- ws < ~ Se ew Stes ODED At | OD POSH O-0 Oe 6-H @ Oo *
< o * +2 8 +e em &.°-4-@ =e © © to? ~* “ -

Pe ee ee ee ed $6-spee. 7 8 OPO One 5-46 8 @ eo +e~- “= Oe Noe ——_

ee ee ee . 2+ O06 OA DO Or CAO OOM DLE OD OOOO OO 8 OH By orl > Ga ONO bot OG tat D ln a Gn Eilyn ete tere Ene Ge ae mei eee

A Ot OO OO Oe © Py I AP a ee ee ee 2 oe th ant es ee ee ee ee Oe OOOO OC OS AE 8m be oo ton O8 Or tw ~ Te Se se ood

<6 tet het Oe 00 te > ine-4 ~~ ae oe a eae Dv SN ee eee a eb aah aae ee oe i thine rte etee th dee ne a ee ee O80 Geile hn 8 Get Bee Or OS.

to Oe Reo Fe Ft FF Ee OOO PEO e OOO O-8-4 8h Mee ae bt het A A AO tn ow att ~Sad: h-Oedn Ore

e@@eGrs oat QA 8 ett Tol » “ 7 Ya ee ee he “~y Pte + Oo nD et & ee »Y ooo 6-36 ae be eee “ea ®t
+ ne w os ar &. : oe he a hoe ee Oe hk Oe ee 00-078 O40 08
owe eee eae aang me ri ea + +e OOOH EHO O4 o>

Aa Nhe +2 bee

" ees ew 0-4 0 thts rar ee ~~, ~~ ve He ag
~ ee ~ e Ontow: q ain Marea a tanatael 0 \-Bin-4-e yw ~ ‘ - ae CO 6 8 ee hd bene e- +
Se mre — Se aren Ea ete oe ee ee hn anneal at *-8 6-058. S 6-tphe-s-@ Sun Se Ae Rtntinlndy seagate Gabe ae rkae 0-8
“ = CoO ee Oe WO Oe SD Ae ee oe Seow e + nee . - ae ten rae eee mere ree ee ee dei OOO 6-9 Ot FOO SO rere Font GAG-O-8-8- ent “te Perret Pe tate Oe & ee O~8-~
~ - we weve teseteensas te ae eae e a - eae Fe 4 ow a” : ee oS ww Oe er ee oe ee ee oe | POOP OS aren erer peop eer re oS ares wees eee arenes -

> eee r ee Se ee nO Bold nll . Wot eo A-try
~a ~ ; : Sietevesassseonenr . : wee enn rad betes
ee ee 26s ae os PO 21-200 FeO ~" 7 i et - ‘ ee oe -e9-* ~ eats oe
ad opens aey we Oe OO Ot ha : Peemyy eae ax te - Mah ot Qua ge o> ation — ~*
5 et eee. . tn Ae then th > tarnne . \ oe eee & an an Ce eee eee
AD oct aes +-+.4 ¢ dah d Oa eas Aen 4 " eo ren
eo enr - > ~— ; ae ereer:
oe one mere : : . ~ ‘ poierd ee et ot oe oe Se
‘ ; " .. et ee rare re ane , 4 v . a, oleate
eee et teem Pe . ’ : P “ ar ee — ee ae Sie > hte ~e- ‘ maton A 4-0 ~tntot'e ——<
rem * c a : . 4 . n b = - aa eal P “t . < - nn? 29 ~ 928-42 6 y
+ . . pte ee ne * * sa ‘ : - ln tom - - a ee ee ere eee me ee
— oe ite . ,- = “= qeinb-bebeed- do ao Sand s-29d-0 9p oan noe and tnn- . o-*
c ew ae-ery rw. aren eo ’

narra el - . “ Saw . - - s 7 - . 2 = a
me Pow : . a “ . “ m Haug 4-9, mse 4 #40
putes +-*

a
42-

OV
Nt OO Tte *

ek ee
<. ‘te @& >
i ee
ieee

88. oA em beens

we tabad- tee

ee ee ee or oe
5 BQ: -

ah

es
*
AT We Og _
A ha* 7"!
ah > §
he -
nee :
if i
i
7
i
Z j
‘
’ i

ee

re" wa ied Geert

i a ig Be

.
i a.) k
; a ae om : ,
5.
ba! nd
Yu
- Tt
ze oy,
ie i is
pe 5
. . _
] “ ,
mm
Dk be
j hie
“ ’
s
r ~
Pp
hy
\
j j '
K
P U "
ay P Ve, .

moe, 6642
#heo/.

THE

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.

aM,
VOLUME THE FORTY-SIXTH. “TA
1890.

LONDON :

LONGMANS, GREEN, AND CO.

PARIS: FRIED. KLINCKSIECK, 11 RUE DE LILLE; F. SAVY, 24 RUE HAUTEFEUILLE.
LEIPZIG: T. 0. WEIGEL.

SOLD ALSO AT THE APARTMENTS OF THE SOCIETY.

MDCCCXC,

List

OFFICERS

OF THE

GEOLOGICAL SOCIETY OF LONDON.

WARAABALAARADRADIAIAN

Elected February 21, 1890.

PBrestvent,
A. Geikie, LL.D., F.R.S.

Wice-PrestVents.

Prof. T. G. Bonney, D.Sc., LL.D., F.R.S. | W. H. Hudleston, Esq., M.A., F.R.S.
L. Fletcher, Esq., M.A., F.R.S. | J. W. Hulke, Esq., F.R.S.

Secretaries.
H. Hicks, M.D., F.R.S. | J. E. Marr, Esq., M.A.

Foreign Secretary.
(Office vacant.)

Creasurer,.
Prof. T. Wiltshire, M.A., F.L.S.

COUNCIL.
Prof. J. F. Blake, M.A. W. H. Hudleston, Esq., M.A., F.R.S.
W. T. Blanford, LL.D., F.R.S. J. W. Hulke, Esq., F.R.S.
Prof. T. G. Bonney, D.Sc., LL.D., F.R.S. Major-Gen. C. A. McMahon.
James Carter, Esq. J. E. Marr, Esq., M.A.
. John Evans, D.C.L., LL.D., F.R.S. H. W. Monckton, Esq.
L. Fletcher, Esq., M.A., F.R.S. E. Tulley Newton, Esq.
A. Geikie, LL.D., F.R.S. F. W. Rudler, Esq.
Prof. A. H. Green, M.A., F.R.S. W. Topley, Esq., F.R.S.
A. Harker, Esq., M.A. Rev. G. F. Whidborne, M.A.
H. Hicks, M.D., F.R.S. Prof. T. Wiltshire, M.A., F.L.S.
Rev. Edwin Hill, M.A. | H. Woodward, LL.D., F.R.S.

Assistant-Secretary, Clerk, Librarian, anv Curator.
(Office vacant.)

Assistants in Pflice, Library, anv Museum.

Mr. W. Rupert Jones.
Mr. Francis E. Brown,

TABLE OF CONTENTS.

