Rhine, as given in ‘ Siluria,’ easily perceived.

The fossils of the ordinary Plymouth limestones, of all colours, are
so well known that no time need be spent in proving them to be the
equivalents of the Eifel limestone, or of the Combe Martin limestones
of North Devon. Unfortunately the special object on which I was
sent did not permit me to examine the Newton Bushel section* ;
but 01 crossing the Devonian slates from Plymouth, by Tavistock,
to Launceston, I found everywhere the same silvery slate which
must be familiar to every geologist who has visited Ilfr.combe. Nor
was I then aware of the importance of identifying the red band of
the Morte slates with the beds about Launceston and Petherwin,
though I now believe them to be equivalents—a point of no little
importance in the geology of Devon and Cornwall; for, in a tole-
rably careful survey of the Launceston beds, I fully convinced myself
(and, on my return, Sir Roderick Murchison) that the Petherwin
limestone-group did not represent the Barnstaple series, as had been
formerly supposed, but that it was a lower band in the Devonian
series}. The reason for this determination will appear by comparing
the following list of fossils, all of which came from the Landlake
and Petherwin quarries, with those above named from the “ Mar-
wood group.”

List of the Petherwin and Landlake Fossils (Upper Devowan).

Petraia Celtica. Pterinea ventricosa.
Amplexus tortuosus. Avicula subradiata.
Cyathophyllum czspitosum. exarata.
Fenestella laxa. Cardiola retrostriata (Cardium pal-
antiqua. matum).
Sanguinolaria? sulcata, Strophalosia caperata, rare.
Ctenodonta (Pullastra) elliptica. —— membranacea, more frequent.
Orthonota (Cypricardia) semisulcata. subaculeata (Leptzena laxispina,
Axinus (Cypricardia) deltoideus. L. fragaria, &c.), abundant.
Aviculopecten granulosus. Orthis interlineata.
transversus. resupinata.
alternatus. Streptorhynchus crenistria.
— arachnoideus. ; Spirifer protensus.

* T have lately seen it, for a single day, in company with Mr. W. Vicary, of
Exeter. It is clear enough that there is an Upper as well as a Middle Devonian
series in this place, the lower limestones of Bradley Woods being quite different
from the higher, close to the town, and containing different fossils. The Upper
or Clymenia-limestones must have existed close by, as pebbles from them, con-
taining the Clymenie, are abundant at Teignmouth (Shaldon).

+ That this determination is not without its value will appear on comparing
the statements made to the above effect in ‘Siluria,’ p. 300, with those in the
Preface to the 2nd Fasciculus of Prof. Sedgwick’s Cambridge work, 1852, or
more lately in the excellent Synoptical Table by Professor King, of Galway, in
which these authors place the Petherwin Slates with Clymenia (the true Upper
Devonian of the Continent) above the Marwood or Coomhola group. In the
Continental sections one or other of these is frequently absent, the true reason
for which will be apparent as we proceed.

484 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

Spirifer Urii SS unguiculus). Bellerophon (trilobatus?), probably B.
lineatus bisulcatus, Roem.
—— Verneuilii. Orthoceras cinctum.
Barumensis ? * laterale.
—— disjunctus, includingS.giganteus. striatulum.
grandeevus. striatum, M‘Coy.
bisulcatus. fusiforme.
Atrypa desquamatat. Cyrtoceras rusticum.
Rhynchonella pleurodon. Nautilus megasipho.
subdentata. Goniatites insignis.
rhomboidea. — bisulcatus.
pugnus ? —— biferus.
Euomphalus serpens. Clymenia lzvigata.
Natica nexicosta. striata.
Pleurotomaria cancellata. -—— linearis.
antitorquata. fasciata.
aspera. sagittalis.
Loxonema sinuosa ? —— plurisepta.
nexilis. valida.
—— tumida. Phacops (Calymene) granulatus.

This list, if may be observed, differs in almost every point from
the Barnstaple list, and the Petherwin beds were probably deposited
in deeper water. It is true that several of the characteristic fossils
are the same in both series ; but there is an entire absence in the
Pilton or Barnstaple series of the Clymenie and Goniatites, so
characteristic of Upper Devonian strata on the Continent, and also
of the Phacops granulatus. I have taken the list as it stands in my
note-books, adding to it the species quoted by Professor Phillips,
for which we are chiefly indebted to the researches of Mr. Pattison.
Mr. Lee, of Caerleon, contributed some good materials.

It will be seen, too, that this list fails in two or three important
points to tally with that of the fossils from the Barnstaple series.
Instead of the large Phacops latifrons, we have the small P. granu-
latus; Spirifer Barumensis is, I believe, quite absent; Productus
prelongus is not found there; and Strophalosia subaculeata takes
the place, as an abundant species, which S. caperata occupies at
Barnstaple. Much of this change may be due to a different depth
of water for the deposit ; but it cannot be wholly so; and I should
look for the equivalent of the Petherwin beds, which are exactly the
‘‘Clymenien-Kalk” of the Prussian geologists, in the red slates of
Morte Bay,

It was in vain to search for the Pilton group along the borders of
the Culm-measures, which, contrary to expectation, I found to be
unconformable to the Devonian beds, at least near Launceston. And
in its lowest beds, very black shales with much chert in them are
the usual state of things in the Culm-measures.

The shales or slates in which the Devonian limestones of Pether-
win occur are very much like, in a general sense, those of Ifracombe—
that is, pale grey slate, with no sandstone-beds, and bearing all the
marks of deep-sea accumulation.

* IT am not sure of this species.
+ This I think doubtful, but it is important to notice it. It may be Atrypa
reticularis,

1863. ] SALTER—UPPER OLD RED SANDSTONE. 485

Further north, in the midst of the undulating trough of Culm-
measures, a locality called Yealm Bridge, north of Launceston, has
long been known as a fossiliferous place. It is a sharp and faulted
anticlinal of hard slate-rocks, about a mile or a mile and a half in
diameter ; and Mr. Pattison, who knows the spot well, told me I
should find Petraia and Phacops latifrons there. This then would
identify the rock with the Barnstaple series, of which we otherwise
have no trace on the south edge of the Culm district. I found this
statement strictly correct; and the list of fossils, imperfect as it
must be (being the result of only two days’ examination), is yet a
sufficient index of the true geological position. The dip being north-
wards, and the Culm unconformable, it was only to be expected that
we should find higher beds in an exposure to the northward; and I
believe this small inlier (to adopt a new and proper phrase, invented
by Mr. Drew) is one of the best proofs we could have that the
Barnstaple or Pilton group overlies the Petherwin group.

§ 4. Somersetshire, Gloucestershire, and Shropshire.

Before passing over to the South of Ireland, it will be well to
notice the general character of the parallel sections further to the
north-east, namely, at Dean Forest, Bristol, and the Mendips; and
to call attention to the newly described section of the Clee Hills, as
given in Mr. Roberts’s and Professor Morris’s account in the Society’s
Journal*. This must necessarily be brief, and it may be at once
stated that all these sections conform nearly to the northern type,
or that of Tenby above described. In all, the thick limestones are
succeeded, in the downward section, by arenaceous shales and thin
limestone-beds, and these by sandy beds, grey, and finally yellow as
they pass into the red marls and sandstones of the Upper Old Red.

In Dean Forest Mr. James givest, below the alternating shale-
series, the following beds :—

; Arenaceous shales.
oes { Coarse yellow sandstone containing Shells.

( Red marl.
Red marl with yellow sandstone.
Coarse yellow sandstone and whitish shale, full of
Upper Old Red.< _— Plants. '
Green shale and sandstone.
Red marl.
\ Thick yellow sandstone, with whitish shale.

Red marl.
Greenish and grey sandstones and shale, very
micaceous, &e.

And so on until the whitish and grey sandstones cease to appear
among the red marls. We must, by comparison with the Tenby
sections, draw the divisional line as above.

In the Lower Purlieu section, in the same district, the limestones,

* Vol. xviii. p. 94. Tt Geol. Surv., Vertical Section No. 12.

486 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

mixed with shale, come close down upon the yellow sandstones, as
is the case at Clydach in Monmouthshire in even a more striking
way*.

The well-known Clifton section also gives the same results, with
the great advantage of being all visible along the Avon. Mr. D. H.
Williams givest, below the thick alternating series of shales and
limestone, crowded from top to bottom, as I have myself seen, with
the same Mountain-limestone species as those common at Tenby,

Grey shale and red marl (thin limestones).

Light quartzose sandstone and conglomerates.

Red and claret-coloured marls and sandstones.

Light grey and brown sandstones and shales.

Red marls and light-grey sandstones, &e. &e.

I must by no means omit to notice the careful section of the Far-
low bedst by Messrs. Roberts and Morris. In this compact paper,
the passage upward from

1. Red sandstone, with cornstone, to
2. Yellow sandstone and conglomerate, containing Holoptychius
giganteus, Pterichthys macrocephalus, and a larger species, and
then to
3. Grey oolitic limestones, bearing Fish, or Crinoids, or Bra-
chiopods in the several bands, and these interstratified again
with clays of various colour,
is completely in accordance with the Pembroke sections. The Bra-
chiopods are mostly identical with those from Tenby. Spirifer cus-
pidatus, and the varieties which seem to connect this species with
S. distans, Sow., together with Athyris, Rhynchonella, and other
fossils, completely recall to mind the Tenby sections.

The Fish too, though far more numerous and better preserved,
are in the main identical. Orodus, Psammodus, Helodus, and Cla-
dodus, among them, are excellent types for the Lower Limestone-
shales.

But the measured thickness of this section gives us no idea of the
masses to be seen in Pembrokeshire ; and we have only the general
accordance—of red sandstones surmounted by yellow grits full of
characteristic Upper Devonian types—to assure us that the Upper
Old Red is here, as in the sections above described, gradually losing
its colour before being overlain by the deeper-water sediments of the
Carboniferous series.

In the Mendips a valuable section by Mr. D. H. Williams$ shows
the same alternations of impure limestone and shale, at the base
interstratified, as at Caldy Island, with red limestones and oolitic
bands; and a thick series of brown calcareous sandstones which can
be exactly paralleled with Nos. 77 to 80 of the Skrinkle Bay section ||.

Then a few alternations of red shale and cherty limestone at the
base conduct us to hard light-grey sandstones, which here form the

* Mr. Rees’s Section, Geol. Surv., Vertical Section No. 12.

+ Geol. Surv., Vertical Sections Nos. 11 & 12.

~ Quart. Journ. Geol. Soe. vol. xviii. p. 95.

§. Geol. Surv., Vertical Section No. 12. || Zbid. No. 12.

1863.] — SALTER—UPPER OLD RED SANDSTONE. ~ 487.

uppermost part of the Old Red, as they do in the sections just quoted.
This is perhaps the nearest approach to the North Devon type that
any of the sections on the parallel of the Bristol Channel present.
These light-grey sandstones and the intervening grey and green-
ish shales should be well searched. ‘They are sure to contain the
characteristic Knorria dichotoma; for this (or analogous Plants) was
found by Earl Ducie in the Tortworth grits. And it would be a
great corroboration of this view if some beds of the Avicula Damno-
mensis could be found among them, as in the West Pembroke section.

§ 5. South Ireland.

While we wait for a memoir on the Irish Upper Devonians, I
cannot do better than give a short abstract of the paper by Mr. J.
Beete Jukes and myself, published in the ‘ Journal of the Geological
Society of Dublin,’ 1855, vol. vii. p. 63.

First, we found it impossible to separate the so-called Yellow
Sandstone of the South of Ireland from the Old Red, for the good
and sufficient reason that it is, as in all the other sections, the upper
part of that formation itself, losing its colour preparatory to the in-
troduction of the Carboniferous series. [The Yellow Sandstone of
the North of Ireland is a different thing; as in Scotland it is there
*the base of the Carboniferous Limestone, and contains Carboniferous
fossils only.] Both in the Yellow Sandstone and the red and green
beds below we found the Knorria and its roots (filicites dichotoma,
Haughton). In more productive beds in Kilkenny and near Cork
Prof. E. Forbes had already found the Anodon? Jukesw, which is
probably a Modiola. Stigmaria and Lepidodendron occurred here,
but no decided traces of Sigillaria, nor do I believe there are any
instances of this genus occurring below the lowest Carboniferous
beds.

Next, the Carboniferous Slate, which overlies the Yellow Sandstone,
is very thin towards the east—that is, in Kilkenny, Waterford, and
Wexford (the fine section at the Hook, Wexford, is the best worth
study); but towards the west it thickens out, and from Cork to Bantry
is interstratified at its base with grits, which form, near Glengariff, a
group 3000 feet thick, and which were termed by us, as they had
been previously by Mr. Jukes and the Irish Survey, “‘ Coomhola
Grits.”

If a line be drawn from Kenmare through Macroom and Cork,
thence south of Youghal to the Bristol Channel, it will coincide with
the boundary between the northern or Herefordshire type of the Old
Red Sandstone and Carboniferous Shale, without the intervention of
the Coomhola Grits, and the southern or Devonian type as seen at
Bantry, Kinsale, and all through Devonshire. It will define also
the northern limit of the “‘ Coomhola Grits.” And, lastly, it is the
boundary-line between the coarse shallow-water deposits of the Old
Red Sandstone, with pebble-beds and Plants, and the more open-sea
Devonian deposits, of thicker mass, finer grain, and lighter colour,
full of marine Shells and Corals. The boundary is not an arbitrary
one, but appears to have been a line of coast, or of shallow water,

488 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

during the period of the deposition of the limestone-shale, as well as
the uppermost beds of the Devonian series.

These grits, we observed, differed little from the Devonian grits
below them, except in being chiefly grey, and having intercalated
beds of dark grey, instead of greenish, shales. The partings of black
or dark-grey shale constitute the only mineral character we could
find to separate the two series.

The fossils of the Carboniferous Slates and Coomhola Series are
as follows :—

Carboniferous Slate.

Among a host of others occur Fenestella plebera, Actinocrinus, Platy-
crinus, Poteriocrinus, and Rhodocrinus, which I think identical
with the Carboniferous forms. With them, however, were in
abundance Spirifer cuspidatus, a Carboniferous form, with S.
disjunctus ? (I believe this to be the wide form of S. bisulcatus,
so common in all the Pembroke sections). In addition were
Orthis Michelin, Streptorhynchus cremstria, Athyris squamosa,
Productus, sp., Rhynchonella pleurodon (abundant), Orthoceras,
Nucula, and, lastly, the Modiola Macadami, Portlock,—a shell
abundant in Lower Carboniferous beds. Annelide-trails and
-burrows were abundant in all the beds, as they are also in the
underlying Coomhola Grits.

Coomhola Series.

In the western part of Cork, and notably at Dunworley Bay, Dirk
Bay, Skibbereen, and Glengariff, we have Encrinites of the same
genera as above, but several of them apparently of different
species from those of the Carboniferous Limestone. Rhyncho-
nella pleurodon, Spirifer cuspidatus? (doubtful), S. dasjunctus
(S. Vernewilii, Murch.); many undescribed bivalves of the genera
Modiola, Ctenodonta (Nucula), Cucullea, Awinus, Avicula, Avi-
culopecten, and a new genus for which I proposed the name

* Curtonotus; Bellerophon, with rounded, keeled, and trilobate
dorsal edges, as in North Devon; Cucullewa of several species,
and C. trapezium; Lingula, new large species; Rhynchonella
pleurodon and KR. laticosta?; and, lastly, the most common
Shell and Plant, Avicula Damnoniensis and Knorria dichotoma
in every shale- bed.

The conclusions we arrived at were :—

1. That in South Ireland the Yellow Sandstone was the upper
part of the Old Red.

2. The Carboniferous Slate, whether well or thinly developed,
contains in its upper part the ordinary Carboniferous types.

3. A local but considerable group intervenes, physically more con-
nected with the Carboniferous, but distinct as to fossils. It has the
same Plants as the Upper Devonian'(that is, Upper Old Red), some few
Shells of the Carboniferous Limestone, and numerous Bivalves pecu-
liar to itself. This group is the equivalent of the Marwood sandstones*.

* In part only: as I have above shown (p. 480), it is the true equivalent of the
Upper Pilton group.—J. W.S.

1863. ] SALTER—UPPER OLD RED SANDSTONE. 489

4. In our postscript we inclined to the view that No. 3 was a de-
cidedly Carboniferous group; but this was owing to the mistaken
notion that the Pilton or Upper Marwood group was the equivalent
of the Carboniferous slate,—a statement made on my own authority,
as above noticed. For all else in this memoir, except the supposed
identification of the Spirzfer disjunctus in the Carboniferous Slate, and
of S. cuspidatus (which I now believe to include S. Barumensis) in the
Coomhola Grit, I am willing to be equally responsible with Mr. Jukes.

§ 6. Foreign Equivalents.

On these I do not intend to say much, having never seen the
French and Belgian Devonian rocks. But the broad and general
view of them given in the second edition of ‘ Siluria,’ together with
Messrs. Sharpe and Godwin-Austen’s papers in our own Journal,
surely entitle us to attempt the parallel, which I hope personal ob-
servation will enable me one day to verify.

In the last edition of ‘ Siluria’ the three or, rather, four subdivi-
sions of the Old Red Sandstone are thus given in ascending order :—

This term has given rise to much con-

1. Tilestones or “ Passage fusion, and the beds would be much
beds.” better called «‘ Ledbury Shales ;” I,
therefore, propose this term for them.

mee Devonian,“ Co- ) on awictarined by Cephalaspis, Pteraspis,

blentzSandstone,” Low-
er Cornstone group of a &c., as well as by pecu-

the Old Red.

3. Middle Devonian, ne: Coccosteus, Asterolepis, Dipterus, Cal-

and Plymouth Lime- ceola, Stringocephalus.

stones, Caithness Flags.
( Holoptychius, Glyptopomus, Cucullea
4. ven eng shies | trapezium, Avicula Damnoniensis,
ae i en te Spirifer disjunctus, Athyris concen-
Spent ROMS, zd trica, Strophalosia subaculeata, Car-

and Kramenzel-Stein, | :
; ; dium palmatum, Clymenice, Phacops
Petherwin Group. L granulosus,

Comparing with the above series the last revision of the Devonian
Geology of the Rhenish Provinces, as given in the Map of Von
Dechen and his associates, we find the following :—

1, Ardennes Schiefer, Co-
blentz-Schichten (or
Spirifer Sandstone),
Wissenbach Schiefer.

2. Lenne-Schiefer, Eifel- | Plymouth and Combe-Martin Lime-
Kalk. } stones.

3. Cypridinen-Schiefer, in-~
cluding the Goniatite- |
shales, Flinz, and Kra- >Petherwin Group in every detail.
menzel-Stein with Cly-
mene. |

VOL, XIX,—PART I, 2%

These are represented truly by our
Linton and Fowey groups, in North
Devon and Cornwall.

——

490 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

4. Verneuilii-Schiefer, Ar- | Marwood (and Pilton?) Group, with
gillaceous Sandstone. exactly the same fossils.

These Verneuilii-Schiefer (a bad name for a group already named
by Sedgwick and Murchison) come up in long parallel folds near
Aix-la-Chapelle and rest on the Eifel-Kalk, without the intervention
(at this place) of the Cypridina-Schist, and are themselves covered
by the Kohlenkalk or Mountain Limestone. This fact is valuable,
as indicating what we have as yet failed to detect in North Devon—
an unconformity between the Marwood group and the other mem-
bers of the Devonian formation*.

In the Bas Boulonnais, Sir Roderick Murchison described, in
1840, some of the Devonian species, but failed to make out that the
whole series was only the uppermost portion of that formation ; nor
was Mr. Godwin-Austen, in 18537, completely set free from the
notion of older Devonian rocks being present, as Delanoue and others
had determined.

But Mr. Austen’s paper gives all the necessary elements for
correcting this view ; the stratigraphy is clear, and the lists of fossils
complete. Below the Mountain Limestone he found a band of shale
(Le Hure, Ferques, &c.), which he passes over without much com-
ment, but which must either be the Limestone-shale or the Pilton
group, and his paper conducts us at once to

The Yellow Sandstone group =“ Gres @ Unio” of Rozet [Psammite
de Ludlow, of the Boulogne Meeting +t], Landrethun to Ferques,
25 feet thick (Bois de Beaulieu, &c.), meeting the Coal-mea-
sures (Dufrénoy), Marwood Sandstone (Austen).

There can be no doubt of the age of this sandstone. Cucullea
Hardingui, C. trapezium, Bellerophon subglobatus, &c., tell the story
at once, and leave us free to consider the strata below them.

If the Boulogne formation were anything like the same in deve-
lopment as our North Devon series, the thickness of 25 feet of sand-
stone would give us a mere capping for the great Marwood series ;
accordingly we find, in descending order,

Bright red shales and clays.

Dark. grey. shales ..°....: 2...

Ferques limestone.—Near Malaise, Bois de Beaulieu, and to the
Chateau de Fiennes. Great abundance of Spirifer disjunctus.

A selected list of the fossils of this limestone gives us the true Pil-
ton group. We have Athyris concentrica, Rhynchonella pleurodon,
Spirifer Bouchardi, S. disjunctus, Strophalosia caperata (S. scabricu-
lus, Sharpe), and Phacops latifrons (P. Latreillii). With these, how-
ever, are a few which are more characteristic of the Newton-Bushel
limestones than the Barnstaple group, namely, Atrypa reticularis,

* Unconformity to the largest extent has long been known between the Upper
and Lower Old Red in South-west Ireland. Sir R. Griffith described it ; Sir R. I.
Murchison, Mr. Jukes, the Members of the Geological Survey of Ireland, and
myself saw it in 1856; and since then Mr. Geikie has described the same thing
as occurring in Scotland. See Quart. Journ. Geol. Soe. vol. xvi. p. 312.

t Quart. Journ. Geol. Soc. vol. ix. p. 251, &e.

+ Bulletin de la Société Géologique de France, vol. x. p. 404, 1840.

Chateau de Fiennes.

1863. | SALTER—UPPER OLD RED SANDSTONE. 491

Terebratula hastata, Spirifer heteroclytus? (S. subconicus), Stropho-
mena Dutertrii, and Strophalosia subaculeata; also Favosites poly-
morpha, Cyathophyllum, and other Corals. Red shale, again, and
dolomitic limestone lead down to the Blacourt Limestone (= Lime-
stone of La Cédule, &c.), which is worked in part for iron-ores. Still
we have the same fossils, with some omissions and additions, and then
a series of shales, which is followed by compact micaceous sandstone
with Ferns*, Calamites (probably Bornia transitionis), &c., with some
of the above fossils. There is nothing in the whole section to indi-
cate that we have reached a lower horizon than that of the Marwood
beds. Mr. Austen’s comparison of them with the Ogwell, Plymouth,
and Linton groups is the only flaw in an admirable paper.

In Mr. Sharpe’s paper in the same volume of our Journal 7, an at-
tempt is made to compare the Belgian series with our British rocks.
Generally speaking, it comes to the same results as those given in
‘Siluria’ above quoted.

But the lower part of M. Dumont’s “ Systéme Condrusien”’ evi-
dently includes the Barnstaple (and Petherwin?) group, resting as
this does upon the Eifel or Middle Devonian series.

For the present it will be sufficient to indicate that the “‘ Systeme
Condrusien’’ may be divided thus :—

Upper = Carboniferous Limestone.
Lower = Barnstaple or Pilton group.

The grey micaceous sandstones and flags of the lower division certainly
point to the same horizon as the sandstones, shales, &c., of the Boulon-
nais, and M. Gosselet’s important papert only confirms this idea.

I take advantage of this opportunity (referring to the abstract by
Mr. Pattison in the Journal for November 1861, vol. xvi. part 2.p.27)
to enumerate the chief divisions of the series as given by M. Gosselet.
In descending order, his numbers are :—

Nos. 1. English equivalents (J. W. S.).

bd

2. } Coal and Carboniferous Limestone.
3.
( Marwood beds; containing Pha-
cops latifrons, Athyris concen-
4, Psammites de een) trica, Spirifer Vernewili, and
| Strophalosia scabriculus (pro-
| bably S. caperata).
f Petherwin bedsand Upper Newton
Bushel limestone; containing
Rhynchonella cuboides, Spririfer
| Vernewilii, Cardium palmatum$.
6. Givet limestone = Plymouth and Ogwell.
7. Calceola slate = Limestone-shale (Chircombe, &c.).

* These fossils should be examined carefully. In all probability the Fern is
Adiantites Hibernicus. Moreover, the so-called Graptolites from Caffiers have
been determined to be leaf-stems or -stalks. Here we have all the analogies of
the Marwood group.

t Vol. ix. p. 18. t Bull. Soc. Géol. de France, 2™¢ sér. vol. xviii. p. 18.

§ The author specially remarks the absence of the Clymenia; but though this

242

5. Slates of Famenne =
|

492 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

Nos. 8, 9, 10, the remaining Devonian groups, are not necessary
{0 our purpose. But it is worthy of remark that the fossils quoted
by M. Gosselet as having been found by M. Hébert in the Burnot
conglomerate are Marwood species (Cuculleea Harding. Productus ?
Murchisonianus, &c.), and must have been obtained from other and
higher beds.

It would appear, from all that has been published regarding the
Upper Devonian beds of Saxony, the Hartz, Nassau, and Westphalia,
that the Marwood beds are absent in these districts,—the Carboni-
ferous Limestone resting at once on the Clymenia-limestone, or
Petherwin group.

In the Rhenish provinces, in Belgium, and in the north-west of
France, on the contrary, the Marwood group is present. And this
variety in the distribution adds strength to the inference already
drawn on other grounds, that the Marwood group is unconformable
to the other members of the Devonian. The Carboniferous Slate is,
as we have seen, only here and there developed to its full extent ;
and as we know that the Mountain Limestone itself is universal over
the greater part of Europe, and has besides a much wider extension,
the reasonable inference would be that, after the filling-up of the
sea-bed towards the close of the Devonian period, a continued sub-
sidence took place, which allowed the older beds to be gradually
covered up successively, first by the Marwood and Pilton group, then
by the Carboniferous Slate or Lower Limestone-shale (the terms
are convertible), and lastly by the thick masses of the Mountain
Limestone itself, which we know in many cases overlaps the whole
Devonian series and rests upon the Silurian slates.

I should scarcely have referred to the North-American area but
for the purpose of directing attention to a very interesting point,
confirmatory of all that has been said above regarding the age of the
uppermost Devonian-——the “ Chemung group” of the New York series.

Of this group Professor Hall has given sufficient details in his
‘Geology of the Fourth District’ to enable us to see that its fossils,
as a whole, agree well with the Petherwin or Upper Devonian group.
It includes several fossils with which we are familiar. Amongst
them, Phacops nupera, Hall (P. bufo, var.) ; Aviculopecten, a great
many species; Orthis interlineata; Spirifer disjunctus, and many
others, including S. Uri (S. unguiculus); Atrypa reticularis, and
many varieties of this variable shell, as in our own Newton-Bushel
limestones, e. g. A. dumosa, A. hystrix, A. tenuilineata, &e.; Pe-
traia, Ceriopora, &c.; also Avicula Damnoniensis in plenty. This
group of species might be easily referred to the Barnstaple group,
but it is more agreeable with the whole of the facts to consider it
the equivalent of the Petherwin or Clymenia-group, and the fossils
are rather in favour of this view. Moreover, Professor Hall lays

omission is of importance, and may render it possible for No. 5 to be a lower
member of the Barnstaple or Pilton group, this is unlikely, as Cardiwm palma-
tum is a characteristic Petherwin species, and rarely, if ever, occurs in the Mar-
wood beds.

1863. | SALTER—-UPPER OLD RED SANDSTONE. 493

stress on its union, as a formation, with the rest of the New York
series—the Portage, Hamilton, and other groups, which represent the
mass of the Devonian. It is covered (unconformably?) by the
Catskill conglomerate, which there can be no doubt represents our
own Upper Old Red, and therefore the Marwood series inclusively.

§ 7. General Conclusions.

If I have thus established clearly, by position, by intercalation
of marine beds with the red sandstone, and by fossils, the identity of
the uppermost Devonian or Marwood group with the Upper Old Red
(I must omit for the present the Petherwin group, which is also
probably, but not certainly, included in this upper division), it re-
mains to be seen whether the same great clue—the fossil evidence—
will suffice to give us the long-wished-for identification of the Middle
and Lower Devonian with the Middle and Lower Old Ked Sandstone.
It is not difficult of proof.

I hold that the masterly suggestion of Sir R. I. Murchison, that
the Caithness Flags, full of Coccosteus, Pterichthys, and a dozen other
genera, belong to the Middle, and that the Cephalaspis-beds of
Scotland belong to the Lower Division of the Old Red, is the great-
est advance made of late years in the classification of the British
Devonian rocks.

Without this clue we were in a sea of difficulties and contradic-
tions. But, following it out, the whole of the Old Red Sandstone
subdivisions fall into their proper places, and can be correlated ac-
curately with the Continental equivalents*.

Thus, in Russia, the Eifel, and the Hartz, Coccosteus, the cha-
racteristic Fish of the Middle Old Red beds, is found associated
with the fossils of the Eifel or Middle Devonian limestone. In
Russia, Sir Roderick Murchison informs me, they have been found
by his friends in the same slab. The identity of this part of the
two formations is thus proved, and need not further be discussed.

But what of the Cephalaspis-beds or Lowest Old Red? And how
are we to identify them with the Lowest Devonian, the Coblentzian
or Rhenane series ?

Professor Ferd. Reemert and Professor Huxley ¢ have unexpect-
edly answered this question for us. The former obtained a fossil
which he supposed to be a naked Cephalopod, allied to the Sepia, and
which he described as Archeoteuthis Dunensis in the ‘ Paleeontogra-
phica’ and the ‘Jahrbuch.’ It came from the Lower or Coblentzian
rocks of Daun. Afterwards it was again obtained from Wassenach,
on the Laacher-see, Lower Eifel. There is no doubt whatever that

* While these pages are writing, Sir Roderick has received specimens, ob-
tained by Mr. C. Peach, from the beds which rise out from under the Caithness
flags, at Ulbster Wick. They prove to contain specimens of the Pterygotus-
type, and are most satisfactory as proving the succession to be what was before
indicated. See Prof. Ramsay’s Anniversary Address to the Geological Society,
Quart. Journ. Geol. Soc. vol. xix. p. xlv. 1863.

+ Palzontographieca, vol. iv. p.72; Leonhard and Bronn’s Jahrb. 1858, p. 59.

~ Quart. Journ. Geol. Soc. vol. xvii. p. 163.

494 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

Professor Huxley is right in referring this fossil to the genus Pter-
aspis—than which Ganoid Fish, abnormal though it be, there is no
more characteristic fossil of the Lower Cornstones of the Old Red
Sandstone. The Lower Devonian is therefore the equivalent of the
Lower Old Red Sandstone.

There remain only the “ Tilestones,” or “‘ Ledbury Shales,’’ which
contain a different fauna from all these, but unequivocally (as I
believe) Lowest Devonian. But as these should form the subject
of a separate memoir, [ will not trench upon that ground at present.

§ 8. Appendia.
CURTONOTUS, gen. nov.

It is necessary here to give the characters of a genus of Bivalves,
often quoted in the preceding pages, and which has long been known
in our lists of fossils without having been sufficiently illustrated.

I believe I proposed the name in the joint memoir by Mr. Jukes
and myself in 1855. The genus is intended to include a number of oval
thick-shelled bivalves related to Myophoria and Axinus, but distinct
at a glance by the general rounded form, and technically by the
simple, not divided, central teeth of the hinge.

The genus is characteristic of the Pilton group throughout, occur-
ring at its extreme attenuated end, or immediately above it, in Pem-
brokeshire, and abundant throughout the Coomhola grits of South
Ireland, while it occurs, though rarely, in the Barnstaple slates.

Some six or eight species are recognizable; some of which are
mentioned in the Explanations of Sheets 197, 198 of the Irish Sur-
vey, pp. 10 e¢ seg.; and one is figured in Professor Jukes’s ‘ Manual,’
2nd edit. p. 508, fig. 14 f.

The following names are used in the Explanatory Sheets for the
Irish Survey, Sheets 197, 198 :—

Curtonotus elegans, Salter, in Jukes’s Manual, as above quoted.

C. rotundatus, Salter, Expl. J. ¢. p. 11, Co. Cork, Ardgroom.

C. elongatus, Salter, Old Head of Kinsale, Dunworley Bay.

These are, on an average, 14 inch wide; and there are some still
larger species in the Irish cabinets.

Generic Characters.—In the typical species, C. elegans, from Angle
Bay, Pembrokeshire, the beaks are prominent and placed at the an-
terior fourth. In one of the species from Co. Cork they are low and
nearly halfway from the anterior end. In C. elongatus they over-
hang the anterior side. However they may be placed, beneath them
in each valve is a thickened hinge-plate with a single strong trian-
gular central tooth, smooth-edged, and not indented below as in
Schizodus. In the left valve this tooth hes behind the deep notch
for the corresponding and equally large tooth in the right valve, this
being in front of it; and in the right valve only is there an obscure
tooth behind the central one. ‘There are no remote cardinal teeth,
nor hinge-lamella for the support of a ligament, which it seems must
have been external. ‘The anterior muscular scar is deep, the poste-
rior less excavated, and placed far inwards; the pallial impression
is entire, at a considerable distance from the edge in most of the

1863. | SALTER—UPPER OLD RED SANDSTONE. 495

species. A thick low ridge extends from the hinge-plate behind
the anterior muscular scar..

Curtonotus ELEGANS, Salter. Figs.3a,36. Jukes’s Manual, 2nd
edit. p. 508, fig. 14, f.
An inch wide, gently convex, regularly oval, not very thick-

shelled; beak small; nearly overhanging the anterior side ; pallial
line near the margin. Surface smooth. Cardinal tooth oblique ;

hinge-plate moderate.
Co. Cork (Pilton group), Dunworley Bay. In the Mus. Irish In-

dustry.

Figs. 3-5.—Shells from the Pilton Group.
3a 30

Curtonotus, three species:—3a,3 6. C. elegans. 44,46. C. centralis.

oa-d d. C. elongatus.

Curtonotus Unto, spec. nov.

Round-ovate, not pointed at either end, about 1 inch high and
14 long, gently convex, the beak rather prominent and nearly over-
hanging the anterior end. A broad callosity runs vertically from
beneath it within the shell. Anterior muscular scar small, but deep ;
posterior placed high up, distinct, oval. Pallial border not very near
the edge; shell thick about the hinge. Cardinal teeth narrow,
nearly direct.

West Angle Bay, W. Pembrokeshire, in the lowest Carboniferous

496 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 20,

Shale, or upper part of the Pilton group. In the Mus. Pract.
Geology.

CURTONOTUS CENTRALIS, spec. nov. Figs. 4a, 4 6.

Transversely oval, rather thick-shelled, convex; the low beak
more than one-third from the anterior end. Cardinal tooth direct ;
hinge-plate moderately thick. Pallial scar rather near the margin.

From the Pilton group, N. of Enniskeen, co. Cork. In the Mus.
Irish Industry.

Curronotus ELONGATUS, Salter. Figs. 5a—5 d.

Transversely oval, gibbous from the prominent beak, which is
terminal, and overhangs the short oblique anterior end. Hinder
margin rounded. Breadth to length as 7 to 18. Surface concentri-
cally striate. Hinge-plate triangular, thick, with a large tooth in
either valve, and a very small secondary anterior one in the left
valve.

From the Pilton group, Co. Cork. Townland of Leheragh, Dun-
worley Bay. Bear Island, Kerry. Old Head of Kinsale. In the
Mus. Irish Industry.

I also subjoin a description of the Serpula from the Upper Old
Red Sandstone, above mentioned, p. 476.

Fig. 6.—WMass of Serpula advena, from the Upper Old Red of Caldy
Island, West side (natural size).

ZONA

MOa\

MKS

\y
aS

SYN vot

ins
>

He i
(i Is
AG a)

XK Os, ae

SERPULA ADVENA, spec. nov. Fig. 6.

Short wavy cylindrical tubes, one-third of a line wide, and about
one inch long, closely aggregated, ascending. The surface is smooth,
or, at least, not roughly ridged (a). The state of preservation does not
permit me to say whether the surface is quite smooth, or marked with
lines of growth. The tubes are filled with solid carbonate of lime,
and lie in a red sandy matrix.

This species occurs 40 feet below the uppermost bed of the Old
Red Sandstone, in Sandtap Bay, west of Caldy Island, Pembrokeshire,
whence it was collected by me in 1854; also in beds of the same
age at West Angle, Pembrokeshire.

“I

1863. ] PRESTWICH—MOULIN QUIGNON. 49

JUNE 3, 1863.

The Rey. Richard Wilson Greaves, M.A., Rector of Tooting, was
elected a Fellow.

The following communication was read :—

On the Srction at Movin Quienon, ABBEVILLE, and on the PECULIAR
CuaracteR of some of the Frint Impiements recently discovered
there. By JosrepH Prestwicu, F.R.S., Treas. G.S.

A snort notice of the age and character of these beds was given by
me in a paper read before the Royal Society in May 1859, and I
should not have recurred to this small section had not the recent an-
nouncement of the discovery of a Human Jaw and of Flint Implements
of a peculiar type, by M. Boucher de Perthes, attracted particular
attention to these beds, and led to questions being raised respecting
both the age of the beds and the genuineness of the remains.