Page
BuakE, Prof. J. F. On the Monian and Basal Cambrian Rocks of
Serpe CE late OVE) i oats ws ob a ldslnwye es wmesee sae 386
Bonney, Prof. T. G. On the Crystalline Schists and their Relation
to the Mesozoic Rocks in the Lepontine Alps................ 187
Buckman, S. S., Esq. On the so-called “ Upper-Lias Clay” of
PE USER Pe Th oleic. le dele sa wlale oe adlod . lite date 518
Coranov, Miss. Ona new Species of Cyphaspis from the Carboni-
Soreemne eS GL MOTKSMITE, 555. ees ek ee toe eb ve ea aw ae 421
Corr, G. A. J., Esq., and J. W. Gregory, Esq. On the Variolitic
mocuor Mont Genévre. (Plate XIII). ............ 0080006 295

Cori, Mons. F. M. On the Catastrophe of Kantzorik, Armenia .. 382

Davis, J. W., Esq. Ona new Species of Coccodus (C. Lindstramz).

lle 9: 9.40) eae ait PI NP Maa ae le ls dod starters gy thake 565
Dawson, Sir J. W. On Burrows and Tracks of Invertebrate Animals
im Paleozoic Rocks, and other Markings. .......... 00.00.00 595
GarpinerR, Miss M. I. Contact-Alteration near New Galloway.
ae PMO FMirtctldye «gts dust ai ieib Ackie sinigle do o> elyarqare & 569
Henpy, J.C. B., Esq. On a “ Wash-out” found in the Pleasley and
eM CU AINC Sinica slats xt Ridlo eis disso g at Wiel dels sine + wyeinle cine’ 432
Hinpe, Dr. G. J. Ona new Genus of Siliceous Sponges from the
Lower Calcareous Grit of Yorkshire. (Plate VI.) .......... 54
Irvine, Dr. A. On the Plateau-gravels of East Berks and West
Surrey; their Age, Composition, and Structure ...........00. 557
Jones, Prof. T. R. On some Devonian and Silurian Ostracoda from
North America, France, and the Bosphorus. (Plates XX. &
Ne RC ete) ieee npheirets sid oe ays di Wha Gls ee 4 oe weet 534

Jones, Prof. T. R. On some Paleozoic Ostracoda from North
America, Russia, Wales, and Ireland. (Plates I-IV.)........ ]

a2

lv TABLE OF CONTENTS.

Page
Jupp, Prof. J. W. On the Propylites of the Western Isles of Scot-
land, and their Relation to the Andesites and Diorites of the

District... (Plates XT Vee eV ws yen ees ee es + 341
LypEKKER, R., Esq. On a Crocodilian Jaw from the Oxford Clay

of Peterborough. 4,.). 22" «dua hema. @ acetee iis «ce eee 284
——. Ona Horn-like Dinosaurian Bone from the Wealden .... 185

. On Dinosaurs from the Wealden, and Sauropterygians from
the Purbeck and the Oxford Clay. (Plate V.).....2..s.005) 36

Ornithosaurian Remains from the Oxford Clay of Huntine-
Glonshine ees vrs: Pe et rr es 429

. On Remains of small Sauropodous Dinosaurs from the
Wealden. ((Plate’LX.) . oss <2 ehleb oa sete ae 182

On the Occurrence of the Striped Hyzena in the Tertiary of
the Vali@Arno © 3:2. .55 «epee oho hep eibese st.) 62

On two new Species of Labyrinthodonts. (Plate XII.) .. 289

Morean, Prof. C. Li. On the Pebidian Volcanic Series of St.
Dawids... |(Blate, 2X.) ei ieeenetees ome at csan iors 5, Gila Shee eee 241

Newton, EH. T., Esq. On some New Mammals from the Red and
Norwich ‘@rags.< (Plate XViMS ntas ys \esinl-t. . hl. de «cree 444

PipGEon, D., Esq. On certain Physical Peculiarities exhibited by
the so-called “‘ Raised Beaches” of Hope’s Nose and the Thatcher
Roek, Devon ai. 3c aie miele G8 aw x ais ses ais cia 438

Prestwicu, Prof. J. On the Relation of the Westleton Beds, or
Pebbly Sands of Suffolk, to those of Norfolk, and on their Ex-
tension Inland; and on the Period of the Final Elevation and _
Denudation of the Weald and of the Thames Valley.—Part I. . 84

——_——., | ees Part aie (Plate VII.) . : 25... ck a ae 120

; Part III. On the Relation of the Westleton —
Shingle to other Preglacial Drifts in the Thames Basin, and on

a Southern Drift, with Observations on the Final Elevation and
Initial Denudation of the Weald; and on the Genesis of the
Thames alate WAT.) ve oe aha. pice 155

Rvutiey, Franx, Esq. OnComposite Spherulites in Obsidian, from
Hot-Springs near Little Lake, California. (Plate XVII.) .... 423

SHRUBSOLE, O. A., Esq. On the Valley-gravels about Reading, with
especial reference to the Paleolithic Implements found in them. . 582

Spencer, Dr. J. W. Origin of the Basins of the Great Lakes of
DRTRCRMCHM Goths oid oh vss. 0s e+ e's oo ans 2 os soy tent 523

4

TABLE OF CONTENTS. v

Page
Srirrn, Capt. A. W. On the Glaciation of Parts of the Valleys of
the Jhelam and Sind Rivers in the Himalaya Mountains of
hy a +, DARL jel gpa JESS A 66

Utricu, Prof. G. H. F. On the Discovery, Mode of Occurrence,
and Distribution of the Nickel-iron Alloy Awaruite, on the
West Coast of the South Island of New Zealand. (Plate
ER et Pi RT AS h Saleh So, bid Yoshino ae ete, b's she afm «wie 619

Ussumr, W. A. E., Esq. On the Devonian Rocks of South Devon. 487

Ving, G. R., Esq. A Monograph of the Polyzoa (Bryozoa) of the
ied) Chalk of Hunstanton. (Plate XIX.) 0.0. ......0. 0000. 454

WETHERED, E., Esq. On the Occurrence of the Genus Girvanella
in Oolitic Rocks, and Remarks on Oolitic Structure. (Plate XI.) 270

Wauiraxker, W., Esq. Ona Deep Channel of Drift in the Valley of

the Cam, Essex 3 Oh ene tae ae lea ORG aiee Many AO a 333
Worth, R. N., Esq. On the Igneous Constituents of the Triassic

Breccias and Conglomerates of South Devon ................ 69

PROCEEDINGS.

emeeedimec OL tlie Meetings +2... 0. ace ee eee eee ewes 1, 0a
MB NSR MMR eM eects cle ay fe kn niche tee ns web eat s Ble's bes wily a wiale oe II
Seeeermmermeten Members ee cc eee ee tt te ea ne eee 21
Sa@uiigielom Correspondents .. 2... 4.6... ence e eee eeeoeeess ay)
EME MARCOMOMECUGLHSES 1.00. Ce ew es neeaeee svete eneenes 23
List of Murchison Medallists ......0...000c0eeeeeececcseueeeees as
Se MCOANISES i. a feces seth him dese ve seeneeans 26
Mmmmmieamy Medalists cee nes cee tliede ees voneseaes 27
Lists of Recipients of Awards of Funds..............%. 2A, 255 26, 27
MMMM GTUS oe alias a cw ee ved Me ene PW Coe e eee Lae 28
Tan NACUIBIR, (COCs yculs cca etx wrk Pa Ok wk teh es ve naw aes es 34.
SE ate e AMAT CS AGH 55 vata! ss vhats ¥ Cama eidle, o/sle solide wx eels, ¥ dayne « 43

Additions to the Library (with Bibliography) ...........0..005: 126

vi TABLE OF CONTENTS.

Page
BatuEr, F. A., Esq. On some specimens of Herpetocrinus Fletcheri
trom-Dudleys. Si aor tec a ora ans ue oe a hee eee 5
Browne, R. M., Esq. As to certain “ Changes of Level ” along the
Shores on’the Westermiside’of Maly. of. 0... 0... open eee 122
ComitTex on Geological Photographs, Circular Letter from the.. 6
Councit, Resolution of the, regretting the Death of Mr. W. 8.
DATLAS ji Guciehs ie stone iath, orstasragal aivihs Hd ls llebel shal ae trc gh seat an 121
Exton, Dr. H. Letter on a series of Specimens from the Wit-
watersrand.(Gold-fields> i (bet. 6. Wikio tle die dale 3
GRESLEY, W.S., Esq. On Evidence furnished by the Quaternary
Glacial-Epoch Morainic Deposits of Pennsylvania for a similar
mode of formation of the Permian Breccias of Leicestershire
and South Derbyshire... osc li awe seine ths oa sek 114
Henpy, J.C. B., Esq. Notes on a “ Dumb Fault” or “ Wash-out”
found in the Pleasley and Teversall Collieries, Derbyshire .... I
Hinpz, Dr. G. J. On some Ordovician Radiolarian Chert from the
Southern, Uplands of Seatlandyn 2) sje. stein ae «/-.-tacee Lie
Konen, Dr. A. von. On the Disturbed Rocks of North-Western
Germany 2205.40 et 2 18. ee ieee eens ess hn 116
PosTLETHWAITE, J., Esq. The Borrowdale Plumbago, its Mode of
Occurrence and probable:Onginig sss s cs ss.) ws eee 124
SriFFE, Capt. A. W. On an ancient Human Skull from the Man-
chester Ship-camal )... gion cob © ele, sa et wiht «22. TL
Waters, A. W., Esq. North-Italran Bryozoa...... «+. a..0 eee 123
Woopwarp, A. §., Esq. On some British Jurassic Fish-remains of
the Genera EHurycormus and Hypsocormus .....00 se ceeeeeees 8

Worrtu, R.N., Esq. Further Note on the Existence of Triassic
Rocks in the English Channel, off the Coast of Cornwall...... 120

LIST OF THE FOSSILS FIGURED AND DESCRIBED
IN THIS VOLUME.

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

Name of Species. Formation. Locality. Page
INORGANIC.
Bulemarks, Figs. 18 & 19 ............ |Carboniferous ...|Nova Scotia...... | f ae
PLANTA.
er Bias ae SUriate, cvsencnes Canada. 0.42.58 613
Buthotrephis Grantii { Fie. el Niagara eh (?) 614
mation.
: ; ‘ Potsd
Trunk-like Concretion. Fig. 13 | Teaces tel | Almonte, Canada | 609

TRACKS, TRAILS, AND BuRRows or Worms, &c.

Astropolithon Hindii. Fig. 10......._|Cambrian......... Nova Scotia...... 606
Burrow, radiating. Fig. 9 ......... |Silurian ......... Ontario, Canada 605
Climactichnites and Protichnites. { |Potsdam Sand- Gninio- Canade 600
ROME eis Sacacd's cadenesesecaaatcs stone.
Duolus, track of. Fig. 5............ OME Ncata cee eet let. valve ws tr 601
Pevrogerma, Fig. 6..,......0.ccce EMME 2 sare ases Ontario, Canada 602
Rusichnites acadicus. Fig. 2 ...... Carboniferous ...|\Cape Breton ... 598
. ‘ > Cambro - Si- . r
—— grenvillensis. Fig. 1 ......... loan Grenville,Canada | 997
P . . : ;
Fi ee nites) a Sa SUUTIA) cnsad ess Ontario, Canada 598
Sabellarites trentonensis. Vigs.11& { |Black - River |Pointe Claire, |
: 607
DME r ck tales koWnorddganstenedens Limestone. Montreal, |
—— phosphaticus .......csccecereeeees Quebec Group...|Kamouraska ... 608
Seolthus. Figs, 7 & 8 ...,.cece.ss0 PUTA) iss eciks Perth, Ontario... | oe
CalciferousSand-|St Anne’s, | | [604
Worm-burrows. Fig. 15 ............ Tn Hg Baad: a 612

Worm-trails and Ripple-marks. Fig. { |Potsdam Ronni | 611
Bandi cb cciers sevawhvccacnvabsomecsiee Sandstone. J | soca Meee gL

Vill FOSSILS FIGURED AND DESCRIBED.

Name of Species.

FoRAMINIFERA.

t (Carboniferous
Limestone.

Inferior Oolite...;Chedworth ......

Carboniferous
Limestone.

| Formation. |

Locality.

\ Chitonten

—— intermedia. PI. xi.f.7......... Coralline Oolite | Weymouth

Coralline Oolite |Weymouth

eeeees

——- pisolitica. Pl. xi. f. 3,4 0... Inferior Oolite...|Chedworth ......

SPONGIDA.

Rhacella perforata. Pl. vi. ......... \Corallian

PoOLYZOA

Ceriopora micropora (?)............08. \
Wrastopora feeeuMda, <2-.c0-.-.-.00-.0. |
— hunstantonensis. PI. xix. f. 10
wars. Pl xix. £.11 2. |
Jessont. (PX. sik. 1.02 ......... |

pap MlOsag EN aree cecmiannec ese ante 5
WACHIANISU(E SOW AM EE ie silat niaie so'emjaiee
MG PAT IS: acemeneeetccss sa 5.0
Entalophora (?), Sp. ......seseeeeees :
NA ELELOPOLA (2) SMeeseienasesecieasaenmae
Hippothoa Simplex:-cs.-a..+04--.-2. 0%
Membranipora elliptica (?) ............

I RULES ee Pe pee rtan etna misn nice oaw'e |
gaultina. WPlPSix. tf. 135.2..27-
Prov GA TEYG)) 4-47 oSege esc nenaap acer es |
Multicrescis variabilis (?) ............
Proboscina angustata, var. PI. xix.

Beem eee meres rere sees OTseesessoness

—— hohemica (2), var. Pl.xix. f. 9) $ Red, Chalk

dilata(?), var. cantabrigiensis (?)
gigantopora. PI. xix. f. 8
gracilis, var. Reussi. Pl. xix. |

unstantonensis. Pl. xix. f. 5.
, var. ampliata. PI. xix.

wpreguiaris. Pl. xix, f.2.......
GESRONG © EAWKAK Ee Micsicisssces
AMON Ue amett helio + acnw ss nn |
te MOS (P esthtemsbea cones sone aay
SWHELE CAUS pacenaensel «ns anjee en's
—— Toucasiana (?) ..... .-..seeeee-
—— uberrima. Pl. xix. f,3......... |
Reptomulticava collis (?) ..... ......
RED IOK (1) )eemea sean tovhaws stun
Stomatopora divaricata .........+...
mae PPACLUS: “yvehh nsensennenqvnrativa'ss

eens ecree

eoreee

Se Sn ee
=

ee eae

480
476
475
475
478
477
477
476
479
480
486
485
485
484
485
482

467
472
473
47]

469
470

470
468
471
473
468
470
472
469
481
48]
463
463

FOSSILS FIGURED AND DESCRIBED. 1z

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

Potyzoa (continued).