The general grounds on which the antiquity of the Human remains
have been questioned are :—1st, the exceptional condition of the Hu-
man Jaw; and 2nd, the peculiar character and fresh-looking aspect
of the Flint Implements. On the first point I do not wish to make
any observations, as the question will be discussed by Dr. Falconer.
Nor will I dwell long on the second point, with regard to which I
have taken a more active part. Up to the beginning of this year
Flint Implements had been rarely found at Moulin Quignon. I had
visited the pit at least seven or eight times, sometimes alone, at other
times in company with my friend Mr. Evans and others, but we had
never succeeded in finding a Flint Implement, nor even in obtaining
a specimen from the workmen. I have two specimens given me by
M. de Perthes, and Mr. Evans has one given him by M. Marcotte.
These, and all those which I had seen in the collection of M. de
Perthes, were invariably stained of a dark yellow or brown colour,
were generally worn, and had the usual lustre of old specimens. Not
only do they possess these characters of Quaternary Flint Implements,
but they possess them in a degree more marked than do those from
any other spot. Nowhere are they so much coloured, and nowhere
so much worn. A number of them are also ruder than any I have
seen anywhere else. When, therefore, on the 13th of April last, Mr.
Evans and I saw the collection of Flint Implements which M. Boucher
de Perthes had obtained from the bed containing the Human Jaw, their
characters struck us as being so exceptional as to raise serious doubts
as to their authenticity. Before, however, pronouncing an opinion, we
went to Moulin Quignon to examine further the section. Unfortu-
nately there had been a fall of the gravel, and the face of the section
was almost entirely obscured, so that it was impossible for us to
obtain the evidence we required. We went, therefore, to the pit at
St. Gilles, and on our way, the workman who accompanied us took
two Flint Implements from his pocket and handed them to me, saying
he had found them at Moulin Quignon. These specimens were rude,
badly shaped, and apparently smeared over with a ferruginous
clayey sand. Upon washing one of these at the first cottage we came

498 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 3,

to, all the soiling came off readily, and left the flint as fresh as though
it were the work of yesterday. In sharpness of angles and in form,
it also differed widely from all previously discovered at Moulin
Quignon. We concluded that these two specimens were forgeries,
and to that opinion I still adhere. On our return to M. Boucher de
Perthes, we took the opportunity to express our doubts as to the
authenticity of the Flint Implements he had recently obtained from
Moulin Quignon, and to suggest how serious a doubt this would cast
upon the jaw itself. We asked him to wash some of the specimens,
and one that he did so wash only confirmed our opinion. At the same
time we should have reserved the general expression of this opinion
until there had been an opportunity for further inquiry, and study of
the section. Our object was merely to caution M.dePerthes. Cireum-
stances led to our being called upon to endorse that opinion before we
had had the opportunity of the further examination we could have
wished ; nevertheless what we afterwards saw of other Flint Imple-
ments recently brought from the same place strengthened our first
impression. In all these recently found specimens there is an entire
absence of all the characters by which we had hitherto distinguished
genuine from false specimens. It is true that both at Menchecourt
and St. Acheul we had met with Flint Implements sharp and not
worn, some not stained, and some rude in form, but, on all, some one
character of antiquity was to be found: on one traces of incrustation
of carbonate of lime; on another, of dendrites; on a third, of
discolouring ; and on a fourth, lustre. So also we could find here and
there a flint, sharp, fresh, and not coloured. But all these were
exceptional characters, whereas in the case of the new Moulin-
Quignon specimens these exceptions become the rule. That one or
even two specimens might be found exhibiting these exceptional
characters might, it seemed, have been possible; but when we found
that all, without exception, exhibited these characters, the impro-
bability of such an occurrence became so great as to cause us to be-
lieve that some imposition had been practised. There were, it is true,
two or three specimens about which I felt more doubt; but, on the
whole, the unfavourable evidence outweighed other considerations.
The intrinsic evidence on the two points was therefore in accord-
ance, and equally unfavourable to the authenticity of the case. The
objections raised to this conclusion by the French naturalists, who
had taken up the subject, led to a friendly meeting in Paris *.
Mr. Evans was unable to attend this meeting; it will therefore
be understood that I no longer refer to his opinion in conjunction
with my own. The inquiry lasted three days, when, unable to agree
in a conclusion, we adjourned for further inquiry to Abbeville. The
discussion was careful and temperate. Each point was fully gone
into at the Paris sittings. Our French allies) not having had, pro-

* The members of the meeting were:—M. Milne-Edwards, president; M. de
Quatrefages, M. Desnoyers, M. Delesse, M. Lartet, Dr. Falconer, Mr. Busk, Dr.
Carpenter (in Paris only), and the author. For full particulars of the inquiry
see the careful account of the “ Proces Verbaux,”’ published by Dr. Falconer and
others, in the ‘ Natural History Review’ for August 1863.

1863. | PRESTWICH——-MOULIN QUIGNON. 499

bably, so much experience as ourselves of the condition of the various
egravel-beds, and of the Flint Implements found in them) were not so
much struck as we were with the exceptional characters of those
recently discovered at Moulin Quignon, whilst, with us, these cha-
racters were considered an insuperable bar to admitting them to be
genuine.

Thus far on this point there was no difference of opinion amongst
the English members of the meeting, and with it some of the French
members concurred. The visit to Abbeville led to a change of
opinion with several, myself amongst the number.

No notice had been given of our intended visit, and we appeared
on the scene quite unexpectedly. Operations were commenced at
seven in the morning of the 12th of May, and were continued,
without intermission, until five in the evening, during which time
some members of the meeting were always present, watching the
work and the workmen. The section was first cleared, and a fresh
vertical surface from the top down to the chalk exposed. The strata
appeared to be in their natural condition, and there was no ap-
parent derangement of the stratification, though it was a good deal
confused, as is common in gravel-beds, but nothing remarkable or
requiring notice. In the course of the day, five Flint Implements—
one of the old and unquestioned type, and the other four of the type
which we had considered spurious—were obtained. They were
found in the lower part of the gravel, 8 to 12 feet from the surface,
and on or a little above the level of the “‘ Black Band,’’ in which the
jaw had been found, and at but a short distance from that spot.
The finding of every specimen was witnessed by some one or other
cause for not accepting the authenticity of the specimens ; nor, as it
member of the party, although I was not so fortunate as to see one
discovered myself; and, notwithstanding therefore the singular and
exceptional character of these Flint Implements, I saw no sufficient
was the unanimous conclusion that no fraud had been practised, and
seeing certain exceptional characters obtaining in this bed and in the
Human Jaw, for contesting the verdict respecting the authenticity of
the latter, though on this latter point I speak with reserve, especially
as my friends Dr. Falconer and Mr. Busk held a different opinion.

The result of this day’s inquiry led me to believe, therefore, that I
was mistaken in attaching undue weight to negative characters, and
that many of these peculiar Flint Implements were really genuine
specimens, thus confirming the researches and opinion of M. Boucher
de Perthes, M. de Quatrefages, M. Abbé Bourgeois, Mr. Brady, and
others, who had examined the section before we had, and arrived at
the conclusion that the Flint Implements were genuine. The lately
discovered specimens are generally rounded at one end, and with a
sharp point at the other; there is another elongated form of a similar
character; a third form is spindle-shaped, with sharp points at both
ends. This last is a novel form—one which I have met with no-
where else; it appeared to me to furnish one independent argument
in favour of the authenticity of the specimens. Some are very narrow
compared with their length, others are broader.

500 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 3,

This curious discovery has necessarily led to the age of the beds
being more closely examined and questioned. M. Elie de Beaumont has
recently given the weight of his high authority in favour of their com-
paratively modern age,—of the age, possibly, of some of the peat-beds
of the Valley of the Somme, or of the Swiss lake-dwellings. I cannot
at all agree with this view, and it is this consideration that is more
particularly the cause of my laying the present paper before the
Society. In the first place, it is assumed that at the time of the
formation of the beds in question the valley had its present depth and
shape, and that the beds at Moulin Quignon result from a secular
wave of translation rushing in from the sea, or from the bursting of
lakes or the sudden melting of the snow of mountain-chains. The
hill at Moulin Quignon is 105 feet above the level of the sea, or
87 feet above the river. I have shown elsewhere how out of the
question it is to invoke any river-floods of the present day ; for as the
Valley of the Somme, between Amiens and Abbeville, is, at a rough
estimate, 6000 feet broad and 100 feet deep below the level of the
high-level valley-gravels, with which I would connect the beds at
Moulin Quignon, the sectional area of the valley at that height is to
the sectional area of the present river at periods of flood about
as 600,000 to 6000. Therefore, a supply of water 100 times greater
than that flowing off during ordinary floods at the present day
would be required to produce a flood rising to the level of Moulin
Quignon,—an occurrence, in the present climatal conditions, perfectly
impossible, as it would require the accumulated rainfall, not of one
month or of one year, but of several years, to fill the valley with
water, even in a state of rest.

The sudden melting of snow on mountain-chains, or the bursting
of inland lakes, is equally untenable, inasmuch as the watershed
separating the Somme from the Oise is only six miles broad and
80 feet high, so that any flood coming from the interior would
almost inevitably transport the débris of one basin into the other,
whereas not a fragment of the oolitic and old rock-débris of the
Valley of the Oise has passed over into the Valley of the Somme.
With regard to a wave coming in from the sea and throwing up or
sweeping down débris of gravel of older Quaternary beds and of
the land-surfaces upon the hill-slopes against which it rose, let us
see what would be the consequences of such an action. If, as the
eminent geologist who offers this explanation supposes, such waves
of translation occurred within the Celtic or Roman times, then we
ought to have in these high-level valley-gravels remains of Man of
that date, whereas no such remains have ever been found.

Secondly, whenever this inroad of the sea took place, the retiring
water, in sweeping down the slopes, besides lodging the gravel on
the higher ground, must necessarily have carried part into the
lower levels; and it should be found intercalated with the alluvial
and peat-beds of the valley, whereas no such intercalated beds are
ever found, the valley-gravels always passing under the entire mass
of alluvium and peat. Thirdly, the débris of the extinct Mammalia
in such reconstructed beds would necessarily be more or less worn,

1863. ] PRESTWICH—MOULIN QUIGNON. 501

and always fragmentary, whereas they are often not in the slightest
degree worn, and parts and the whole of entire skeletons are not
unfrequently found with every bone in place. Fourthly, the small
delicate and fragile land- and freshwater-shells would have been
generally destroyed, whereas they frequently occur in a state of
perfect preservation, and, in the case of the bivalves, with the two
valves occasionally not separated. Fifthly, it would behove the sup-
porters of this view to show beds whence the remains of the extinct
Mammalia could have been derived, whereas none such exist in the
district. I will not occupy the time of the Society longer with other
objections, as the subject in other forms has been often discussed.

Fig. 1.—Section of the Gravel-pit at Moulin Quignon.

eo Co

Qa

es re YW o

a. Brown sandy clay, with angular gravel. = g. Light-grey sand.

b, d, f. Ochreous gravel-seams. h. The “ Black Band.”
ce. Yellow sand. a. Chalk.

e. Light-green sand.

Fig. 2.—Section of the Gravel-pit at St. Acheul.

a. Brick-earth, with angular gravel. d, Ochreous gravel.
6. Whitish sand and marl, with land e. White sand.

and freshwater Shells. f. Light-coloured gravel.
e. Light-coloured gravel. g. Chalk.

On the other hand, we have at St. Acheul and Montiers fiuviatile
Shells in the high-level gravels, and the same occur in the low-level
gravels at Menchecourt, and probably at Mautort. For these and
other reasons, into which I need not now enter, I have attributed
the formation of these beds to river-action continued through a long
period of time, and gradually excavating the valley from the level

502 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 3,

of the high-level gravels (low-water level, fig. 3) to that of the low-
level gravels (on and below the sea-level, fig. 6).

In this particular case the shell-evidence is wanting, but I pur-
pose to show that, notwithstanding a certain difference, the beds at
Moulin Quignon can be correlated with those of St. Acheul, whilst
both have been already shown to hold the same relative position to
the modern river, or to be about 100 feet above its present level.
Fig. 1 represents the section of the gravel-pit at the former place.
The stratification is rude, the beds contorted, and the seams of sand
are subordinate. ‘The upper bed (a) consists of a coarse brick-earth
full of fragments of flint, mostly white and angular, but mixed with
some subangular gravel. The under surface of this bed is very
irregular, and it often descends in funnel-shaped cavities down into
the body of the gravel. If we eliminate the variable ingredients (7. e.
the subangular gravel) from this bed, the residue will be found to be
identical with the coarser bed of brick-earth which overlies the flu-
viatile beds at St. Acheul (fig. 2, a), and which also contains a variable
proportion of angular flints peculiar to it, and of subangular gravel
derived from the underlying beds. These upper beds I would there-
fore refer to one and the same cause, and consider as local variations
of Loess. The section I have given of the gravel-pit at St. Acheul
(fig. 2) represents the different beds in their least disturbed state, but
the contact between the Loess and the fluviatile beds is at places as
irregular as at Moulin Quignon. The same variations exist in the
lower fluviatile beds. At Warean’s pits, St. Acheul, the beds of sand
(5) have almost entirely disappeared, no Shells are found, and the
gravel is as coarse and irregular as at Moulin Quignon, and with only
occasional seam of sand. At Moulin Quignon itself, however, the
beds of sand are always most developed in the upper part of the sec-
tion, and sometimes they there replace the gravels for a short distance.
In both places the intercalated seams of sand occasionally show oblique
bedding, none of the beds are persistent, the grains of quartz are
worn and rounded, and the bulk of the flints subangular. The dif-
ference of colour is one of no importance, that being for the most
part a change subsequent to the deposition of the beds. In all the
physical conditions there is, therefore, an agreement between the
beds at St. Acheul and Moulin Quignon. The presence of organic
remains in all gravels of this age is of very local occurrence.
Although scarce, remains of the Elephant have been occasionally
found at Moulin Quignon, whilst teeth of the Horse and Ox have
been found at the adjacent pit of St. Gilles.

On the opposite side of the valley is Mautort, and on the slope of
the hill above the village is a deposit of gravel presenting the same
general characters as that at Moulin Quignon, and overlain by a bed
of Loess, which is here, however, well marked and developed. No
Shells are found, but some of the seams of gravel have a more sandy
and fluviatile appearance than at Moulin Quignon, arising probably
from a somewhat greater depth of water; for the level of this bed
is about 10 to 15 feet lower than that of Moulin Quignon. In all
probability we have in both these places part of the bed of the old

1863.] | PRESTWICH—MOULIN QUIGNON. 503

river, when it flowed in a channel higher by nearly 100 feet than the
present river-bed. In the diagram-section, fig. 3, I have given
what I consider may have been the section of the valley at that
period, showing a shallow and broad river with numerous, generally
dry, shoals and shingle-banks, but during floods, arising from the
melting of the winter snows and a greater rainfall than at the pre-
sent day, rising to a height of 40 to 50 feet above its ordinary level,
flooding the adjacent country, and depositing, out of the course of the
main current, the fine silt now forming the Loess. Mixed with this
high Loess are angular fragments of flints washed down from the ad-
jacent heights or carried from the shores by floating ice. As I have
entered into this question fully in another paper*, I will not go fur-
ther into it here than is necessary to apply it to this particular case.
As the valley was by degrees excavated, such portions of the old river-
bed as escaped denudation emerged gradually from the level, first of
the river, and later of the river-floods, as shown in fig. 4. At this
time the high-level gravels of Mautort and Moulin Quignon (A’ and
B’) would have acquired their full thickness, but would, during floods,
be subject to disturbance by ice-floes, and would gradually be co-
vered up by Loess. At the same time the draining-off of the water
and the percolation of the rain-water through the permeable gravel-
beds, acting through a long period on the chalk, would attack and
dissolve the weakest parts, and gradually give rise to the numerous
gravel-pipes we find on this level, both at Moulin Quignon, Mautort,
and elsewhere ; whilst the depression formed on the top of the gravel
thus let down would in process of time be filled up with Loess by
the successive floods, levelling the irregularities of surface thus pro-
duced.

Fig. 5 represents the valley at the time of the formation of the
low-level gravels, when the excavation had attained nearly its present
depth, and when the deposits of Mautort and of Menchecourt, with the
many fluviatile and estuarine shells and the abundant Mammalian
remains of the latter place, were in course of formation. The section
does not traverse Menchecourt, but it intersects the low-level beds of
the “‘ Carrée de Six” at the gates of Abbeville, where several fine
molars of Elephas primigenius and some Flint Implements were found
during the making of the moat by M. Boucher de Perthes. Here the
high-level gravels, A’ and B”, are dry and out of the reach of the
floods which formed the lower-level Loess of Mautort and Menche-
court.

Fig. 6 gives the section of the valley at the present time, show-
ing the relation of the high-level gravels of Moulin Quignon, B’”,
and Mautort, A’”’, to the lower-level gravels of the valley, and
of these to the recent alluvium with peat which has filled up and
covered the irregularities left by the latter, the two showing an
origin entirely separate, and an existence perfectly independent.

Whatever may be the conclusions drawn respecting the Jaw and the
Flint Implements recently discovered at Moulin Quignon, the age of
the beds is to me perfectly well determined, as belonging to an early

* Proc. Roy. Soc. vol. xii. No. 49, March 1862, p. 38.

| June 3,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

504

“spooy SuLMp soatt oy} ‘suonsod popeys-coqy St] oyj {10;vM MOT 4v JOATA ayy yuosordoas suoyaod popeys ATyxep otout oy4 C-E ‘SSI UT

‘y[eyO °a ‘qvog pue UINTANTye saa * "SSo0TT ‘9 *[PABLL) [OAOT-YSTFT “9 “JOARID) [OAOT-MOTT *D
*[PAd]-BIG or —-. oe LS PU Cute .) ' ots ae 4 “ 5 = AL AO ay te ante OCS ah ee atti

» O
ee a i Bane *oTTA0qqy *4109Ne Ay *74.10]N PAT -oqauason 04
- TH. TMoyJAL aaoqge szid pig prod ayy UO [ITT
aug quasaud ayp yn aunuog ay) fo hazy ayp ssouov woyosg—'g “Sty “AN
*[aAaT-Bag
[29] 1948.\-mory— = E Bowe : re = ——— ee
*[2a9]- tS 7 5: EES] ee ee ge 8 -
bets se e/a 2

2
uV

‘spaanub-lajo 4 aaaj-samory ayy fo uornusog yp £0 Uy ayn 1 oUuMog oy fo hayny ayn fo worry 1VI4AL0IY,, —'G "Bq

*[PAIT-B9S x : ao N
* [PA9T IOJVM-MO'T — \ ie — = ee pa
*[242|-p00|W -- =— > -- SSE

‘spannub-hayny 19haj-ybuy ayy fo souabsowpy oy) fo aur oy yw aunuog ayn fo haywg ayy fo woroy 1090004, —'F “SIT

"13 00% "35 SOT

zo pore ieee “Vy O01 “IW 090z
MOAQT OIG el cmtay ewig -e, ter ben ee ee ere eee ;
*[PAZT JoyvVM-MOrl — pa, aa Meir a . A ; eas
*[aAa[-poo, ga #2e4!— =e, eee

‘spanib-hayng janaj-ybuy ayy fo uoynuog a4p fo amy ay 10 aunuog ayy Jo hayny ay) Jo uonoay 109Y49.L09Y, J, —'e 3

1863. ] PRESTWICH—-MOULIN QUIGNON. 505

Quaternary or Post-pliocene period, that they are older than the
Menchecourt deposits, and that they date before the excavation of
the Valley of the Somme. Nor is the question of the contemporaneity
of Man with these particular beds affected by any conclusions that
may be arrived at relative to this recent inquiry. Whatever diversity
of opinion there may be respecting certain Flint Implements, others,
the genuineness of which cannot be questioned, have been found
from time to time during the last fifteen years, both in the Moulin-
Quignon pit and, in more considerable numbers, in the adjacent and
equivalent beds of the «‘ Champ de Mars” and St. Gilles, which place
beyond dispute the occurrence, in situ, of Flint Implements shaped
by early Man in these, amongst the oldest of the high-level gravels
of the ancient Valley of the Somme.

Note.—Further and more deliberate inquiry, on the part of myself
and others, than was possible on the occasion of the conference at
Abbeville, leads me now to revert to my original opinion, and to be-
lieve that we were mistaken in concluding on that occasion that no
fraud had been practised. In addition to the objections originally
urged, I found, on washing a portion of the gravel containing the
Flint Implements (an experiment contemplated but unaccountably
omitted in May last), the discordance between the mineral condition
of the flint fragments and the Flint Implements to be so great as to
render it evident that the two could not possibly have been subjected
during the same time to the same influences. Further, instead of
being confined to a special bed and a special level, we found, on a
subsequent visit, that specimens had been brought by the men from
Epargnette (a bed on a yet higher level and hitherto unproductive) ;
and, again, we were given, at Mautort, at a low-level valley-gravel-
pit, three Flint Implements of precisely the same type and in the
same condition as those of Moulin Quignon ; whilst, from the indica-
tions given by the men, the specimens would have been taken from
a bed of gravel subordinate to the Loess, and not even part of the
mass of fluviatile low-level gravel. Our verdict in this case respect-
ing the Flint Implements (leaving apart the question of the jaw)
will, therefore, I fear, have to be reconsidered. The precautions we
took seemed to render imposition on the part of the workmen im-
possible; still, although it remains undetected, I cannot, with the
strong and increased doubts (not one of them since removed) attached
to the point, continue to accept the authenticity of these specimens.
The essential fact, however, of the occurrence of genuine Flint Im-
plements at Moulin Quignon, the Champ de Mars, and Menchecourt
receives additional confirmation from every fresh investigation, and
places M. Boucher de Perthes’s important origmal discovery beyond
all doubt.—[J. P., Oct. 1863. |

VOL. X1X.——PART TI, 2M

506 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17,

JUNE 17, 1863.

Frederick George Finch, Esq., B.A., Tudor House, Blackheath,
was elected a Fellow.

M. Boucher de Perthes, of Abbeville; Dr. M. Hornes, Keeper of
the Imperial Mineral Cabinet of Vienna; M. N. von Kokscharow,
of St. Petersburg; M. 8. Lovén, of Stockholm; General della
Marmora, President of the Imperial Academy of Sciences of Turin ;
F, A. Graf Marschall von Burgholzhausen, Archivist of the Imperial
Geological Institute of Vienna; M. H. Nyst, of Antwerp; Dr. F.
A. Quenstedt, Professor of Geology at the University of Tubingen ;
Dr. F. Senft, of EKisenach; Prof. Edouard Suess, of the University of
Vienna; Dr. B. F. Shumard, of Louisville; and the Marquis de Vi-
braye, of Paris and Abbeville, were elected Foreign Correspondents.

The following communications were read :—

1. On the Recations of the Ross-surre Sanpstones containing Ruprr-
LIAN Footprints. By the Rev. Gzorcr Gorpon, LL.D., and the
Rev. J. M. Joass. With an Introduction by Sir R. I. Murcurson,
K.C.B.. EF R.8s, 2-G.s.*

[Communicated by Sir R. I. Murchison, K.C.B., &e.]

In the introduction Sir R. I. Murchison gave a sketch of the geology
of the Tarbatness promontory, which is composed of variously
coloured sandstones, having a conformable dip to the N.W. In
these strata the authors had found footprints f (of animals believed
to be Reptiles) similar to those found in the sandstones on the coast
of Elgin; and it was therefore desirable to prove whether these
rocks really belonged to the Paleozoic series, or, as some geologists
suppose with regard to the Elgin sandstones, to the Trias. In
order to solve this problem, if possible, the Rev. Mr. Joass made a
careful survey of the coast from Geanies to Tarbatness Lighthouse,
and round along the north shore of the promontory to the inlet at
Inver ; and he found a conformable succession between the undoubted
Old Red Sandstone of Geanies and the track-bearing sandstone of
Tarbatness.

The Rey. Dr. Gordon gave a description of the various tracks:
the smaller kind were referred by him to an unknown Crustacean ;
the larger and more definite impressions, however, he considered to
be the footsteps of some kind of Reptile. He also stated, as con-
. firmatory of the ‘ Old Red’ age of the beds, that the Oolitic beds of
Shandwick are unconformable to the Old Red Sandstone.

Mr. Joass then described the beds and their stratigraphical rela-
tions as follows :—In a paper published in the ‘ Transactions of the

* The description of the beds by Mr. Joass, and a statement of their relation
to the Oolitic deposits by Dr. Gordon, are given in full, the Introduction and
the remainder of the’ paper in abstract.

{+ Footprints in the Tarbatness Sandstones were first discovered by the Rev. G.
Campbell, in the summer of 1862.

1863. ] GORDON AND JOASS—TARBATNESS. 507

Geological Society of London,’ 2nd ser. vol. iii. parti. p. 150, 1828,
I find it stated, on the authority of Sir R. I. Murchison and Prof.
Sedgwick, that «‘ Under Geanies’ Mill are seen some grey, brownish-
grey, and greenish-grey calciferous sandstones, alternating with some
bituminous, laminated, caleareous beds, on one of which were some
Fish-scales, and some fragments ” (since found to be plates of the
Coccosteus); that “between Geanies’ Mill and Balloan Castle the
phenomena are of less interest, the beds in the ascending order pre-
serving nearly the same characters ;” and that “ from Balloan Castle
to the extreme point of Tarbatness no subordinate calcareous beds
like those above described” had been observed, “although some of
the greenish-grey sandstones were calciferous.”

To the above I have nothing to add by way of general description,
as its accuracy has been but confirmed by subsequent investigation ;
but I hope that the following detailed remarks may be of interest in
connexion with the recent discovery, by the Rev. Mr. Campbell, of
Tarbat, and myself, of undoubted Reptilian footprints, and probable
Crustacean tracks, in the sandstones of Portmahomack (Tarbat).

In the cliff at the western boundary of Geanies (fig. 1, A),
superior to a well-defined ferruginous bed of red sandstone, there
occur several bands of calcareous shale, with subordinate belts of
grey and brownish sandstone, dipping nearly N.W., as indicated by
the arrows on the map.

Throughout these beds fossil remains of Devonian age eccur in
abundance, such as Fucoids, Fish-scales, and Coprolites, especially at
the undernoted localities and among the debris at the foot of the cliff.

The uppermost of these fossiliferous shale-beds dips under the
Drift at the top of the Strone-a-chapull road, at the site of the old
Mill of Tarrel, near D (fig. 1), but is continued on the beach at F.
At this point undoubted Old Red Fishes have been found, while a
nearly entire specimen of Coccosteus has been left im situ, at the
point marked a on the Map (fig. 1).

By the kindness of Mr. Murray of Geanies, who placed some men
at my disposal, a collection of fossils has been made from the débris
of the cliff at A, from the shale-beds in situ at B and D, and from
the beach-rocks at C, E, and F. Some of these fossiliferous rocks,
as seen on the shore, although dipping in an opposite direction to
the cliff-beds, are yet believed to be undermined and fallen masses,
from their identity of lithological structure with the calcareous beds
in the cliff at the base of which they lie. The above collection, now
at Geanies’ House, for the inspection of all interested in the matter,
will, it is believed, be sufficient authority for regarding this portion
of the section as of undoubted Devonian age, and therefore a
proper starting-point for an upward examination of the beds with
a view to establishing their conformable stratigraphical sequence
onwards to the Ichnites of Camus Shandwick and Portmahomack.

From F eastwards, to G, the cliff presents a good section of con-
formably bedded, reddish, yellow, and particoloured sandstones ; and
where the reading of this is partially interfered with by drift, the
beach-rocks, in normal dip, carry us easily onward to the village of

2m 2

[June 17,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

508

N W

‘NZIS UL Yo] ‘snagsoo00p YA qei{g “Dv ‘saqtqordog 4. *SOTBOS-YSTT — ‘soqrayoT AA

WN Ree aac
"] areas

aS)

~

iF

*

_

4

Space between
high- and low-
water mark.

— (wd

cI
S

a
*T[Indeys-e-auox
‘apyseg uvol[tg 3

*yOIMputng snureg

*a [UL IUO JO aTvIg

ferrell oh ee leet

‘ssoupngun,y, fo uoyog pun dnw-yopyy—Z YT “Sst

1863. ] GORDON AND JOASS—TARBATNESS. 509

Rockfield, J, at which point the cliff is nearly obscured by drift, and
the shore-beds much broken and rolled, as shown in the Map and
Section, figs. 1 and 2. This is especially the case below Balloan
Castle. Throughout all this irregularity, however, the beds are
easily traceable as persistent, by walking along their exposed surfaces
between high- and low-water mark; and in proceeding eastwards
the normal dip becomes distinctly visible in the cliff. Where this
is partially obscured by drift, as at L, the beach-rocks carry us
clearly forward, through conformable strata of yellowish sandstone,
to the thinly bedded and more ferruginous rocks of Wilkhaven. At
this point, M, there occurs a well-defined pebbly band, which
differs from a previous belt of similar nature west of Rockfield, at
H, in containing pebbles of a purer quartz; whilst among the
rolled stones on the beach there are many hard felspathic pebbles,
together with numerous cherty fragments like calcedony, resembling
the more highly indurated portions of the Lossiemouth Cornstones
on the opposite coast.

From this point onwards to the Lighthouse the rocks become more
ferruginous in their appearance, which character they present over
a well-exposed beach round by the north shore up to O, where
there is a band of gritty sandstone containing gneissose and quartz-
ose pebbles.

Interstratified with a few belts of light-coloured and good building-
sandstone, the flaggy red beds continue, with little variation of colour
or character, to P, maintaining the normal N.W. dip, at an average
angle of 25°.

Here, and at Q, in red and thinly bedded sandstones, there occur
distinct Reptilian tracks, persisting over considerable surfaces.
Without important variation of lithological character, save the
normal recurrence of the gritty bed O, the beach presents a regular
descending succession of beds to T, where Ichnites of similar ap-
pearance to those at P and Q occur in considerable numbers. The
specimen already forwarded to the Museum of Practical Geology was
found at 8, and the Crustacean tracks previously mentioned occur at R.

At U there is a recurrence of the pebbly bed M, as also in the
line of strike of the rocks, at Balnabruach. To the westward, for
about a mile, the beds are concealed by sand; but near the inlet to
Inver, a few detached outcroppers at W show the northerly dip and
normal inclination, which are also observable at X, in the bed of
a streamlet running nearly north from the steading at Arboll.

To the above I have but to add that the excavation of Ichnites
was carried on under the superintendence of the Rev. Mr. Campbell
of Tarbat. There is now at the Manse of Tarbat a large collection,
of Crustacean and Reptilian tracks, on blocks too unwieldy for
carriage to a distance, but which will be gladly submitted to the
inspection of all whose interest in the important question at issue
induces them to visit the locality. —[J. M. J.]

The Rey. Dr. George Gordon then gave the following description
of the unconformity existing between the Oolites and the Sandstones

510 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17,

of Cromarty :—Accompanied by Mr. Stables, Mr. Joass, and Major
H. Drummond, of the Bengal Engineers, I spent the whole of one
day on and around the Nigg, or North Sutor of Cromarty. We ex-
amined it minutely in reference to the sketch sent to Sir R. I. Mur-
chison by Miss C. Allardyce. This sketch represents the Oolites lying
conformably to the Old Red Sandstone, and as if they occurred on
the west or inner side of that Sutor, namely the northern one*.

We examined all the bits of rock or strata that were to be seen
cropping out along the Cromarty Firth shore of the North Sutor,
and found in them nothing but Old Red Sandstone.

We then proceeded down the Moray Firth as far as. Shandwick,
landing at different points, and walking along almost the whole
shore, spending a considerable time at Gaan Righ. Here, so far
as we could see, the Oolites first appear. Covered at high water,
and lying at the base of a cliff about 250 feet high, these Gaan-
Righ Oolites are evidently an extension of the well-known deposit
of the same series at Shandwick. The tide was low, and most
favourable for our work over this part of the coast.

The complete unconformity of the Shandwick Oolitie beds to the
Old Red Sandstone is acknowledged on all hands; and the seeming
conformity of the Oolitic beds at Gaan Righ to the Old Red arises
from the accidental change of dip (caused by a fault, or rather by a
slip or slide) in a large mass of the rock (Old Red) in the overhang-
ing cliff. The strata of this mass, if projected on their present
plane, would most probably overlie the Oolites! The persistent
northern dip of the Old Red Sandstone, in this line of coast all the
way down to Shandwick, comes out distinctly, when seen, as on our
return to Cromarty, from the boat when sailing in the offing.

Faults and slips there are in many places, but they do not present
any difficulty. I am, therefore, convinced that the great question at
issue—the age of our Reptiliferous beds—is not in the least affected
by any appearance presented by the Oolites at Gaan Righ—the
locality, I am persuaded, alluded to by Miss Allardyce in her note to
Sir R, I. Murchison.—{G. G. |

2. On some Tertiary SuEtxs from Jamaica. By J. Carrick Moors,
Ksq., M.A., F.R.S., F.G.8. With a Note on the Corats; by
P. Martin Duncan, M.B., F.G.8.: and a Note on some NuMMULINZE
and Orsrtoipes; by Professor T. Rupert Jonzs, F.G.S.

Tue late Mr. Barrett formed a collection of Tertiary fossils in
Jamaica from some beds which were referred to in the ‘ Geologist’
for 1862, p. 373. The collection was forwarded to Mr. Woodward,
who, seeing their relation to the San-Domingan fossils, asked me
to examine the Mollusca, while the Corals were submitted to Dr.
Duncan. In comparing the Shells with fossil and recent forms, I

* The examination of the North Sutor was made on May 14, 1863. The
sketch referred to is one by the late Hugh Miller, in the possession of Miss C.
Allardyce, Cromarty.

1863. ] MOORE—JAMAICAN TERTIARIES, 511

have been kindly assisted by Mr. Woodward, Dr. Baird, Mr. Hamilton,
and Mr. Lovell Reeve, and now lay the results before the Society.

Excluding such shells as are too small or too imperfect for
determination, the collection contains 71 species, referable to the
following genera :—

SP. SP. SP.
0 ee 2 Purbanel ba) iccdsa- 9.2: 1 Sol a 1
Cassidaria ............ 1 LON pis g. aebaaaaas 1 Cyclostrema ......... 1
EEFOMDUS .:.......... 2 |. Waresinella ess... +. PY Dentalnam |... 1
2 Se 1 Columbella............ 2 Vermebtas? ...0. 00.0%: l
ee 7 Cancellaria............ 2 Wienilerstiiedt cess: 7
Murex od ee l Pleurotoma ......... 7 ry Cr 2
SS 1 TRCRORES: Seicavsca> cues. 1 SSA oh. l
Ranella RE aes Messe « 1 BEM Te Sc oes coe ee 2 varia... 3
WER ec, 1 Cerium” £7. 6)50 527: 1 Corbuala |. 8.2: 1
Ancillaria ASS: Take 1 Watied. scree 4 Pectunculus ......... =
Mitra Ai oe 2 Dua e id) fo scedex distaste l ce § Leen ee 3
Fasciolaria ............ 1 OTHE on. 58s. 423, 1 Chaamige | i. :5-4 canes 2

71

Of these, the following 19 are found in the San Domingo beds,
and are not known in a recent state :-—
Conus validus, Sow. Natica subclausa, Sow.

planiliratus, Sow. , Spec. unnamed.
Murex Domingensis, Sow. , Spec. unnamed.

Triton simillimus, Sow. Solarium quadriseriatum, Sow.
Mitra Henekeni, Sow. © Turbo, spec. unnamed.

, Spec. unnamed. Cardita, spec. unnamed.
Fasciolaria semistriata, Sow. Venus, spec. unnamed.
Terebra bipartita, Sow. Cardium Haitense, Sow.

Phos, spec. unnamed. Corbula, spec. unnamed.

Arca consobrina, Sow.

__ Twelve others have been identified with recent species+ inhabiting
West Indian seas :—

Strombus fragilis. *Natica mamillaris.
Ranella crassa. _ *Venus Paphia.
*Turbinella infundibulum. *Lucina Pennsylvanica.
*Oliva reticularis. *Pectunculus pennaceus.
*Marginella coniformis. *Arca Noe.
*Natica sulcata. *Chama arcinella.

It thus appears that, of the whole 71 Jamaica shells, 12 are still
living, and 28 are common to Jamaican and San Domingo.

Dr. Duncan, in his Memoir lately read before the Society ¢, finds the
same relations between the Jamaican and San-Domingan beds from a
comparison of the Corals,—three of the seven Jamaican Corals being
common to both formations, whilst the number of extinct forms
justifies the age formerly attributed to the San-Domingan Tertiaries.
It will be remembered that the Miocene date was assigned to the
latter from the great proportion of extinct species of Mollusca, and
also from the presence of four species of Fish, all known in the
Miocene beds of Europe and America, and in no newer formation.
Here the proportion of extinct Mollusca and Corals is about the same
as in the San-Domingan beds; and the number of fossils common to

Those marked with an asterisk are also found in San Domingo. ¢ See p. 406.

512 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17,

both is sufficient to prove their synchronism. But we are able still
further to extend the limits of this Miocene Sea. In the cutting for
the Panama Railway, shelly beds were passed through near Navy
Port, at a height of 15 feet above the sea, from which Mr. Saunders
collected some fossils which he presented to this Society. Most of
them are too imperfect for determination; but out of less than a
dozen, which are tolerably distinguishable, five are certainly identical
with San Domingan Shells: they are, Conus Domingensis, a Malea, a
Natica, a Venus, and a Cardium*.

In my Reports on the San-Domingan Shellst, I mentioned that one
or two seemed identical with Shells now living in the Pacific, and
that the nearest analogues of several others were to be found in the
Pacific, and not in the Atlantic Ocean: several striking instances of
these resemblances were mentioned. The collection now before us
also presents the same feature; for although all the specimens I
have identified with recent Shells are now living in the West Indian
seas, yet the affinities of several others are decidedly with Shells of
the Pacific Ocean. I may mention a Venus belonging to a group
confined to Australia; a Corbula scarcely distinguishable from C.
modesta, Philippine Islands ; a Plewrotoma very near, if not identical
with, P. nigerrima, Panama; and another very close to P. gubbosa,
Cumana; besides which, some of the San-Domingan Shells which
presented this character in a marked degree also occur in Jamaica.
Observing this in the San-Domingan collection, I formerly threw out
the conjecture that the separation between these seas may not have ©
been so complete in early Tertiary times as at present. Dr. Duncan’s
Memoir, just quoted, throws great light on this question. It results
from his studies, that the relation between these fossil Corals and
those now living in the Pacific or China seas is even more intimate
than that indicated by the Mollusca. Some of these species are
actually now living in the Pacific, and others belong to genera of
which all the living species are confined to that ocean.