Stomatopora granulata ............... \ (| 464
—— PEER ea ite scceiaiecises sees 465
SeeMCATES) Coc gccciccsacsescecsccssscee | 466
[O00 S071 ee || 465
DOs odie occ ai eos asarasen ‘Red Chalk ...... Hunstanton...... <4 | 465
IA VED COUIS Do. iccin = dxove+saserecens 483
Unitubigera papyracea ............... | 479
Zonopora irregularis (?)............+8- | | 482
SC PVAMIAMEIIS. «0.4. .ccacesesaseces ») \} 482
CRUSTACEA.
Aichmina Byrnesi. Pl. iii. f. 9-11. |Lower Silurian {Cincinnati ...... ee
spinosa. PI. iii. f. 4-8......... Upper Silurian |New-York State 11
Bairdia anticostiensis. Pl. xxi. f.3 (Silurian ......... AMMICOSE <./95.ans 548
Beyrichia equilatera. Pl. ii. f.6... |Upper Silurian {New-York State 18
ae e
Ss Seb Upper Silurian { cee ows \ 552
Buchiana (?), Pl. iii. f£. 25... |Lower Silurian |Cincinnati ...... 16
—— ciliata. Pl. iii. f. 12-16, ata Lower Silurian {Cincinnati 19
a EPs aR TS 2 Seg oie aan a Ca
— Clarkei. Woodcut, f. 2 ...... Upper Silurian {New-York State 17
= deyonica, Pl. xx. f. 1, 2,3 ... ‘|Devonian...... { oo Bee 536
PUORUS arcicic sein J
COCCI 3.0 oy Silurian \.ooccgea: PAMUPACOSEL .-.02cai's 546
—— granulata. Pl.i.f.3 ......... Upper Silurian |New-York State 15
Cuultenty Ply Xxisf. 2 00.0... Suluetan 522-0 BHILCANY .cnewcsae 554
ener av. ft. 2) ..........0- Upper Silurian |New-York State 15
hamiltonensis. Pl. iif. 3...... Hamilton Group|New-York State 19
—— Kolmodimi. Pl. xx.f.6 ...... Devonian......... badiana egccands 538
—— Kleedeni, var. Pl. xxi. f. 1... |Devonian......... New-York State 538
ECT cnc oc ce cacscasssecececcecs STUNG ec een oe Dundas, Canada 550
— oculifera. Pl. iv. f. 19,20 ... |Lower Silurian |Cincinnati ...... 21
Seeeaculitian Fl, 1.f, 4 ....2....... Upper Silurian |New-York State 16
—— parasitica. Woodcut,f.1 ... |Upper Silurian |New-York State 16
meee tcueulata. Pi. xx.f.14 ...... Silirian 2.005. SATGIMIA see sct cos 539
Trenton lLime-|Lorette Falls,
See TS icnise DPE eR ics aisisiees ainisicrnstmin stone. Quebeciss cme 553
Chazy Limestone] Quebec City
subquadrata. Pl. xx. f. 4...... Devyonian.::...... New-York State 537
eee ATER GULALA sa. vsciencvccsasancveace’ ce (552
_—— par. DYONMI 02... serssceee Upper Silurian { crane: Nova 18
— , var. pustulosa. Pl. ii. f. 1 aaa Slat (532
Peenta. PL if 2 -sencaceee Upper Silurian |New-York State 14
Bollia bilobata. Pl. xx.f. 12 ...... Devonian......... New-York State 540
1 aL b>, at Se Be Devonian......... New-York State 540
Mia PL, i. fe LB a secediees Upper Silurian |New-York State 12
semilunata, Pl. xxi. f.9...... SUDPIAN. scence ATITIGOSET J sanaws 548
eV IMACETIGH | ancailchccenesinevecs Upper Silurian |New-York State 12
?) SPsssseersesescseeesceennersers Devonian......... New-York State 540
ee ears (7) Lindsir wemns. | Pl. Xxt. SSUIUDIBM Saasaete AnticOstl ... 20.00. 548
Bythocypris (2) obtuday Plo xxi. f4 “|Silurian® ..i...... Anticosti ......... 549

Entomis rhomboidea. PI. ii. f. 9,10 Hamilton Group [New-York State 10

x FOSSILS FIGURED AND DESCRIBED.

Name of Species. | Formation. Locality. — Page

Crustacea (continued).

Eurychilina reticulata ............... Devoniansc...222: New-York State 539
fsochilina cristata; Pl. uf. 8. ..... Lower Silurian. |Lake Champlain 23
(yeyabacers Bi wie f. Vr cck. Hamilton Group |New-York State 22
erecariay PI i t9, 00" f.s.: Lower Silurian {Lake Champlain 22
bregian WE). WOES 8.8 22: Hamilton Group |New-York State 21
Poe at a { |\Chazy Formation|/Ottawa, Canada 551
ch apie ag rag ogg ee 2 | |Chazy Formation|Aylmer, Quebec 559
DCOLVis e SE LANE. 7 sec cnsw erent Lower Silurian |Lake Champlain 22
NISMS Ne fabO. “aches samtac Lower Silurian |Lake Champlain 23
Klcedenia notata. Pl.iv. f. 22,23. [Upper Silurian |New-York State 13
Leperditia alta, var. Pl.i.f.6 ... |Upper Silurian |New-York State 25
Claypoler. Plpimiet) 17. isc. Lower Silurian |Cincinnati ...... 25
FTORTANSA TRV eR £18 eae. Silurian. ewes Anticosti'....cace: 547
hudsonica. Pl.i. f.5 &11... |Hamilton Group |New-York State 24
oa (2). EN T. ZO coeur Lower Silurian |Cincinnati ...... 25
MORES. Sopee smear ate cass oe Upper Silurian |New-York State 25
——nana(?). Pliv.f.4 2.2.0... Lower Silurian |Wales ............ Dli
— (?) seneca. Pl.i.f. 13,14... |Hamilton Group |New-York State 23
(7) sinuatas Pasi: 12° 2 1. Upper Silurian |Nova Scotia...... 24
(\Trenton Lime-|Lorette Falls, \
| | stone. Quebec. |
Somer Silo) asin daetag eee sear ictdeue «fe { |Birds’-Eye For- Ontario, Canada }+| 553
|| mation. |
\ |\Chazy Limestone Quebec City ... )
pe ee ere einen eee Aikicastl oe 549
Moorea Kirkbyi. Pl. xx. f. 9,10... |Devonian......... ‘New-York State 542
Octonaria Linnarssoni. P|. xx.f.7. |Devonian......... (Indiana, 7. sopheme 541
12 oe Cope eee) El. SB. Silurian: sees o. ‘Anticosti occa 550
{ Trenton Lime-\Lorette Falls, =
9 SPo neecerccecccceecececs ten renseceee l | ae | Quebec. \ coe
Primitia Billings. Pl. xxi. f. 10. (Silurian .........| AnticoSti .cce.0e 547
— Clarkei. Pl. xx. f. 11 ......... ‘Devonian......... New York State 535
Grau! ae seco
f. ue ie ee : ': | Lower Silurian [Wales ........-.-- 5
—— minuta. PI. iii. f. 18, 19, 21- | [Upper Silurian (Russia ............ "i
5) REE OE | \Lower Silurian (Cincinnati ...... }
— Morgani. Pl.iv.f.6 ........ ‘Lower Silurian |Wales ..........+. 5
( Silurian’ ....2.4 ‘Dundas, Canada 550
| |Upper Silurian Arisaig, Nova 552
Scotia.
TMT ULAR eee ects cp eavele nyse { |Utica Formation Ottawa, Canada 551
Trenton Lime- Lorette, Quebec yoo
| stone.
\ Chazy Limestone Quebec City... 553
: , Aree /
£7 ya eee t in } Lower Silurian ‘ IWVGRLGS « un canals sae 5
GVAGANE Voc rete beer baatontdann capa { Upper Silurian pam sie 552

—- seminulum. Pl.ii.f.2 ...... Hamiiton Group |New-York State 5

FOSSILS FIGURED AND DESCRIBED.