M. @Orbigny, in his great work, ‘L’Amérique Méridionale,’
shows that five of the Cretaceous fossils from the western side of
South America are identical with five in the Paris Chalk, while of all
the Tertiary fossils on the two flanks of the Cordilleras not a single
one is common to both formations ; and he thence infers that a com-
munication must have subsisted between those two oceans during
the Cretaceous period, and that at its close the upheaving of the
Cordilleras effected that separation which has subsisted to this day.
But it is to be observed that the Tertiary fossils collected by M.
d@Orbigny were all found south of latitude 30° 8., whereas those
from Jamaica and San Domingo are in latitude 18° N. Even if
some connexion had existed between the two oceans in the district
of Panama, as is now supposed, the Mollusca living on the two
flanks of South America, 40° to the south of that opening, might
be expected to be distinct, just as those at present living on the

* See Quart. Journ. Geol. Soc. vol. ix. p. 132.
t Ibid. vol. vi. p. 40, and vol. ix. p. 129.

1863. | MOORE—JAMAICAN TERTIARIES. 513

opposite coasts of Chili and of Patagonia are distinct, though there
is free communication by Cape Horn. No negative evidence can
counterbalance positive facts; and when it is recollected that the
summit of the Panama Railway is but 250 feet above the sea,—
that that inconsiderable height must have been less when the shelly
beds of Navy Port (contemporaneous with those of Jamaica and San
Domingo) were formed,—that some few of these Mollusca and Corals
are now living in the Pacific,—and that the nearest allied forms of
several more are to be found on the western side of America, it will be
admitted to be most probable that the complete separation of these
oceans did not take place until after the commencement of the Ter-
tiary period.

P.S.—Dr. Duncan has kindly supplied me with the following
facts, which he has ascertained since the reading of his Memoir on
the Corals :—‘ The Foraminifer so common in the European Mio-
cene and in the San-Domingan beds, Amphistegina Hauert, is found
in abundance in the Jamaican Corals; also the Coral sent over by
Mr. Barrett, and known as Montliwaltia ponderosa, is amongst a
collection from Travancore, with T'rochocyathus cornucopia, a San-
Domingan and common Viennese Miocene species. The occurrence
in Jamaica of <Astrocenia decaphylla, a Gosau fossil, is very re-
markable ; but the same kind of thing occurs in San Domingo, where
Phyllocenia sculpta and a Barysmilia very little differing from B.
tuberosa, Reuss, both Gosau fossils, are noticed.”

Note on the Fossit Corars accompanying the Testacea from JAMAICA.
By P. Martin Duncan, M.B., F.G.8., &e.

The majority of the Corals have been described in my communi-
cation, referred to by Mr. Moore, and published in this Number of the
Society’s Journal, on the Fossil Corals of the West Indian Islands.

1. MonTLIVALTIA PONDEROSA, Edwards & Haime.

Two specimens of this great simple Coral, which is found both in
the Miocene of Guadaloupe as well as in that of San Domingo, are
amongst the collection ; the San-Domingan specimen is in the British
Museum.

2. PracocyatHus Barrerrit, nobis. “Fossil Corals of the West
Indies,” p. 437. Pl. XVI. fig. 1.

From San Domingo and Jamaica.

3. PracorrocHus ALVEOLUS, nobis. ‘Fossil Corals of the West
Indies,” p. 438. Pl. XVI. fig. 2.

4, ASTROCHNIA DECAPHYLLA, Michelin, sp.

The specimen can only be considered as a very slight variety of
the well-known Astrea decaphylla, Michelin, of Gosau. The Astro-
cenia ornata of Turin and Antigua is only distantly allied. Astroccnia
decaphylla is a very marked species, and its occurrence in the

514 PROCEEDINGS OF THE GEOLOGICAL society. [June 17,

Jamaican Tertiaries is very remarkable: like Phyllocenia sculpta in
San Domingo, and the Isastreeans in Antigua, it belongs to a Coral-
fauna which died out in the Miocene period.

5. Tuysanus EXcENTRICUS, nobis. ‘‘ Fossil Corals of the West Indies,”
p. 439. Pl. XVI. fig. 3.

These beautiful Corals are allied to the Thysani of San Domingo.
From Jamaica and San Domingo.

The other Fossil Corals from Jamaica, in this collection, and which
I have described already, are Alveopora Dedalea, Dana, and Sider-
astrea grandis, nobis—[P. M. D.] -

Note on some NumMvutin& and Orxitoies from JAMAICA.
By Professor T. Rupert Jonzs, F.G.S.

In connexion with Mr. J. C. Moore’s researches on the Tertiary
Molluscs of Jamaica, the following remarks on some specimens of
Nummulites * and Orbitoides from the same island will be of
interest.

Some time since, Mr. 8. P. Woodward, F.G.S., submitted to my
examination a water-worn piece of Orbitoidal limestone from
Healthful Hill, St. Thomas-in-the-East, collected by the Hon. Edw.
Chitty. Among the Orbitoides constituting the mass of this hand-
specimen (6 inches x 23 x 2), three or four Nummuline are visible
on the surface, and their internal structure has been sufficiently well
exposed by weathering. The Orbitoides are similar to those found
fossil in the Upper Chalk of Southern France and the Pyrenees,
and in the Nummulitic beds of Scinde (0. media, O. dispansa, &e.).
The Nummuline, differing only in size one from another, belong to
the sinuo-radiate groupy, and are near to the forms known as
Nummulina perforata and N. Rouaulti. The largest is about 7 inch
in diameter and ;, inch in thickness,

Orbitoides are not confined to this nodular limestone in Jamaica,
but are there found as low down as the Cretaceous Limestone, with
Nerinea and Barrettiat; and here the thick variety (O. Fortisic)
and the thin (0. papyracea) are both abundant.

When Mr. Barrett, the late Director of the Geological Survey of
the British West Indian Isles, was in England last year, he showed
me, by the following diagram, the position of this Orbitoidal Limestone
in the geological series of Jamaica. He stated that it occurred as
nodules in clay just underneath the great ‘“ White Limestone,” which,
with overlying shaly and sandy beds, I understood him to refer to

* De la Beche has recorded the occurrence of ‘‘ Nummulites” in Jamaica
(Geol. Trans. 2nd ser. vol. ii. p. 170); but it is doubtful whether the fossils he
alludes to may not have been Orbitoides, which are common in that island.

+ See Ann. Nat. Hist. 3rd ser. vol. viii. p. 233, and Carpenter’s Introd.
Foram. p. 275.

t See Mr. Woodward’s paper on ‘‘ Barrettia and other Hippurites,” in the
‘ Geologist,’ vol. v. p. 873. De la Beche seems to have regarded some of the ~
Orbitoides as ‘* Encrinal remains” (Geol. Trans. 2nd ser. vol. ii. p. 158), as
Mr. Woodward has remarked.

1863. | DE GROOT—DUTCH EAST INDIES. 515

the Pliocene *. The nodular limestone he regarded as forming, with
some underlying beds, the Middle Tertiary series}; whilst the Plant-
bearing shales, still lower down, are of Eocene age, and overlie the

Section of the Tertiary and Cretaceous Rocks of Jamaica.

Hippurite Limestone. Eocene. _ 0) a

-_—_—~--~_ ae
Miocene. Pliocene.
a. White Limestone. 6. Nodular Orbitoidal Limestone.

Cretaceous Hippurite-lmestone, containing Nerinea, Acteonella,
Radiolites, Barrettia, Inoceramus, Ventriculites, and Orbitoides. The
last-mentioned limestone, with its flint-nodules and intercalated
shales, as well as the underlying porphyries and conglomerates, were
described by Mr. Barrett in the Quart. Journ. Geol. Soc. vol. xvi.
p. 324 +.

It may be remarked as a point of interest, that the Nummuline
and Orbitoides above alluded to are such as are found in the South
of Europe and in India; whilst in the neighbouring continent of
America Nummulinc are, it seems, wanting ; and the Orbctordes (in
Alabama $) is O. Mantelli, which occurs also in Scinde, but is not
dominant there.—[T. R. J.]

3. Notes on the Minrratoey and Grotoey of Bornzo and the apsa-
cent Istanps. By Mijnheer Corn. pz Groot, Chief of the Mining
Department in the Dutch East Indies.

(Extracted from a letter to Sir R. I. Murchison, K.C.B., F.G.S8.)

THe steam-coal formation of Borneo underlies the Nummulitic Lime-
stone, and, so far as I am at present able to judge, belongs to the
KS Etage Suessonien” of D’ Orbigny. From the Nummulitic Lime-
stone the following fossils have been obtained, namely, Nummulina
depressa, LV. lenticularis, N. mamilla, and NV. polygyrata ; also Hu-
patangus ornatus and Phaculina Fawasu. The last-named fossil is,

* In Mr. Woodward’s paper above referred to, this limestone is termed
‘¢ Miocene.”

+t In the Western Hemisphere, Ordztotdes and Nummulina are very rare in
beds above the Eocene group.

{ The woodcut at p. 325 incorrectly represents the shales and limestone-bands
as unconformable.

§ See Lyell on the so-called Nummulitic formation of Alabama, Quart. Journ.
Geol. Soe. vol. ii. p. 409, and vol. iv. p. 11; and Manual Elem. Geol. 5th edit.
p. 233.

516 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17,

I know, found in the Maestricht Beds; but, according to Bronn, it
occurs also in the ‘ Etage Suessonien.’

In a search for lodes of copper in the western part of Borneo,
north of Pontianak, made on behalf of private adventurers by Mr.
Everwijn, the strings of copper that were found, though very
rich, were too small to pay for working. There are also some poor
copper-lodes near the Singkarah Lake, in the mountains east of
Padang, in the Island of Sumatra; but the veins, though large, are
too poor to be worked. |

A search for tin-veins was made in the Island of Blitong (Billi-
ton), by Mr. Akkeringa, one of our mining-engineers, in 1860-61,
with the following result:—at Brang no metalliferous veins were
found; but on the Tadjouw Hill (goenoeng Tadjouw) a vein 4 to 5
feet wide, and containing much tin-ore, was discovered ; its exploi-
tation was commenced last year. Granite and elvan were found on
the south, and eurite (elvan) on the north of Tadjouw Hill.

A large vein of manganese-ore (pyrolusite) occurs in porphyry,
close to the Nummulitic Limestone, in the south-eastern part of
Borneo. This manganese-ore would have been extracted for the
European market more than two years ago, had it not been for dis-
turbances in that part of the island.

A limestone occurs in Timor Island (near Timor koeping) contain-
ing Encrinites in abundance*.

Twelve years ago, when I first arrived in India, it was generally
considered that the stream-tin found in the Island of Banka was not
derived from veins in the granite of the island, but from mountains
on the continent of Asia, whence it had been washed down to
the bottom of the sea; and that the sea-bottom had been subse-
quently upheaved so as to form the Island of Banka. This sup-
position appeared to me erroneous, and I therefore endeavoured to
collect facts bearing upon the question. In 1853 I inspected all
the stream-works in the island, and found, in the district of Pankal-
pinang, three parallel veins running nearly east and west, one of
them containing tin-ore in grains, like those found in the stream-
works. In 1855, Mr. Akkeringa surveyed the Jeboes district, and
found grains of tin-ore disseminated in granite. I also found that
in every river which was streamed for tin the largest grains were
found nearest the hills, and that further away towards the sea they
gradually became smaller. Now, as the rivers of Banka run from
the interior in all directions towards the sea, these facts proved that
the stream-tin is the detritus of the rocks and veins containing tin-
ore occurring on the island.

* M. de Groot has sent a specimen of this limestone, and specimens of the rocks
and minerals he mentions, as well as of some fossils from the clay and the marly
sandstone of the tertiary formation of Java. The last-named specimens were
found near the Seela Hill (goenoeng Seela), in the Preanger regency, about 2000
French feet above the level of the sea. He has also sent some specimensof fossil
Mollusca from the clay separating two beds of workable coal in Borneo. The
rocks and minerals are in the Museum of Practical Geology, and the fossils
in the Museum of the Geological Society, having been presented by Sir R. I.
Murchison, K.C.B., F.R.S., &.—Ebir.

1863. ] MACDONALD—THECIDIUM ADAMSI. 517

The Government Surveyors publish their papers in the ‘ Natuur-
kundig Tijdschrift voor Nederlandsch Indié,’ and at present they
only map what is actually seen. They are now engaged, under my
direction, in surveying the Island of Banka.

4, Descriprion of a new fossil Tuecrpium (Thecidium Adamsi) from
the Miocene Beps of Matra. By J. Dents Macponaxp, Ksq.,
F.R.S., Surgeon of H.M.S. ¢ Icarus.’

Amonest the many interesting fossils occurring in the lower part of
the calcareous sandstone of Malta, there is a beautiful little Theci-
dium; and as I believe it has not yet been described or named, it
may be worthy of a brief notice.

It appears to me that the nearest ally to the little Shell which I
am about to describe is the recent Thecidium Mediterraneum. The
species about to be described is, however, very much smaller, being
only 4th of an inch in length; besides which many other decidedly
specific differences present themselves on closer inspection. As to
its general figure, it much resembles a horse’s hoof in miniature, the
fixed ventral valve corresponding to the unguis or body, the hinge-
area to the soft posterior part of the “frog,’’ and the dorsal valve
to a shoe-plate. This comparison gives a good idea of the obliquity
of the shell in the longitudinal plane, the great depth of the ventral
valve, and its lengthened surface of attachment (figs. 1-3).

The dorsal valve (fig. 1, 6) measures rather more transversely than
longitudinally. The hinge-line is straight, but interrupted in the
middle by a small subquadrate cardinal process (fig. 3, a), fronted
above by a depressed but very distinct umbo, and below by a deep
excavation (0d) receiving a trifid process (fig. 2, b) of the ventral valve
for the attachment of the adductor muscles. From the hinge-line
forwards the margin of the dorsal valve (fig. 3) is rounded, but it is
slightly cut off or sinuated in front. It is, moreover, as a character
of the genus, minutely granulated inferiorly (d). The tooth (c) on
either side of the base of the cardinal process (a) is rather small,
and received into a corresponding dental socket in the opposite valve,

The internal calcareous framework. is very complex in appearance,
consisting of the following parts, namely :—first, an outer simple
loop (fig. 3, ¢) following the contour of the shell, but lying a little
within the granulated margin; 2ndly, two half-loops or hook-like
processes (fig. 3, #) included by the former, and turning inwards and
forwards posteriorly ; and 3rdly, an inner perfect loop (fig. 3, g), with
the free central portion, or bight, reflected downwards and forwards,
and giving off from its concavity a median crest (h), which projects
backwards, and is flanked on either side by the inverted hook-like
ends of the intermediate kalf-loops. The attached surface of all the
parts just mentioned is very considerable, and the simple and reflected
portions of the inner loop are connected by a more or less perfect
calcareous expansion.

Just below the hinge, and connected with the ventral valve, there

518 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17,

is a trifid shelly process (fig. 2, 6), noticed above as giving attach-
ment to the adductor muscles; but as this lies above the middle
portion of the outer loop (c), while it occupies the hollow (fig. 3, 5)

Figs. 1-3, illustrating Thecidium Adamsi.
Hier: Fig. 2.

Fig. 1. Superior view of the exterior. Fig. 3. Interior view of the dorsal
a. Ventral valve. valve.
6. Dorsal valve. a. Cardinal process.
c. Umbone. 6, Recess for the adductor
a d. Hinge-area process of the ventral valve.
e. Deltitium. ec. Hinge-tooth.
d. Granulated margin.
Fig. 2. Inferior view, with a por- e. Outer simple loop.
; tion of the ventral valve f. Intermediate half-loops.
(a) broken away to show: — g- Inner reflected loop.
the adductor process (4), the h. Median crest.
outer plain loop (c), the 2. Points of origin of the parts
intermediate half-loops(d), composing the internal
and the median crest (/). framework.

in front of the cardinal process (a) of the dorsal valve, it follows that
when the shells are intact they cannot be forcibly separated without
breaking the loop (fig. 2, c) upon the adductor process (6). I there-
fore, very cautiously, broke away the ventral valve from below, as
shown in fig. 2, and by simply studying the relations of the parts, I
was enabled to perfect the scheme of the loop-apparatus, as given in
fig. 3.

The hinge-area (fig. 1, d) slopes downwards and a little back-
wards from the line of union of the valves to the beak; and

1863. ] _ SALTER—CRUSTACEAN FROM GLASGOW. | 519

the deltidium (¢), which is rather prominent, may be said to occupy
a little more than the middle third of its surface. It only remains
to be remarked that the originally attached part in all my specimens
is indicated by a longitudinal groove on the inferior surface of
the ventral valve,—being evidently moulded upon a stem or branch
of some dendritic animal or algal form (fig. 1), and often extending
to within a third of the anterior margin. I have named the species
after my friend Dr. Leith Adams, of the 22nd Regiment, who first
pointed it out to me in an evening ramble.

5. On the Sanpstones and Suauzs of the OoxrrEs of ScARBOROUEH, with
Descriptions of new Species of Fossit Puants. By J. Leckensy,
Esq., F.G.S.

[The Publication of this Paper is deferred. |
(Abstract.)

Tue true position of the well-known Plant-bed at Gristhorpe Bay,
below the grey limestone, was first pointed out by Prof. Williamson,
and afterwards by Dr. Wright; and Mr. Leckenby showed that all
the Plants hitherto referred to the Upper Sandstone, Shale, and Coal
belong to the Lower Sandstones and Shales, but few Plants having
been found in the true Upper Sandstones and Shales overlying the
grey limestone. The author gave lists of fossil Plants occurring in
the two sets of strata, as well as of those occurring at the separate
localities ; and he concluded by describing some new and some im-
perfectly known species of Ferns.

6. A Monograph of the Ammonites of the CAMBRIDGE GREENSAND.
By H. Srstzy, Esq., F.G.S.
[The Publication of this Paper is deferred. |
(Abstract. )

THE excavations in the Upper Greensand of Cambridge have furnished
Mr. Seeley with an opportunity of examining a great number of
specimens of the different species of Ammonites occurring in that.
formation, and he now communicated the results of his examinations
to the Society, giving detailed descriptions of the species.

(ee Se

7. On a new Crustacean from the Guase¢ow CoaL-FIELD.

By J. W. Sauter, Esq., F.G.S., A.L.S.

In a previous memoir* I endeavoured to collect together what was
known of the long-tailed Malacostraca of our coal-fields,—fields, it
may be observed, almost untrodden by the palontologist. My
friend Mr. James Russell has since found a new species, which I
eall Palewocarabus Russellianus. _

It is from the Palace Craig “ Black band,” in the Upper Coals,

* Quart. Journ. Geol. Soc. vol. xvii. p. 528.

520 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (June 17,

above the “ Rosslyn Sandstone or Moor Rock,” and lies some 20
or 24 fathoms above the Ell Coal. Anthrapalemon Grossarti, de-
scribed by me in the above-quoted memoir, was from a bed 960 feet
below that coal.

PALMOCARABUS RUSSELLIANUS, Spec. Nov.

P. biuncialis. Cephalothorax oblongus, quadratus, ad latera scaberrimus, haud
divisus, nisi a sulco cervicali punctato vie conspicuo transverse sectus. Rostrum
latum, profunde serratum. Antenne parvule. Antennule ad basin late ex-
panse, spinulose. Abdomen? Cauda?

Figs. 1 & 2.—Carapace and portions of the Appendages of Paleo-
carabus Russellianus.

Fig. 1.

Fig. 1. Natural size. :
Fig. 2. Outline slightly enlarged: a. Antennule; 3. Antenna; c. Scale of
the Antenna.

Description.—The carapace is convex, for it is partly pressed on one
side. The serratures are as in the other Glasgow species, Anthra-
palemon Grossarti, but the central keel reaches the posterior margin,
and joins as strong a cervical furrow as in A. dubius. This cervical
‘furrow is marked out by a line of deep punctations, not furnished
with spines; and a rather deep depression occurs near the anterior
angle of the gastric (?) space (where a spine is present in A. dubius).
The rostrum appears to be a very prominent and triangular mass,
with a broad, strongly serrate, plate-like crest running down its
lower part as far as the cervical furrow. The front part (if I do
not deceive myself) is destitute of this crest, and is moreover sepa-
rated by a rather deep furrow from the hinder portion, so as easily
to break off and present the appearance given by A. dubius*. I do
not, however, speak with certainty concerning this rostral portion—
it is much obscured. The general surface is punctate, the puncta-
tions small and scattered; but towards the margin and front the
carapace is roughly and closely granular.

* Quart. Journ. Geol. Soc. vol. xvii. p. 531, fig. 6.

1863. ] _ SALTER—CRUSTACEAN FROM GLASGOW. 521

The appendages are well preserved, both inner and outer antenne
at least ; and the latter, strange to say, are smaller than the anten-
nules*. Both have widely expanded basal joints, with short spines
overhanging the front border of the carapace. The antennules
(fig. 2, a) have at first four large joints: the first is narrow ; the second
almost square, with a projecting subspinous outer angle; the third tri-
angular ; the fourth broader at the base, wider than long, and followed
by asingle, long, filiform appendage of short close joints. The antenne
(fig. 2, 6)—for they cannot be the interior pair pushed outwards by
pressure—have also broad basal joints, three in number, but not
more than half the diameter of those of the antennules. The basal
joint is broad, the next longer than wide, the third wider than long,
and bearing two filamentary antenne, with some remnants of the
protecting scale (c). The latter is small and not very definite; the
filament is more slender than that of the antennule, but double, and
of longer joints. As I have not seen more of any of the filaments
than 3-10ths of an inch, nothing more can be said of them.

But there is enough of this beautiful Crustacean to show that it
belongs to Paleocarabus, and not to Anthrapalemon, and to show
also that the genera may be now more clearly defined. In addition
to the characters given in my former paper?, I have to add that
Anthrapalemon has the antennz with large basal joints, the anten-
nules with small joints, the carapace with but a faint cervical furrow,
and the ridge incomplete.

Palceocarabus has the antenne smaller than the antennules, but
with expanded basal joints (and the usual scale of the Palemonde),
and the antennules with broad large basal joints; the cervical
furrow and carapace-ridge are complete.

The species just described is certainly new; and I have great
pleasure in dedicating it to Mr. J. Russellt, of Chapel Hill, Airdie,
who kindly forwarded the specimen to me.

ADDENDUM.

Macrura in Bohemian Coal.—Since this paper was read, my friend
Mr. H. Woodward has shown me two specimens of a Macrurous
Crustacean from the Upper Coal-measures (overlying Lower Silurian
rocks) of Beraun, Bohemia. They show the five pairs of limbs and
the bases of the maxillipedes, with the terminal portions of the ab-
domen ; but they are too imperfect to prove the exact nature of this
latter portion. Both specimens expose only the ventral surface,
and both are so flattened as to be little more than black stains in a
brownish-grey schist. The chelz are small; and from the general
aspect of the fossils, I should think them Palemonide rather than
Astacide. The surfaces are covered with tubercles.—[J. W. 8.]

* In Thenus and such genera the outer antenne are largely expanded, but the
antennules are very small in comparison.

t Loe. cit. pp. 529, 530.

t Formerly of the Borneo Antimony Company.
VOL, XIX.—PART I, 2N

522 PROCEEDINGS OF THE GEOLOGICAL society. [June 17,

8. On the OccurRENcE of a Brrominovs Sunstance near Movunt-
GERALD, By Dr. G. ANDERSON,

{In a Letter to Sir R. I. Murchison. ]
(Abstract.)

Tue section exposed by some deep cuttings for the Ross-shire Rail-
way, two miles north of Dingwall, was described by Dr. Anderson
in this letter. The rock in these cuttings is a grey, micaceous,
regularly bedded, and almost horizontal conglomerate, but exhibit-
ing enormous convolutions and twistings of the beds. The strike is
N.W. to S.E., and the rock, in some places, passes into a fine com-
pact sandstone. It is traversed at intervals by what appear to be
perpendicular veins or fissures, lined for the thickness of an inch or
two with a black, shining, compact, bituminous substance having a
black streak and a conchoidal fracture. It burns with smoke and
flame, and becomes electrical when rubbed; and it does not exhibit
any trace of organized matter. Its composition is said to be similar
to that of the Albertite of New Brunswick.

A bituminous substance has long been found in veins at Strath-
peffer in quantities sufficient for burning in the neighbouring cottages.
To what extent these veins may go down in the adjoining rocks
is not known. At Mountgerald the seams are not thicker than an
inch or two ; but in the beds of the Boulder-clay, immediately above
the sandstone-conglomerate, small pieces of the coaly matter occur
in abundance. The bituminous shale comes in near the sandstone-
conglomerate in which the black matter occurs, and, as the author
believes, above it; and he traced the former thence over the ridges
looking down on the Cromarty Firth as far as into Strathskea,

9. On the OccurRENcE of a Bituminous Mrnerat at MountTgERALD,
Scorznanp. By A. C. Mackenztg, Esq.

{Communicated by Professor Tennant, F.G.S.]
(Abstract. )

Tue author first gave a history of the discovery of this bituminous
substance at Mountgerald, stating that it was first noticed. about
fifteen years ago, by the tenant of the farm of Woodlands (Mr.
M‘Ewan), whilst making a drain. The farmer followed the seam as
far as he was able, and procured several cartloads of the mineral,
which he used as fuel. -

Mr. Mackenzie then noticed the similarity of this substance to the
Albertite of New Brunswick ; he also stated that he first saw it,
about five years ago, in a field on the farm of Woodlands, and that,
more recently, a railway-cutting on the farm of Mount Rich, 400
yards south-east of the former locality, enabled him to make the
following observations regarding its mode of occurrence.

The line of railway here passes through a cutting in what is
called the Craig, and it was in this cutting that further quantities

1863.] MACKENZIE—BITUMINOUS MINERAL. 523

of the mineral were discovered, from which the specimens in the
Society’s possession were taken.

Where the cutting commences, about 1} mile frem Dingwall,
the rock consists of a grey sandstone similar to that of the Tulloch
Quarry, and having a north-west dip; but the strata are much
disturbed and broken. The beds continue for about 18 yards, at
the end ef which space there appears a shaly rock mixed with clay,
dipping north at a sharp angle, and underlying the sandstone for
about 12 yards.

Where the shale disappears below the cutting, the sandstone recurs
for abeut 20 yards, also dipping north; and it was here that the
first vein ef the mineral appeared, running S.E. to N.W. through
the bed of sandstone. For these 20 yards the rock is much broken
and arched, in rather thin beds, bending from south te north; after
which the shaly rock reascends, alternating with the grey sandstone,
and with occasional clay-seams between the beds of shale and sand-
stone, between which the mineral is again found in veins varying
in thickness from 3 inch to 14 inch. The arched strata of shale
and sandstone somewhat resemble the fig. 21, p. 199, of Dr. Daw-
son’s ‘Acadian Geology.’ Occasionally the clay rests behind the
mineral, and between the shale- and sandstone-strata.

Similar rocks continue for 60 yards, during the whole of which
portion of the cutting they are much disturbed and contorted, and
the mineral lies in thin veins, The dip of the rocks is here still
N.W., and the veins of the mineral run through them W.by N. The
sandstone appears by itself for about 8 yards, and then the shaly
rock. Here the mineral has been found in greater quantities and
thickness, running in veins of 1, 2, and 3 inches, and adhering
very firmly to, and intimately blended with, the exterior face of the
sandstone. It also outcrops at the surface of the sandstone-rock
under the clay which covers the surface of the hillside. The mi-
neral found adhering to the sandstone is very fine and pure, and
superior in quality to that found in the shale and clay.

Shaly rock continues after this for 6 yards, dipping 8. W. to N.E.;
after which the uplifted sandstone appears for 20 yards, in much
thicker beds and less broken than the previous rock, and dipping §. ;
but no mineral appears. The shaly rock then reappears for 22
yards, also dipping 8.; but about 5 feet behind the face of the
railway-cutting the sandstone shows itself, overlapping the shale;
and at the junction a thin vein of inferior mineral, about 4 inch thick,
lies like packing between the two strata. Conglomerate next ap-
pears upon the top of the sandstone, and the vein of mineral goes
quite through it.

From where the sandstone overlaps the shaly rock, the conglo-
merate appears alone for about a quarter of a mile, at the end of
which distance the cutting is continued through clay.

The conglomerate strikes east and west, and has a slight dip to the
north, whilst the veins of the mineral, which are very numerous,
varying from 7 inch to 3 inches in thickness, traverse the conglo-
merate at an angle of almost 45° in the direction S.E. to N.W.

2Nn2

524 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 17,

Whenever the mineral appears between walls of conglomerate, the
faces of the latter are perfectly smooth. There are several other
breaks in the beds of conglomerate, running N.E. to 8.W., but in
none of them was any mineral discovered.

The cutting varies from 12 to 25 feet in depth, and is throughout
about 200 yards from the shore. In several places, when, in blast-
ing the sandstone, rock was reached below the conglomerate, finer
and thicker specimens of the mineral were discovered closely ad-
hering to the sandstone, and reaching 34 inches in thickness.

No boring has as yet been attempted; but during the length of
the cutting above mentioned, as many as thirty-six separate veins
of the mineral were met and cut through.

10. On the Occurrence of Rocxs of Upper Crerackous AcE im
Eastern Beneat. By T. OrpHam, LL.D., F.R.S., F.G.S., &e.

Durine the years 1851-52, I had an opportunity of visiting the
Khasi Hills, in Eastern Bengal, and made a tolerably large collection
of the fossils oceurring in the rocks there. At that time the Geological
Survey of India had no office or place in which these fossils could
be opened out for examination, nor were there in India any collec-
tions sufficient for comparison, or any libraries containing the books
necessary for reference. I was, therefore, compelled to be satisfied
with such a cursory examination as could be made during the pack-
ing up of the specimens. This examination was even more cursory
than it would otherwise have been, inasmuch as my deeply re-
gretted friend Edward Forbes had promised to go carefully over all
these fossils and to describe any that proved new or interesting.
I had, by letter, poimted out to him the great interest which at-
tached to them, inasmuch as many of them strongly recalled some
of the forms which he had then recently described from the beautiful
collections of Messrs. Kaye and Cunliffe from South India, while
other beds contained undoubted Nummulites and several known
‘“ Nummulitic” fossils. The collection which I had made was
chiefly from the Nummulitic Limestone, close to the station of
Cherra Poonji; but there was also a good number from the sand-
stones underlying this limestone, to which I especially requested
Prof. Forbes’s attention, as they appeared to me to be of Cretaceous
rather than Tertiary age.

These latter were, however, much fewer in number, because the
only season of the year during which I could visit these hills being
that of “the rains” (during which the average fall of rain at
Cherra Poonji is about 600 inches, concentrated in these four or five
months), it was not safe to do more than pay an occasional visit to
the lower country. But there was a sufficient number to have
yielded, on careful examination, a decisive result.

I anxiously waited the result of this examination by Prof.
Forbes, and deferred the publication of any report on the geology of

1863.] OLDHAM—CRETACEOUS ROCKS OF BENGAL. 525

these hills, hoping to have his conclusions. But, unfortunately, the
whole of this collection, which had cost much time and trouble, was
lost in its transmission to England.

I could, however, no longer delay the description of these hills,
and in 1854 a short account of them was published in Calcutta. In
this I pointed out how incomplete any report on their structure
must unavoidably be, until the final results of the comparison of the
fossils were known. And I also said, “ It is to me a source of great
regret that, owing to the season of the year during which I visited
these hills, I was unable to examine the lower parts of the ridge, or
te proceed along the base, where many points of great geological
interest still await solution. Densely covered as these portions are
with close grass-jungle, a sojourn there during the wet and hot
months of summer would be almost certain death to a European;
and I was, therefore, obliged to forego my desire of visiting these
districts. It will be seen that in consequence several questions of
interest have been left still unsolved.”

This being the case, and all the valuable fossils, on which alone
any sound conclusions could be based, having been lost, I was com-
pelled to leave the question of their age undecided. The only section
I could, at that season, examine seemed to show continuous sequence
and conformity of the beds. And in describing this I added, “It is
possible that some of the sandstones may have been geologically
coeval with the upper or latest portions of the Cretaceous group of
Europe,” thus leaving the age of these sandstones undecided, while,
from the abundance of Nummulites, there was no question as to the
age of the limestone resting on them.

Further, at that time (1853), the knowledge of the fossils of the
beds forming the upper limits of the Cretaceous era, and of those
constituting the lowest limits of the Tertiary period, was infinitely
less perfect than it now is.

I did not, however, forget the impression which those fossils had
left on my own mind, that they were Cretaceous, and I failed not to
take every opportunity to replace, so far as possible, the collections
which had been lost. I got, from year to year, some additions
through friends who had visited the place ; and in 1859 I despatched
one of the staff of the Geological Survey to these hills, in the hope
of being able to obtain a good collection. But the prevalence of
cholera drove him from the place ; and as with myself, so with others,
the extreme nature of the season during which they visited the hills
prevented much being done in the lower grounds. And, therefore,
almost the only additions I received were of fossils, often extremely
imperfect, from the limestone, which, occurring at the upper levels,
is easily accessible, but regarding the geological epoch of which there
was no doubt.

During last year (1862), however, I received from W. L. Atkinson,
Esq., a small collection from Cherra Poonji, among which, in addi-
tion to the ordinary Limestone fossils, there were a few from the
lower sandstones; and a few months later Dr. T. C. Jerdon brought
down another small collection, almost entirely from these sandstones.

‘526 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [June 17,

Among the first (those brought by Mr. Atkinson) there was one
small fragment of an undoubted Terrilite; and it was therefore with
no small interest that I opened Dr. Jerdon’s collection and found in
it specimens of Ammonites and Baculites, together with other dis-
tinctive fossils.

It was thus conclusively established that these sandstones were
really, as I had always suspected, of Upper Cretaceous age.

I shall not dwell on the immense importance of this result, as
bearing on Indian geology; it will be obvious to all who have
made themselves acquainted with the results hitherto published ;
and to make it clear to others would require a much more lengthened
explanation than could now be given.

I shall simply give a list of genera, and a few species, which have
been distinguished in the small collections we now have, and hope
soon to be able to obtain better and more complete data. I have
had the valuable aid of Dr. Stoliczka in going over these fossils.

Ammonites. Turritella Pondicherriana, Fortes,
Turrilites.. ——, two species.
Baculites. Vermetus.
Pterocera, very near P. angulata, Trochus.
Zekeli, from Gosau. Turbo.
Tritonium loricatum, Sow. Cynulia decurata, Sow.
—— sp. (?). , two species.
Fusus Dupinianus, D’ Ord. Bulla, or Ovula.

, four species. Terebratula, very near T. arabilis.
Rostellaria carinata (?). , very near T. tamirandus, Sow.
— granulata, Sow. Rhynchonella, two species.

palliata, Forbes. Gastrochzena.

Pleurotoma subtilis, Zekelz. Pecten, two species.
——, near P. costata, Sow. Janira, sp.
Voluta septemcostata, Forbes. Ostrea.
Camdeo, Forbes. Plicatula.
Mitra cancellata, Sow. Spondylus tenuistriatus, Sow.
Cyprea, two species. Anomia.
Eulima. Cardium, two species.
Natica lyrata, Sow. Lima Heriana, D’ Ord.
pagoda, Forbes. —-, sp., probably L.parallela, dV’ Orb.
Cerithium scalarioideum, Forbes. Echinoconus.

; probably C. provinciale, Sow. — Cidarites,
, aspecies not yet published, but Toxaster.
which oecurs at Gosau. Ananchytes.

It is certain that. these rocks extend considerably to the east,
beyond the parallel of Cherra Poonji. And it is not improbable
that a large area in Munnipore and Burmah, hitherto supposed to be
of Tertiary age, will prove on closer examination to be of the same
Upper Cretaceous age as the rocks now referred to.

Among the fossils from the Nummulitic Limestone, most of which
were imperfect, were

Natica longispira, D’ Arch. Pecten, probably P. Fauvei, D’ Arch.
Cyprea depressa, Sow. Nummulites Beaumontii, D’ Arch.
Oliva, probably 9. virginea, D’Arch. —— obtusus, Sow.

527

DONATIONS
TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From April 1st to June 30th, 1863.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

Abbeville. L’Abbevillois. 24™° Année. No. 2578. May 21, 1863.
No. 61.

La machoire humaine qui a été trouvée récemment prés d’Abbeville, 2.

American Journal of Science and Arts. Second Series. Vol. xxxv.
Nos. 104 £105. March and May 1863. From Prof. B. Silliman,
For.Mem.G. 8S.

T. Sterry Hunt.—Chemical and Geological History of Bitumens, 157.

E. B. Hunt.—Growth and Chronology of the Florida Reef, 197.

QO. C. Marsh.—Mineral Localities in New Brunswick, Nova Scotia,
and Newfoundland, 210.

J. D. Dana.—Existence of a Mohawk-valley Glacier in the Glacial
Epoch, 248.

Report on specimens collected in Frobisher Bay, 293.

J. D. Dana.—Echinoderm from the Blue Limestone of Cincinnati,
Ohio, 295.

J. Hall_—New Crustacean from the Potsdam Sandstone, 295.

T. Coan.—Crater of Kilauea, 296.

Arsenides of Copper from Lake Superior, 296.

J. W. Dawson.—On American Devonian, 309.

——. Flora of the Devonian Period in North-eastern America, 311.

A. G. Ramsay.—Glacial Origin of certain Lakes in Switzerland, the
Black Forest, Great Britain, Sweden, North America, and else-
where, 324.

L. Lesquereux.—Some questions concerning the Coal-formations of
North America, 375.

J. Hall.—Observations upon some of the Brachiopoda, with reference
n we genera Cryptonella, Centronella, Meristella, and allied forms,

H, Rose.—On the composition of Columbite, 426.

528 DONATIONS.

American Journal of Science and Arts. Second Series. Vol. xxxv.
Nos. 104 & 105 (continued).

T. Korovaeff—Kischtimite, a new mineral, 427.

T. A. Conrad.—Catalogue of the Miocene Shells of the Atlantic
Slope, 428.

A. DeCandolle.—Etude sur l’Espéce, 4 l'occasion d’une révision de
la Famille des Capuliféres, 431.

Anthropological Review. No.1. May 1863.
Lyell’s ‘ Antiquity of Man,’ noticed, 129.
Wilson’s ‘ Pre-historic Man,’ noticed, 137.

A. Tylor.—Human Remains from Moulin-Quignon, 166.
H. Falconer.—Reputed Fossil Man of Abbeville, 177.

Assurance Magazine. Vol. xi. Part 1. April 1863. From the In-
stitute of Actuaries.

Atheneum Journal. Nos. 1849-61.

Notices of Meetings of Scientific Societies, &c.

Primeval Man, 459, 523.

W. B. Carpenter.—Discovery of a fossil Human Jaw at Abbeville, 523.

A. C. Ramsay’s ‘ Physical Geology and Geography of Great Britain,’
noticed, 553.

Antiquity of Man, 555, 586, 817.

Human Jaw at Abbeville, 682, 747, 779.

Ossiferous Cavern at Gibraltar, 716.

Atlantis. Vol. iv. Nos. 7&8. 1863.

W. K. Sullivan and J. P. O’Reilly—Sulphate of Soda in the Valley
of the Jarama, near Aranjuez, in Spain, 288.

. Chemical composition of a Lacustrine Dolomitic Limestone

from the neighbourhood of Madrid, 315.

Geology and Mineralogy of a part of the Spanish Province

Santander, 319.

Berlin. Monatsberichte der k. preuss. Akademie der Wissenschaften
zu Berlin. 1862.

Beyrich.—Vorkommen St.-Cassianer Versteinerungen bei Fiissen, 27,

Lagerung der Lias- und Jura-Bildungen bei Vils, 647 (plate).

Ehrenberg.—Die obersilurischen und devonischen mikroskopischen
Pteropoden, Polythalamien und Crinoiden bei Petersburg, 599
(plate).

Rammelsberg.—Zur chemischen Kenntniss mehrerer Mineralkorper,
237.

. Schwefelungsstufen des Hisens und das Schwefel-Eisen der

Meteoriten, 681.

. Angeblichen Stickstoffgehalt des Roheisens, 692.

G. Rose.—Meteorsteinfall im Kaukasus nach Abich’s Bericht, 186.

——. Meteoriten auf Grund der Sammlung in dem mineralogischen
Museum der Universitat von Berlin, 341, 362, 551.

Asterismus der Krystalle, insbesondere des Glimmers und des
Meteoreisens, 614 (plate).

H. Rose.—Zusammensetzung des Columbits, 138.

——. Zusammensetzung niobhaltiger Mineralien, 166.

——. Zusammensetzung des Samarskits, 622.

DONATIONS. 529

Berlin. Zeitschrift der deutschen geologischen Gesellschaft. Band xiv.
Heft 4. August-October 1862. |

Von Cotta.—Die Erzlagerstiitten Europas, 686.

Von Albert.—Vorkommen yon Kohlenkalk-Petrefakten in Ober-
schlesien, 689.

J. G. Bornemann.—Ansichten von Stromboli, 696 (4 plates).

C. Schliiter.—Die macruren Decapoden der Senon- und Cenoman-
Bildungen Westphalens, 702 (4 plates).

C. Rammelsberg.—Analysen einiger Phonolithe aus Bohmen und der
Rhon, 750.

——. Ueber den Glimmer von Gouverneur, nebst Bemerkungen
tiber Natron- und Baryt-Glimmer, 758.

F. Roemer.—Ueber die Auffindung einer senonen Kreidebildung bei
Bladen unweit Leobschiitz in Oberschlesien, 765.

G. vom Rath.—Geognostisch-mineralogische Beobachtungen im
Quellgebiete des Rheins, 770.

Band xy. Heft 1. November 1862—January 1863.

A. Seacchi.—Ueber die Polyedrie der Krystallflachen, 19 (8 plates).
Dean Se en die Kreide am Zeltberg bei Liineberg, 97
plate).
A. Oppel.—Ueber das Vorkommen von jurassischen Posidonomyen-
Gesteinen in den Alpen, 188 (3 plates).
W. Sartorius von Waltershausen.—Einige Bemerkungen iiber die
Zusammensetzung der krystallinischen Gesteine, 218.

Berwickshire Naturalists’ Club. Vol.iv. No.6. 1863.

Brussels. Annuaire de l’Académie Royale des Sciences, &c., de Bel-
gique. 29me Année. 1863.

——. Bulletin de l’Académie Royale des Sciences, &c., de Belgique.
3lme Année. 2me Sér. Vol. xiii. 1862.

Malaise—Age des phyllades fossiliféres de Grand Manil, prés de
Gembloux, 168.

Dewalque.—Systéme eifélien dans le bassin de Namur, 146.

. Non-existence du terrain houiller 4 Menin, 201.

Dejardin.—Systémes scaldisien et diestien, ainsi les couches supéri-
eures prés de la ville d’Anvers, 470 (2 plates).

P. Gervais.—Sur les Squalodon, 462 (plate).

Vol. xiv. 1862.

Reuss’s ‘ Die Foraminiferen der Crag von Antwerpen,’ noticed, 449.
E. de Verneuil.—Paradoxides et Conocephalus dans la province de
Téruel (Aragon), 170.

oe

——. Mémoires couronnés, &c. Coll. in-8vo. Vol. xii. 1862.
A. Perrey.—Note sur les tremblements de terre en 1859, avec supplé-
ments pour les années antérieures.
Vol. xiv. 1862.

A. Perrey.—Note sur les tremblements de terre en 1860, avec supplé-
ments pour les années antérieures.

———————

530 DONATIONS.

Caleutta. Asiatic Society of Bengal. Journal. New Series. No. exiv.
1862.

J. L. Sherwill.—Glaciers of the Kanchunjingah Group in the Sikkim
Himalaya, 457 (plate).

. Journal of the Asiatic Society of Bengal. NewSeries. No. cxv.
1863, Part 1.

Canadian Journal. New Series. No. 44. March 1863.
E, J. Chapman.—Minerals and Geology of Canada, part 5, 111.

Chemical Society. Journal. Ser.2. Vol.i. Nos.5&6. May and
June 1863.

How.—Pickeringite occurring in Slate in Nova Scotia, 200.

Colliery Guardian. Vol. v. Nos. 118-130.

Notices of Meetings of Scientific Societies, &c.

J. Morris. —Coal, 265, 285.

W. W. Smyth.—Lectures on Mining, 266, 289, 309.

Dip and Underlie, 269.

M. Fryar.—Economic products of the Carboniferous System, 288, 305.

A. C. Ramsay’s ‘ Physical Geology and Geography of Great Britain,’
noticed, 291.

R. Hunt.—Mining and Metallurgy, 327.

Denudation and its Causes, 365,

Igneous Rocks, 365.

Coal of New South Wales, 375.

Geological Epochs, 588.

Formation of Glaciers, 389.

J. B. Jukes.—Lectures on Geology, 407, 430, 447, 468, 490, 507.

J. Fulton.—Broad Top Coal-region, 411.

Subterranean Forest at Hull, 417.

Extinct Ox in the Fens, 417.

J. W. Watson.—Ironstone of the Forest of Dean, 427, 467.

J. Dickinson.—Coal-strata of Lancashire, 448, 468.

Geology of North-west British America, 467.

G. Wild.—-Fulledge Section of the Burnley Coal-field, 485.

Mine-pumps, 485.

Methods of Working Coal, 488.

Influence of the Blast in the quality of the Iron, 488.

Duration of the Northern Steam-coalfield, 489.

Fossil Star-fish from the Wenlock formation near Dudley, 493,

Glasgow School of Mines, 496.

G. V. Du Noyer.—Bituminous Coal of the Arigna District, Counties
of Roscommon and Leitrim, 508.

Copenhagen. Det kongelige danske Videnskabernes Selskabs Skrifter.
5 Rekke, Naturvidenskabelig og Mathematisk Afdeling. Vol. v.
1861.

Oversigt over det kgl. danske Videnskabernes Selskabs For-
handlinger, &c. 1861.

J. Steenstrup.—Fremviser og oplyser et i en Torvemose i Fyen funde
uscedvanlig stort Bjornecranium (af Ursos aretos, L.), 165,

DONATIONS. 531

Copenhagen. Questiones, que in anno 1863 proponuntur a Societate
Regia Danica Scientiarum cum preemii promissu.

Cotteswold Naturalists’ Club. Proceedings. Vol.i. 18538.

S. P. Woodward.—Geology of the district explored by the Cottes-
wold Club, 2.

J. Lycett.—Fossil Conchology of the Great Oolite of Minchinhampton,
aye

Distribution of the Fossil Conchology of the Oolitic Forma-

tions near Minchinhampton, 21.

On Trichites, a fossil genus of bivalve Molluscs, 42 (plate).

1 = Brodie.—Geology of the Neighbourhood of Grantham, Lincoln-

_ shire, 52.

J. Lycett.—Tabular view of Fossil Shells from the middle division
of the Inferior Oolite in Gloucestershire, 62 (plate).

T. Wright.—Section from Round Tower Point to Alum Bay, Isle of
Wight, 87.

—. Strombide of the Oolites, 115.

J. pikes of a new and remarkable Pteroceras, 118

ate).

ie Wrickh—Stratigapbical account of the section of Hordwell,
Beacon, and Barton Cliffs, 120.

Cidaride of the Oolites, 134 (3 plates).

—. Cassidulide of the Oolites, 174 (2 plates).

——. Paleontology of the Isle of Wight, 229.

J. Lycett.— Gryphea of the Gryphite Grit in the Cotteswolds, 235.

——. Additional notice of the genus Tancredia (Lycett), 237.

P. B. Brodie.—Lias near Newnham, and Pleistocene Deposits in the
Vale of Gloucester, 241.

J. Lycett.—New species of Trigonia from the Inferior Oolite of the
Cotteswolds, 247 (plate).

J. Buckman.—Cornbrash of the Neighbourhood of Cirencester, 262.

—. Lnbellula Brodieci, a fossil Insect from the Upper Lias of
Dumbleton, Gloucestershire, 268.

——, ——. Vol.u. 1860.

T. Wright.—New species of Echinodermata from the Lias and Oolites,
17 (8 plates).

——. Fossil Echinodermata of the Island of Malta, 55 (4 plates).

J. Lycett.— Perna quadrata, 118.

T. Wright.—New genus of fossil Cidaride, 121.

——. New species of Hemipedina from the Oolites, 128.

J. Lycett.—On the subgenus Limea, Bronn, 131.

P. B. Brodie.—Inferior Oolite and Lias of Northamptonshire and
Gloucestershire, 132.

J. Lycett.—On the genus Quenstedtia, 155.

P. B. Brodie.—Lias of Barrow, Leicestershire, 159.

J. Lycett.—Sands between the Inferior Oolite and Lias, 142.

——. Fossil genus Jsodonta, Buy.,in the English Jurassic Rocks,
153.

——. Upper Lias at Nailsworth, Gloucestershire, 155.

W. V. Guise.—Inferior Oolite near Bath, 176.

Vol. ii. Appendix. 1860.
J. Jones,—Rhynchonella acuta, 1 (plate).

=e
2 e

§32 DONATIONS.

Cotteswold Naturalists’ Club. Proceedings. Vol. ii. pp. 1-95.
1861-62.

J. Lycett.—Ammonites of the Sands between the Upper Lias and
Inferior Oolite, 3.

kh. Witchell.—Sections of the Lias and Sands at Stroud, 11.

W. 8. Symonds.—Drifts of the Severn, Avon, Wye, and Usk, 31.

F. Smithe.—Geology of Churchdown Hill. Part L., 40.

J. Jones.—Gryphea incurva and its varieties, 81 (6 plates).

‘Critic. Vol. xxv. Nos. 635-637. April-June 1863.

Notices of Meetings of Scientific Societies, &c.
Lyell’s ‘ Antiquity of Man,’ noticed, 295.

Dublin Geological Society. Journal. Vol. x. Part 1. 1863.

T. W. Kingsmill.—Geology of the East Coast of China, 1.

The Dhurmsalla Aérolith, 7.

J. B. Jukes.—Calamine at Silvermines, County of Tipperary, 11.

R. H. Scott.—Granitic rocks of Donegal, 18.

M. Taylor.—Geology of the District of Shorapoor, or Soorpoor, in
the Dekhan, 24.

A. B. Wynne.—Geology of parts of Sligo, &e., 33.

Hey. Holribent<Groclboikal Structure of Finland, 41.

Geologist. Vol. vi. Nos. 64-66. AprilJune 1863.

Notices of Meetings of Scientific Societies, &c.

S. J. Mackie.—The Parallel Roads of Glen Roy, 121 (plate).

——. Species of Ptychodus from the Chalk, 161 (plate).

——. Physical and Cosmical Phzenomena, 178.

——. Ripple-drift in Mica-schist, 201 (plate).

C. C. Blake.—New Fish-jaw from the Gault at Folkestone, 183.

P. Simmons.—Glacial Action in Scotland, 163.

W. King.—Glacial and Postglacial Deposits of the British Isles, 168.
C. C. Blake.—Chelonian Scutes from the Stonesfield Slate, 183.

R. L. Guppy.—Older Parian Formation of Trinidad, 204.

S. R. Pattison.—Land-surface under Drift on the Coast of Suffolk, 207.
Correspondence, 134, 184, 208. Notes and Queries, 154, 197, 234.
Reviews, 156, 198, 237.

Geologists’ Association. Proceedings. No.9. 1862-63.

Excursion to Hastings, 248.

G. E. Roberts.—Bone-beds ; their occurrence in sedimentary deposits,
and possible origin, 251.

C. Evans.—A Superficial Freshwater deposit near the Blackfriars
Road, 264.

R. J. L. Guppy.—Older Parian Formation at Pointe-a-Pierre, Trini-
dad, 267.

Excursion to Cambridge, 271.

S. Cuming.—Ancient Flint Implements from the fields of Bridling-
ton, Yorkshire, 273.

Visit to the Main Drainage Works, 277.

Visit to the International Exhibition, 279.

J. Morris.—Coal-plants, 289.

C. C. Blake.—Fossil Mammalia of South America, 308.

Heidelberg, Verhandlungen des nat.-med. Vereins zu. Vol. iii. No. 1.
1863.
R. Blum.—Ueber die Grosse der Krystalle, 1.

DONATIONS. 533

Horticultural Society. Proceedings. Vol.ii. No.5. May 1, 1863.

Institution of Civil Engineers. Abstracts of Proceedings, Nos. 14,
16-18, 20-22. Session of 1862-63.

Intellectual Observer. Nos. 16 &17. May and June 1863.

Klagenfurt. Jahrbuch des naturhistorischen Landesmuseums von
Karnten. Heft 5. 1862.

Liége. Mémoires de la Société ee des Sciences de Liége.
Vol. xvii. 1863.

Linnean Society. Journal of the Proceedings. Vol. vu. No. 26.
——. list of Fellows, &. 1862.

——. Transactions. Vol. xxii. Part 3. 1862.

—. ——. Vol. xxiv. Partl. 1863.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xxv. Nos. 169-171. May and June 1863. From Dr. W.
Francis, F.GS.

EK, C. H. Day.—Lias of the Dorsetshire Coast, 409.

N. S. Maskelyne and V. von Lang. —Mineralogical Notes, 482 (4
plates).

Tschermak.—Origin of Amygdaloid Rocks, 491.

R. I. Murchison.—Permian Rocks of North-eastern Bohemia, 552.

H. B. Holl.—Inferior Oolite of the Middle and South of England, 554,

H. Porter.— Drifted Wood in the Oxford Clay, 554.

H. Woodward.—New Macrurous Crustacean from the Lias of Lyme
Regis, 554.

J. Fergusson.—Recent Changes in the Delta of the Ganges, 555.

London Review. Vol. vi. Nos. 144-156. April—June 1863.

Notices of Meetings of Scientific Societies, &c.

The Fossil Preadamite, 514.

Abbeville J a 560.

J. Ruskin.—Alps of Savoy, 642.

Ansted’s ‘The Great Stone Book of Nature,’ noticed, 691.

Longman’s Notes on Books. Vol. ii. No. 33. May 30, 1863.

Manchester Geological Society. Transactions. Vol. iv. Nos. 5-7.
Session 1862-63.

T. T. Wilkinson.—Drift-deposits near Burnley, 108.

Geinitz.—The Dyas or Permian Formation in England, 121.

J. Dickinson.—Coal-strata of Lancashire, 155.

J. Whitaker.—Some teeth and a flint found i in the Drift at Barrow-
ford, near Burnley, 176.

G. Wild. —Fulledge Section of the Burnley Coal-field, 179.

H. Bramall.—Sinking through Drift, 194 (2 plates).

Mechanics’ Magazine. New Series. Vol. ix. Nos, 223-230. April-
May 1863.

Notices of Meetings of Scientific Societies, &c.

534 DONATIONS.

Melbourne. The Yeoman Newspaper. Vol. ii. No. 71. February 7,
1863.

Exhaustion and Renewal of Soils, 288.
Live Moa near Lake Wakatipu, New Zealand, 294.

Milan. Atti del Reale Istituto Lombardo di Scienze, Lettere, ed
Arti, Volume iii. fasc.9 & 10. 1863.

——. Atti della Societa Italiana di Scienze naturali. Vol. iv., for
1862. )

Meneghini—Resti di due fiere trovati nelle ligniti mioceniche di
Montebamboli, 17 (2 plates).

Gastaldi.—Sugli elementi che compongono i conglomerati miocenici
del Piemonte, 34.

Sella.—Sul modo di fare la Carta geologica del Regno d’ Italia, 155.

Bianconi.—Cenni storici sugli studj paleontologici e geologici in
Bologna, 241.

A, Villa.—Gite malacologiche e geologiche nella Brianza, 299.

Stoppani.—Nuove osservazioni sull’ Infralias, 316.

Mining and Smelting Magazine. Vol. iii. Nos.16-18. April—June
1863.

Dip and Underlie, 209.

G. Darlington.—Deposit of Calamine at Silvermines in the county
of Tipperary, 211.

D. T. Ansted.—Bituminous Minerals, 340,

Abstracts and Reviews, 214, 270.

Notes and Memoranda, 232, 295.

Correspondence, 294.

Munich. Sitzungsberichte der k. bayer. Akademie der Wissenschaf-
ten zu Munchen. 1862. Theil 2. Hefte 3 & 4.

—. —. 1863. Thelll. Hefte 1 & 2.

Palzontographical Society. Monographs. Volume for 1860. 1862.

T. Davidson.—British Fossil Brachiopoda. Part 5:—A Monograph
of the British Carboniferous Brachiopoda. Appendix and Conclu-
sion (8 plates).

R. Owen.—British Fossil Reptilia from the Oolitic Formations.
mie , :—Scelidosairus Harrison and Pliosaurus grandis (12

ates).

Te eupest Jones.—A Monograph of the Fossil Estherie (5 plates).

T. Bell—A Monograph of the Fossil Malacostracous Crustacea of
Great Britain. Part 2:—Crustacea of the Gault and .Greensand
(11 plates).

Volume for 1861. 1863.

T. Wright.—British Fossil Echinodermata from the Oolitic Forma-
tions. Vol. 11. Part 1:—Asteroidea (12 plates).

J. Lycett—Supplementary Monograph on the Mollusca from the
Stonesfield Slate, Great Oolite, Forest-marble, and Cornbrash (15
plates).

Paris. Annales des Mines. Sixiéme Série. Vol. ii. Livr. 6. 1862.
Delesse et Laugel.—Extraits de Géologie pour Année 1861, 427,

DONATIONS. 5S;

Paris. Annales des Mines. Sixiéme Série. Vol. iii, Livr. 1 & 2.
1863.

Drouot.—Sources thermales de Bourbonne-les-Bains, 1 (2 plates).
L. Moissenet.—Filons du Cornwall et du Devonshire, 161.

Bulletin de la Société Géologique de France. Deuxiéme-
Série. Vol. xx. feuilles 1-12. March and April 1863,

A. F, Nogués.—Les gypses secondaires des Corbiéres, 12.

Matheron.—Les dépots fluvio-lacustres des environs de Montpellier,
de l’Aude, et de la Provence (résumé), 15,

De Helmersen.—Les grés d’Artinsk (Oural), etc., 26.

Buteux.—Quelques opinions émises au sujet des silex travaillés du
département de la Somme, 30,

G. de Saporta.—Une nouvelle classification des terrains tertiaires
lacustres du sud-est de la France, 31.

Des Cloizeaux.—Les modifications permanentes et temporaires que
Vaction de la chaleur apporte 4 quelques propriétés optiques de
plusieurs corps cristallisés, 41.

H. Coquand.—La convenance d’établir un nouvel étage dans le
ere de la craie moyenne, entre les étages angoumien et proven-
cien, 48.

Collenot.—La présence des Astéries dans la zone a Avicula contorta,

Li. Aucapitaine —Un dépot d’Huitres dans l’étang de Diane (Corse),
5

J. J. Bianconi.—Observations sur la note de M. Pareto: Coupes 4
travers Apennin, 59.

_ J. Fournet.—Apercus relatifs 4 la Carte géologique de la Savoie, du

Piémont et de la Ligurie, de M. A. Sismonda, 68.

H, Coquand.—L’existence de la craie blanche dans le 8.-O. de la
France et en Algérie, 79.

Ed. Hébert.—Le non-synchronisme des étages campanien et dordo-
nien avec la craie de Meudon et celle de Maestricht, 90.

Guillier.—Une note de M. l’abbé Bourgeois, relative au terrain crétacé
du département de Loir-et-Cher, 101.

L. Semann.—La succession des faunes dans le bassin tertiaire de
Vienne (Autriche), 103.

Levallois—Sur une nouvelle édition de son ‘Apercu de la constitu-
tion géologique du département de la Meurthe,’ 107.

Ed. Hébert.—Sur Vouvrage de M. Figuier intitulé ‘La terre avant
le déluge,’ 107.

Melleville.—Réponse aux observations de M. Hébert sur sa note
relative aux ‘Terrains de transport superficiels du bassin de la
Somme,’ 108.

E. Dumortier.—Sur deux nouveaux gisements du calcaire a fucoides
de l’oolithe inférieure, 112.

Harlé.—Deuxiéme note sur la vallée de la Seine dans le département
de la Seine-Inférieure, 114.

. Sur le niveau géologique des calcaires crétacés de Sarlat
(Dordogne), 120.

P. Dalimier.—Sur la géologie comparée du plateau méridional de la
Bretagne, 126 (plate).

Sir R. Murchison.—Sur l’existence du gneiss fondamental ou lauren-
tien et sur le développement des dépéts de l’Age permien en Bohéme,
155.

Th. Ebray.—Sur la position des calcaires caverneux autour du plateau
central, 161 (plate).

536 DONATIONS.

Paris. Bulletin de la Société Géologique de France. Deuxiéme
Série. Vol. xx. feuilles 1-12 (continued).

A. Boué.—Lettre sur divers sujets, 189.
J. Gosselet.—Sur lage du calcaire de Blaye, 191.

——. Comptes Rendus des Séances de l’Académie des Sciences...
1862, Deuxiéme Semestre. Vol. lv.
Damour.—Aunalyse d’une pierre météorique tombée le 3 octobre 1815
a Chassigny, prés la ville de Langres, 591.
Domeyko.—Les grandes masses d’aérolithes trouvées au désert
d’Atacama dans le voisinage de la Sierra de Chaco, 873.
G. de Uhagon.—La dynamique des corps flottants, 98.
Delesse.—Carte agronomique des environs de Paris, 635.
Lefort.—Formation naturelle de deux sulfates ferroso-ferriques par
la décomposition de la pyrite martiale, 919.
Moissenet.—Etudes sur les filons du Cornouailles et du Devonshire.
Transport des cercles du réseau pentagonal au point aiv; directions
, utiles pour étain, cuivre ou plomb, 759.
Elie de Beaumont.—Remarques sur les accidents stratigraphiques du
département de la Haute-Marne, 76, 118, 163.
Passy.—Communication accompagnant la présentation de sa carte
géologique de la Seine-Inférieure, 260.
Fournet.—Apercus sur la structure de la partie des Alpes comprise
entre le Saint-Gothard et l’Apennin, 857.
Marcel de Serres. —Empreintes de gouttes de pluie de l’ancien monde,
et leur reproduction artificielle, 105.
Hébert.—Nouvelles observations relatives au calcaire 4 Lophiodon de
Provins: son extension dans la Beauce, 149,
E. Dumas et P. de Rouville-—La carte géologique de l’arrondisse-
ment de Lodéve (Hérault), 192.
Trigen.—Un tableau des divisions générales de la carte géologique de
la Sarthe, 203.
Beguyer de Chancourtois.—La distribution des gites minéraux par
alignements paralléles aux directions des systemes de montagnes
dans le tiers nord-est de la France, 312.
Raulin.—L’age des Ophites de Dax (Landes), 669.
Favre.—La carte géologique des parties de la Savoie, du Piémont et
de la Suisse voisines du mont Blane, 701.
De Rochas.—La formation des iles de corail de la mer du Sud, 705.
Nogués.—Des sédiments inférieurs et des terrains cristallins des
Pyrénées-Orientales, 874.
Dalimier.—La géologie comparée du plateau méridional de la Bre-
tagne, 922.
Terreil.— Analyse de divers échantillons de kaolins et d’une argile
rouge de la province d’Almeria (Espagne), 60.
Phipson.—Le zinc natif, 218.
Le soufre arsénifére des solfatares de Naples et sur la prépa-
ration du sélénium contenu dans ce soufre, 108.
Pisani.—Le grenat octaédrique de Vile d’Elbe, 216,
Sur Vesmarkite de Brakke en Norvége, 450.
——. Sur la spinelle de Migiandone, dans la vallée de la Toce
(Piémont), 924.
Semann et Pisani.—La cancrinite et la bergmanite de Barkevig en
Norvége, 884.
Damour.—Analyse de la pierre météorique de Chassigny, trés-rap-
poe par sa composition du péridot ferrugineux ou hyalosidérite,

DONATIONS, 537

Paris. Comptes Rendus des Séances de l’Académie des Sciences.
1862, Deuxiéme Semestre. Vol. lv. (continued).

. Robert.—“ Gisement celtique de la montagne Sainte-Genevidve &

rae ” et “Nouveau gisement celtique 4 la Gare de Paris,” 45,
, 800.

Montucci.—Le gisement des silex travaillés de Saint-Acheul et sur
ene d’ossements humains dans les couches qui les renferment,

Gaiffe et Benoit.—Note accompagnant des piéces trouvées dans un
gisement contenant & la fois des ossements humains et des armes
et instruments en pierre, 569.

A. Milne-Edwards.—L’existence des crustacés de la famille des
Raniniens pendant la période crétacée, 492.

De Saporta.—Etude sur la végétation du sud-est de la France a
lépoque tertiaire, 396.

Bidard.—Des empreintes qui se voient a la surface d’une roche du
département de l’Orne, et qui simulent les traces de pas de grands
ruminants, 218.

Ch. Sainte-Claire Deville—Les émanations volcaniques des Champs
Phlégréens, 583.

Becquerel.—Nouvelles recherches sur la température de lair et sur
celle des couches superficielles de la terre, 897.

Dugast.—Commotion sous-marine ressentie prés de Sumatra par
Péquipage du navire Eucharis et Paul, 200.

Rossignol-Dupare.—Sur diverses questions de physique du globe et
de physique des étres organisés, 203.

P. Cappelletii—Une lettre signale une erreur commise par le capi-
taine Layrle relativement 4 la date du tremblement de terre, qui,
en 1861, a détruit la ville de Mendoza, 675.

Ch, Sainte-Claire Deville, Le Blanc et Fouqué.—Les émanations 4
-gaz combustibles qui se sont échappées des fissures de la lave de
1794, a Torre del Greco, lors de la derniére éruption du Vésuve, 75.

Rambosson.—Un tableau figuré montrant différents ages du volcan
de Vile de la Réunion, 791.

yi » , rome ly. . Nos, 5-23.

Parthenon. Vol.ii. Nos. 49-55. April and May 1863.
Notices of Meetings of Scientific Societies, &c.
A. C. Ramsay’s ‘Address to the Geological Society of London,’
noticed, 418.
Earthquake-phenomena, 442.
Fossil Bones of the Flint-folk, 465.
Monographs of the Paleeontographical Society, noticed, 538,
T. Davidson’s ‘ Brachiopoda of Nova Scotia,’ noticed, 538.

Philadelphia, Journal of the Academy of Natural Sciences of. New
Series. Vol. v. Parts 2&3. 1862.

W. M. Gabb and G. H. Horn.—Fossil Polyzoa of the Secondary and
Tertiary Formations of North America, 111 (8 plates).

, Proceedings of the Academy of Natural Sciences of. 1862,

Nos. 7-12. July-December.
A. Winchell.—Fossils from the Marshall and Huron Groups of Michi
gan, 405. |
T. A. Conrad.—Miocene Shells of the Atlantic Slope, 559,
—. New Recent and Miocene Shells, 583,
VOL, XIX.—PART I, 20

538 DONATIONS,

Philadelphia, Proceedings of the Academy of Natural Sciences of.
1863. Nos. 1 & 2. January—March.

A. Winchell.—Fossils from the Yellow Sandstone beneath the “ Bur-
lington Limestone” at Burlington, Lowa, 2.

Transactions of the American Philosophical Society. New
Series. Vol. xii, Part 3. 1863.

Photographic Journal, Nos, 182-134, April-June 1863,

Presburg, Correspondenzblatt des Vereins fiir Naturkunde zu. Erster
Jahrgang. September—December 1862.

G. A. Kornhuber.—Ueber ein gefiedertes Fossil aus dem lithogra-
phischen Kalke von Solenhofen, 97.

E, Mack.—Geologisches aus dem Banat, 17.

Ueber das Vorkommen der sogenannten Marmaroscher Dia-
manten und des Steinsalzes in Marmarosch, 26.

A. Thieriot.—Ueber das Vorkommen und die Gewinnung des Stein-
salzes in Wieliczka, 75.

D. v. Mednyansky.— Ueber Gleichenberg, 113.

Miscellaneous, 30, 63, 92, 125,

Quarterly Journal of the Chemical Society. 2nd Series, Vol. i.
No. 4. April 1863.
F, A. Abel.—Composition of some varieties of Native Copper, 89.

Quarterly Journal of Microscopical Science. New Series. No. 10.
April 1863.
Reader. Nos. 14-26. April 4 to June 27, 1863.

Notices of Meetings of Scientific Societies, &c.
Brydie’s ‘Tableau from Geology,’ noticed, 528,
Ansted’s ‘Great Stone Book,’ noticed, 546.
Jaw-bone of Abbeville, 580.

Royal Asiatic Society of Great Britain and Ireland. Journal.
Vol, xx. Part 2.

Royal Dublin Society. Journal. No. 29. April 1863,
R. H. Scott.—Mineral-localities of Donegal, 114.

Royal Geographical Society. Proceedings. Vol. vii. No. 2. 1863.
H. Rink.—Discharge of water from Glaciers in Greenland, 76,

Royal Horticultural Society. Proceedings. Vol. iii. No. 6. June
1863. ;

Royal Institution of Great Britain. Proceedings. Vol. iv. Part 1.
No. 37.

J. Lubbock.—Ancient Lake-habitations of Switzerland, 29,
Royal Society. Proceedings, Vol. xii. No. 55.

Society for the Suppression of Mendicity. Forty-fifth Report.
1863,

DONATIONS, 539

Society of Arts. Journal. Vol. xi. Nos. 541-553. April 3rd to
June 26th, 1863, ice

Notices of Meetings of Scientific Societies, &c,
D. T, Ansted.—Combustible Minerals, 408.

Vienna, General-Register der ersten zehn Bande des J ahrbnehes
der k.-k. geologischen Reichsanstalt, yon A. F, Graf Marschall
- von. Burgholzhausen.

Jahrbuch der k.-k. geol. Reichsanstalt. Vol. xii. No. 4.
September—December 1862.

VY. Lipold.—Das Steinkohlengebiet im nordwestlichen Theile des
Prager Kreises in Bohmen, 431 (4 plates).

F, Stoliczka.—Die geologischen Verhaltnisse der Karlstadter k.-k.
Militargrenze, 526.

A. Pichler.—Zur Geognosie Tirols, 531,

Vol. xiii, No.1. January-March 1863.

F’, Stoliczka,—Uebersichtsaufnahme des siidwestlichsten Theiles von
Ungarn, 1.

E. Suess.—Ueber die einstige Verbindung Nord-Afrika’s mit Sud-
Europa, 26.

F, Karrer.—Ueber die Lagerung der Tertiirschichten am Rande des
Wiener Beckens bei Médling, 30.

D. Stur.—Geologische Uebersichtsaufnahme des siidwestlichen Sie-
benbiirgen, 33.

G.vom Rath.—Die Lagorai-Kette und das Cima d’Asta-Gebirge, 121, .

J. ee ce potage zum Studium des Beckens von Eperies,

G. Schupansky.—Ueber einige Stérungen durch eruptive Gesteine
“ — Lagerung der Steinkohlenflotze bei Rakonitz in Bohmen,

SSS
e

W. Haidinger.—Zur Erinnerung an Franz Zippe, 143.
Verhandlungen der k.-k. geol. Reichsanstalt 1863, 1.

Warwick. Proceedings of the Warwickshire Naturalists’ Field-club.
1862,

P. B, Brodie.—Succession of life on the Earth, 2.
——. Geology of the neighbourhood of Leckhampton Hill, 9,
Geology of Cleeve Hill, 10.

Zoological Society of London. Proceedings. 1863. Parts 1 & 2.
——. Transactions. Vol.iv. Part 7. Sectionii, 1862,
—. ——. Vol.v. Parts1&2, 1862 & 1863.

540 DONATIONS.

iT; PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 3rd Series. Vol. xi.
Nos. 65 & 66. May and June 1863.

F. V. Hayden’s ‘ Geology and Natural History of the Upper Missouri,’

noticed, 371.
E. Suess.—Former connexion of North Africa with South Europe,
429,

T. L. Phipson’s ‘ Phosphorescence,’ noticed, 456.

Leonhard und Geinitz’s Neues Jahrbuch fur Mineralogie u. s. w.
Jahrgang 1863. Zweites Heft.
H. Tasche.—Ueber die geologischen Aufnahmen Schwedens, 129.
K. Zittel.—Beitriige zur Palaontologie von Neuseeland, 146.
F. von Hochstetter.—Bemerkungen hiezu tiber die Flora von Neu-

seeland, 160.

U. Schlénbach.—Die Schichtenfolge des unteren und mittleren Lias
in Norddeutschland, 162.

K. Rothe.—Ueber einige krystallinische Gesteine, welche im Ries

vorkommen, 169.
—. Chemische Analysen einiger Trasse aus der Umgebung des

Rieses, 177.
Letters; Notices of Books, Minerals, Geology, and Fossils.

LInstitut. I Section. 31° Année. Nos. 1525-1533.
—. 2°Section. 28° Année. Nos. 327 & 328.

Natural History Review. No. 10.. April 1863.
C. Lyell’s ‘ Antiquity of Man,’ noticed, 211.
T. Rupert Jones.—Fossil Estherie, 262.
Paleontographica, herausgegeben von Dr. Wilh. Dunker. Vol. ix.
Lief. 4. February 1863.
F, Roemer.—Neue Asteriden und Crinoiden aus devonischen Dach-
schiefer von Bundenbach bei Birkenfeld, 148 (7 plates).

, herausgegeben von H. von Meyer. Vol. x. Lief. 6. April
863.

H. A. Hagen.—Neuroptern aus der Braunkohle von Rott im Sieben-
gebirge, 247 (pls. 43-45).

R. Ludwig.—Zur Palaontologie des Ural’s: Pflanzen aus dem Roth-
liegenden im Gouvernement Perm, 270 (pl. 46).

——. Meer-Conchylien aus der productiven Steinkohlen-Formation
an der Ruhr, 276 (pls. 47-49).

H. von Meyer.—Heliarchon furcillatus, ein Batrachier aus der Braun-
kohle von Rott im Siebengebirge, 292 (pl. 50. figs. 1-4).

Sphyrena Tyrolensis aus dem Tertiar-Gebilde von Haring in
Tyrol, 305 (pl. 50. figs. 7-11).

O. Bottger.—Clausilien aus dem tertiaren Landschnecken-Kalk von
Hochheim, 309 (pl. 51).

DONATIONS, 541

III. GEOLOGICAL AND MISCELLANEOUS BOOKS. —
Names of Donors in Italies.

Annales Hydrographiques, recueil d’avis, instructions, documents, et
mémoires relatifs 4 Phydrographie et 4 lanavigation. 4° trimestre
de 1862. 1862.

,»——.- 1* trimestre de 1863. 1863. From the Dépét de la
Marie.

Anon. Unity of System. Part ii.

Ansted, D. T. The Correlation of the Natural History Sciences.
The “ Rede Lecture,” delivered in the Senate-house before the
University of Cambridge, on Tuesday, May 12th, 1863. 1863.

——. The Great Stone Book of Nature. 1863.