Name of Species. | Formation. Locality. Page
CrusTAcea (continued).
f|\Trenton Lime-/Lorette, Quebec 552
Pa EMIRL A SO cae disiin ices sien a eseeseesani stone.
Chazy Limestone/Quebec City 553
UPC MM i ccewidcecaksssssaeesdeees Utica Formation |Ottawa, Canada 551
Uirtenre Ulsive f. 1, 2,3 i... Lower Silurian |Canada ......... 6
unicornis. Pl. iv. f. 8-13 Lower Silurian |Wales ...........- 7
— (?) Walcotti. Woodcut, f. 1... ! Devonian oe est 543
— Whitfieldi. Pl. iii. f. 24 ...... Lower Silurian |Cincinnati ...... 9
ee Pynceaitera. oe oe Hamilton Group |New- York State 9
. ’ 4 eaeeereeeeerseeeeesesneeerene
f Hamilton For-|Thedford, Oan-
larder 5 542
{| mation. ada.
Strepula plantaris. Pl. xx. f. 8 Devonian New-York State 540
sigmoidalis. Pl.ii.f.4 ...... Hamilton Group |New-York State 11
Ulrichia Conradi. Woodcut, f. 2... , |Devonian ra ph 544
ayers Hl. ww. f Shi \ |Lower Silurian (freland......0...0: | 28
PIscES.
STOECOUUS ALMATUS) <2. 20.0% .000.s. cece Cretaceous ...... WEDANON: . 2. .nai0. 567
Tmasivem~,.) Pi. xxii.:........ Cretaceous ...... PEDRO, 5. cepjnns 565
Cyphaspis acanthina. Fig.5 ...... \
— Cerberus. Fig. 3.......ceccccose |
—coronata. Fig. 4 ............... \ |Carboniferous ...|Yorkshire ...... 422
PRAWISsONG, HIP. 2... see .ceees |
megalops. Big. 1........0c.000s Z
IUPYEORWIUS STANGIS ...............00 Bimeridge Clay jHly ........sc0sses { sey
Prypsocormis Leedsil...............06 Oxford Clay...... Peterborough ... { ge
L
BOMMIGOSULIG | Foc ne 2s. coceesenvese Oxford Clay...... Peterborough ... { ce
REPTILIA.
eee Poemntiewss Fer) Purbeck .....,Portland «ne 47
Dinosaurian horn-core (?). Fig. ... |Wealden ......... Isle of Wight ... 185
Eryops Oweni. P'. xii. f. 2-4 ...... Karoo Formation|South Africa 293
ne | (Wealden ........ Belgium sss... 37
— Dawsoni; ilium. Fig. B...... Wealden \..0:.: Hastings ......0.. 37
— Fittoni; ilium. Fig.C......... Wealden ......... Hastings .......,. 37
— hollingtoniensis; ilium. Fig. ) |,, tae ty
Bie cight femur, woodcut, f. 1 a Wealden ......... Hastings ......... 37, 41
Mantelli; ilium. Fig. D...... NV GRIGOR: diseases Hastings ....ccss: 37
Iguanodon ; vertébra. Fig. 3 ...... Weald6n:.. 0000 Hastings ......46 44
Macromerium scoticum. Pl, xii. | |Lower Carboni-|Gilmerton, near | 290
MUP cincidescrstokiisn wel boxdasleaie« ferous, Edinburgh. }

Xll FOSSILS FIGURED AND DESCRIBED.

REpTixia (continued).

Megalosaurus Dunkeri; metatarsus. |
g > ( Wealden

et ee ee Car A GdieH See ketee Hastings) <.cc..e
Metriorhynchus Moreli. Fig. 1 .... |Oxford Clay...... Wiltshire coe encrn-
Metnorliynehus;: tooth. Fig. 4.0 4°") s.2ikis Willesden ......
Pleuroccelus valdensis ; tooth. Fig. } mac leen Sussex and Isle
Werieiiees gin ARs siso0us ets sqo es nook of Wight.
Piiosaumns feroxing Ply.) 5. s0c. cue Oxford Clay......| Peterborough ...
gion EELS TESTE BE Oxford Clay...... Huntingdonshire
Suchodus durobrivensis. Figs.2&3 'Oxford Clay...... Peterborough ...
MAMMALIA.
Ailurus anglicus. Pl. xviii. f. 9.... /Red Crag......... Boyton...
—— fulgens. Pl. xviii. f. 10 ...... IRGGent es. os- ee India’ (cae en
Hyena striata; teeth. Figs. A,B. /|Tertiary ......... Val d’Arno ......
Putraoubia. lexi f. 1.63.05... Red Crag iiee. eee Woodbridge
HiCever, CENA XVI, ToD 6 seca. oe Norwich Crag ...|Bramerton ......
Mesoplodon fioris. Pl. xviii. f. 7... |Red Crag......... Trimley, Suffolk
scaphotdes. Pl xvii. ft. 8 ... |Red Gras 24 Woodbridge
iPhoce Moart. El, Xvill. £3... <<. Red Crarsco Woodbridge
Phocanella minor. Pl. xviii. f. 4... |Red Crag......... Woodbridge
ee minus. Pl. xviii. : Red Cue Woodbridee

Name of Species. Formation. Locality.

Page

EXPLANATION OF THE PLATES.

PLATE ‘ Pace

r} Nortu-AMERICAN PaL#ozoic OstrRaAcoDA.

TII. Norta-AMERICAN AND RusstAn PALzZozoIc OsTRACODA.
TV. Norrn-American, WELSH, AND IrIsH OsTRACODA.
To illustrate Prof. T. R. Jones’s paper on some Paleozoic
IE TESLEOIE Che oot Benet sO M MO Wp re oe a ee

vy. { Putosaurus FEROX, to illustrate Mr. R. Lydekker’s paper on
: some Dinosaurs and Sauropterygians ................0005 eeeees
VI RuAXELLA PERFORATA, to illustrate Dr. G. J. Hinde’s paper
; on a Siliceous Sponge from the Cale-grit of Yorkshire ...

Tuames Basu, to illustrate Prof. Prestwich’s paper on the

DIAGRAM-SECTIONS OF THE PREGLACIAL DRIFTS OF THE
WHI.
MCR ElChOM eH Sem AND, . i nccececcndesteccvacestsnseccccsectes

Map or THE Pree@uaciaL Drirt-Beps or THE BASIN OF THE

VEEL. Tames, to illustrate Prof. Prestwich’s paper, Part IIL,
on the Westleton Shingle and the Southern Drift .........

Ix PLEUROCG@LUS VALDENSIS, to illustrate Mr. R. Lydekker's paper

: QM HOMig SAUTOVOCOUS DIMOSAUTS ....5.........2..cecsarsenecscece

Mr. C. LU). Morgan’s paper on the Pebidian Volcanic Series

Sxercu-Mar or Sr. Davin’s District, N. W., to illustrate
xX
PUTER CRNG ee 1c eiheic . Cra ee neea canadien ecsuarcaseunva swe oho

XI GirvAneLLA, to illustrate Mr. E. Wethered’s paper on

Dens aie ate MECN: 0). ate aaa tet ae ice teas acinancacebownaviveeuneheneecs :

am ee Lasyrintuoponts, to illustrate Mr. R. Lydekker’s

paper on two new species of Labyrinthodonts ............... 2

Ianrous Rocks or Mont Genévee, to illustrate Messrs. Cole
XIII. and Gregory’s paper on the Variolitic Rocks of Mont
Ue Ne Aah cE Wallin a uta davtwavenveusenatedessavavugetieuuas

XIV. Scorrisn Anpzsirus AND ProryuitEs.
XV. Awnvusites or Ben Hranr.
To illustrate Prof. J. W. Judd’s paper on the Propylites

54

120

155

295

of the Western Isles of Scotland.............cccscceccocsecces 341

xiv EXPLANATION OF THE PLATES.

PLATE PAGE

MonrAn AND CAMBRIAN Rocks or Suropsurre, to illustrate
XVI. Prof. Blake’s paper on the Monian and Cambrian Rocks
| OLSHTOPSAULe .. 05006) ss. atepnedicinoasbesce Js denamen en ean eee 386

XVII Composite SpuervuLites 1N OssrprAn, to illustrate Mr. F.
‘| Rutley’s paper on Spherulites in Obsidian from California 423

XVII ’ British Prrocene Mammazs, to illustrate Mr. EK. T. Newton’s
; paper on New Mammals from the Red and Norwich Crags 444

Ponyzoa oF THE Rep CuHatk, to illustrate Mr. G. R. Vine’s

as paper on the Polyzoa of the Red Chalk of Hunstanton ... 454
ae Paleozoic Ostracoda from North Ameri
XXL paper on some Palozoic Ostracoda from North America,

Hrance,and the Bosphorus... «ace. «-«s0is-706~-5ee oe eee 534

Coccopus Linpstrami, to illustrate Mr. J. W. Davis’s paper

XXII. on anew Fish from the Lebanon Chalk..................0cee0: 565

Rocks rrom nEAR New GaAxrioway, to illustrate Miss M. I.