Austin, C. E. Geological Notes on the Locality in Siberia where
Fossil Fish and Estheriw have been found. With a Note on
Estheria Middendorfi; by Prof. T. Rupert Jones, F.G.S. From
Prof. T. R. Jones, F.GS.

Bayfield, H. W. Pilote du Golfe et du Fleuve Saint-Laurent. 1°°
partie: Golfe Saint-Laurent. Traduction par A. le Gras. 1863.
From the Dépét de la Marine.

Beke, C. T. Who discovered the sources of the Nile? A letter to
Sir R. I. Murchison, K.C.B., &c., President of the Royal Geogra-
phical Society ; with an appendix containing a letter to the Right
Hon. the Lord Ashburton, when President of the Society. 1863.

Canada. Geological Survey of Canada. 1. Parallelism of the Quebec
Group. Description of a new species of Harpes. On the Spiral
Coils of Cyrtina, with description of a New Species ; by E. Billings.
2. Description of a new Trilobite from the Quebec Group; by T.
Devine. 3. On the remains of the Fossil Elephant found in
Canada; by E. Billings. 1863. From E. Billings, Esq., F.GS.

Carter, H. J. On Contributions to the Geology of Western India,
including Sind and Beloochistan. 1863.

Catalogue. Bibliothéque de M. le Baron de Stassart léguée 4 l’Aca-
démie Royale de Belgique. 1863. From the Royal Academy of
Belgium.

Catalogue of the Natural and Industrial Products of New South
Wales; with a Map and Introductory Account of its population,
commerce, and general resources. International Exhibition of
1862. From Sw Daniel Cooper, Fe. Fe.

Cooper, D, Australian Coal. 1862.

Dana, J. D. On the existence of a Mohawk-valley Glacier in the
Glacial epoch. 1863.

542 DONATIONS.

Delesse, A. Matériaux de Construction. Exposition Universelle de
1862. 1863,

Deshayes, G. P. Description des Animaux sans Vertébres découverts
dans le bassin de Paris, pour servir de supplément 4 la description
des coquilles fossiles des environs‘de Paris, comprenant une revue
générale de toutes les espéces actuellement connues, xxxl—xxxiv°
livraisons (11°-14° du tome 1.), 1863.

Deslongchamps, E. Eude-. Etudes critiques sur des Brachiopodes
nouveaux ou peu connus. 1 et 2° fascicules. 1862,

——. Notes pour servir a la Géologie du Calvados. 1863.

Desnoyers, M. J. Note sur les Indices matériels de la Coexistence
de ’homme avec l’Elephas meridionalis dans un terrain des envi-
rons de Chartres, plus ancien que les terrains de transport quater-
naires des vallées de la Somme et de la Seine. 1863.

Dupont, E. Sur le Calcaire Carbonifére de la Belgique et du Hai-
naut Francais. 1863.

Garrigoir, F. Etude Chimique et Médicale des eaux sulfureuses
@Ax (Ariége). 1862,

L’Homme Fossile, historique général de la question et dis-
cussion de la découverte d’Abbeville. 1863.

—. Mémoire sur les cavernes de Lherm et de Bouichéta (Ariége).
1863,

Gemitz, H. B. Dyas oder die Zechsteinformation und das Rothlie-
gende. Heft 1. Die animalischen Ueberreste der Dyas. 1861.

- Guiteras, H. Guia de la Cueva de Bellamar. (A guide to the cave
of Beilamar). 1863.

Haliburton, R. G. New Materials for the History of Man, derived
from a comparison of the customs and superstitions of nations.
1863.

Hartley, C. A. Description of the Delta of the Danube, and of the
works, recently executed, at the Sulina mouth. 1862,

Hébert, EH. Du terrain jurassique de la Provence; sa division en
étages ; son indépendance des calcaires dolomitiques associés aux
gypses. 1861.

———. Gisement des couches marines de Sinceny (Aisne). 1860.

Mémoire sur les formations d’eau douce du bassin de Paris
et en particulier sur les calcaires lacustres a Lophiodon de Provins
et leur extension dans la Beauce. (Résumé.) 1862.

Observations sur les rivages de la mer jurassique a l’époque
de la grande oolite dans les bassins méditerranéen, jurassique et-
parisien. 1861,

DONATIONS. 543

Hébert, H. Observations sur les systémes bruxellien et lackénien de
Dumont, et sur leur position dans la série parisienne, faites 4 l’oc-
casion du mémoire de M. Le Hon. 1862.

——. Observations sur l’existence de !Homme pendant la période
quaternaire. 1863.

Sur l’argile a silex, les sables marins tertiaires et les calcaires
d’eau douce du nord-ouest de la France. 1862,

Sur le non-synchronisme des étages campanien et dordonien
de M. Coquand avec la craie de Meudon (1) et celle de Maestricht,
Réponse 4 M. Coquand. 1862,

Herschel, J. Sur les nébuleuses; sur l’hygrométrie; sur les varia-
tions périodiques de l’atmosphére, &c. Extrait d’une lettre a M.
Quetelet. 1863. From the Royal Academy of Belgium.

Holmberg, H. J. Forteckning och Afbildningar af Finska Forn-
lemningar. I. Stenaldern. II. Bronsaldern. 1863.

Holmes. The Magneto-electric light, as applicable to Lighthouses,
1863.

Jaubert. Notice sur la vie et les travaux de M. Cordier. 1862.
Jones, T. R. On Fossil Lstherie and their distribution. 1863. _
On the Fossil Hstherie. 1863.

Keene, W. Coal and Collieries of New South Wales. 1862. From
Sir Daniel Cooper.

Kerhallet, P.de. Manuel de la Navigation dans la Mer des Antilles
et dans le Golfe du Mexique. Deuxiéme partie. Deuxiéme
édition. 1863. From the Dépét de la Marine.

Lea, I. Description of a New Genus (Goniobasis) of the Family
Melanide, and eighty-two new species. 1862.

———-. Description of a new genus (7rypanastoma) of the family
Melanide, and of forty-five new species. 1862,

——. Descriptions of eleven new species of Melanide from the
United States. 1862.

. Descriptions of ten new species of Unionidae of the United
States. 1862.

Descriptions of two new species of Exotic Uniones, and one
Monocondylea. 1862.

Observations on the genus Unio, together with descriptions
of new species, their soft parts, and embryonic forms, in the family
Unionide ; and descriptions of new genera and species of the
Melande, Vol. ix. 1868,

544 DONATIONS.

Lecoq, H. Sur la Géologie du plateau central de la France et sur
la carte géologique du département du Puy-de-Déme. 1863.

Logan, W. EH. Letter addressed to Mr. Joachim Barrande on the
Rocks of the Quebec Group at Point Levis. 1863.

Lyell, C. Appendix to the ‘ Antiquity of Man.’ 1863.

Montagna, C. Sulle anomalie geognostiche e paleontologiche delle
formazioni apenniniche delle provincie meridionali. 1863.

Norie. Guide du Marin et du Caboteur sur les cétes est de la mer
du Nord depuis le cap Grisnez jusqu’au nord du Danemark sur
les cdtes de la mer Baltique, sur les cétes ouest de Norvége et sur
celles de la mer Blanche. Traduit de louvrage anglais par M. P.
Guery. 1863. From the Dépét de la Marine.

Parker, W. K., and T. R. Jones. On the Nomenclature of the Fora-
minifera. Part vil. Textularia. 1868.

Pattison, S. R. “The Antiquity of Man.” An Examination of Sir
Charles Lyell’s recent work. 1863.

Puggaard, C. Description géologique de la péninsule de Sorrento dans
le royaume de Naples, contenant de nouvelles observations sur les
Dolomies. 1858. From Su C. Lyell, V.P.GS.

Deux Vues géologiques pour servir la description géologique
du Danemark. To geologiske billeder af Stevns Klint og Moens
Klint. 1863. From Sir C. Lyell, V.P.GS.

. Mémoire sur les caleaires plutonisés des Alpes Apuennes et
du Monte Pisano. 1860. From Sir C. Lyell, V.P.GS.

Rames, J. B., F. Garrigou, et H. Fithol. L’Homme Fossile des Ca-
vernes de Lombrive et de Lherm (Ariége), avec une introduction
historique et critique. 1862.

Ramsay, A. C. The Physical Geology and Geography of Great
Britain ; a course of six lectures delivered to working men in the
Museum of Practical Geology. 1863.

Reeve, ZL. Conchologia Iconica. Monographs of the Genera Palu-
dina, Adamsvella, Chondropoma, Anatina, Turgonia, Chamostrea,
and Pterocyclas. 1863.

Routier de la céte sud et sud-est d’Afrique. De Vile Robben &
Natal. 1863. From the Dépét de la Marine.

Volborth, A.v. Ueber die mit glatten Rumpfgliedern versehenen
russischen Trilobiten, nebst einem Anhange iiber die Bewegungs-
organe und tiber das Herz derselben. 1863.

Whitney, J. D. Notice of the progress of the Geological Survey of
California up to May 1863, 1863.

THE

QUARTERLY JOURNAL

GEOLOGICAL SOCIETY OF LONDON.

EDITED BY

THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.

VOLUME THE NINETEENTH.

1863.

PART II. MISCELLANEOUS.

2

Aya Bed

‘4

“

fs a RO Ai i) ot] py 40 Hinde

ie fhe we o
Fi

a

y, ai ,
/ yep rs
2 pw Pehl! ht A Helin

a re

; (tee “ y) aca
Sn ae gr a iu ” See
TARRY AY nies wee: aM aoe
v4 GS ue
ee ‘ H ce ey
aL vey Ae hye

CONTENTS OF PART IL.

Alphabetically arranged—the Names of the Authors in capital letters.

Alps; G. DE MorriLuet on the Strata of the Italian and French
Peer UO e it sobs meals ere ce os tes page recs Pelee eee oy
Austria, KNER on the Fossil Fishes of... ....5....000ceeseeeeees

Coal-formation between Prague and Pilsen, R. Lupwie on the ....
Coal-pits of S. Pedro da Cova, Oporto, C. Rrprrmo on the........
Coexistence of Man with Elephas meridionalis, DESNOYERS on the. ,
Comparison of the Strata of the Italian and French Slopes of the

Pipe Gt DE MoRtrnner Ona UT. POT oe 6 ed Sls eee eet we
Cretaceous Strata of Konigeratz and Chrudim (S8.E. Bohemia), C.

eee ATs OMTNG vn s 2. SN ene ct y es, Verma eaten dete wakes

Dalmatia, Fr. von Havunr, STACHE, and Z1ITTEL on the Geology of. .
DersnoyvErs, J. Upon the Material Indications of the Coexistence
of Man with Elephas meridionalis in Beds, near Chartres, more
ancient than the Quaternary Gravels of the Valleys of the Somme
PUES IOUS + fas av ¥ae sfx '0 ca ae sO nied ON Jule bl eee ate el deed bes

Elephas meridionalis, DESNOYERS on the Coexistence of Man with ..
Hocene Fossils from Istria, STACHE ON 2... . eeu c cece cee ccenes
Europe, A. SzaB6 on the Pleistocene and Recent Phenomena in the

PARC —OBNt OP VV bean ea os AIR A PET Pe ee ca eh

#ossil Fishes of Austria, Kw, on the. .......00 000d eee cians
Fossils from Guadaloupe, PAYEN on some ........... eee ee ee eee

Peomey of Cyprus, UNGER Of the onc vis ody sin eg 0 og ole a ridlee wien the
of Dalmatia, Fr. von HAUER, STACHE, and ZiTTEL on the ..
Guadaloupe, PAYEN on some Fossils from .............eeceseees

HaveEr, Fr. von. On the Neogene Plastic Clay (Tegel) of Olmiitz,

LL le pera Ree ag air eR bac Coe Red © Sagas 07 ee CI er
, STACHE, and ZiTTEL. On the Geology of Dalmatia ........
Hungary, Peters on the Lias of Fiinfkirchen .................:
, ZITTEL on the Upper Nummulitic Strata of.............04.

Ssinia, STACHE on Mocens Mocsile-from ... creer es cee docenuns

Japan and the Philippines, F. von RicHTHOFEN on the occurrence of
fue Nonmliuliine NOrmawen in” 2.76... ee ae eee

lV

Kner, On the Fossil Fishes of Austria... 0.0555. 5200.0505-.55es
Koniggratz and Chrudim (8.E. Bohemia), C. H. M. Paun on the

Cretaceais Straten geiae cit. os sie's.- ois cc els eer epitome eee eee 22
Lias of Fiinfkirchen, Hungary, PETERS on the .............+005. 16
Lupwie, R. On the Coal-formation between Prague and Pilsen .. 25
Mammalian Remains, E. SuEss on some recently discovered ...... 51
Moravia, Fr. von Haver on the Neogene Plastic Clay (Tegel) of

ON RAN een eee CRE ee DE et ie ENT nee 15
MortinteT, G. bE. A Comparison of the Strata of the Italian and

French Slopes-of the-Alpe vate st cen one sere ta a gree 23
Neogene Plastic Clay (Tegel) of Olmiitz, Moravia, Fr. von HAvER

Ol) Che 4°F5 biechs gating? cds Sage ceeadee, meen dee edie ee beset aye ee sore
New Zealand, ZirTE on the Paleontology of ............s.000. 20
Nummulitic Formation in Japan and the Philippines, F. von Ricut-

HOFEN on the occurrence of the 24... oaw ts cease ws tesa ee eee 32
Oporto, C. RrBEerro on the Coal-pits of 8. Pedro da Cova ........ 9
Paleontology of New Zealand, ZITTEL on the ............seeee. 20
Paut, C. H. M. .On the Cretaceous Strata of the Circles of Konig-

oratz and, Chrudim (5.1. Bohemia )p,. ye sctecisnjele sSceotehh toe sie meee 22
PayEN. On some Fossils from Guadaloupe ..........66. dae 30
Peters. . On the Lias of Fiinflirchen, Hungary ................ 16
Pleistocene and Recent Phenomena in the South-east of Europe,

J. SZABO, On the. 34 vc we wives Tiere byes oe lcevews OE eee Qe cee 1

Prague and Pilsen, R. Lupwie on the Coal-formation between.... 25

RrBerro, C. On the Coal-pits of S. Pedro da Cova, in the Concelho

de.Gondomar,. District, of Oporto... cos. fac 0:5 15 on eee 9
RIcHTHOFEN, F. von. On the Occurrence of the Nummulitic For-

mation in Japan andthe Philippines .0: sesarc) uo senn's eee ca 52
Rocks and Minerals, ZrrKEt on the Intimate Structure of ........ 21
Sracue. . On Eocene Fossils, from Istria, 1.5 .5.i119 50s iene 51
——, Fr. von Haver, and Zirret. On the Geology of Dalmatia . 30
Susss, E. On some recently discovered Mammalian Remains .... 31
SzaBo, J. On the Pleistocene and Recent Phenomena in the South-

east Of MUrope oi .ates dante os oe cued aly nepra cl ailaus fe eons Cie ee i!
UncEr. On the Geology of Cyprus .........0ecesaeseceeauees 21
ZiRKEL. Intimate Structure of Rocks and Minerals ..........+5 21
ZITTEL. On the Paleontology of New Zealand ...........0.0%8 20
——. On the Upper Nummulitic Strata of Hungary ...........6. 8

——, Fr. von Haver, and Sracue. On the Geology of Dalmatia.. 30

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the PiztstoceNr and Recent Puenomena in the SourH-xast of
Evrorzt. By Dr. Josepx §zano.
[Egy continentalis emelkedés és siilyedésrél Eurépa délkeleti részén. Szabé Jézsef,
&e. Magyar Tudom. Akad. Evkonyvei, Tizedik Kotet, 6 Darab.]

Introduction.—In this paper the author endeavours to show that in
the South-east of Europe, and especially on the northern and western
parts of the basin of the Black Sea, the elevation and submergence
of that part of the continent, and the subsequently modified action of
the denuding agents, were forces competent to effect the changes
which distinguish the present geological conditions from those imme-
diately preceding, and, especially, to produce the present physical
configuration of the surface of the diluvial and alluvial deposits.

Recent Geological Phenomena.—His researches were first based on
the present conditions of the river-system of the area now drained
by the middle and lower portions of the Danube; and he afterwards
considered in succession the physical history of geological periods of
a gradually increasing age, until finally a period was reached when
the geological phenomena were essentially different from the present.

By the first series of observations which he recounts, it is proved
that the beds of the great majority of the existing rivers have been
excavated out of pleistocene deposits, and that, more especially in
Hungary, the Danube and all its tributaries, as well as the Russian
rivers which empty themselves into the Euxine, have very deeply
excavated the diluvial strata; while the Theiss and its confluents flow
between lower banks, and have not cut so deeply into the mass of
the pleistocene formation.

The author then brings forward data to show that the present
areas of inundation are surrounded by older ones, which are in all
respects similar, but lie higher and are more extensive; they are,
therefore, indications of a former period when the beds of the rivers
were not so deeply excavated as they are now—that is, when the
water flowed nearer to the level of the surface of the adjacent plains,

VOL, XIX.— PART. II. B

2 GEOLOGICAL MEMOIRS.

and consequently flooded a larger area. The deposits of the older
inundational areas are of alluvial origin, as also are those now being
. formed ; therefore, in determining the limits between the pleistocene
and modern formations, the outlines of the former may prove to the
geologist a valuable guide.

He also describes old, and now abandoned, river-beds; the best
opportunity of examining which is afforded in the tract of land in
Hungary between the Theiss and the mountainous western boundary
of Transylvania. Similar ancient river-beds are to be found along
the Danube, and especially on the plains of Moldavia, where they
appear as valleys of erosion having connexion with that river; and
they also occur along the Pruth and Sereth. All these channel-like
depressions are now dry, or if they are sometimes conveying water,
yet it is in a quantity quite inadequate to the dimensions of the
excavation, which are greater than those of the beds of the adja-
cent rivers; and being as regards the direction identical with the
latter, they must be regarded as constituent parts of the present
river-system: and they may also be considered as relies of a period
subsequent to that in which the existing mountains and valleys were
formed, but when the water flowed at a higher level, that is, nearer
to the surface of the plains, and was also conveyed in a greater
number of channels than it is now. The beds of the present rivers
were developed from these in such a manner that, as the water sank
gradually in a deeper basin, its fall became greater, its eurrent more
rapid, and therefore it was enabled to cut out deeper beds. It
selected, out of the many shallow channels, those few which offered
the least resistance to the excavating power. The ancient river-
beds on the left bank of the Theiss are as curvilinear as the modern
ones ; while those on the Moldo-Wallachian plains are as straight
as the present rivers of that district. This coincidence may be
regarded as indicating that the collateral circumstances are the same
now as they were during those periods when the ancient river-beds
were in full request.

Dr. Szabo then refers to the chief points of interest in individual
localities, not only in the course of the Danube, but in its basin
further inland, where, on heights that are now quite unattainable
by floods, incontestable traces of alluvial deposits are found super-
imposed upon the Loess. The most remarkable of such places are
Zimony (Semlin) and Csernayoda. On the former, situated opposite
Belgrade, the loose deposits forming the precipitous sides of the
Danube consist, for the most part, of diluvial strata; in the lower
portion of which bones of Elephas, Rhinoceros, Bos, &c., are met
with. The upper portion is the true Loess, and it is covered with
newer strata consisting partly of sand of about 15 ft. in thickness
and containing pleistocene fossils, partly of clayey materials, from
5-9 ft. thick, with fragments of earthenware, bones of Bos and
Cervus, charcoal, flint worked by man, and, in some places, fresh-
water shells such as Unio pictorum and U. Batavus. The whole for-
mation becomes thinner inland, and thicker towards the Danube,
where it also becomes abruptly cut off.

SZABO.—SOUTH-EAST OF EUROPE. 3

Beyond an enormous tract of marshy land which lies upon the left
bank of the Danube, and upon the opposite side of that river, but
many miles off, precipitous walls of Loess are again met with of
the same character as before, the connecting portions having occupied
the place where the Danube now flows. At Csernavoda*, the valley
through which the railway passes was formed by erosion; and the
surface-configuration of its side suggests that it must once have been
filled with water, and that this was the water of the Danube itself,
towards which the valley opens. ‘This conjecture is rendered almost
certain by the examination of the bottom, which is covered by an
immense quantity of shells, all belonging to species now living in
the Danube and on its banks (Tvchogonia Chemnitzii, Fér., Mela-
nopsis acicularis, Fér., Neritina Danubialis, Ziegl., Paludina achatina,
Brug., Melanopsis Esperi, Fér., &c.).

Besides this, there is another place in the same valley which con-
tains some of these Mollusca, and also remains of human art of a
more recent age, at a height of about 100 ft. above the level of the
Danube. These human remains consist of fragments of urns, roof-
tiles, bones of domestic animals, and, what is more significant than
all, a piece of laminated metal which proved to be lead.

The systems of plains forming the steppes or the large valleys are
then treated of; and in concluding this portion of his subject the
author describes the present shores of the Black Sea, to which the
pleistocene deposits are continued, stating that the Loess forms
the shore on the Kilia arm, where it constitutes cliffs of from 42 to
50 feet above the sea-level, but that towards Odessa the cliffs rise
gradually to a height of more than 200 feet, of which the upper
portion is typical Loess, while the lower consists of the well-known
Neogene limestone.

On the St. George arm, portions of the secondary rocks of the
Dobrudscha Mountains are visible as far as the banks of the Danube;
but in places a mass of Loess, forming a range of hills, occurs; and
at Kustendje the cliffs are composed in some places entirely of Loess,
in others partly of it and partly. of older formations. The latter
rocks gradually crop out towards the Balkan range, and in the same
ratio the Loess thins out; so that at the Cape of Kalakvi (Gulgrud),
near Varna, the tertiary limestone forms the surface and the entire
cliff; this limestone is probably the Leithakalk of the Vienna
geologists. It may be therefore inferred that the Loess forming the
sea-shore obeys, in thinning out, the same law as that of the plains:
in other words, it thins out only towards the mountains, and above
a certain level large masses of it are never found; but towards the
Black Sea it does not thin out at all. The interruption of it on the
shore must have been, of course, posterior to the time of its formation,
Commencing from Odessa, and proceeding as far as the mouth of the
Danube, and again from here to Kustendje and the Bay of Varna,
the Loess is never found covered by a marine deposit.

From the above observations the author infers that the water

-* Thé Danube station of the Danube and Black Sea Railway.
B2

J GEOLOGICAL MEMOIRS.

formerly flowed in the Hungarian rivers at a level of from 10 to
30 feet higher than it does now, viz., when their floods were able
to rise to the height of the old inundational areas and to occupy the
ancient river-beds.

Again, the beds of the rivers must have been from 30 to 70 feet
higher than they are now, when land now lying at that height above
the present level of the Danube was covered with its water, and in
which, for instance, the alluvium of Csernayoda was deposited.

Also the land must have been raised from 100 to 130 feet since
the deposition of the old alluvial deposits at Zimony (Semlin), Gomba,
Kis-Terenne, &e.

And, lastly, there has been an upheaval of the district under
consideration to the extent of from 130 to 200 feet since the terrace-
system was formed; these terraces, however, are not the result of
the action of rivers, but of that of a vast expanse of water, which
covered the whole area of the diluvial deposits.

Pleistocene Period.—Towards the margin of the Hungarian basin
the Pleistocene (diluvial) deposits consist of gravel overlain by sand.
In the central portion of the great basin bordering the course of the
Theiss, the lower beds are formed of a bluish mud and sand, but the
upper portion consists of Loess. Frequently, however, the latter
lays immediately upon the older formations. Besides this, a calcareous
tufa occurs under interesting circumstances, though not over any
considerable area. The average thickness of the diluvial deposits
may be estimated at 200 feet; they are overlain by alluvium, and
repose upon the highest pliocene deposit, and especially the Congeria-
beds.

The gravel is characterized by boulders of trachyte, basalt, and
the opaline minerals pertaining to the rhyolite-group. By the
decomposition of some felspathic minerals the natural soda of
Hungary and a calcareous tufa are formed, either immediately upon
the surface or under a thin cover of soil. At a very typical spot,
between Szeged and Dorozsma, where a great quantity of soda is
obtained, and at a depth of 3 to 4 feet in the Soda-lake, the author
found grains of the size of a pea, and all of the same external ap-
pearance. The analysis proved them to be labradorite; and, in
ascending towards the surface of the lake-bed, they are found to be
more and more decomposed. The origin of this volcanic ejection
must be attributed to a volcano which was discovered by the author
some years ago in the basin of the Theiss, north of the Matra
Mountains, near Ajnacsko.

The Loess occurs not only in Hungary, covering the greatest part
of the central plains and the adjacent valleys, but it is also found
greatly developed in the Danubian Principalities, and on the shores
of the Black Sea, as far as Odessa ; further the author has not carried
on his investigations, but there is every reason to believe that it
covers a great part of the northern Pontic plain. Southward from the
mouth of the Danube it forms the upper stratum towards the Balkan
Mountains. In some localities, cliffs of from 80 to 100 feet appear
quite homogeneous, but in most instances distinct lines of stratifi-

SZABO.—SOUTH-EAST OF EUROPE. 5

cation may be followed uninterruptedly for several miles. The
Nummulites at one locality, not far from Gran, form a layer nearly
1 foot thick; at another place the true Loess-shells are mixed with
Melanopsis, Cerithium, and other fossils of the Congeria-beds. The
Loess strata are nearly horizontal.

According to the evidence of the organic remains, the Loess may
be divided into two portions. The great Mammalia occur in the
lower, while the Loess-shells are only exceptionally found in that
portion. The upper division abounds with Loess-shells, but the
remains of Pachydermata are absent, and even the Cervus, Bos, and
Equus are only occasionally found. This distinction refers only to
districts where the formation is well developed, the thickness being
not less than 100 feet; but in other cases, both portions sometimes
appear to be confusedly brought together.

The Surface in the Pleistocene Period.—As regards the deep channels
of the rivers, it is quite certain that where the banks are more or less.
vertical, and the beds on each side correspond, the place occupied
now by the river was originally filled up by a continuation of the
same strata which now constitute the banks, and that the uninter-
rupted plain thus formed was furrowed posteriorly. The restoration
must be effected on a much greater scale where two or more great
rivers joined. An example of this kind occurs at the southern end
of the boundary-line between the Danube and the Theiss, where, in
the midst of an extensive area formed by alluvium (of both ages), a
small egg-shaped plateau, consisting of typical Loess, and having
vertically broken cliff-like walls, remains like a column of earth to
mark the extent of former denudation.

Having thus restored to one continued plain the Pleistocene
deposits in Hungary and in the Danubian Principalities, the author
proceeds to consider the similar phenomena in the neighbourhood of
the Black Sea ; and he states that the Loess does not thin out towards
the sea, but, on the contrary, becomes more largely developed, and
that the shore is formed by abruptly broken cliffs.

The method of restoration hitherto pursued by Dr. Szabé reclaims
from the sea a large portion of the areas now occupied by it, and
proves that, at some period after the deposition of the Loess, that
part of the Euxine which is necessary for the restoration of the Loess-
plateau was not covered by water, but was so much elevated that
the Loess-strata now wanting touched each of the corresponding ones
which now form the shore. Now, if we suppose that water has
covered the whole area over which, at the same low level, the Loess
would be found as an uninterrupted mass, we obtain a lake, the
water of which covers, besides the Pontic lowland, probably the
whole Arabio-Caspian depression, as suggested by Pallas, Humboldt,
and all the naturalists who have travelled there.

But such a sea was possible, in the Pleistocene period, only upon
the supposition that the present Black Sea did not then exist as such,
but that its present bottom was elevated to such an extent that the
Loess plateau could exist in its original completeness. A natural
consequence of this condition is, that it was not in connexion with

6 GEOLOGICAL MEMOIRS.

the ocean, but was a constituent part of the great Arabio-Ponto-
Caspian or mediterranean lake. At one place the boundary of its
basin is decidedly known, and has been described by Herr Stur*,
who states that ‘‘ the dividing-line of the pleistocene plateaux is not
only such a one for the Rivers Bug and Dneister, but it is at the
same time part of the great dividing-line between the Black Sea and
the East Sea. South of this limit all the strata are covered by Loess,
while north, on the plain, sand, black soil, and erratic blocks are
spread. The same dividing-line acted as such even previously to
the Pleistocene period.” The lowland of Hungary was a great bay
of a Pleistocene lake, and was connected with it by the “narrows”
(or “ straits”) of the Iron-gate, in the same manner as the Euxine
is, by the Bosphorus, connected with the Sea of Marmora.

The author then enters into the details of the configuration of the
bottom of this lake, of which some remains are to be met with.
Such are certain hills, commonly called tumuli, but of which only a
small number are real tumuli, the greatest number being geological
mementos of the Pleistocene period. He is acquainted with about
130 tumuli erected by man, but with above 600, in Hungary alone,
which have been formed by successive depositions of the same strata
as those which form the lowland of that country. The left bank of
the Theiss may be considered a classical ground for the study of
these remarkable formations. Guided by the geological tumuli, and
the law of their distribution, he points out that the original depres-
sions are remains of the bottom of the Loess-lake, and of the depres-
sions formed subsequently by denudation. This statement refers
especially to one of the bays of the Pontic depression, and perhaps
has a further bearing upon the question of the probable form of the
bottom of the Pleistocene lake.

Three great depressions may be distinguished, which were divided
by two longitudinal elevations. Of those basins the middle (the
Caspian) was the deepest. The water of the lake having been by
some means carried off, the dividing-lines were rendered dry ; and
they act as natural barriers between the basin of the Aral and the
Caspian Seas on the one side, and between the basin of the latter
and that of the Euxine on the other, to the present day. The level
of the Caspian is reported as being, in some places, only 23 feet
above the level of the Black Sea.

Inauguration of the Recent Period.—Having sufficient proof that
the Loess, notwithstanding its local uniformity, is in most cases
stratified, it follows that it was deposited in water, and was not the
result of any form of ice-action; and, the strata being nearly hori-
zontal, the water must have occupied the adjacent depression of
Europe and Asia after the formation of the general configuration of
the territory.

The general outline of the land was formed during the period of
the trachytic and basaltic eruption which also destroyed the Congeria-
sea. The end of this period is marked by great movements of

* Jahrbuch der k. k. geol. Reichsanstalt. Wien, 1860 (On the Pleistocene
Plateaux in Gallicia).

SZABO.—SOUTH-EAST OF EUROPE. 7

upheaval and subsidence ; and consequently the first stratum of the
Pleistocene formation consists of a specifically heavy material, espe-
cially near the mountain-borders ; and the higher we ascend in the
series, the finer do the particles that were carried in appear to be,
and at last the finest detritus, forming the Loess, was deposited.
The Loess-sea was an inland lake, of which the area now occupied by
the Euxine was a constituent part. The author infers that two
branches were then extended from the Caucaso-Crimean chain
towards the west, the principal one connecting the Balkan with it,
while the others stretched towards Fidonisi, the only island in the
Euxine, and continued as far as the Dobrudscha Mountains on the
right bank of the St. George arm of the Danube: the existence of
the former was proved by Capt. Spratt, by sounding the Black Sea.
That geologist found a submarine elevation on the line connecting
the Crimean and the Balkan Mountains. These branches may have
constituted the coast of the Loess-sea.

A considerable difference in the relative position of the whole of
the basin of the Loess-sea, and that part of it which is now occupied
by the Euxine, was caused by the subsidence of the latter. Thus
the Loess-sea and the ocean were brought into communication, the
water of the former was emptied into the latter, while, on the other
hand, that enormous land of steppes was formed of which Ritter, the
great geographer, says, it is, with its negative levels*, of all Asiatic
plains the most continental, being on no side open towards the ocean f.

The author then enters into the changes in the surface-configura-
tion of the sea-bottom of that period, of which some unmistakeable
traces on a large scale are to be met with, especially in Hungary.
He explains the mode of formation of the best soils which occur in
Hungary under similar circumstances, as the black soil in the Danu-
bian Principalities called by the proprietors ‘‘ Tschernosem.”

The best soil is always to be found most largely developed on the
slowly inclined plain of the Pleistocene basin, which at one time
formed the gradually sloping bottom of the Loess-sea ; while towards
the line of greatest depression the particles become more and more
decomposed, both chemically and mechanically, and the fitness of the
soil for the support of a luxurious vegetation decreases, and a
peculiar kind of soil, called in Hungarian “Szek,” is found on the
banks of the Theiss: in this soil spots occur which are quite barren.

The Bed of the Danube occupies the line of a fault.—Commencing
at Vacz, about sixteen miles above Pesth, and proceeding towards the
Black Sea along the sinuous course of the Danube, it may be observed
that the right bank is always the higher. The most striking instances
of this peculiarity are afforded beyond the Iron-gate, near Orsova ;

* The signs + and — being sometimes used to distinguish between areas
above and below the level of the sea, the levels of the latter are consequently
termed “negative.” —Ep. Q. J. G. S.

t De Verneuil, in his “‘ Mémoire Géologique sur la Crimée”’ (Mém. Soc. Géol.
France, 1838), makes a distinction between freshwater, brackish, and marine
deposits, and, though chiefly treating of the older formations, infers that the
change of the freshwater lake into dry land, and the formation of the Euxine,
have both taken place in the most recent, even perhaps in historical times.

8 GEOLOGICAL MEMOIRS.

while above this point, between Bazids and Pesth, interruptions are
often met with. The bed of the Danube may be regarded as a curved
line marking the direction of a fault, the plan of which is somewhat
inclined, and on which a movement of upheaval has taken place on
the right bank, and of subsidence on the left; while the Danube
itself occupies the depression thus caused. This statement is based
upon the fact, that wherever any trace of a formerly higher level of
the present river-system is found, it is always upon the right bank,
without any corresponding elevation on the left. The author refers
here especially to Csernavoda and other localities enumerated on p. 2.
The relation of the History of Man to the Pleistocene Period.—From
the fact that in Pleistocene deposits, as well as in bone-cayerns, in
Hungary and the South of Russia no human remains have hitherto
been found; and as the relics of human industry date also from a
later period, the author infers that during the flint-period, and even
the subsequent stone-period, this part of Europe was not inhabited,
but that it became peopled during the bronze-period, and that its
first inhabitants witnessed the draining of the great freshwater lakes.
From written history we may only infer that since the time of
Trajan no considerable change has taken place respecting the levels
of the two banks of the Danube and its affluents ; but changes that
might have taken place previous to this date would not have been
recorded. Nevertheless, the recollection of the tradition of such an
event as the draining of a great lake going on successively before the
eyes of several generations remained for a long time deeply impressed
upon the minds of the inhabitants of the district, and is not yet
totally effaced—the view still prevailing among the inhabitants of
Hungary being “ that these plains were once covered by a freshwater
sea (mare dulce), the water of which afterwards found its way
through the ‘ narrows’ of the Iron-gate.” [San

On the Upper Noummvtitic Strata of Hungary.
By Dr. Zirret.

[Proceed. Imp. Acad. Vienna, October 9, 1862.]

Accorpineé to the observations of Prof. Peters, these strata rest on
the great wide-spread Nummulitic Limestone. Paleontologically
they are equivalent to the strata of Ronea, forming, with other coéval
beds, a distinct geological horizon, generally known as the Upper
Nummulitic formation, Among 68 species of organic remains
occurring in this formation in Hungary, 19 are new; 23 are met
with at Ronca and in the Vicentin ; 22 in the Calcaire grossier of
Paris; only 4 in Oligocene deposits: and of these last, 3 species
have also been found in decidedly Eocene beds.

Dr. Zittel hence infers that the freshwater and marine deposits
around Gran, including some coal-seams, together with the fossilife-
rous sands near Stuhlweissenburg, belong to the Upper Nummulitic
formation, and are far more nearly allied to the deposits of the
Eocene than to those of the Oligocene periods. [Counr M.]

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the Coat-pits of S. Pepro pa Cova, mm the ConceLHo DE Gonno-
MAR, District of Oporto. By Senhor Carxos Rrserro.

[Die Steinkohlen-Grube von S. Pedro da Cova im Concelho de Gondomar,

’ Distrikt von Porto, von Herrn Carlos Ribeiro. Aus dem Portugiesischen
iibersetzt und bevorwortet von Herrn W. Reiss.* Neues Jahrbuch fir Min.
u. s. w. Jahrgang 1862. Drittes Heft, pp. 257, &c.]

Procrepine from the granite of Oporto beyond 8. Pedro da Cova,
towards the east, the following systems of beds appear succes-
sively :—

1. Gneiss, alternating with mica-schist, extending laterally from
Campanha to the neighbourhood of the Serra de Fanzeres. The strike
is from N. 10°-20° W. to S. 10°-20° E., and the dip is very rapid
towards E. 20° N.

2. Greyish-green, silky-looking slate, and clay-slate of various
colours, having the same inclination as the preceding system.

3. Breccia made up of fragments of the rt a mentioned rocks ; black
clay-slate with impressions ‘of Plants ; sandstone; and coal- beds. All

- these beds strike from N. 20° W. to S. 20° E., and dip EK. 20° N.

4, Quartzite, clay-slate, and unfossiliferous greywacke, overlying
the foregoing systems. "They have a strong inclination towards
E. 20° N., while further eastward they dip W. 20° N., or also E. 20° N.
Upon them, in fact, rests conformably clay-slate with Trilobites and
other fossils of the Lower Silurian formation.

5. Quartzite, greywacke, clay-slate, and metamorphic rocks; they
are all destitute of fossils, and extend from the left bank of the Ribeiro
da Murta over the Serra de Vallongo as far as the granite of Baltar
(which strikes from N. 20° W. to S. 20° E. ), thus taking in a breadth
of from 9 to 10 kilometres.

* On November 29, 1848, the late Mr. D. Sharpe read before the Society a
paper “On the Geology of the Neighbourhood of Oporto, including the Silurian
Coal and Slates of Vallongo” (Quart. Journ. Geol. Soe. vol. v. pp. 142, &e.) ; and
on April 6, 1853, he read a paper ‘‘ On the Carboniferous and Silurian Forma-
tions of the Neighbourhood of Bussaco, in Portugal’? (Quart. Journ. Geol. Soc.
vol. ix. pp. 135, &.), compiled from letters received from Senhor C. Ribeiro in
November 1850 and during some months afterwards ; and in this latter paper
he stated (at p. 142) that Senhor C. Ribeiro’s views of the geological relations of
the Coal of Vallongo then coincided with his own. The memoir of which an
abridgement is now given appeared in the ‘ Neues Jahrbuch,’ as a German trans-
lation of the first part of one published in Portugal by Senhor C. Ribeiro, on the
Coal-bearing beds of Oporto, in 1853, and again republished, with other essays,
under a general title, ““ Memorias sobre as minas de carvao dos districtos do
Porto e Coimbra e de carvao e ferro do districto de Leiria, por Carlos Ribeiro”
(Mem. Acad. Real das Sciencias de Lisboa, vol. i. part 2, 1858), in 1858, from
which it appears that, in 1853; Senhor Ribeiro no longer agreed with Mr. Sharpe 8
views with respect to the age of the Coal in question.

VOL, XIX.—PART II. , Cc

10

GEOLOGICAL MEMOIRS.

The following section shows the order of succession and the strati-
graphical relations of these several systems :—

(15 miles.)

Section from the Mouth of the Douro to Baltar,

Ponte Ferreira.

S
&0
g
=
iC
>

e. Clay-slate.

f, g. Carbonaceous shales and sandstones, containing Coal, and with Trilobites

in the upper part (2).

d. Sandstone.

Micaceous schist,
e. Gmeiss.

SHarpe.—a, Granite and Syenite.
b.

é. 4th System. d. 5th System.)

g, f. drd System.

(4, c, &. Ist and 2nd Systems.

Carboniferous (Huila).

Ff. Devonian.

J.

b, ec, d. Crystalline schists.

é. Silurian.

Riserro.—a. Granite.

This section has been
already given by Mr. D.
Sharpe in his paper “ On
the Geology of the Neigh-
bourhood of Oporto” * ; it
represents the relations
which apparently exist
between the foregoing
systems of rocks and the
coal-beds, the latter ap-
pearing to dip beneath the
former.

Even if the manner in
which the coal-beds here
crop out intimated their
true geological situation in
reference to the rocks of
the fourth system, which
appear to cover them, it
would still remain tobe ex-
plained why the mining-
works that have been car-
ried out in the neighbour-
hood of S. Pedro da Cova,
Covelo, and Povoa have
always been in that zone
in which the valuable beds
are exposed, and why the
attempt has never been
made further east, in
which direction the coal
dips at an angle of about
35° under the coal-shale.
If it had been discovered,
through the first work-
ings, that the coal-beds
continued further beneath
and dipped under the Si-
lurian beds, 1t would have
been attempted to win the
coal again by shafts sunk
to the east of the inter-
mediate zone. As _ this,
however, has not taken
place, there is every rea-
son for doubting this con-

' * Quart. Journ, Geol. Soc.
vol. v. 1849, p. 145.

RIBEIRO—COAL OF S. PEDRO DA COVA. 11

tinuation of the coal-beds in depth, and, therefore, also the geological
position which they here appear to possess.

And, in truth, these coal-beds, so far from belonging to the Lower

Silurian formation, as their stratification might appear to prove, and
as Daniel Sharpe * has assigned them, are much younger, and must
be considered of Devonian or Carboniferous age, as will be shown
hereafter.
* The mica-slate and the gneiss composing the first system are well
displayed beyond the beds of Oporto and 8. Pedro da Cova, without,
however, showing a regular connexion or covering a great area.
Excepting the Serra da Freita for the mica-slate, and the Valley of
Cambra, with the banks of the Caima and the Vouga, for the gneiss,
these crystalline rocks everywhere appear more as the results of
local metamorphism—produced through the alteration of the clay-
slate and tale-slate where those formations were exposed to the in-
fluence of the intrusive granite—than as a definite, uniform, meta-
morphic formation covering a large superficial area.

But the azoic tale-slate and clay-slate, besides the extreme uni-
formity of connexion and development which they exhibit in the
before-mentioned zone, cover large spaces in Portugal, and contri-
bute largely to the peculiar features of many districts in that
country. We must, therefore, consider that stripe which appears
between Oporto and Baltdr as isolated, through its being cut off by a
mass of granite. This is by no means the case with the fossiliferous
beds of the zone in question. Although the fossiliferous beds may be
shown to be clearly independent of the azoic group, both in regard to
their geographical position as well as their distribution and strati-
graphical relations, this cannot yet be done in regard to the relations
which the coal-beds show to that fossiliferous group.

On the contrary, a geographical dependence of the one system upon
the other can be recognized, as has been observed in the neighbour-
hood of Oporto, Bussaco, and at some places in Beira-Baixa.

The author then gives some details respecting the lithology, dip,
and direction of the foregoing beds of the first and second systems,
and of the members of the third system. The latter series he
divides into two groups, distinguished by peculiar mineralogical
characters and fossil Plants, as well as by the different dips of their
individual beds.

A section from west to east, about the neighbourhood of the
Igreja velha de S. Pedro da Cova, through those beds, will show the
following series, in ascending order :—

First group.

1. Greenish and grey, lustrous slate,’dipping from 70° to 80° towards

EK. 20° N. Upon this slate rest the coal-bearing beds.

2. Breccia, formed out of the angular fragments of the argillaceous

slate which forms the basement-bed of this group (1).

3. Blackish and very micaceous clay-slate, alternating with thin

beds of micaceous sandstone, in which appear also small pieces of
felspar.

* Quart. Journ. Geol. Soe. vol. v. 1849, pp. 145-148.
c2

12 GEOLOGICAL MEMOIRS.

4. Coal, having a medium thickness of about 1 métre, and called
a Devesa.

5. Beds of micaceous sandstone, interstratified with clay and grey
psammite, all being carbonaceous. A great number of fossil Plants
and a few veins of carbonate of iron are found in these beds.
ic Coal, about one métre in thickness, and called Camada do Poso

to.

7. Beds of pudding-stone and coarse-grained micaceous sandstone of
a bright-yellow colour, in which occur broken pieces of rock identical
in character with the quartzite and slate of the fifth system. These
beds are called ‘the roof” (telhado) by the miners of the district.

These rocks compose the first group of the coal-bearing series of
beds, and are all inclined about 30° to 35° towards E. 20° N.

The second group, immediately superimposed upon the first, com-
prises the following beds :—

1. Clay-slate, partly blackish grey and partly of a bright ash-grey
passing toa reddish colour, containing some fossil Plants; and beds
of coarse-grained, micaceous sandstone passing into conglomerate ;
they dip from 40° to 50° towards E. 20° N.

2. Black psammite, with large leaves of mica, passing into a fine-
grained, micaceous, and hard schistose sandstone, and containing many
fossil Plants whose forms appear to have been slightly altered through
the contortions of the beds. These strata alternate with beds of black,
bituminous, and very hard pudding-stone; and they all dip approxi-
mately 54° towards EK. 20° N. Inthem occur here and there thin bands
or veins of anthracite, which expand, in places, almost suddenly, to
form nests of as much as 6 métres in diameter, the anthracite being
sometimes soft and dull, and sometimes hard, with a beautifully
lustrous fracture. With these anthracite masses, and in contact with
them, occurs a very black graphitic slate.

3. Pudding-stone, sandstone, and shale, alternating variously with
one another, all very hard and slightly micaceous. This subdivision
consists mostly of thick beds of conglomerate, in which can be dis-
cerned fragments of the quartzite, greywacke, and clay-slate of the
second, fourth, and fifth systems. The beds dip from 60° to 65° to-
wards E. 20° N.

Then follow the Silurian slate and quartzite of the fourth system,
which dip from 60° to 80° towards E. 20° N.

After giving some further details of the third system, the author
proceeds to describe the various rocks in regard to their geographical
distribution and mutual relations, more particularly in regard to the
two groups of the coal-bearing beds; and he gives the following

lists of Plants found in each :—

Fossil Plants of the First Group.

Pecopteris oreopteridis. Pecopteris lepidorhachis.
gigantea. murieta.
arborescens. | —— Serlei.
alata. | cristata.

— Pluckeneti. | choerophylloides.

— aquilina. | Bucklandi.

~— cyathea. eae es heterophylla.

— unita. exuosa.

—— leptophylla. elegans ?

RIBEIRO—COAL OF S. PEDRO DA COVA. 13

Fossil Plants of the First Group (continued).

Neuropteris Villiersi. Asterophyllites foliosa.
auriculata. Annularia longifolia.

Sphenophyllum Schlotheimi. brevifolia.

Walchia. Calamites approximatus.

-Asterophyllites equisetiformis. canneeformis.

— tuberculata. Equisetum columnare.
comosa. Lepidodendron Harcourti.

With many other, as yet undetermined, genera and species.

Fossil Plants of the Second Group.

Pecopteris oreopteridis. Sphenophyllum Schlotheimi.
—— gigantea. Cyclopteris orbicularis.
—— longifolia. Lonchopteris Bricei.
— affinis. Calamites pachyderma.
polymorpha. Poacites.
—— Grandini. Knorria.
arguta. Lepidodendron.
abbreviata. Asterophyllites ?

Sphenophyllum erosum.
With many other undetermined species.

The Trilobite-slates of the Lower Silurian formation do not
everywhere border the eastern side of the coal-bearing beds. From
Monte Alto to beyond Cancella velha, east of Pacal, they are dis-
placed several hundred métres towards the east, and the rocks of
the coal-group rest upon those unfossiliferous slates and quartzites
which the author is inclined to consider as the lowest member of the
Lower Silurian Formation, or rather as the newest member of the
Cambrian. The Trilobite-slates, however, by no means underlie the
newer formation, for they are clearly seen at their eastern boundary
reposing upon the azoic slates and quartzites. This formation is
therefore represented, on the right bank of the Douro as well as on
the left, as a narrow band, which runs parallel to the coal-bearing
beds. It has an mdependent strike from N.N.W. to S.8.E., and it
was deposited in a basin of unfossiliferous slates and quartzites.

The rocks of the fifth system, as exhibited in the Serra de Santa
Justa and near Vallongo, are next described ; and the author remarks
that from the structure of that “ Serra” it may be easily perceived
that the elevation of the beds is not the result of forces which have
affected this mountain-range only, but has been produced by an im-
mense lateral pressure, which caused the slates to be folded over one
another in undulations, through which the fifth system lost much of
its original extension at the surface, and was compressed into a
narrower space. The strike of the granite of Oporto and Baltar being
parallel to that of these rocks, that is E. and W., Senhor Ribeiro
considers the unheaval of that igneous mass to have produced the
upheaval and compression already alluded to, which also affected
similarly the Trilobite-slates containing Calymene Tristana, C'. Arago,
Ogygia Guettardi, O. Edwardsi, Illenus Lusitancus, I. giganteus,
and many other fossils, which are often distorted in consequence of
the disturbance which the beds have sustained. It is, however,

14 GEOLOGICAL MEMOIRS.

remarked, that the contortions of the Trilobite-beds are slighter than
those in the fifth system and the remaining parts of the fourth.

After enumerating the places where the coal-bearing beds may be
seen to dip under the slate and quartzite of the fourth system, and
describing the appearance of the rocks at each place, he states that
near the summit of Monte Alto the contorted shale of the second
coal-group may be seen reposing unconformably upon the beds of
the fourth system, and notices similar appearances of unconformity
in other localities between the coal-beds and the Trilobite-slates. —

Although he considers these and other ‘similar facts sufficient to
correct the erroneous idea of the age of the coal-beds which their
position would at first cause to be entertained, he again calls atten-
tion to the fact mentioned at p. 13, that, while in some places the
Trilobite-beds border the Coal-series, as at Cancella velha, at others
they occur at some distance apart; and he also states that on the
banks of the Rio Ferreira, near the brook of Boloi, the beds of the
second system are immediately succeeded by those of the fourth,
without the occurrence of any of the members of the Coal-series,
while this does not occur in passing from the strata of the fourth
system towards the 'Trilobite-beds.

And if to all these facts we add the one already referred to at
pp. 9 & 12, that the conglomerate of the Coal-series is mostly formed
of pebbles of slate and quartzite identical in character with those
rocks of the fourth system; and also bear in mind that, while the
Silurian fossils are generally distorted, in consequence of the con-
tortion and compression of the beds, the fossil plants of the Coal-
series, and especially those of the first group, are beautifully pre-
served; as well as the fact of the beds of the last-named group not
being at all disturbed, though those of the second group are slightly
so, but in a much less degree than the Silurian quartzite,—the fol-
lowing conclusions may be drawn :—

1. The Silurian slate existed prior to the formation of the coal-
beds, and formed the sides of the basin in which they were deposited.

2. The second group of these beds appears overlying the first,
through the inversion of the former. Consequently the overlying
second group is the older of the two, and they are both covered by
the still older Silurian rocks.

It is therefore seen, from the visible line of strike of the several
systems, and from the undulations of the strata into anticlinals and
synclinals whose axes are in the same direction (namely N. 20° E.),
that a parallel overthrow has taken place, through which the beds now
lie in an inverted order to that in which they were originally de-
posited. We also see that the heaving operation of the granite,
while it exercised an immense lateral pressure upon the rocks,
pushed together the beds into a smaller space than they originally
occupied.

The investigation of the stratigraphical relations of those rocks
shows us that the principal contortions took place before and during
the deposition of the Trilobite-beds; and the complete absence of
the Upper Silurian strata, which are represented in the neighbour-

HAUER—TEGEL OF OLMUTZ. fs

hood of Coimbra by the blackish and grey slate with Cardiola
interrupta, intimates that the disturbance of the rocks continued in
the Lower Silurian period, when that area was already elevated
above the sea. The stratigraphical relations of the coal-beds de-
scribed above also show that during their deposition the disturbance
of the strata ceased, and that the most westerly portion of the fourth
system must at that time have been a valley in connexion with the
sea, forming a narrow strait or an estuary, into which the fresh-
water drainage of the country was discharged. In this estuary the
beds of the second group of the Coal-series were deposited, certainly
before the formation of the conglomerate seen near Varziela, on the
east of the Valle de Deao and near Sete Cazaes. This conglomerate
leans against the steeply inclined beds of the fourth system, which
formed the eastern side of this basin. This and other facts, especially
the unconformity of the stratification, lead the author to the opinion
—already expressed by Herr E. Schmitz—that the second group of
the Coal-series must be considered of Devonian age.

The author then describes what he conceives to have been the
prevailing physical conditions of the period immediately succeeding
the formation of these Devonian strata, during which the first Coal-
group was deposited. He considers this group to represent the
Carboniferous formation (Hulla) for the following reasons :—The
thick mass of breccia separating it from the Devonian strata; its
occurrence in small basins; the difference in the fossil Plants of the
two groups, and the difference in mineralogical characters.

The manner in which the present relations of the several series
have been produced is then treated of, including the effect of
denudation in exposing the strata; and the author concludes by
stating his belief that the coal-beds of Vallongo and those of S. Pedro
da Cova are of the same age. (ih. Mee. |

On the NeocrneE Puastic Cray (Tegel) of Ormirz, Moravia.
By Franz von Haver.

[ Proceed. Imp. Geol. Instit. Vienna, Dec. 16, 1862.]

Mr. Watpricu found in this clay specimens of Phasianella Eich-
waldi, Hornes, Bulla Utricula, Brocchi, Ervilia pusilla, Phil., Venus
multilamella, Lam., and Lucina exigua, Eichwald. All these species
are also met with in the Tertiary basin of Vienna, the first three near
Steinabrunn and Baden, the fourth at Gainfahrn, and the fifth at
Steinabrunn. The sands intercalated with this clay yielded, upon
washing, some few traces of Bryozoa, spines of Cidaride, some
Nullipore, and, more abundantly, some fine species of Cypridine.
_ Foraminifera are rather scarce, and only represented by some few
forms. Among these are predominant :—

Asterigerina planorbis, D’Ord., in the Vienna basin, occurring near

Nussdorf.
Polystomella crispa, D’Orb., near Nussdorf and Baden.
Rosalina Viennensis, D’ Orb.

16 GEOLOGICAL MEMOIRS.

The following species are of very rare occurrence in the Olmiitz
sands :—

Polystomella Fichteliana, D’ Ord.

Nonionina communis, D’ Orb.

Amphistegina Haueriana, D’ Orb. \ from Nussdorf.

Bulmina elongata, D’ Orb.
Triloculina inflata, D’ Orb.

The strata from which these sands were produced belong evidently
to the Upper Marine Neogene beds of the Vienna Basin, and cer-
tainly stand next to the Amphistegina-zone of the Vienna Tertiaries.

(Count M.]

On the Fosstu Fisuzs of Austria. By Professor Kner.
[ Proceed. Imp. Acad. Vienna, May 8, 1862.]

Prorressor Kwer has described three species of Acanthopterygian
fishes from the Calcaire grossier of the Leitha Hills, between Lower
Austria and Hungary. One of these fishes is a Labroid—Julis
Sigismund ; another, Palimphanus anceps, is a representative of a new
generic type. The third, known only by a single specimen (wanting
the head and the whole fore part of the body), is undoubtedly a
Sparoid, and probably belonged to a species of Pagrus, for which
the appellation P. priscus is proposed. The late distinguished ich-
thyologist Heckel published two species, as Labroids, from the same
locality ; one of them (Labrus Agassiz) is probably a species of Julis,
while the other (Labrus parvulus) 1s certainly not a Labroid.
[Count M. ]

On the Lias of Finrxrrcnen, Huneary. By Professor Prrers.
[ Proceed. Imp. Acad. Vienna, July 24, 1862. ]

Eacu of the three Liassic subdivisions, with its subpelagic fauna
(comparable to the Lias of Swabia), is represented in the Fiunfkirchen
district. The lowest subdivision (of great practical importance on
account of its rich coal-seams) rests on beds poorer in coal (pro-
bably analogous to the Bone-bed series); and these last cover a
sandstone destitute of coal, which, lying upon the Muschelkalk, is
analogous with the Keuper. The limestones of the Upper Alpine
Trias and of the Rheetic subdivision (Dachstein-limestone) are con-
sequently wanting.

The pelagic subdivisions of the Alpine formations appear again in
the Jurassic series, in the form of Ammonite-limestones, analogous
to the marbles of Trient, Campo Rotondo, and other localities of the
Southern Alps. The Stramberg strata are represented by some
isolated organic forms.

The whole series under notice comprehends the formations from
the Upper Triassic beds (and a red sandstone of problematic age) to
the Jurassic, both inclusive. [Count M.]

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

Upon the Martertat Inpicarions of the Corxistence of Man with
ELEPHAS MERIDIONALIS in Beds, near CHARTRES, more ancient than
the QuATERNARY GRAVELS of the Vauueys of the Somme and the
Serve. By M. J. Desnovers.

[Note sur des Indices matériels de la Coexistence de l’Homme avec I’ Elephas

meridionalis dans un terrain des environs de Chartres, plus ancien que les
terrains de transport quaternaires des vallées de la Somme et de la Seine;

par M. J. Desnoyers. Comptes Rendus des séances de l’Académie des
Sciences, vol. lvi., No. 23, pp. 1073-1083. June 8, 1863.]

Tue researches of Dr. Falconer and M. Lartet have made known
that amongst the fossil Proboscidea there are at least three perfectly
distinct species of Hlephas, each characterizing a distinct portion of
the later tertiary period. A résumé of the well-known fauna of each
of these stages is first given by M. Desnoyers, and he then enunciates
the several kinds of evidence from a consideration of which the
coexistence of man with extinct animals may be inferred, namely :—

1. The association of human bones with the bones of extinct
Mammalia.

2. The occurrence of objects of human industry, principally
instruments of stone (pierre*), in the same beds which contain bones
of the large Mammalia.

3. The traces of the hand of man upon those bones.

The last kind of evidence the author considers to have a value
perhaps superior to that of the other two, because it unites in one
specimen the evidence of the action of man with the indication of the
coexistent species. Many observers, and especially M. Lartet, have
called attention to the occurrence, in caverns, of bones marked in this
manner.

In the middle of last April M. Desnoyers examined the sand-beds
of Saint-Prest, near Chartres, well known as a remarkable deposit,
containing bones of Elephas meridionalis, Rhinoceros leptorhinus,
Hippopotamus major, several species of Deer, a large Ox, a Horse
similar to that of the Val d’Arno, and of other extinct Mammalia
considered to belong exclusively to the Pliocene period.

After giving a description of the beds of Saint-Prest, and noticing
the various memoirs that have been written upon them, as well as
the principal collections of the bones obtained therefrom, which he
had examined, M. Desnoyers remarks that, in partly disengaging the

* This expression is intended by the author to include only flint implements,
and evidently does not refer to implements of stone as technically understood.—Ep.
VOL. XIX.—PART II. D

18 GEOLOGICAL MEMOIRS,

tibia of a Rhinoceros from the sand investing it, he was struck with
the appearance of strie, varying in form, depth, and length, which
could not have resulted from fracture or from desiccation (the evi-
dences of which were also apparent), because they had evidently been
formed prior to that operation, and traversed the bone in the direction
of its breadth, passing also over its ridges, and otherwise following its
contours. These strie, or traces of incisions—very sharp, some very
fine and very smooth, the others larger and more obtuse, and as if
they had been produced by sharp flakes or denticulated pieces of
flint—were accompanied by small incisions or elliptical notches,
which were clearly defined, as if they had been produced by the
blow of a sharp instrument. <A great many of these strie and
cavities were covered by ferruginous dendrites and sand, and were
also nearly all a little worn, in consequence of the friction and rolling
to which the greater number of the bones and teeth had undoubtedly
been subjected, before and during their deposition. They immediately
recalled to his mind analogous incisions upon the bones of Mammalia
from the caverns, the gravels, and the peat-bogs, and also from the
infinitely more recent deposits in tombs of various ages.

Although perfectly convinced in his own mind of the human origin
of these marks, yet, for fear of bringing forward an incomplete state-
ment, he examined all the collections of bones from Saint-Prest, that
he could get access to, in company with M. Lartet, by whom the species
were determined.

M. Desnoyers then states that the examination of more than one
hundred bones, of which several are a metre in length, has con-
vinced him that the notches (the traces of incisions, of excoriation,
and of blows), the striz, whether transverse, rectilinear, sinuous,
or elliptical (these being sharper at one end than the other), some- .
times polished, sometimes subdivided into several striz occupying
the cavity of the larger indentation,—in a word, that marks alto-
gether analogous to those which are produced by cutting-instruments
of flint, with more or less sharp points and more or less jagged edges,
are seen on the greater number of these bones. Upon some of them,
and particularly upon a portion of the skull of an Elephant belonging
to the Muséum d’Histoire Naturelle de Paris, may be perceived traces
of arrows, which appear to have glanced upon the osseous material
after having traversed the hide and the flesh. A sharp triangular
cavity caused by the point, and some lateral notches produced by the
denticulations of an arrow of flint or of bone, may also be distin-
guished. The Mammalia the bones of which present these different
appearances are—Hlephas meridionalis, Rhinoceros leptorhinus,
Hippopotamus major, several species of Deer, of which two are of
very great size (Megaceros Carnutorwm, Laugel), a large Ox, and a
much smailer species.

All the skulls of Deer which M. Desnoyers has seen appear to
have been fractured near the insertion of the two horns, by a violent
blow given upon the frontal bone, towards their origin.

After enumerating the various kinds of bones which present the
most distinct traces of incisions, and noticing the occasional occur-

DESNOYERS—COEXISTENCE OF MAN WITH ELEPHAS MERIDIONALIS. 19

rence of bones which appear to have been split open for the purpose
of extracting the marrow, the author remarks that several bones
of Hippopotamus, especially a metatarsus, are finely furrowed in
every direction by very distinct striz, which he is disposed to refer
less to the action of man than to another cause; he then gives his
reason for believing them to have been produced by the action of
blocks of ice transporting grains of sand. He sums up the result of
his observations as follows :—

1. Some fossil bones of several animals (see p. 18), considered as
characteristic of the Upper Tertiary rocks or Pliocene, and discovered
in an undisturbed deposit of that geological period, bear numerous
and incontestable traces of strie and of gashes.

2. These notches and these striz are perfectly analogous to those
which have been observed upon fossil bones of newer species of
Mammalia; namely, the extinct species accompanying the Elephas
primagenius, Rhinoceros tichorhinus, Hyena spelea, &e., and those
that are now living, such as the Reindeer, several Deer, and the
Aurochs, found in the ossiferous caverns and in the Drift. Similar
appearances have also been recognized upon numerous bones of living
species collected in Gallic, Gallo-Roman, Breton, and Germanic
tombs.

3. The marks upon the most ancient bones appear to have, in great
part, the same origin as those of the more modern, and cannot, there-
fore, be attributed to any other cause than the hand of man.

4. Some other striae—finer, rectilinear, and crossing one another—
are also seen in great number upon the bones from the Pliocene beds
of the environs of Chartres, and other localities, and appear to be
analogous to those which have been observed upon the pebbles and
blocks which have been striated, scratched, and polished by glaciers,
The motion due to torrential waters would with difficulty produce a
similar result.

5. The beds of Saint-Prest, unanimously recognized as Upper
Tertiary, or Pliocene, and certainly as anterior to all the Quaternary
deposits which contain Elephas primigenius, include numerous bones
of Elephas meridionalis, and of the greater number of the large
Mammalia characteristic of the Upper Tertiaries ; upon these bones
both kinds of notches and striz may be observed.

6. From these facts it seems possible to conclude, with a very
great appearance of probability, until some other more satisfactory
explanation better elucidates this double phenomenon, that man
lived upon the soil of France before the great and first Glacial period
—at the same time as the Hlephas meridionalis and the other Pliocene
species of the Val d’Arno, in Tuscany ; and that he was contemporary
with these large animals, anterior to the epoch of the Elephas
primigenius and the other Mammals whose bones have been found
mixed with the remains of man in the gravels, or Quaternary beds of
the great valleys, and in the caverns.

7. Finally, the beds of Saint-Prest furnish, as yet, the most ancient
example in Europe of the coexistence of man with extinct animals,

———— [H.M.J.]
D2

20 GEOLOGICAL MEMOIRS.

On the Patmontotoey of New Zeatanp. By Dr. Zire.
[Proceed. Imp. Geol. Instit. Vienna, January 20, 1863.]

THE collection of organic remains brought to Vienna by Prof.
Hochstetter is the most considerable that has ever been brought to
Europe from this remote part of the globe. it is at present under
examination by the Vienna paleontologists, who are preparing the
results of their investigations for publication in the scientific section
of the work on the Voyage of the‘ Novara.’ Prof. Unger has under-
taken the descriptions of the Plants ; Chey. F.de Hauer will describe
the Jurassic Ammonites and Belemnites; M. Karrer and Dr. Stache
have undertaken the Foraminifera; Dr. Zittel is preparing descrip-
tions of the Mollusca and Echinodermata (about fifty to sixty species,
among which six still exist); and Prof. Suess will describe the
Brachiopoda.

The most ancient fossiliferous deposit of New Zealand is a
greywacke-like rock, characterized by the extraordinary abundance
of two species of Monotis. One of these—Monotis Richmondiana,
Zittel—sometimes constitutes whole strata, and, although greatly
resembling the Monotis salinaria of our European Trias, differs
essentially from it by its more vaulted shape and by its stronger,
less numerous, and more distinct ribs. The second species, Monotis
decipiens, Zittel, is rather similar to Halobia Lommel. ‘Together
with these Triassic forms, a species of Spzrigera, and other fossils,
declared by Prof. M‘Coy to be Paleozoic, occur in this greywacke.
The stratum next in ascending order contains a deeply grooved
Belemnite (Belemnites Aucklandicus, Hauer) and a new species of
Ammonite (Ammonites Novo-Zelandicus, Hauer), together with a
very characteristic Aucella (Aucella plicata, Zittel), a Placunopsis,
anc several other bivalves of Jurassic type.

The succeeding deposits, far more abundant in organic remains,
and evidently of Tertiary age, may be brought under two paleeontolo-
gically distinct groups. The first of these groups offers no traces of
any living species, although the genera of Mollusca and Echino-
dermata met with in it are such as have arrived at their full de-
velopment in the present period, or did so in the Tertiary epoch.
Among these, Pecten, Ostrea, Hemipatagus, Schizaster, Brissus, and
Nucleolites are remarkable for their abundance. Taking into con-
sideration the absence of any living forms whatever, we may be
justified in correlating this group with the most ancient of our
European Tertiaries. The second group, which occurs in a great
number of localities on the Southern Island, has a fauna closely
allied to that now existing round New Zealand and Australia; some
species (a few of which were determined by Mantell and Forbes) are
identical with recent ones, and the rest belong to genera peculiar to
the present period. This fossil fauna is strongly marked with the
characteristic features of the present marine fauna of New Zealand,
and even genera of most limited range (as Struthiolaria) are repre-
sented in it by extinct species. This second group may safely be
considered as an equivalent of our European younger Tertiaries.

——— [Counr M.]

ZIRKEL—STRUCTURE OF ROCKS AND MINERALS. 21

On the Grotocy of Cyprus. By Prof. Uncrr.
[Proceed. Imp. Acad. Vienna, February 5, 1863.]

Tuts island exhibits, on a surface of only 173 square miles, two
distinct mountain-systems,—the larger occupying the south and
south-west portion, and partly rising to a height of 6000 feet
above the level of the sea; the other running parallel with the
north coast in a lengthened range of steep cliffs. The funda-
mental rock of both is greenstone, with its varieties, as diorite,
gabbro, uphanite, &c., extending into a continuous mass in the
south and west of the island, while in the northern chain it occurs
only in small subordinate domes. This igneous rock, associated
with a small portion of trachyte, is everywhere overlain by sedi-
mentary deposits. In the north chain these are red cliff-limestone
and white compact limestone, the latter containing Corals of an Upper
Jurassic appearance. The Jurassic strata are overlain by non-fossili-
ferous, fine-grained sandstone, which may be identified with the Vienna
Sandstone (Cretaceous and partly Eocene); it crops out only along the
north chain,and disappears in other partsof theisland beneatha deposit
of Tertiary marls and marly limestones. These Tertiaries sometimes
include large layers of gypsum, and are prevalent in the eastern and
southern slopes of the main mountain-mass. The most recent
deposits are conglomerates and sandstones, filling up the depression
between the two mountain-systems and bordering the whole island.
Their numerous and well-preserved organic remains denote their
Quaternary age, belonging to a time when the geological constitution
of the Mediterranean basin was nearly the same as at present. The
upheaval by which this marine sediment was raised above the level of
the sea and the present physical features were given to the island must
have established a land-communication with Syria. This supposition
alone may account for the concordance of the Cyprian fauna and flora
with those of the neighbouring continent. The communication may
have been taken away by the sinking of the isthmus shortly before
the beginning of the historical period, in consequence of one of those
commotions which in later times, and even in our own days, have.
conyerted several places on the island into heaps of ruins.

[Count M.]

Intimate StructuRE of Rocks and Minerats. By Dr. ZrrKet.
[ Proceed. Imp. Acad. Vienna, March 12, 1863.]

Tuer author has submitted to microscopical examination extremely
thin lamine of rocks and minerals. All the varieties of quartz
entering into the composition of granites, porphyries, and trachytes
show innumerable cavities containing liquids; some of them are so
small that, even under a magnifying power of 2000*, they appear only
as minute points. These varieties of quartz, and the felspar associated
with them, include particles of matter, fused by igneous action, which

* This measurement is probably superficial, in which case it would be equal
to about 45 diameters. —

93 GEOLOGICAL MEMOIRS.

have been incorporated during the gradual increase of the crystals,
and which have become solidified into vitreous or lithoid cavities or
pores*. During refrigeration small acicular crystals of a black
substance have been deposited within the vitreous cavities, which, like
the water-cavities, generally include a vesicle. Transitions between
vitreous and lithoid cavities occur frequently, and in great variety,
together with empty cavities resulting from the development of
gaseous substances. The whole of these structures, only visible by
the aid of the microscope, may throw some light onthe origin of the
rocks in question, being indicative of the simultaneous action of
water and vapours and of the igneous fusion of solid substances. In
nearly all varieties of granite the quartz includes myriads of crystals
of vitreous felspar, irregularly spread in every direction. <A polarizing
apparatus connected with the microscope proves the small quartz-
~ granules of the granites to be a combination of minute crystals. The
fundamental mass of the euritic porphyries, showing three distinct
types, has proved to be really (as it has been generally supposed to
be) an intimate mixture of quartz and felspar; the quartz in many
of them, however, is more prevalent than geologists generally are
ready to admit. The basalts, appearing to the naked eye merely as
a homogeneous mass, exhibit, under the microscope, their various
constituents, and, by examining a great number of varieties, the
progress of decomposition, so interesting in these rocks, may be
followed through all its stages. The pitchstones, generally admitted
to be composed of an amorphous vitreous substance, have proved to
consist of a confused aggregate of innumerable acicular crystals,
imbedded in a comparatively small proportion of vitreous matrix, the
nature of which is still doubtful. Obsidians, cautiously heated with
hydrofluoric acid, exhibit microscopical acicular crystals, which may
be also seen, as shown by the late Prof. Leydolt, in artificial glass
when acted upon by the same acid. [Count M.]

On the Creracrous Srrata of the Crrctes of Konteeratz and
Curvupim (8.E. Bonrmia). By C. H. M. Pant.

[ Proceed. Imp. Geol. Instit. Vienna, January 20, 1863. ]

Tnesz strata have been shown by Professor Reuss to rest on the Gault,
and consequently they represent M. d’Orbigny’s “ Cenomanien ”
and “ Turonien.”

Their subdivisions are, in descending order:—1. Pliner; 2. Quader
Marl; 3. Quader Sandstone; 4. Quader Conglomerate.

The Pliner (1) consists of thinly laminated, argillaceous (locally
caleareous) marls, with Jnoceramus Cuvieri and J. planus (both
abundant); also Micraster cor-anguinum, Pecten membranaceous,
Nucula pectinata, Terebratulina chrysalis, and Tellina tenmssima. The
Quader Marl (2) may be further subdivided into (a) an inferior,

* Synonymous with the ‘‘stone-cavities” of Sorby; see Quart. Journ. Geol.
Soc. vol. xiv. p. 466.—Epbir.

MORTILLET—ITALIAN AND FRENCH ALPS. 23

argillaceous, thinly laminated portion, much resembling Planer,
with but few fossils, locally containing the chele of Callianassa
Faujasi in abundance ; ;.(6) calcareous fossiliferous strata (Beyrich’s
Planer-sandstone) ; and (c) an upper portion, thicker, highly arena-
ceous, and fossiliferous. Inoceramus Cuviert, I. mytiloides, and Lima
multicostata occur abundantly; next to them’ come Inoceramus
Brongmarti, Leguminaria trunculata, Ostrea vesicularis, Janira
quinquecostata, Pecten levis, Arca glabra, Hippurites ellipticus,
Hamites rotundus, H. plicatilis, Heniaster bufo, and Micraster cor-
anguinum. The Quader Sandstone (3) may be subdivided, upon the
same principle as the Marl, into an upper, highly glauconitic portion
(Green-sandstone), and an ‘inferior white portion without any trace
of carbonate of lime, with intercalations of shales from five to ten
feet thick, and containing a thin seam of coal. The Conglomerate (4), _
which is entirely composed of rolled fragments of quartz, without any
trace of organic remains, is here, as everywhere within the Creta-
ceous districts of Bohemia, the lowermost deposit of this formation.

[Count M.]

A Comparison of the Srrata of the Irattan and Frencu Stopes of
the Atrs. By M. Gapriex DE Morritter.

[Terrains du versant italien des Alps comparés a ceux du versant francais; par
M. Gabriel de Mortillet. Bulletin de la Sceiété Géologique de France,
vol. xix. 1862, pp. 849-907. ]

Te central axis of the Alps consists of a series of channels which
have been formed by crystalline rocks. The fossiliferous rocks, to
adopt the expression of M. Elie de Beaumont, lie around them like
the edges of vast button-holes. It may, therefore, be presumed that
the sedimentary rocks are the same on both sides, though hitherto
this has been denied.

It would follow from this that the upheaval of the Alps is more
ancient than is generally admitted; that it was effected during suc-
cessive epochs, and was accompanied by oscillations of level. The
sediments on the two slopes have thus been deposited independently
of each other ; nevertheless they have a general correspondence.

Although, as a whole, the crystalline rocks form the axis of the
chain, yet, on the Italian side, they are prolonged to its extreme
boundary ; and in Piedmont they rise immediately from the plain,
constituting the advanced guards of the mountains.

Silurian and Devonian rocks have as yet been recognized only
towards the extreme north-east of the Austrian Alps. M. de Mortillet
notices, in connexion with them, Sir R. Murchison’s views respecting
the probable metamorphism of strata.of this age, and concludes that,
at this epoch, the axis of the Alps consisted of a protuberance almost
wholly above the waters.

Carboniferous rocks have been detected in the eastern portions of

24 GEOLOGICAL MEMOIRS,

the district; they are of marine origin, and contain traces of fossil
Plants. The anthracite-deposits thin off towards the Alps of Savoy
and Dauphiny.

The Trias is well developed on both sides of the chain, as at
Hallstatt on the north and St. Cassian on the south. M. Mortillet
gives for this, as for each formation, lists of the fossils from various
localities, and institutes a comparison of them. During this epoch
the land continued raised above the sea, but volcanic eruptions
occurred on a large scale.