Patzozorc OstracopA, to illustrate Prof. T. Rupert Jones’s
{ Gardiner’s paper on Contact-Alteration .............ceceeee 569

XXIII,

(Microscoric Secrions or PrripoTiTE rroM THE Rep Hr

| AND THE OnivinE Ranez, New Zzauanp, to illustrate
XXIV.{ Prof. G. H. F. Ulrich’s paper on the Discovery, Mode of

| Occurrence, and Distribution of the Nickel-iron Alloy

Pe AAVERWIE. 0.5 eon aap din oes om agles Seen eines beet cael a ee ee 619

WOODCUTS AND OTHER ILLUSTRATIVE FIGURES

BESIDES THOSE IN THE PLATES.

FIG. PAGE
IIE, PUT ASILICH (oc. ce vnneceosceencaneseorececnecon+sseeensccansaness he,
RR PON TICU ots crcemic! «en catenn ini sajcaihnee wade sane ene cescecasanccaes Ly

Sketch-plan of the District of Tortoum, where the Catastrophe
eer COAT ATIOUSt: LOO oxic seas deadtatcins sanbiap aces sveeesqowses
1, A-E. Left Ilia of Wealden Species of Iguanodon ............... 37
2. Right Femur of Jguanodon hollingtoniensis ............0.s.eeeeeees 4]
peemervies! Vettebra Of. an Teuanodon, secs c.ceseccsceccseceenscacaaees 44
4, Left metatarsals of Megalosaurus Dunkeri ......cececseeeenceeeees 46
5. Centrum of a Dorsal Vertebra of Cimoliosaurus portlandicus... 48

Oe fe Re a eee ee

7)

Partor a lett Manilla of Hyena striata... 12... sce.esceceoenesese 63
General Section of the Westleton Beds on Westleton Common 96
EMO TPIRIC,OVEUNEMS CUM. fii cc. stede cence dwivkeescscesseveseosneceden 99
Section at the base of the Cliff near Trimingham.................. 100
Section at the south end of Kessingland Cliff ..................0.. 10]
Section at the base of the Cliff north of Pakefield ............... 102
Meme eS GHON OMe ecepana ete ie Uiatincesssscdcessbuacet cuceesese 104
Penunonror Olitt newr MGM eslOy o.2......6..cc-esececcscsccvevauseuates 106
EGO HH VV OR UNUMEOU Sac: tess crnevweveccrccsusdecccectessucenetevack 110
MERMOMrOn Mel suOd COMINAOI fo) sceescsse ccd ssscsvcasteverecencetneeees 124
Pea MOP HEMIIEIERSOIN ype Pi ui odsdncy's de acee'enseceaasiesenenankesles 125
INCRE IM IOEN Vey ecient < opunehmanertecestadssentaceeswavaasredats 127
Beaton near VW alton=On-CHe-NAZOr ous cecessccvessscccseccencadwacwes 128
sea AE TER ENA MIUL) ce Pe hecsdlen tsk vs oa vcOas evs nat ween oreanurcnvaaashes 12

rohit tagegh ust peta) Sites SR okies Ae ie, Sa Se NewS Bey eer Sai 131

xvi‘ WOODCUTS AND OTHER ILLUSTRATIVE FIGURES,

FIG. PAGE
7. Section between Chapple and Mark’s Tey..............sseesseeeeees 132
8. “Sechton meat W whan cc anecesesten vee ot es ion nat unesies svemaen eee eee 132
9... Section near so rainy SG ie. dawsic <a neaececee <1 o> 52> ase mak ene eee 133

10:. ‘Seetion means Wiercted y.00.3.0c enced. 2oscs dees ca cesee jeceaeee ee eee 134

11. Section from Hatfield Brick-pit to near Digswell Junction ... 138

12. Section near Goring.............. Folecdeaucuge sine ts eet daa eee 140
13. Diagram-section of the Thames Valley at Goring ............... 149
14. Diagram-section of the Lea Valley at Ware ..........0+......06 150
15. Diagram-section from Goring to near Oxford ................00085 151
1. Section‘on West-Hio Hill... 0. .cs.2 jos. odes ssn ese 158
2. Section near Hasthampstead | 2..0...0.50ce00++0-0ne cae 161 |
3. Section of disturbed Gravel on Brentwood Common ............ 164 |
A, ‘Seefionitiear ShanmiOre 2 ssa scc0n sect ones ecient sia 166
Ho Sechrousabove Lenham gn 662 .. ioc ceventenee ccc ues ee as 208
6. Theoretical Section from Well Hill to the Wealden Range...... 170
7 Sheoretrcal Seetion of Well Hill..........5.i5.-2..sen0 sete eee 170
8. Course of the valley of Smitham Bottom restored ......... anes 172
9. Section in front of the Chalk-escarpment above Merstham..,... 173
10. | Diagram of the Lines of Elevation bounding the Tertiary Basin 2
OE the VhaMses 22.45 sessed as abe esnde dee ocesedee skeen 178
Month ol Plewmocelus Valdensts :s...<s0sss0eeves tote cheat eee eee 182
iiownecore (7) Of a DimOsalir sc.e. .--nsseebaaheuath ae. eae 185
1. Diagram-section across Lake Ritom and the, Vall Pioran see 200
2. Section in the lower part of Ravine S.E. of Lake Ritom ...... 206
3. Section in the upper part of Ravine S.E. of Lake Ritom ...... 207
4, Diagram-section between Pian Alto and Fongio ......:csesees 208
5. Sechionanhavine; Val Canaria, 8. as: a.ueesues toe ae saaaee eee 210
G. Diagrammatic interpretation of fig. D. ci... s¢<ansccmesssectoo+ cnn eee 210
7. Diagram-section on West Flank of Scopi.............csseecssseeees 215
6. Dinprem-seetion, ‘Alp Viteita 2... vPcenees caress n<sosasecasabeurs 217
I> (sieignemeap of Sb. Non's Bay: 2... acedemn. lds rawhves anaysomes consti 244.
2. Severo (i, St; None Bay, cn, nk nardmasrennsetecenppsssecmsens 245
Ph eee ESPERO ABI 95, Ruandinn ecctds Sieh surg aescbeei Ape neanidn ca Ligine Manat 246

4 i Faulted Junction of Conglomerate and Pebidian at Ogof
PRCA aren: bsaesralcvienns cae cante lyin tase case denesscmbudneds sacs Desenegretae 248

WOODCUTS AND OTHER ILLUSTRATIVE FIGURES. XVll

FIG. PAGE
5. Diagram-section across St. David’s Promontory ..... ............ 257

a Mandibles and Teeth of Suchodus durobrivensis and Metrio-
CES TES a ee ee a 287
1. Map of the Variolitic Rocks of Mont Genévre.................... 300
2. The Col du Chenaillet, from the north ...............cccceceeneeeees 305

3, { Rock-face on the West slope of the North ridge of the Che-
SEE EEIEE Mehsana Acts dy caine ca Sy dedhik ac eddbecle's SUL oe castanade 309
4&5. Variolite-diabase at the North end of the Chenaillet Ridge 311, 312
eenpesestope G! Tie Ohonaillot: . oo... ec. ke ccc see ece ck cee cas cevceoes 318
Semmes cot, Hory 8) Map oas...c0. sec clissccaceucucsaeeostencsavevens 322
8. Part of Map by Zaccagna and Mattirolo ................ cee 322
1. Outline-map of Littlebury, with Sites of Wells..................... 336
SMS INGMPAGOSS AuittlObULy 2.22. /....0ccccccecscucececdsclscascsccueseres bo7
1. Sketch-map of Ben Hiant, Ardnamurchan .....................005 374
2. Diagram-profile of Ben Hiant........... URE NE eas soni: Seen mone 375

1 Section across the Northern part of the Longmynd and the
TAME fee oe ae Nene Oneen slang Maabledasisbn dense nat waceey nen 392

2 Section across the Southern part of the Longmynd and the
: MRM MME errr ye ern chau, « Socata eh vate nw nese os commons nation 392

3 Section across the extreme South part of the Longmynd to the
ACAPULCO VARUNITER F.5d Juiuts alaicln wk GhieeeeNc cok dy Ae suinbacecics snghisbanee 392
4. Junction of Slate and Grit south of Narnell’s Rock............... 395
5. Section across the Volcanic Hills near Church Stretton ......... 409
Reeeniot a OMAT ICOM, TANG) 9 lip... ule cicece acta cee eseescecwencecdnedes 409

7 Geological Map of the District from Charlton Hill to Welling-
r Pert CAS LHS VV DERI 5 hc. in eh bees esse seceeusecnsceue ceases 410
8. Section from Charlton Hill to the Wrekin .......0::0sseecee 411
9. “Porphyry in Red Grit at Cardington...............cscecceseseeeeeees 412
1-4. Outlines of some Oyphaspides..................cccccsceseee eeecseonens 422

14. Bones of Rhamphorhynchus Jessont ........ccccccecceeeseeveeeeeees 43

1 Plan of the Teversall and Pleasley Collieries, showing the
ee UR URein CMe? x con ION N SE ies oacctv adi ssp otassegeetacan's 43e

o_r J Sections of the Wash-out in the Teversall and Pleasley Col-
oT SNRs Mace Ree Pie cctac rec sielteul Mucucy se huecuhesstaunuiebonewns 434

1. Map of the Devonian Rocks in the district West of Torquay... 400

y. { Map of the Devonian Rocks in the district between the River
j eR eG BO Pinon ELS 9.05 cay wavasseusnsisedueccesvabesnrasnes AYO

VOL, XLVI. h

XVili WOODCUTS AND OTHER ILLUSTRATIVE FIGURES.

FIG, AGE
Map of the Drainage of the Ancient Laurentian Valley,now

obstructed and forming the Great Lakes ...........02¢.06 coven Dae

ba Peete (OVA DCO cos wis c Anas s,qunaele onlin anette sas eeatee hee euce te stem 545

2s ULI AAL COURT sa sai des ies doks's bs ouanude Sein ee arene pale ol reeeare eee 544

1, J Map of the Hill and Burn of Knocknairling near New Gallo-
vA), PONVEI Vom ebitais CaN orien emeiaweivsi.cneaietn s oxedenis oe henaiden ae 571

Contorted Flags and Grits near Knocknairling Hill

bo

3. Junction of the Flags and Granite on Knocknairling Hill...... 576

Section of the Gravels at the Tilehurst Road, Reading ......... 585

1. Rastchnites gremvillensis 0. 0ee sense sesvaesentaenen eucltaal ee maeeeenie 597

Qn. LRUSUER TILES. CCAMICUS: 60 ve only devin elaine eden even san +esosce ore eee eee 598

3. iusichnites (Psammichnites) clintonensiS ......».«isncstuasnmeneeenn 598

4. .Climactichnites and Protichnttes..........-+-.-.s0000s sanundere ene 600

5. Marks made jy L7wlus 00. cca faceee neces ones pee eee 601

Onn OU MUCEOR CT IE 5 cau cccGh wad tects Hans ols <ceeeties een Made 602

WUC oh SCONES). 5 cauvbern dd'gevediane nieve ed eusick sawndine « aceasta 603, 604
9. Radiating Burrow.........0..0.6 EN ess oo ee 605

WO PASH OpOlNON FLUNG. ccc. cccrs tiles te sncsveqens .0iet neice eee 606
WAG V2.5 USAOCHATACES TPENTONENSIS 1... 0cse.cn0st-asnes enue ntherei eaten 607
13. Trunk-like Concretion ...... Sbednates Seles saeco one ne eae iotte O09
14;°*-Worm-tracks and Ripple-marks |...:.......s..0.c10) see eeeeneene 611

1d) Wie burrOws 00.0.b0e.t.ecesesaeelseeethhs 4 or 612

16. ..Buthatrephis Grantit (Carboniferoms) ..........seseocescsenesceeees 613

17. Backowephis*Granvit (Silurian) 22. ..0crgs iss was pae eee 614

HS 20e WORE TAINS 5s ericua eosin diaeh aca oabvenescdadtee eink sinaices Ce ee 615, 616

Sketch-map of part of the West Coast of the South Island,
New Zealand

CORRIGENDA.

Page 27, line 3 from bottom, for “fig. 17” read “ fig. 12.”
Page 28, line 8 from bottom, for “ Div. G” read “‘ Div. A.”
Page 93, line 1, insert “ Mr. Woodward’s” after “ and.”
Page 99, line 28, for “(g)” read “ (h).”
Page 101, line 17, ensert “ec” after “ clay.”
Page 102, line 7, after “ of” insert “the deposit containing.”
Page 103, line 5, after “‘f” insert “ fig. 2.”
Page 103, line 13, for “ be” read “ represent.”
Page 105, line 13, after “‘m” insert “ fig. '7.”
Page 106, fig. 7, insert “ f” to the bed below “e” and “‘m” to the bed below ‘<7,’
Page 106, line 3 from bottom, insert “ these” before “ very.”
Page 106, line 2 from bottom, dele “ also.”
Page 108, line 1, for “to” read “ and.”
Page 108, note §, insert “ as myself” after “ conclusion ”
Page 109, line 40, after ‘ Shingle ” insert “(f to 2).”
Page 110, for “‘c” above the letter f on the right of fig. 8, read “ e.”
Page 111, line 9, after 8” insert “, dotted outline underneath, to the left.”
Page 187, last line, insert ‘‘ venture ” before “to.”
Page 422, line 23, for ‘‘ Cephalaspides ” read “‘ Cyphaspides.”
Page 458, add to the List, 1* :—
1864. Seeley, H.G. Fossils of the Hunstanton Red Rock. Ann. & Mag.
Nat. Hist. (3) vol. xiv. pp. 276-278.
1866. Seeley, H. G. Fossils of the Carstone Formation. Jbdid. vol. xvii.
p. 18!.
1869. Wiltshire, T. Red Chalk of Hunstanton. Quart. Journ. Geol. Soc.
vol. xxv. p. 187.
1883. Whitaker, W. Presidential Address. Proceed. Norwich Geol. Soc.
vol. i. p. 234.

In the Map, Pl. XVI., the areas represented as “ Volcanic basic rocks ”’—
three at Westcot, three at Gatton, and one to the north of Castle Pulverbatch
—are Baryta Veins.

On the same Map the thick black lines indicate Mau/és.

51 gah Petal

Sees. Evie ight at Ue sala? va oe
ele ET OO ARN | C4 ‘ Ole
i reve ans rv
ual Tw ‘ we if

“@

rr, 2 he & PEE geek Mk ae,

vee ba BT | vO ie) ee
‘ ¥ ¥ ‘2 ; - ~~ <
i sate
. : a Na ty
y i ’ % : Se dl oben ie eG, ay
at en 7 rl ; ‘ sin " iA
rn ne Ts 4 may ath Tt roy ‘ti « WOE HVE 6
+ Ai Gols Bae be i ot ft t fi ea ee ay
wis Ye eh ORE BS fe fs py Bah
bs aN ‘
i‘.
y ‘
A ae |!
>'s of
er ae fer i
im 4
e os
‘ : v ‘ age '
“y
; , ‘ \
. byte BY, gk fhe:
r hy \
nee RG A
*
' ‘oh F* pueh> a
4 ? ‘ ‘an e ‘
¥ y PR Via (9
7 .
.
‘
'
4 ‘
\
r £ v i. a

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

Vom XLV. E.

1. On some Patzxozorc Ostracopa from Norta America, WALES;
and Iretanp. By Prof. T. Rupsrr Jonss, F.R.S., F.GS.
(Read November 6, 1889.)

[PuarEs* I.-IV.]