Lower Lias has been shown to exist in Lombardy on one side and
in Dauphiny on the other. The Middle and Upper Lias are largely
developed on the French side, and are found on the Italian slope
also. During the deposition, the eastern portion of the chain was
raised and. the western depressed. The succession of the Jurassic
rocks shows that the upheaval of the Alps was a slow, continuous
movement, with local oscillations. Sections of the Cretaceous rocks
are given, from which it is deduced that in Italy there is an unbroken
succession from the Oxfordian into the Neocomian; whence the
writer concludes, that whilst in some parts of the earth there existed
modifying causes producing intermediate deposits, in other parts
free from disturbing causes the same fauna may have continued to
exist. The Eocene deposits south of the Alps are eminently littoral ;
and they are found northwards in the High Alps in a continuous line ;
here, also, they contain evidence of littoral conditions, and are ana-
logous to similar beds on the south side.

Miocene beds are extensively developed in Venetia, but not in the
French or Swiss Alps, save in the Molasse of the plains, of which the
upper beds are Phocene.

The Quaternary deposits are divisible into ancient alluvium, gla-
cial deposits, and modern alluvium. Under the first division may
be placed the frequently occurring débris of ancient lakes; upon
this rest the striated boulders of the second period, as M. de Mortillet
has shown in his map of the old Italian glaciers: under the head of
“recent alluvium ” are placed all the deposits formed subsequently to
the retreat of the glaciers, some of which contain the remains of
extinct Mammals. The author maintains that there has been but
one Glacial period, in opposition to the views of M. Scipio Gras and
M. Morlot, who have propounded the theory of the existence of two.

The conclusions to which the author has arrived are expressed in
a table of correlations, which shows that the upheaval of the Alps,
effected during the Palzozoic period, was succeeded by a submer-
gence during the Liassic ; and since that time the central portion has
been raised by a series of oscillatory movements extending through
all subsequent periods to the close of the Miocene, when the chain
attained its maximum height. There has been an intermixture of
the faunas on the Italian side, not only of formations immediately
succeeding one another, as of the Cretaceous and Eocene strata, but
also of others, such as the Oxfordian and the Neocomian.

Sere At

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the Coat-ForMATION between PRacvuE and PILseEn.
By Herr R. Lupwie.

[Die Steinkohlenformation zwischen Prag und Pilsen: von Herrn R. Ludwig.
Notizblatt des Vereins fir Erdkunde, &c., zu Darmstadt. Folge ii. Heft 1.
Nos. 7,9, 11,12. 1862.]

Tue productive Coal-formation of Bohemia is underlain either by
Silurian and metamorphosed slates or by granite and crystalline
quartzose rocks ; but other marine deposits are altogether wanting,
whether of Devonian, Carboniferous, Permian, Triassic, or Liassic
age. In fact, from the Silurian Period to the Cretaceous, the district
was a continent free from the presence of the sea.

_ In consequence of the productive coal-beds between Prague and
Pilsen reposing neither upon Devonian rocks nor upon marine beds
of the Carboniferous formation, but upon much more ancient rocks,
and because they are not covered by well-marked Rothlegende,
neither by Zechstein, Trias, nor Jurassic rocks, it is impossible to
determine their age with the same certainty as that of other Coal-
formations, such as those of Zwickau and Westphalia. It only re-
mains, therefore, to endeavour to determine the age of the coal-beds
from a comparison of their fossils with those of other localities.
Fortunately the Bohemian beds are extremely rich in Plant-remains
in a good state of preservation.

The Coal-formation occupies. a broad band extending from Staab,
across Pilsen, to Kralup beyond Prague, 14 German miles in length,
from 1 to 2 in breadth, and which may be divided into three large
basins: namely, that extending from Staab to Plass, and which the
author terms the Basin of Pilsen; that extending from Kralowiz to
Lana, or the Basin of Rakonitz ; and that commencing at Schlan and
extending beyond Kladno, to Kralup, which Herr Ludwig calls the
Basin of Buschtiehrad.

Each of these basins is composed of a greater or smaller number
of unconnected troughs, and the whole band is bounded on the north
and south by several outlying basins. The author then gives a
general sketch of their physical features, and he afterwards remarks
that in some of the larger basins there is an upper or younger coal-
formation, separated from the lower one by very thick beds of con-
glomerate and sandstone, and which Reuss, in his Memoir on the
geological relations of the Basin of Rakonitz, referred to the Roth-
legende.

The individual troughs of one and the same basin possess, as Herr
VOL, XIX.—PART II, E

26 GEOLOGICAL MEMOIRS,

von Ettingshausen has proved in his Memoir upon the Basin of
Radnitz*, different floras—a circumstance which enables one to con-
clude either that they were formed in succession or that the coal-
beds were produced under varying conditions (as high-level or as
low-level bog-formations), and that the greater or less humidity has
exercised an influence upon the flora.

The basins and troughs lie upon very various kinds of rock: the
basin of Harr is in gneiss, that of Merklin lies upon granite and
crystalline schist, and that of Pilsen rests upon the same descriptions
of rock in the south-west portion, and upon Silurian rocks in the
north-east; upon the last-named formation repose also the other
basins. The author believes that from the absence of all contem-
poraneous marine formations, and even from the facts already
mentioned, it may be concluded that the Bohemian coal-deposits
have been formed in bogs and lakes in the midst of a somewhat
extended continent (or an island), which met the sea in the region
of the county of Glatz (Silesia), where the Carboniferous Limestone
now occurs, containing Productus latissimus, &c. This long series of
bogs was perhaps in connexion with those of Trautenau, Walden-
burg, and other places in the district of Glatz ; but the Upper Silesian
and the Moravian basins lay upon the other side of the sea-gulf. The
variation in the flora of the individual basins may perhaps be ex-
plained by the difference in situation : the Sigillaria- and Stigmaria-
bogs were perhaps on a high level, while those rich in Ferns but poor
in coal were on a low level, and those which contain Stigmaria in
the lower beds and many Ferns and Calamites in the upper were
probably high-level bogs which became changed to low-level bogs
through oscillations of level.

Herr Ludwig then describes the basins and troughs in the follow-

ing order :—
1. Basin of Pilsen. 8, Basin of Rakonitz.
a. Trough of Wilkischen. ~ a. Coal-beds in the lower portion
6. Trough of Nurschan, of the Carboniferous formation.
2. Basin of Radnitz. 6 Coal-beds in the upper portion
3. Basin of Horschowitz. of the Carboniferous formation.
4. Basin of Miréschau. e. Coal-beds in the Rothliegende.
5. Basin of Merklin. 9. Basin of Klein-Prschilep.
6. Basin of Wranowa, near Mies. 10. Basin of Stradonitz.

' 7, Basin of Steindorfel, near Manetin. | 11. Basin of Buschtiehrad.

In the beds below the coal-seams in the Wilkischen and Nurschan
districts (Basin of Pilsen) occur the Stigmaria ficoides, and thick,
long roots, which perhaps belong to Calamites, both very abundant.
In the beds above the coal-seams occur :—

Sigillaria elegans, Brongn. Lepidodendron rimosum, Sternd,
ornata, Brongn. undulatum, Szernd,
alveolaris, Brongn. Calamites equisetiformis, Sternd,

Lepidodendron dichotomum, Sternd.

No Ferns have yet been found in these districts.

To the north of Pilsen the flora consists of Sigillarice, Lepidodendra,
and Calamites, and some species of Neuropteris are said to be abun-
dant here. From the trough of Plass (Babina), Herr von Ettings-

_* Abhandl. der k.k. geol. Reichsanstalt. vol. ii, 1855,

communis, Httingsh.

LUDWIG——-BOHEMIAN COAL-BASINS, oT

hausen mentions, in his work already quoted, Neuropteris obovata,
Sternb., and NV. rubescens, Sternb.

Herr Corda, Graf Sternberg, and Herr yon Ettingshausen have
investigated the flora of the Radnitz Basin, from which about.138
species have been determined by them ; of these, 82, or 60 per cent.,
are peculiar, while the remaining 56, or 40 per cent., occur also in
other districts. Four species are found also in Devonian rocks, and
two in the Rothliegende.

In the Miréschau Basin Herr von Ettingshausen has found Newro-
pteris acutifolia, Brongn., and N. obovata, Sternb. ; and in the Basin
of Merklin Alethopteris Sternbergi, Brongn.

Northward from Senetz, near Lubna, in the Rakonitz Basin, and
probably in the lower portion of the Carboniferous formation, Herr
Stur has found Calamites communis, Ettingsh., Sphenopteris rutefolia,
Gutb., Stigmaria ficoides, Brongn., Flabellaria Sternbergi, Ettingsh.,
and Neeggerathia foliosa, Sternb. ; “put the author remarks that these
few remains are scarcely sufficient to determine the age of the beds
from which they were obtained.

The upper part of the Coal-formation in the Rakonitz Basin is
seldom coal-bearing ; but at the Belschanka, near the Rischlaw mill,
there is a bed of coal 3 feet thick, the roof of which is composed of
white and yellow shale containing many Fern-remains, as Vewropteris
acutifolia, Brongn., Cyclopteris rhomboidea, Ettingsh., Sphenopteris
Haidingeri, Ettingsh., Asplenites elegans, Ettingsh., Asplenites Reussi,
Ettingsh. Lepidodendra and Calamites are comparatively rare ; but
Neggerathia foliosa, Sternb., is somewhat abundant.

Nearer Rakonitz are two coal- beds, the beds aboye which are rich
in Lepidodendron obovatum, Sternb., L. dichotomum, Sternb., and
Sigillaria elongata, Brongn. The shale above the upper coal-seam
contains likewise Neggerathia foliosa, Asplenites elegans, A. Reussi,
and Cyclopteris rhomboidea.

The beds in the Rothliegende contain no Plants; sometimes, how-
ever, pyritized Wood is found, or brandschiefer with Fish-remains,
—namely, teeth of Diplodus, sp., Xenacanthus Decheni, Beyr., and
Pygopteris, sp. ; scales and fins of Acanthodes gracilis, F. Romer ; and
head-bones and other remains of Palwoniscus. All the coal-beds
have brandschiefer above them.

The author gives the following summary of the characters of the
Basin of Rakonitz :—

1. This basin is similar to those of Pilsen and Radnitz in being
divided into several coal-bearing troughs, separated by barren ridges.

2. These small troughs are richest in coal in the southern and
south-western portions of the basin, while those in the eastern can
scarcely be described as coal-bearing.

3. The lower portion of the Coal-formation contains the thicker
beds; in them Sigillaria, Lepidodendron, and Calamites predominate.

4. The upper portion of the formation includes coal-beds in which
are Neggerathia and Ferns similar to those from Stradonitz, and
equally abundant.

5. In the Carboniferous formation in the northern portion of the

E2

28 GEOLOGICAL MEMOIRS.

basin there are only afew, thin coal-seams; but, on the other hand,
the thickly developed Rothliegende here contains some productive
coal-beds. It is to be hoped that the Rethliegende in this portion
of the basin, where it dips beneath the Cretaceous beds, will be still
further worked for coal.

The Basin of Stradonitz, which is situated about two German
miles south of the south-eastern border of the Rakonitz Basin, in
the neighbourhood of Beraun, contains, so far as is known at pre-
sent, no coal-beds. The fossil Plants occurring in the sandstone and
shale have been described by Herr von Ettingshausen; they are the
following :—

Chondrites Geppertianus, Httingsh.
(perhaps the root of a land-plant).
Calamites Volkmanni, Httingsh.
Sphenophyllum Schlotheimi, Brongn.
Annularia longifolia, Brongn.
Neuropteris gigantea, Sternd.
Loshii, Brongn.
coriacea, Httingsh.
squarrosa, Hittingsh. (=
pteris Brongniarti, Guzb.).

Dictyo-

Cyclopteris tenera, Httingsh.
rhomboidea, Httingsh.
Sphenopteris Haidingeri, E¢tingsh.
intermedia, EHttingsh.
trifoliata, Brongn.

Asplenites elegans, Ettingsh.
Reussi, E¢tingsh.
Cardiocarpum orbiculare, Httingsh.
Cordaites borassifolia, Unger.
Palmacites caryotoides, Sternb.

It is remarkable that this basin contains especially the remains of
Ferns, some of which correspond with those found in the upper beds

of Rakonitz.

It is certain that those fossils are not found at any

other locality in Bohemia, and are unknown from other coal-fields.
From Kladno, in the Basin of Buschtiehrad, the author obtained

the following plants :—

Calamites communis, E¢tingsh.
tenuifolius, Ht¢tingsh.
Sphenophyllum Schlotheimi, Brongn.
Neuropteris acutifolia, Brongn.
rubescens, Sternd.

— obovata, Sternb.
Sphenopteris meifolia, Sternd.
acutifolia, Brongn.
tenuissima, Sternd.

—— obtusiloba, Brongn.
elegans, Brongn.

rutzefolia, Guzo.

Cordaites borassifolia, Unger.
Asplenites Sternbergi, Ktzingsh.
lindsxeoides, E7¢tingsh.
Cyatheites oreopteroides, Goepp.

Cyatheites undulatus, Goepp.
setosus, Httingsh.
Pecopteris pennzeformis, Brongn.
Glockerana, Goepp.
Lepidodendron dichotomum, Sternd.
aculeatum, Sternd.

—- Sternbergi, Lindl.
brevifolium, H¢tingsh.
—— plumarium, Lindl.

—— Haidingeri, Httingsh.
crassifolium, Httingsh.
Sigillaria elongata, Brongn.
rhomboidea, Gezn.
mammillaris, Brongn.
Stigmaria ficoides, Brongn.
Araucaria Cordai, Sternbd.

According to Herr Stur, the following species also occur :—

Cyatheites arborescens, Goepp.
Miltoni, Goepp.

Pecopteris Silesiaca, Goepp.

The flora of this basin corresponds in general with that of the
Basin of Radnitz. Some short lists of Plants found at other loca-
lities in the Basin of Buschtiehrad are then given; the most im-
portant of these lists are the following, of Plants occurring in the
roofs of two coal-beds worked in the Rappiz (Hrapic) district, and
near Buschtiehrad, as well as near Wotowitz and Koletz,

LUDWIG—BOHEMIAN COAL-BASINS. 99

From above the lower coal-bed (10 feet* thick), according to
-Stur, were obtained :— |

Calamites communis, Ettingsh. Cyatheites Miltoni, Goepp.
Annularia fertilis, Sternd. arborescens, Goepp.
Asterophyllites chareformis, Sternd.| Pecopteris Silesiaca, Goepp.

(=Calamitestenuifolius, Ztingsh.).| Lepidodendron Haidingeri, Ettingsh.
Schizopteris Gutbierana, Presi. plumarium, Lindi.

Dictyopteris Brongniarti, Guz. Cardiocarpon emarginatum, Goepp.
(=Neuropteris squarrosa, Eiz.). Stigmaria ficoides, Brongn.
Asplenites Sternbergi, Ettingsh. Cordaites borassifolia, Unger.
cristatus, Gutd. Flabellaria Sternbergi, Ez¢ingsh.
Cyatheites oreopteroides, Goepp. Sigillaria mammillaris, Brongn.

From above the upper coal-bed (20 feet* thick) Herr Stur ob-
tained :—

Calamites communis, E¢tingsh. Cyatheites orepteroides, Goepp.
Sphenophyllum emarginatum. Miltoni, Goepp.
Alethopteris pteroides, Brongn. Cordaites borassifolia, Unger.

Sphenopteris tenuissima, Sternd.

Herr Ludwig concludes with the following summary of results :—

1. The Bohemian coal-beds have not been formed of drifted Wood
or floated Plants, but of Plants which grew in the localities where the
coal is now found, partly in high-level and partly in low-level bogs. —

2. The formation of coal was faster and more continuous in the
‘southern portion of the coal-field than in the northern,—probably
because the former afforded more favourable situations for the growth
of Sigillaria, Stigmaria, and Calamites, while the northern district
was a more suitable locality for the growth of Ferns.

3. In all the basins the coal occurs in shallow unconnected troughs.

4, The coal-formation consists of two divisions. The greater
number of troughs belong to the lower, which is also the richest in
coal. To the upper division belong the beds of Stradonitz and some
seams near Rakonitz.

5. Above the Carboniferous formation are beds belonging to the
Rothliegende, and which contain coal in the Basin of Rakonitz.
In the Basin of Pilsen the red clay [Letten] and sandstone occurring
between Pilsen and Nirschan belong to this formation, as also in all
probability do the greater part of the sandstones and conglomerates
of the Basin of Buschtiehrad.

6. Like the Rothliegende, the coal-beds of Bohemia are terrestrial
[Festland] and freshwater formations.

7. The flora of the Bohemian coal-beds proves that they were
formed almost contemporaneously with those of the remaining
German coal-fields. The Bohemian beds have, it is true, only about
40 per cent. of Plants in common with other German coal-fields, the
remaining 60 per cent. being peculiar to them; and it should also
be mentioned that, as Herr Stur observes, the occurrence of Knorria
umbricata, Sternb., and Sagenaria Veltheimiana, Sternb., renders it
probable that the formation of the coal-beds in Bohemia began
earlier, and, as it extended into the Rothliegende, ended later than
in most other German coal-fields. [H.M.J.]

* German feet.

30 : GEOLOGICAL MEMOIRS,

On some Fosstis from Guapatoure, By M. Payen.

[Sur divers fossiles trouvés aux Environs de la Basse-Terre (Guadeloupe). Par
M. Payen. Bulletin de la Société Géologique de France. Deuxiéme Série,
Juillet 1863, vol. xx. p. 475.]

Tue fossils which are described in this paper were obtained from

two localities in the neighbourhood of the Basse-Terre, elose to the

Old Fort, Guadaloupe. They belong to the genera Pecten, Tere-

bratula, Cyprwa, Spatangus, and Echinus, and were imbedded in a

white or greyish-white limestone, haying the appearance of chalk.

One locality is about 50 yards from the shore, and about 40 yards

above the level of the sea. The bed which contains the fossils ap-

pears to have been deposited against the flank of a meuntain, whick
is composed of volcanic tufa. The other locality, which is about

100 yards from the former, is 200 yards from the sea, and has an

altitude of about 100 yards above high water. It forms the summit

of a conical hill; and the stone, which is burned for its ime, hes in
horizontal beds on the volcanic formation.

M. Deshayes considers the fossils to have belonged to the Quater-
nary period, and the two fossiliferous beds to have been elevated
contemporaneously with the formation of the existing contours of
the Island of Guadaloupe. The Terebratula, however, is considered
to belong to a new species. Ne recent Terebratule have yet been
found on the shores of Guadaloupe, and M. Schram, who is well ac-
quainted with the Natural History of the region, denies their ex-
istence in the West Indian seas. He notices, however, the Orlicula
Antillarum, D’Orbigny, as having been found living on the reefs.
M. Charles Sainte-Claire Deville had previously noted the existence
of the calcareous stratum in 1842. FP. M. D.]

On the Gronoey of Darmatia. By Fr. Rirrer von Haver,
Dr. Sracuz, and Dr. Zrrreu.
[ Proceed. Imp. Geol. Instit. Vienna, March 3, 1863.]

Barren and denuded ranges of limestone of Cretaceous or Eocene
origin, running parallel to the coast, with abrupt slopes towards
longitudinal or transverse valleys, or towards the coast of the Adriatic,
impress this country with a peculiar feature. Some strata of Eocene
Carpathian sandstones, intercalated between the undulating beds of
more ancient limestones, and some freshwater basins (as those of
Siverich and of Sign, with Lignite-beds and abundant Mollusca),
are met with in some localities. The Eocene series (in descending
order) consists of (1) sandstones and conglomerates, (2) Nummulitie
Limestone, (3) Borelis limestone, and (4) freshwater (Casina) strata,
They form a broad continuous band in the interior of the country,
between the River Kerka and the Mane de Novigrad, giving off some
branches southward, and gradually thinning towards the Cretaceous
deposits. Three Eocene ranges may be traced through Southern
Dalmatia,—one running from Spalato along the coast, over the
mouths of the Narenta, Ragusa, and Bocca di Cattano (with in-
creasing breadth) to Budua; another from Xernoyizza (EK, of Spa~

SUESS——MAMMALIAN REMAINS. ax

lato), over Vergoraz, to the banks of the Narenta; anda third through
the Isle of Lerina and on the south side of the Peninsula of Sabion-
cello. The Cretaceous rocks, here and there interrupted by Eocene,
and vece versd, prevail along the coast; and on the islands their
upper strata are characterized by Caprotine, and their lower beds
by Radioltes and Hippurites. Old Carpathian or Vienna Sandstones
(probably equivalent to the Upper and Middle fossiliferous Creta-
ceous strata) are totally wanting in Dalmatia. Jurassic, Triassic,
and eruptive rocks are confined toe some few isolated and very re-
stricted localities. [Count M. ]

Ow Kocrne Fossits from Isrrta. By Dr. Sracue.
[ Proceed. Imp. Geol. Instit. Vienna, March 3, 1863. ]

THESE organic remains were found in a Nummulitic Limestone of
Middle Eocene age, equivalent to the “Calcaire gressier” of the
Paris tertiaries. Their special locality is the Colle Canis, near Pisino,
where they occur in a marly conglomerate, immediately above a very
thin seam of inferior Nummulitic Limestone resting on Cretaceous
limestone. Among them are Cancer punctulatus, Desm., Nautilus
lingulatus (not known before from the Istrian Eocenes), Nautilus
umbilicaris, Desh., Pleurotomaria Deshaysiri, Lam., Voluta crenulata,
Lam., Cassidaria carinata, Lam., Scalaria crispa, Lam., Corbula
exarata, Lam., Newra Pisinensis (a new species of a genus but
scarcely represented in the Paris Eocenes), Vummulites distans, Desh.,
and Nummultes Dufrenoyi, D’Arch. & Haime, with undetermined
species of the genera Carcharias, Oxyrhina, Voluta, Xenophora, Te-
redo, Oardium, Trochocyathus, and Micraster,
[Count M.]

On some recently discovered MamMatian Remains. By Prof. Svzss,
[ Proceed. Imp. Geol. Instit. Vienna, March 2, 1863.]

A WELL-PRESERVED, although strongly compressed, skull of Hyothe-
rium Meissnert, a Porcine Pachyderm, has lately been found at
90 fathoms’ depth, in the brown coal of Hart, near Gloggritz (south
of Vienna). ‘The incisor, canine, and molar teeth of both jaws are
distinctly perceivable. These remains prove the brown coal of Hart
to be coeval (as are also the brown coals of Tauling and Schauer-
leithen) witL the Marine Neogene deposits of the Vienna Basin,
A fine and uncommonly large canine tooth of Anthracotherium mag-
num has been found in the coal of Lukawitz (N.W. Bohemia). This
fossil, together with the vegetable remains found there by the late
Mr. Jokely, prove this coal to belong to the Oligocene period, and
consequently to be coeval with those of Solzka in Carniola, Zo-
vencedo in Venetia, and Monte Promina in Dalmatia.
[Count M.|

82 GEOLOGICAL MEMOIRS.

On the OccurRENCE of the Nummvtiric Formation in Japan and the.
PuitrePines. By Frerpinanp von RicHTHoFEn.

[Ueber das Vorkommen von Nummulitenformation auf Japan und den Philip-
pinen; von Ferdinand Freiherr von Richthofen. Zeitschrift der Deutschen
geologischen Gesellschaft. Band xiv. Heft 2. Februar—April 1862, p. 357.]
Toe Nummulitic formation has hitherto been known to extend east-
wards only so far as British India, and southwards scarcely so far as
the Tropic of Cancer. In Java it has not been found; for it appears
that in this island the Orbitolites, which occur very abundantly in
Trachyte-tuff, have been mistaken for Nummulites. The mining
engineers of the Dutch East Indies mention the presence of Nummu-
litic rocks in the southern part of Borneo, where they are said to
contain coal. It is possible, however, that these beds are a repeti-
tion of the Orbitolite-containing strata of Java. The author was
therefore all the more interested in finding, in September 1860,
evidence of the Nummulitic formation in Eastern Japan, and conse-
quently about fifty degrees further eastward than it was known
before to occur. In May 1861 he also discovered the formation in
Luzon, near the fourteenth degree of north latitude.

In the stone-polishing establishments at Yokohama, near Yeddo,
the author purchased small boxes and pebbles, consisting of a blackish
marly limestone, containing abundance of Nummulites; he was in-
formed that the stone was obtained from a mountain lying eastward
from Yeddo,—probably in the Principalities of Simosa and Kadsusa,
and that it oceurred in very large masses. These few pieces are
sufficient to prove the occurrence in Japan of the Nummulitic forma-
tion ; and of it they are at present the only evidence.

In Luzon, on the contrary, the Nummulitic formation appears to be
very widely distributed, and is an important element in the consti-
tution of the island. The author then describes the distribution of
the limestone in the neighbourhood of the well-known limestone-
quarry near Manila, called the Caeva de San Matteo; he remarks
that fossils have often been searched for in this limestone, but that,
as none had been found, it was supposed to be at least of Jurassic
age; he was so fortunate, however, as to search in a quarry where
Nummulites occurred in it in abundance, together with a few obscure
Oysters. The Nummulites are of various sizes, and belong to several
species.

Herr von Richthofen also found the same Eocene formation on
the south coast of the Island of Mindarao, where it possesses, how-
ever a more varied lithological character—consisting of limestone,
sandstone with Plant-remains, shale, and marl. He concludes by
remarking on the improbability of the Nummulitic Limestone of
Nippon and Luzon being isolated patches, and infers that the limits
of the old Nummulitic sea must be extended from the Himalaya
Mountains through China to Japan, and also so as to include the
remaining Philippine Islands. [H. M. J.]

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. |

Abbeville, flint implements from, 497 ;
section at Moulin Quignon, near,
497, 501.

Aberuchil quarry, sketch of contortions
in slate in, 194.

Acrodus Flemingianus, 17.

,n. sp., 16.

Adams, Dr. A., on the Miocene beds
of Malta, 277.

Agaricia agaricites, 437.

undata, var., 437.

Alge, 467.

Alveolites septosa?, 4.

Alveopora Dedalza, var. minor, 426.

, var. regularis, 426, 442.

fenestrata, 426, 437.

microscopica, 426.

America, Crustacea from the Coal-mea-
sures and Devonian rocks of Bri-
tish North, 75; Devonian Plants of
North, 458; flora of the Devonian
period in north-eastern, 157.

Ammonites of the Cambridge Green-
sand, Mr. H. Seeley on the, 519.

Amphipeltis paradoxus, 76.

Anarthrocanna Perryana, 461.

Anderson, Dr. G., on the occurrence of

a bituminous substance near Mount-
gerald, 522.

Anniversary Address of the President,
xxix-lii. _ See also Ramsay, Prof.
A. C.

Annual Report, i.

Anomia Lawrenciana, 6.

Anthracomya elongata, 79.

Anthracoptera carbonaria, 79.

Anthracosaurus Russelli, 56; affinities
of, 62; Prof. T.. H. Huxley on, 56.

Antigua, fossil Corals from, 412, 445;
geology of, 408.

Antrum of the hyzna-den at Wookey
Hole, 260.

Applegath, Capt. A., on the geology of
a part of the Masulipatam district,
32.

Argas, 90.

Argyleshire, 40-feet beach of, 253; list
of Shells from, 254.

Artesian wells at Barracas and Buenos
Ayres, comparative sections of the,
69; detailed section of the, 70.

Artiodactyla from Wookey Hole, 271.

Asia (central) during the Glacial period,
257.

Astrea Antigquensis, 419.
Antillarum, 443.
Barbadensis, 421, 444.
cellulosa, 417.

, var. curvata, 418.
costata, 422.
crassolamellata, 412,

, var. magnetica, 415.
, var. magnifica, 417.
, var. minor, 416.

, var. nobilis, 416.

, var. Nugenti, 416.

, var. pulchella, 415.
cylindrica, 434.
endothecata, 434.

, var. 1, 419.

, var. 2, 420.

, var. 3, 420.

— megalaxona, 420.

radiata, var. intermedia, 421.
tenuis, 421.

Astreina Dendroidea, 442.
Astroceenia decaphylla, 440, 514.
ornata, 425,

Astroria affinis, 425.

BOUeeeeuene

INDEX TO THE PROCEEDINGS,

Astroria Antiguensis, 425.

polygonalis, 424.

Athyris subtilita, 170.

Austin, C. E., Esq., geological notes on
the locality in Siberia where fossil
Fish and Esther have been found,
with a note on LEstheria Midden-
dorfii, by Prof. T. Rupert Jones, 71.

Award of thé Wollaston Donation-
fund, xxviii; medal, xxvii.

Aymestry Limestone at Mocktree, sec-
tion in the, 369.

Azoic rocks of Bavaria and Bohemia,
304.

Barbadoes, fossil Corals from, 444, 452.

Barbuda, fossil Coral from, 443, 452.

Barracas, section of the Artesian well
at, 69, 70.

Barysmilia intermedia, 431.

Bassenthwaite, Skiddaw slates of, 114,
119.

Bath, section from Cheltenham to, 309.

Bavaria and Bohemia, Gneiss, and
other Azoic rocks, and the Paleozoic
formations of, 354; geological sketch-
map of, 356.

Bed of the Brahmapootra, change in
the, 333.

Belgium, Devonian rocks of, 489.

Bellerophon decipiens, 8.

Jonesianus, 9.

orientalis, 9.

Bengal, Upper Cretaceous rocks in
Eastern, 524.

Ben Ledi, 187; section of, 188; Nevis,
204; porphyry-vein in granite at,
205.

Beyrichie, 90.

Bhagaruttee River, 338.

Bigsby, Dr. J. J., on the Cambrian
and Huronian formations, 36.

Binsey Crag, Skiddaw slates of, 114.

Bischof, Prof. G., award of the Wol-
laston Medal to, xxvii.

Bituminous mineral from Mountgerald,
Dr. G. Anderson on a, 522; Mr.
A. C. Mackenzie on a, 522.

Black Comb, section across, 131 ; Skid-

- daw slates of, 131.

Black Mount, 200.

Black Ven, 280; vertical section of the
Middle Lias at, 281.

Blairgowrie, 196.

Bohemia and Bavaria,geologicalsketch-
map of, 356; Gneiss, and other Azoic
rocks, and the Palzozoic formations
of, 354.

Bohemia, Permian rocks of north-
eastern, 297 ; Silurian rocks of, 364.

Bones found in Wookey Hole, table of
the, 266.

Borneo and the adjacent Islands, mine-
ralogy and geology of, 515.

Bouldon quarry, vertical section of the
beds exposed at, 233.

Brachiopoda of Nova Scotia, Mr. Da-
vidson on the, 158.

Brachycyathus Henekeni, 426.

Braemar, 200; section from Glen Shee
to, 201.

Brahmapootra River, 330; change in
the bed of the, 333.

Brick-pit at Lexden, near Colchester,
Coleoptera from the, 400; fossils
from the, 398; section through the,
395; the Rey. O. Fisher on the, 393.

British North America, Mr. J. W.
Salter on Crustacea from the Coal-
measures and Devonian rocks of, 75.

Bryozoon?, 137.

Buenos Ayres, section of the Artesian
well at, 69; thickness of the Pam-
pean formation near, 68.

Burton Cliff, Lias of, 287.

Bute, clay-slate formation of, 182.

Caldbeck-fells, Skiddaw slates of, 124.

Caldy Island, Upper Old Red Sand-
stone of, 476.

Camarophoria? globulina?, 171.

Cambrian and Huronian formations,
Dr. J. J. Bigsby on the, 36; rela-
tions of the, 51.

Cambrian epoch, stages in the, 40.

Cambrian formation, abundance of life
above the, 42; characters of the, 37 ;
geographical conditions of the, 36;
paucity of fossilsin the, 41 ; stratigra-
phical characters of the, 40; synopsis
of the, 44; typical form and distri-
bution of the, 37.

Cambridge Greensand, Mr. H. Seeley
on the Ammonites of the, 519.

Canada, Devonian Plants of, 465;
Huronian formation of, 45.

Carboniferous and Permian periods,
faunz of the, 161.

Carboniferous Brachiopoda of Nova
Scotia, 158; Reptiles, Dr. J. W.
Dawson on the dermal coverings of
certain, 469 ; slate, fossils of the, 488.

Carnivora from Wookey Hole, 269.

Carpolithes lunatus, 464.

? stliqua, 465.

spicatus, 461.

Carrock-fells, Skiddaw slates of, 124.

Caryocaris Wrightii, 137.

Caverns near Ulverston, 20.

eal Asia during the Glacial period,
257.

Ceratiocaris, 90.

Ceratites Buchianus, 13.

Davidsonianus, 13,

INDEX TO THE

Ceratites Flemingianus, 10.

Hauerianus, 12.

latifimbriatus, 13.

Lawrencianus, 14.

— Lyellianus, 12.

—- Murchisonianus, 11.

planulatus, 12.

Change in the bed of the Brahma-
pootra, 333.

Changes in the course of the River
Teesta, 341; delta of the Ganges,
historical evidence of, 348 ; valley of
the Ganges, 329.

Cheltenham to Bath, section from, 309.

Cidaris Forbesiana, 4.

Clay-slate and Mica-slate of the south-
ern Grampians, 197.

Clay-slate formation of Bute,182 ; Loch
Creran, 202.

Cleavage-foliation in Mica-schist from
Muchuls, 405.

Clisiophyllum Indicum, 3.

Coal-field, new Crustacean from the
Glasgow, 519; Labyrinthodont from
the Lanarkshire, 56.

Coal-formation of Nova Scotia, Mr.
O. C. Marsh on a new Enaliosaurian
from the, 52.

Coal-measures of British North Ame-
rica, Crustacea from the, 75.

Celoria dens-elephantis, 424.

Colchester, Brick-pit at Lexden, near,
395.

Coleoptera from the Brick-pit at Lex-
den, near Colchester, 400.

Comrie, 189; section at, 190.

Coniferous wood (Dadoxylon et Apo-
roxylon), 460.

Contortions in slate, Aberuchil quarry,
sketch of, 194.

Coomhola series, fossils of the, 488.

Coprolites with Lingul, 42.

Corals from Jamaica, Dr. P. Martin
Duncan on, 515; of the West Indian
Islands, Dr. P. Martin Duncan on
the fossil, 406.

Cordaites (Pychnophyllum) flexuosus,

462.

Cotteswolds, Inferior Oolite of the, 310.

Council, Report of the, i.

Cretaceous and Tertiary rocks of Ja-
maica, section of the, 515.

Cretaceous rocks in Eastern Bengal, Dr.
T. Oldham on the occurrence of Up-
per, 524 ; list of fossils from the, 526.

Crustacea from the Coal-measures and
Devonian rocks of British North
America, Mr. J. W. Salter on, 75.

Crustacea, Mr. J. W. Salter on a new
genus of Silurian, 87.

Crustacean from the Glasgow coal-field,

PROCEEDINGS.

Mr. J. W. Salter on a new, 519
from the Lias of Lyme Regis, Mr.
H. Woodward on a new, 318.

Crustacean tracks, 92, 234; from the
Old Red Sandstone near Ludlow,
Mr. G. E. Roberts on, 233.

Crustaceans, tracks of, 42, 233.

Cumberland, Skiddaw slates of, 119.

Curley, T., Esq., on the gravels and
other superficial deposits of Ludlow,
Hereford, and Skipton, 175.

Curtonotus centralis, 496.

elegans, 495.

elongatus, 496.

Unio, 495.

Cyclopteris Brownii, 463.

Jacksoni, 462.

Rogersi, 463.

Cyperites, 460.

Cyphastrza costata, 441, 443.

Dalton Road Pit, near Ulverston, plan
of, 28.

Darwin, C., Esq., on the thickness of
the Pampean formation near Buenos
Ayres, 68.

Davidson, T., Esq., on the Lower Car-
boniferous Brachiopoda of Nova
Scotia, 158.

Dawkins, W. B., Esq., on a hyzna-den
at Wookey Hole, near Wells, No. IL.,
260.

Dawson, Dr. J. W., further observa-
tions on the Devonian Plants of
Maine, Gaspé, and New York, 458 ;
notice of a new species of Dendrer-
peton, and of the dermal coverings of
certain Carboniferous Reptiles, 469.

Day, E. C. H., Esq., on the Middle
and Upper Lias of the Dorsetshire
coast, 278.

De la Beche’s, Sir H., subdivision of
the Dorsetshire Lias, 278.

Delta of the Ganges, eastern gap in
the seaward face of the, 332; histo-
rical evidence of changes in the,
348 ; increase seaward, 350; Mr. J.
Fergusson on recent-changes in the,
321.

Deltas, mode of elevation of, 328;
secular elevation of, 326.

Dendrerpeton, Dr. J. W. Dawson on
a new species of, 469.

Oweni, 470.

Dentalium Herculeum, 8.

Derwentwater, Skiddaw slates of, 114,
tS:

Devonian fossils from Landlake and
Petherwin, list of Upper, 483; Plants
of Maine, Gaspé, and New York,
Dr. J. W. Dawson on the, 458;
period, flora of the, 157; rocks,

INDEX TO THE PROCEEDINGS.

Mr. J. W. Salter on the Upper Old
Red Sandstone and Upper, 474; of
British North America, Crustacea
from the, 75.

Devonshire and South Ireland, gene-
ralized section in, 479.

mites Upper Devonian rocks of,
478.

Diagram illustrating the secular eleva-
tion of deltas, 327.

Diagram-section across the bed of a
river, 325.

Diagrams illustrating the junctions of
tributary streams with main rivers,

Diatomacex, deposit containing, near
Ulverston, 19.

Diatomacez in the Lindale Cote de-
posit, near Ulverston, 29; list of, 30.

Dichocenia tuberosa, 482.

Dichograpsus aranea, 137.

, branchlet of, 137.

Sedgwickii, 137.

Dictyocaris, 90.

Didymograpsus, 137.

Diplostylus Dawsoni, 77.

Dithyrocaris, 90.

Donations to the Library, xi, 96, 210,
372, 527; Museum, viii.

Dorsetshire coast, Taias of the, 278;
generalized section of the, 288.

Dorsetshire Lias, subdivision of the,278.

Down Cliffs, 284; vertical section of
the Middle and Upper Lias at, 285.

Duncan, Dr. P. M., note on the fossil
Corals accompanying the Testacea
from Jamaica, 513; on the fossil
Corals of the West Indian Islands
(Part I.), 406.

Dunkeld, 196.

Echinide of Malta, Dr. T. Wright on
the, 277.

Elevation of the banks of rivers, 324;
deltas, mode of, 328; secular, 326.
Enaliosaurian from the Coal-formation
of Nova Scotia, Mr. O. C. Marsh on

a new, 52.

England, Inferior Oolite of the middle
and south of, 306.

Entomostraca of the Carboniferous and
Permian periods, 162.

Eosaurus Acadianus, 52; chemical
composition of the vertebrz of, 55;
habits of, 55; locality of, 53; verte-
tebrze of, comparison with other ver-
bre, 54; microscopic structure of
the, 54; osteological description of
the, 53.

Estheria, 90.

Estheria concentrica, 153.

elliptica, 154.

Estheria exigua, 145.

Forbesii, 155.

Kotahensis, 149.

Mangaliensis, 149.

membranacea, 142.

—— Middendorfii, 73, 155.

minuta, 146.

, var. Brodieana, 148.

oo ee ionie 154.

ovata, 151.

—- Portlockii, 146.

— striata, 143.

, var. Binneyana, 144.

tenella, 144.

Estheriz and their distribution, Prof. T.
R. Jones on, 140; from Siberia,71,73.

Estheriz and Leaiz, table of the fossil,
141.

European Trias, Estheria minuta in
the, 146.

Eurypterus, allied to H. Scouleri, 78.

? (Arthropleura) ferox, 86.

—— (Arthropleura?) mammatus, 85.

—— pulicaris, 78.

— Scouleri, 82.

(2) tail of, 78.

Fenestella megastoma, 5.

? Sykesit, 5.

Fergusson, J., Esq., on recent changes
in the Delta of the Ganges, 321.

Filices, 464.

Fish from Siberia, 71. -

Fisher, Rev. O., on the Brick-pit at
Lexden, near Colchester ; with notes
on the Coleoptera, by T. V. Wollas-
ton, Esq., M.A., 393.

Fishes in the Roth-liegende, 303.

Flabellum dubium, 429.

—, sp., 430.

Fleming, Dr. A., fossils from India dis-
covered by, 1

Flint implements found at Moulin
Quignon, Mr. J. Prestwich on the
peculiar character of some, 497.

Flora of the Devonian period, Dr. J.
W. Dawson on the, 157.

Footprints of Reptiles from the Ross-
shire sandstones, 506.

Fort William, 204.

Fossil Corals from Jamaica, Dr. Dun-
can on the, 437, 451, 518; of the
West Indian Islands, Dr. Duncan on
the, 406 ; list of, 410 ; Crustacea from
the Coal-measures and Devonian
rocks of British North America, Mr.
J. W. Salter on, 75; Echinidz of
Malta, Dr. T. Wright on the, 277;
Estheriz and their distribution, Prof.
T. R. Jones on, 140; Fish and Es-
theriz from Siberia, Mr. C. E. Aus-
tin on, 71.

INDEX TO THE PROCEEDINGS,

Fossil Plants from the Oolites of Scar-
borough, 519 ; Wood in the Oxford
Clay near Peterborough, Dr. H. Por-
ter on, 317.

Fossils in the Cambrian formation, pau-
city of, 41; Lias of the Dorsetshire
coast, 290 ; Roth-liegende, 302 ; from
British North America, 75; India,
Prof. de Koninck on, 1; Jamaica,
511; Landlake and Petherwin (Up-
per Devonian), list of, 483; the
Brick-pit at Lexden, near Colches-
ter, 398; Nummulitic limestone of
eastern Bengal, 526; Skiddaw
Slate, Mr. J. W. Salter on, 135;
Upper Cretaceous rocks of eastern
Bengal, list of, 526; Carboniferous
Slate, 488; Coomhola series, 488;
Inferior Oolite, geographical distri-
bution of the, 316; Lowest Silurian,
42; Primordial zone, 43; summary
of the, 44; Upper Ragstone, 313.

Fourfoot Hill, Lias of, 286.

France, Devonian rocks of, 489.

Ganges, alterations in the bed of the,
334; historical evidence of changes
in the delta of the, 348; increase
seaward of the delta of the, 350;
physical changes in the Valley of the,
329; recent changes in the delta of
the, 321; silt held in suspension in
the, 350.

Gareloch, section on, 182.

' Gaspé, Canada, Devonian Plants of,
465.

Generalized section in Devonshire and
South Ireland, 479 ; Pembrokeshire
and North Ireland, 479.

Geological distribution of Phyllopoda,
90; notes on the locality in Siberia
where fossil Fish and Estheriz have
been found, 71; sketch-map of Ba-
varia and Bohemia, 356; Ludlow,
177 ; structure of thesouthern Gram-
pians, Prof. J. Nicol on the, 180.

Geology and mineralogy of Borneo
and the adjacent islands, M. Corn.
de Groot on the, 515.

Geology of Antigua, 408 ; a part of the
Masulipatam district, Capt. F. Ap-
plegath on the, 32.

Germany, Devonian rocks of, 489.

Glacial action on the west side of Scot-
land, 258.

Glacial period, central Asia during the,
257 ; history of the, 251.

Glasgow coal-field, Labyrinthodont
from the, 56; new Crustacean from
the, 519.

Glencoe, 203.

Glen Nevis, section of the south side

of, 205; upper part of, 206; Roy,
Mr. T. F. Jamieson on the parallel
roads of, 285; Shee, 200; section
from, 201 ; Treig, glacier of, 247.

Gloucestershire, Upper Devonian of,
485.

Gneiss and other Azoic rocks of Bava-
ria and Bohemia, Sir R.I.Murchison
on the, 354.

Gneiss and Quartzite of the southern
Grampians, 199.

Golden Cap, 282; vertical section of
the Middle Lias at, 283.

Goniatites? Gangeticus, 14.

Gordon, Rey. Dr. G., and Rev. J. M.
Joass, on the relations of the Ross-
shire sandstones containing Repti-
lian footprints; with an Introduction
by Sir R. I. Murchison, K.C.B., 506.

Grampians, geological relations of the,
207 ; structure of the southern, 180.

Granite, porphyry-vein in, 205.

Granite with the Tertiary strata near
Kingston, Jamaica, Mr. J. G. Saw-
kins on the association of, 35.

Graptolites from the Skiddaw Slate,
135.

Gravels and other superficial deposits
of Ludlow, Hereford, and Skipton,
Mr. T. Curley on the, 175.

Gravels, sections illustrating the forma-
tion and emergence of, 504.

Gravel-pit at Moulin Quignon, section
of the, 501; St. Acheul, section of
the, 501.

Greensand of Cambridge, Ammonites
of the, 519.

Groot, Mijnheer C. de, notes on the
mineralogy and geology of Borneo
and the adjacent islands, 515.

Ground-plan of the hyzna-den at
Wookey Hole, 261.

Guadaloupe, fossil Corals from, 452 ;
list of, 412.

Giimbel, M., geological sketch-map of
Bavaria and Bohemia, 356.

Halfway House, section at the, 307.

Harkness, Prof. R., on the Skiddaw
Slate Series; with a note on the
oe by J. W. Salter, Esq.,

13.

Hereford, gravels of, 179; section
across, 178.

Historical evidence of changes in the
delta of the Ganges, 348.

Hodgson, Miss E., on a deposit con-
taining Diatomacez, Leaves, &c. in
the iron-ore mines near Ulverston, 19.

Hof to Selb, section from, 360.

Holl, Dr. H. B., on the correlation of
the several subdivisions of the In-

INDEX TO THE PROCEEDINGS.

ferior Oolite in the middle and south
of England, 306.

Hoogly River, 338.

Horner, L., Esq., reply on receiving
for Prof. Bischof the Wollaston Me-
dal, xxvii.

Horton Rectory, section near, 310.

Huronian and Cambrian formations,
Dr. J. J. Bigsby on the, 36; rela-
tions of the, 51.

Huronian formation, characters of the,
45; connexion with the Laurentian,
47 ; geographical distribution of the,
46; geological position of the, 45;
igneous rocks in the, 47; lithological
characters of the, 46; of Canada, 45 ;
Norway, 49; the south shore of
Lake Superior, 48 ; regional affinities
of the, 45; synopsis of the, 52;
typical form of the, 46.

Huxley, Prof. T. H., description of
Anthracosaurus Russelli, a new La-
byrinthodont from the Lanarkshire
coal-field, 56.

Hyzna-den at Wookey Hole near
Wells, Mr. W. Boyd Dawkins on a,
260; plan of the, 261.

Hymenocaris, 90.

Tgneous rocks in the Huronian forma-
tion, 47.

India, Prof. de Koninck on fossils
from, 1; table of the Mesozoic and
Paleozoic formations of, 150.

Inferior Oolite from Cheltenham to
Bath, section of the, 309; geogra-
phical distribution of the fossils of
the, 316; of the Cotteswolds, 510;
middle and south of England, Dr.
H. B. Holl on the, 306; south side
of the Mendips, 307.

Treland (North), generalized section in
Pembrokeshire and, 479.

Ireland (South), generalized section in
Devonshire and, 479.

Treland, Upper Devonian of South, 487.

Iron-ore mines near Ulverston, Miss-
E. Hodgson on a deposit containing
Diatomacee, Leaves, &e. in the, 19.

Isastrea arachnoidea, 3.

conferta, 422.

turbinata, 423.

Jamaica, association of Granite with
the Tertiary strata near Kingston,
35; Dr. P. Martin Duncan on Co-
rals from, 437, 451, 518; Mr. J. C.
Moore on Tertiary Shells from, 510;
Prof. T. Rupert Jones on Nummu-
linze and Orbitoides from, 514; sec-
tion of the Tertiary and Cretaceous
rocks of, 515.

Jamieson, T. F., Esq., on the parallel

roads of Glen Roy, and their place
in the history of the Glacial period,
235.

Jaws and teeth found in Wookey Hole,
table of the, 267.

Jeffreys, J. Gwyn, Esq., list of Shells
from the 40-feet beach of Argyle-
shire, 254.

Jellinghy River, 338.

Jennai River, opening of the, 333.

Jessore group of rivers, 334.

Joass, Rev. J. M., and the Rev. Dr. G.
Gordon, on the relations of the Ross-
shire sandstones containing Repti-
lian footprints; with an Introduc-
tion by Sir R. I. Murchison, K.C.B.,
506.

Jones, Prof. T. Rupert, on Estheria
Middendorfii, 73 ; on fossil Estherize
and their distribution, 140; on some
Nummulinz and Orbitoides from
Jamaica, 514.

Junctions of tributary streams with
main rivers, 342.

Kingston, Jamaica, association of Gra-
nite with the Tertiary strata near, 35.

Kishnaghur group of rivers, 338.

Koninck, Prof. L. de, descriptions of
some fossils from India, discovered
by Dr. A. Fleming, of Edinburgh, 1.

Labyrinth-Berg, near Hof, to Selb,
section from the, 360; the Watch-
tower, section from the, 360.

Labyrinthodont from the Lanarkshire
coal-field, Prof. T. H. Huxley on a
new, 56.

Lake-district, Skiddaw slates of the
eastern margin of the, 126.

Lake Superior, Huronian formation of,

Lanarkshire coal-field, Prof. T. H.
Huxley on a new Labyrinthodont
from the, 56.

Lancaster and Carlisle Railway, section
at the Summit-cutting on the, 130.
Landlake and Petherwin fossils, list

of, 483.

Laurentian formation, connexion with
the Huronian, 47.

Leaia, 155.

Leaiz, table of the fossil Estherie and,
141.

Leaves, deposit containing, near Ulver-
ston, 19.

Leckenby, J., Esq., on the Sandstones
and Shales of the Oolites of Scar-
borough, with descriptions of new
species of fossil Plants, 519.

Leintwardine, section at Mocktree near,
368.

Leny limestones, 186 ; old lime-quarry,

INDEX TO THE PROCEEDINGS.

oe at, 187; section in Pass of,

D.

Leperditia, 90.

Leptophleum rhombicum, 462.

Lexden, near Colchester, the Rev. O.
Fisher on the Brick-pit at, 393.

Lias of the Dorsetshire coast, Belem-
nite-beds of the, 289; brown sands
and sandstones of the, 293 ; Cephalo-
poda-beds of the, 295; generalized
section of the, 287; green Ammonite-
beds of the, 291; grey and brown
sands with nodules, 292; marlstone
with its Pleurotomaria-bed, 293;
Mr. E. C. H. Day on the, 278;
Shell-bed of the, 291; Starfish-bed
of the, 292; three tiers of the, 291 ;
upper Lias limestone of the, 295;
Lyme Regis, new Macrurous Crusta-
cean from, 318.

Library Committee, report of the, iv.

Library, donations to the, xi, 96, 210,
372, 527.

Lightbody, R., Esq., notice of a section
at Mocktree, 368.

Lindale Cote deposit, Diatomaceze in
the, 29; Plants in the, 29; Mines
to Urswick Tarn, section from, 26;
district, near Ulverston, map of, 21 ;
Moor, swallow-holes on, 23.

Lingule, phosphatic coprolites with, 42.

Linley Brook, sketch of the Upper
Ludlow rocks and the passage-beds
at, 231; vertical section of the beds
exposed at, 232.

Linley, Salop, Upper Silurian passage-
beds at, 229.

List of Diatomacee in the Lindale
Cote deposit, near Ulverston, 30;
fossil Corals of the West Indian Is-
lands, 410; fossils from India de-
scribed by Prof. de Koninck, 2;
the Nummulitic limestone of eastern
Bengal, 526; Upper Cretaceous
rocks of eastern Bengal, 526; of the
Upper Ragstone, 313; Liassic fossils
from the Belemnite-bed, 290 ; brown
sands and sandstones, 293; Cepha-
lopoda-beds, 295; green Ammonite-
beds, 291; grey and brown sands
with nodules, 293; marlstone with
its Pleurotomaria-bed, 294; shell-
bed, 292; upper Lias limestone,
295; Petherwin and Landlake fossils
(Upper Devonian), 483; Plants com-
mon to the Carboniferous and Per-
mian periods, 162; Shells common
to the Carboniferous and Permian
periods, 163, 165; from the 40-feet
beach of Argyleshire, 254; Tertiary
Shells from Jamaica, 511.

Lithostrotion basaltiforme, 3.

irregulare, 3.

Loch Creran, clay-slate of, 202; Earn,
mica-slate of, 194; to Loch Tay,
section from, 195; Leven, 203 ; Lo-
mond, 183; section on, 183; Long,
182; Tay, section from Loch Earn
to, 195.

Lower Carboniferous Brachiopoda of
Nova Scotia, Mr. T. Davidson on
the, 158; Silurian Crustacea, tracks
of, 92.

Ludlow, Crustacean tracks from the Old
Red Sandstone near, 233 ; Hereford,
and Skipton, Mr. T. Curley on the
Gravels of, 175; geological sketch-
map of, 177; section across, 178.

Lycopodites comosus, 462.

Richardsoni, 461.

Lyme Regis, new Macrurous Crusta-
cean from the Lias of, 318.

Macdonald, J. D., Esq., description of
a new fossil Thecidium (Thecidium
Adams?) from the Miocene beds of
Malta, 517.

Mackenzie, A. C., Esq., on the occur-
rence of a bituminous mineral at
Mountgerald, Scotland, 522.

Macrocheilus avellanoides, 10.

depilis, 9.

Macrurous Crustacean from the Lias
of Lyme Regis, Mr. H. Woodward
on a, 318.

MadooporeJ ungle, upheaval of the,329.

Madrepora, sp., 445.

Meandrina filograna, 433.

.

, sp., 424.

Maine, Devonian Plants of, 459.

Malta, fossil Echinidz of, 277; Mio-
cene beds of, 277; new Thecidium
from the Miocene beds of, 517.

Map of Bavaria and Bohemia, 356;
Ludlow, 177; the Lindale district,
near Ulverston, 21; Skiddaw slate
district, 115.

Marsh, O. C., Esq., description of the
remains of a new Enaliosaurian (o-
saurus Acadianus), from the Coal-
formation of Nova Scotia, 52.

Masulipatam district, Capt. F. Apple-
gathon the geology of a part of the, 32.

Matabangah River, 338.

Matterdale to Uldale, section from, 120.

Megra River, 331.

Mendips, Inferior Oolite of the south
side of the, 307.

Mesozoic and Palzeozoic formations of
India, table of the, 150; periods,
faunz of the, 160.

Metamorphism of mica-schist, Mr. H.
C. Sorby on the, 401.

INDEX TO THE PROCEEDINGS.

Mica-schist from Muchuls, contorted
“ Ripple-drift” in, 405.

Mica-schist, Mr. H. C. Sorby on the
original nature and subsequent alter-
ation of, 401.

Mica-slate of Loch Earn, 195; the
southern Grampians, 197.

Michelinia favosa, 4.

Middle Lias, definition of the, 279.

Mineral from Mountgerald, Dr. G.
Anderson on a bituminous, 522;
Mr. A. C. Mackenzie on abituminous,
522.

Mineralogy and geology of Borneo
and the adjacent Islands, M. Corn.
de Groot on the, 515.

Miocene beds of Malta, Dr. A. Leith
Adams on the, 277; Mr. J. D. Mac-
donald on a new Thecidium from
the, 517.

Miocene formation of the West Indian
Islands, 452.

Mocktree, Mr. R. Lightbody on a sec-
tion at, 368; section in the Aymes-
try Limestone at, 369.

Montlivaltia ponderosa, 433, 441, 513.

Montserrat, fossil Coral from, 443,452.

Moore, J. C., Esq., on some Tertiary
Shells from Jamaica; with a note
on the Corals, by P. Martin Dun-
ean, M.B., F.G.S.; and a note on
some Nummuline and Orbitoides,
by Prof. T. Rupert Jones, F.G:S.,
510.

Moulin Quignon, Abbeville, Mr. J.
Prestwich on the section at, 497;
peculiar character of flint imple-
ments from, 497; section of the
gravel-pit at, 501.

Mountgerald, bituminous
from, 522.

Murchison, Sir R.I., on the Gneiss
and other Azoic rocks, and on the
superjacent Paleozoic formations of
Bavaria and Bohemia, 354; on the
Permian rocks of north-eastern Bo-
hemia, 297; on the relations of the
Ross-shire sandstones containing
Reptilian footprints, 506; reply on
receiving for Prof. Senft the Wollas-
ton Donation-fund, xxviii.

Museum Committee, report of the, ii;
donations to the, xiv.

Naiadites levis, 79.

Natore group of rivers, 336.

Nautilus Burtini, 15.

Flemingianus, 15.

Nebalia, 90.

Nematoxylon crassum, 466.

tenue, 467.

Nerina ?, n. sp., 10.

mineral

Nertchinsk, geology of the neighbour-
hood of, 71.

Newlands to Sunderland, section from,
116.

New York, Devonian Plants of, 468.

Nicol, Prof. J., on the geological struc-
ture of the southern Grampians, 180.

‘No Ground,” swatch of, 351.

North America, Crustacea from the
Coal-measures and Devonian rocks
of British, 75.

Norway, Huronian formation of, 49.

Nova Scotia, Lower Carboniferous
Brachiopoda of, 158; new Enalio-
saurian from the Coal-formation of,
52.

Nummulinz and Orbitoides from Ja-
maica, Prof.T. Rupert Jones on,514.

Nummulitic limestone of eastern Ben-
gal, 524 ; list of fossils from the, 526.

Oculina, sp., 445.

Oldham, Dr. T., on the occurrence of
rocks of Upper Cretaceous age in
eastern Bengal, 524.

Old Red Sandstone and Upper Devo-
nian rocks, Mr. J. W. Salter on the
Upper, 474.

Old Red Sandstone near Ludlow,
Crustacean tracks from the, 233;
of the southern Grampians, 197.

Oolite of the Middle and South of
England, Dr. H. B. Holl on the In-
ferior, 306.

Oolites of Scarborough, Mr. J. Lecken-
by on fossil Plants from the, 519.
Orbitoides from Jamaica, Prof. T.

Rupert Jones on, 514.

Organic remains from the Brick-pit at
Lexden, near Colchester, 398.

Orthoceras decrescens, 16.

rachidium, 16.

vesiculosum, 15,

Oscillations of rivers, table of the, 324.

Oxford Clay, near Peterborough, fossil
wood in the, 317.

Paleocarabus Russellianus, 520.

Palzozoic and Mesozoic formations of
India, table of the, 150; periods,
faune of the, 160.

Palzozoic formations of Bavaria and
Bohemia, Sir R. I. Murchison on
the, 354.

Pampean formation near Buenos Ayres,
Mr. C. Darwin on the thickness of
the, 68.

Paradoxides Davidis, 276.

in Britain, Mr. J. W. Salter on
the discovery of, 274.

Parallel Roads of Glen Roy, height of
the, 255; horizontality of the, 255;
in their relation to the Glacial pe-

INDEX TO THE PROCEEDINGS.

riod, 251; Mr. T. F. Jamieson on
the, 235; theories of the, 237.

Passage-beds at Linley, Salop, 229.

Pass of Leny, section in, 185.

Peat of Lexden Brick-pit, Coleoptera
from the, 400.

Pecten Asiaticus, 7.

crebristria, 8.

Flemingianus, 7.

Peltocaris, 87, 90.

aptychoides, 88.

—— ? Harknessi, 88.

——, Mr. J. W. Salter on, 87.

(?), Track of, 93.

Pembrokeshire and North Ireland,
generalized section in, 479.

Pembrokshire, Upper Old Red Sand-
stone of, 476.

Perissodactyla from Wookey Hole,
ye

Permian and Carboniferous periods,
faunz of the, 161.

Permian rocks of North-eastern Bo-
hemia, section across the. 301; Sir
R. I. Murchison on the, 297.

Perry, Maine, Devonian Plants of, 459.

Peterborough, fossil Wood in the Ox-
ford Clay near, 317.

Petherwin and Landlake fossils, list
of, 483.

Philocrinus cometa, 4.

Phosphatic coprolites with Lingule,
42

Phylloccenia limbata, 433.

sculpta, var. tegula, 432.

Phyllograptus, 137.

Phyllopoda, geological distribution of,
90

Phyllopora? cribellum, 6.

? Haimeana, 6.

Physical changes in the Valley of the
Ganges, 329.

Pilton group, sketches of Shells from
the, 495.

Placocyathus Barretti, 437, 513.

, var. 1, 428.

, var. 2, 428.

Placotrochus alveolus, 438, 513.

Lonsdalei, 428.

Plan of Dalton Road Pit, near Ulver-
ston, 28 ; the hyzna-den at Wookey
Hole, 261.

Plante incerte sedis, 467.

Plants common to the Carboniferous
and Permian periods, 162; from the
Oolites of Scarborough, Mr. J. Lec-
kenby on, 519; in the Lindale Cote
deposit, near Ulverston, 29; of
Maine, Gaspé, and New York, Dr.
J. W. Dawson on the Devonian,
458.

Poaka Beck, list of Diatomaces in the,
30; swailow-hole of the, 24.

Polypora fastuosa, 5.

Porites, 442.

Collegniana, 437. P

Porphyry-vein in granite, Ben Nevis,
sketch of, 205.

Porter, Dr. H., on the occurrence of
large quantities of fossil Wood in the
ee Clay, near Peterborough,

Prestwich, J., Esq., on the section at
Moulin Quignon, Abbeville, and on
the peculiar character of some of
the flint implements recently dis-
covered there, 497.

Primordial Zone, fossils of the, 43.

Proboscidea from Wookey Hole, 272.

Productus Cora, 174.

semireticulatus, 174.

Psilophyton, 461.

princeps, 465.

Sue vie of the southern Grampians,
199.

Ragstone, fossils of the Upper, 313.

Ramsay, Prof. A. C. (President), ad-
dress on presenting the Wollaston-
medal to Mr. Leonard Horner for
Prof. Gustav Bischof, xxvii ; and to
Sir R. I. Murchison on handing to
him the residue of the Wollaston Do-
nation-fund for Prof. Senft, xxviii;
anniversary address, February 20,
1863, xxix ; Notices of deceased Fel-
lows:—Mr. R. Trench, xxix; Prof.
Dr. C. C. von Leonhard, xxix; Mr.
R. Bald, xxx; the Rev. Prof. J.
Cumming, xxxi; Mr. J. C. Nesbit,
xxxi; Prof. Dr. H. G. Bronn, xxxii;
M. Bertrand de Doue, xxxiii; Dr.
T, 8. Traill, xxxiv; Marquis of
Breadalbane, xxxiv; breaks in the
succession of the British Palzozoic
strata, xxxvi; Laurentian Gneiss,
xxxvi; Lingula-flags, xxxvii; Tre-
madoce Slate, xxxviii; Llandeilo and
Caradoc beds, xxxvili; Llandovery
or Pentamerus-beds, xxxix; Table
of Lower Llandovery fossils, x1;
Wenlock Shale, xli; summary of
breaks in the Silurian series, xlii;
Old Red Sandstone and Devonian
rocks, xlii; of Shropshire, xliii; of
the south-west of Ireland, xlv; of
Scotland, xlv; Devonian rocks, xlvi;
division of the, xlvi; Carboniferous
series, xlvii; Permian strata, xlviii ;
enumeration of breaks in the Pale-
ozoic strata, xlix; coincidence of
breaks with changes in the fossils,
xlix; not necessarily accompanied

INDEX TO THE PROCEEDINGS.

by sudden convulsions, xlix; .illus-
trated by a review of the Silurian
formations, 1; contemporaneity of
strata, li;
sented by strata in Britain, li.

Randall, J., Esq., and G. E. Roberts,
Esq., on the Upper Silurian passage-
beds at Linley, Salop, 229.

Recent changes in the delta of the
Ganges, 321.

Report, Annual, i; of the Council, 1;
Library and Museum Committee, ii.

Reptiles, dermal coverings of certain
Carboniferous, 469.

Reptilian Footprints in the Ross-shire
sandstones, 506.

Retepora? lepida, 6.

Retrocession of the junctions of tribu-
tary streams with main rivers, 342.
Rhenish Provinces, Devonian rocks of

the, 489.

Rhodarea irregularis, 426.

Rhynchonella Acadiensis, 172.

Dawsoniana, 172.

——- pugnus ?, 173.

—, sp., 173.

Ripple-drift in mica-schist, 405; in
unaltered sandstone, 402.

River, diagram-section across the bed
of a, 325; Jennai, opening of the,
533.

Rivers, elevation of the banks of, 324;
Jessore group of, 534; junction of
tributary streams with, 342; Kish-
naghur group of, 338; Natore group
of, 336.

Roberts, G. E., Esq., on some Crusta-
cean Tracks from the Old Red Sand-
stone, near Ludlow, 2338; and J.
Randall, Esq., on the Upper Silurian
passage-beds at Linley, Salop, 229.

Rolling Bank quarry, 313; section of
the, 314.

Ross-shire sandstones containing Rep-

tian footprints, the Rev. George.

Gordon and the Rev. J. M. Joass
on the relations of the, 506.

St. Acheul, section of the gravel-pit at,
D901; Croix, list of fossil Corals
from; 412; Thomas, list of fossil
Corals a 412.

Salter, J. W., Esq., note on the Skid-
daw Slate. fossils, 135; on a new
Crustacean from the Glasgow coal-
field, 519; on Peltocaris, a new
genus of Silurian Crustacea, 87; on
some fossil Crustacea from the coal-
measures and Devonian rocks of
British North America, 75; on some
species of Eurypterus and allied
forms, 81; on some tracks of Lower

lapse of time unrepre-.

Silurian Crustacea, 92; on the dis-
covery of Paradoxides in Britain,
274; on the Upper Old Red Sand-
stone and Upper Devonian rocks,
474.

San Domingo, fossil Corals from, 426,
449

Saurians in the Roth-liegende, 302.

Saurichthys? Indicus, 17.

Sawkins, J. G., Esq., on the association
of granite with the Tertiary strata,
near Kingston, Jamaica, 35.

Scapheus ancylochelis, Mr. H. Wood-
ward on, 318.

Scarborough, Mr. J. Leckenby on fossil
Plants from, 519; on the Oolites of,
519.

Scotland, glacial action on the west side

of, 258.
* Serees,”’ 114.

Section across Black Comb, 131; Here-
ford, 178; Ludlow, 178; Skipton,
178; the bed of ariver, 325; Perm-
ian rocks of north-eastern Bohe-
mia, 301; at Bouldon quarry, 233 ;
Leny old lime-quarry, 187; Linley
Brook, 232; Sunny Hill, 308; the
Halfway House, 307; Summit-cut-
ting on the Lancaster and Carlisle
Railway, 130; from Glen Shee to
Braemar Mountains, 201; Lindale
Cote Mines to Urswick Tarn, 26;
Loch Earn to Loch Tay, 195; Mat-
terdale to Uldale, 120; Newlands to
Sunderland, 116; the Labyrinth-
Berg, near Hof, to Selb, 360; to the
Watch-tower, 360; Ullswater to
Wastdale Crag, 127; Vadadzry, east-
wards, 33; in Devonshire and South
Ireland, 479; Pass of Leny, 185;
Pembrokeshire and North Ireland,
479; the Aymestry Limestone at
Mocktree, 369; hyzena-den at Woo-
key Hole, 262, 263, 264, 265; near
Horton Rectory, 310; Stow, 313;
of Ben Ledi, 188; « Ripple-drift ”
in mica-schist, from Muchuls, 405 ;
in unaltered sandstone, 402; Tar-
batness, 508; the Artesian well at
Barracas, 70; gravel-pit at Moulin
Quignon, 501; St. Acheul, 501; In-
ferior Oolite from Cheltenham to
Bath, 309; Middle Lias at Black
Ven, 281; Golden Cap, 283; at
Westhay Cliff, 282 ; “ Rolling Bank”
quarry,314; south side of Glen Nevis,
205; Tertiary and Cretaceous rocks
of Jamaica, 515; upper part of Glen
Nevis, 206 ; Valley of the Somme at
the present time, 504; at the time
of the formation of the High-level

INDEX TO THE PROCEEDINGS.

Valley-gravels, 504; of the Lower-
level Valley-gravels, 504 ; at the time
of the emergence of the High-level
Valley-gravels, 504; on Gareloch,
182; Loch Lomond, 183; through
the Brick-pit at Lexden, 395 ; com-
parative, of the Artesian wells of
Barracas and Buenos Ayres, 69.

Secular elevation of deltas, 326; dia-
gram illustrating the, 527.

Seeley, H., Esq., a monograph of the
Ammonites of the Cambridge Green-
sand, 519.

Selb, section from near Hof to, 360.

Senft, Prof. F., award of the Wollaston
Donation-fund to, xxviii.

Serpula advena, 496.

Shells common to the Carboniferous
and Permian periods, 163; from
Jamaica, Mr. J. C. Moore on Ter-
tiary, 510; the 40-feet beach of Ar-
gyleshire, 254; Pilton group, 495.

Shropshire, Upper Old Red Sandstone
of, 485.

a Mr. C. E. Austin on a part of,

2.

Siderastrza crenulata, var. Antillarum,
435.

grandis, 441.

Silt held in suspension in Ganges’
water, 350.

Silting up of the Sylhet Jheels, 331.

Silurian Crustacea, Mr. J. W. Salter on
a new genus of, 87; tracks of Lower,
92.

Silurian, fossils of the lowest, 42 ; rocks
of Bohemia, 364.

Sketch-map and section of Tarbatness,
508 ; of Bavaria and Bohemia, 356.

Sketch of contortions in slate, Aberu-
chil quarry, 194; the Upper Ludlow
rocks and the passage-beds at Linley
Brook, 231.

Skiddaw Slate district, map of the,
115.

Skiddaw Slate series, fossils of the, 135 ;
Prof. R. Harkness on the, 115.

Skiddaw Slates of Bassenthwaite, 114,
119; Binsey Crag, 114; Black Comb,
131; Caldbeck-fells and Carrock-
fells, 124; Cumberland, 119; Der-
wentwater, 114, 119; Lake-district,
eastern margin of the, 126.

Skipton, gravels of, 179; section across,
178.

Solenastrzea Turonensis, 422.

Solenopsis imbricata, 8.

Somersetshire, Upper Devonian of, 485.

Somme, sections of the Valley of the,
504.

Sorby, H. C., Esq., on the original na-

ture and subsequent alteration of
-mica-schist, 401.

Southern Grampians, Prof. J. Nicol on
the geological structure of the, 180.
Special General Meeting, Resolutions

at the, 157.

Spheroma, 79.

Sphenopteris recurva, 464.

Spirifera acuticostata, 171. °

glabra, 170.

Spiriferina cristata, 170.

Squilla, 79.

Stephanoccenia dendroidea, 452.

tenuis, 423.

Stigmaria pusilla, 460.

Stonebarrow Hill, Lias of, 281.

Stow, section near, 315.

Strath Earn, 189.

Streptorhynchus crenistria, 173.

Strophomena analoga, 173.

Stylophora affinis, 436.

, var. minor, 436.

Summary of Primordial fossils, 44.

Sunderland, section from Newlands to,
116.

Sunny Hill, section at, 308.

Swallow-holes, near Ulverston, 21.

Swatch of ‘‘ No Ground,” 351.

Sylhet Jheels, silting-up of the, 331.

Synopsis of the Cambrian formation,
44; Huronian formation, 52.

Synoptical Table of the Mesozoic and
the Palzeozoic formations of central
and north-eastern India, 150.

Table of organic remains from Woo-
key Hole, 266, 267 ; distribution of
Estheria minuta in the European
Trias, 146; fossil Estheriz and Leaiz,
141; fossils of the Primordial Zone,
44; Mesozoic and Paleozoic forma-
tions of central and north-eastern
India, 150; oscillations of rivers,
324.

Tarbatness, sketch-map and section of,
508; track-bearing sandstones of,
506.

Tarns near Ulverston, 20.

Teesta, changes in the course of the,
341.

Terebratula sacculus, 169.

Tertiary and Cretaceous rocks of Ja-
maica, section of the, 515.

Tertiary Shells from Jamaica, Mr. J. C.
Moore on, 510.

Tertiary strata near Kingston, Jamaica,
My. J. G. Sawkins on the association
of Granite with the, 35.

Tetragrapsus, 137.

Thecidium Adamsi, from the Miocene
beds of Malta, Mr. J. D. Macdonald
on, 517.

INDEX TO THE PROCEEDINGS,

Theoretical section of the Valley of the
Somme at the time of the formation
of the High-level Valley-gravels,
504; of the Lower-level Valley-gra-
vels, 504; at the time of the emer-
gence of the High-level Valley-gra-
vels, 504.

Thysanus corbicula, 430.

excentricus, 439, 514.

Tracks of Crustaceans, 42, 92.

Trias of Europe, Estheria minuta in
the, 146.

Trichomanites filicula, 464.

Trochocyathus cornucopia, 428.

Tyndrum, 200.

Typhis, tail-piece of, 79.

Uldale, section from Matterdale to, 120.

Ullswater to Wastdale Crag, section
from, 127.

Ulverston, caverns near, 20; map of
the Lindale district near, 21; Miss
FE. Hodgson on a deposit containing
Diatomacee, Leaves, &e., near, 19;
swallow-holes near, 21; tarns near,
20.

Upheaval of the Madoopore Jungle,
29

Upper Lias, definition of the, 280.

Upper Silurian passage-beds at Linley,
Salop, Messrs. Roberts and Randall
on the, 229.

Urswick Tarn to Lindale Cote Mines,
section from, 26.

Vadadry, section at, 35.

Valley-gravels, sections illustrating the
formation and emergence of the, 504.

Valley of the Ganges, physical changes
in the, 329; Somme, sections of the,
504.

Wastdale Crag, section from Ullswater
to, 127.

Watch-tower, section from the Laby-
rinth-Berg to the, 360.

Wells, ancient physical geography of
the district near, 272; hyzna-den
at Wookey Hole, near, 260.

Westhay Cliff, 281 ; vertical section of
the Middle Lias at, 282.

West Indian Islands, fossil Corals of
the, 406 ; Miocene formation of the,
452 ; Seas, ancient physical geogra-
phy of the, 454.

Wollaston Donation-fund, award of
the, xxviii; Medal, xxvii.

Wollaston, T. V., Esq., note on the re-
mains of Coleoptera from the Peat
of Lexden Brick-pit, 400.

Woodward, H., Esq., on a new Ma-
crurous Crustacean (Scapheus ancy-
lochelis) from the Lias of Lyme
Regis, 318.

Wookey Hole near Wells, Mr. W.
Boyd Dawkins on a hyzena-den at.
260,

Wright, Dr. T., on the fossil Echinidx
of Malta; with notes on the Miocene
beds of the island, by Dr. A. Leith
Adams, 277,

THE END.

PRINTED BY TAYLOR AND FRANCIS, RED LION COURT, FLEET STREET.

=

i’ B4a420y-—-

aA To 14,92 Wty

<oglirn, cthees$ inl) te wyicens

4 or et
aa% i <_e Wetec > a - ht 1 mii
* ye : ee re Va; Fey a rie

eons

pos 4 ‘ rt re is an ies anstsaieoght

an

oe pe a

eT a a a 7 as ro |
Wath hin |
¢ 9 th = Pi) gan @ De, SvVTAL

; f¥e* note 3). Minit Bilin pea
p ie eee ss, a
>» Tees > _ Doe 2ee >
ae. pen Ji. eek Gag wre
iq Yintkappear® 4) Oe, » de hs ee
x shadin dynes the S45 Heatey Bp eine We
‘ an ol} sea pepe 1 iit dhity Lode rane ¥en, ae . _
: “> ar tre oe eal His-uniai mar ;

“ wo; 7 lhe Si Lee

“ALUN
3 9088 01350 1630