Introduction.—1. Some good specimens of North-American Ostracoda
from the Lower-Helderberg and Cincinnati Groups, in the British
Museum and my own collection, have given occasion for a critical
revision and careful illustration of several forms shown in PI. III.
figs. 1-20, 24, 25, and Pl. LV. figs. 16-24. For comparison with
some of these, three Russian specimens (PI. III. figs. 21-23) are
introduced.

2. In the ‘ Paleontology of New York,’ vol. iii. 1859, several of
the Palaozoic Ostracoda of New-York State were described, but
pls. 79 4 and 798, intended to contain figures of some of
them, could not be then produced. With Dr. James Hall’s per-
mission, copies of some of the original drawings have been cour-
teously supplied by Mr. J. M. Clarke, of Albany, and are here
reproduced (Pl. I. figs. 1-6, and woodcut, fig. 1), thus enlarging our
knowledge of the Lower-Helderberg fauna by the illustration of seven
out of the ten forms originally intended for the unpublished plates +.

3. Prof. R. P. Whitfield, of New York, having kindly sent a
large series of Paleeozoic Ostracoda, collected in the Lake-Champlain
district and elsewhere in North America, for examination, they are
illustrated in Pl. I. figs. 7-15, and Pl. II. figs. 1-13. Figs. 7-10
and 15 of Pl. I. are from the Lower Silurian of Lake Champlain ;
Pl. I. fig. 12 and Pl. I. figs. 1 and 6 are from the Upper Silurian
‘ * These Plates have been drawn with the aid of a Grant from the Royal

oclety. -

t Only “Leperditia parvula,” op.cit. p. 376, pl. 794, figs. 9a, 6, remains
now unrepresented,

Q.J.G.8. No, 181. B

2 PROF. T. R. JONES ON SOME PALZZOZOIC OSTRACODA

of Nova Scotia; Pl. I. figs. 11, 13, 14, and PL II. figs. 2-5 and
7-13, are from thes Hasndlton Group of Lake Erie.

4, The specimens shown by Pl. IV. figs. 1-3, belonging to ihe
“‘ Utica Slate” series, were given to me by Mr. J ohn Young, ¥G.S:,
of Glasgow, who had them from Ontario, Canada.

©. An interesting series of five Lower-Silurian (Ordovician)
species, from near Welshpool, Montgomeryshire (Pl. IV. figs. 4-13),
comprising a characteristic Cincinnati species, were sent to me by
Mr. J. Bickerton Morgan, F.G.S., of Welshpool.

6. Lastly, Pl. LV. figs. 14, 15, represent a rare Paleeozoic Cythe-
roid Ostracod from Kildare, Ireland, collected by Mr. Joseph
Wright, F.G.S.

‘€ The specimens are described as nearly as possible in the order
of their natural relationship; and thus, besides adding to the known
forms, they illustrate the modifications exhibited by the genera and
species of these minute bivalved Crustaceans, both in limited dis-
tricts and in different regions, as indicated in the following List
(p. 3) of 44 species (with notable varieties) belonging to 11 genera.

Range of some Paleozove Genera of Entomostraca.

Bodie sitoiculans
@ || = Sol see
w a Ss = = =
o) o 5 iS EI a
Ba B., eee
A |P A O | |
Seis TeE OME A Si ctoicl ae dselc 6.0’ = Niele Siviaisecin nies p's * * xH | x
PAGE HIVES ediee ma icisou cons seicige ss beoas cs * | *
RH Coe LAMA de rersich plete tacos nacrliebsdaloinmnte ole % * H
POSER MMM ee cece ae» seconde neuvasien ase *» | * | *«H | *
SEE PTANMMELOWSI)” sch. b oe taeeeodecvorencacent -pieateel vallel
PETG RANG OMIAT 0600 sdisinssucavececceceos *
SUSI AA OMAR re ue sic « <’eie.oaeete's gap we'einek bag. tear * H x
POOLE renee net ar cc tuedeecoscea@eee es « NA fee
fC TEEN NIL AME ates he nino Rip Dida C hieo dies ouawam tes ee
Acorn CMG onic cdddcessaawdesuces'ees sui) tl Soak
PSUR tic w eh saseueiaeelf Aves powias * *
SON OTST AIRE gia Sa sica v'aniesvesavveseems ecg. ll aae
Sp OY PUM ee siiclen ania n nndleincie sjonecnnes S67 ia oe MT ae
NGG Maat aetddanenn’s s+ oncldunese cm wag nfo ae see * | *
OUNCE Reba ri es enkecets nasa sadecnbetenes x | x H
VIO ONAN eerie cisiee ce eos wrere'd s wiz,daacione cerns ce Niele Shs *
Mali suit... gos sss.'s= eee re os 1 RAE seeder ae
OCRGNATIA, coecese ss wis season eee <pe tusk
ESR IUMA Rl eee siciten cu vom ceccnceeaey ese be lagi
ieee as US... 6st a00. dav seweneae oe * | P| x
PORbOCYPTIS seuss. sesrccecsocsaines eee P|“ % ont) i Ieee
A tee ots senate co div.de Sees eapies on oe * * *
Py O OWS eae 500 eanasaceetensustsaies P adi a Cn ea
Oythere. .....-.00 paar ee Theat meee on x | * | *
GBT BURRIS Soy o5ckt Sees ban foebewss scttenn * * an ee
CODER Sais donne noah be tase eng iniea|| inv * * * *
Cytherellina .......cssccesessssceseena| ove *

Norr.—H means that the genus is represented in the ‘“ Hamilton Group”
of the United States.
Of the 11 genera marked *, 44 species are described in the present paper.

FROM NORTH AMERICA, WALES, AND IRELAND. 3

List of some new or not well-known Paleozoic Ostracoda from
— North America and elsewhere.

’ J. Pra. Genus ranging from the Cambrian to the Carboniferous.

1. P. mundula, Jones, var. cambrica, nov. Pl. IY. fig. 7.
Lower Silurian. Wales.

2. P. humilis, J..& H., var. humilior, nov. Pl. IV. fig. 5.
Lower Silurian. Wales.

. P. seminulum, Jones. Pl. II. fig. 2. Hamilton group.
New-York State.—Upper Silurian. Europe.

. P. Morgani, sp.nov. Pl. [V. fig. 6. Lower Silurian. Wales.

. P. Ulvicht, sp.nov. Pl. IV. figs. 1,2,3.. Lower Silurian.

~ Canada.

. P.unicornis (Ulrich), Pl. IV. figs. 8-13. Lower Silurian.
Wales, Cincinnati.

» P. minuta (Hichwald). Pl. ILL. figs. 18, 19, 21-23. Lower
Silurian. Cincinnati.—Upper Silurian. Russia.

. P. Whitfield, sp. nov. Pl. ILI. fig. 24. Lower Silurian.
Cincinnati.

Ci is Coe CUR cS

II. Prruiriopsts. Known also in the Upper Silurian of Scandinavia.
Peeeweenciuicjera (Hall), Pl. I. figs. 7,12, 13. Hamilton-
Group. New-York State.

III. Enromrs. Known in the Upper Silurian, Devonian, and Carbo-
niferous.

1. E. rhomboidea, sp.nov. PI. II. figs.9,10. Hamilton Group.
New-York State.

IV. Srrevvra. In the Lower and Upper Silurian of Britain and
Scandinavia.
1. L. sigmoidalis, sp. noy. Pl. II. fig. 4. Hamilton Group.
New-York State.

Y. Aicumina. In the Upper Silurian of Britain and Scandinavia.
1. 4. spinosa (Hall). Pl. III. figs. 4-8. Upper Silurian.
New-York State.
2. 4. Byrnesi (Miller). Pl. III. figs. 9-11. Lower Silurian.

Cincinnati.

VI. Bortia. A Lower- and Upper-Silurian Genus.

1. B. symmetrica (Hall). Upper Silurian. New-York State.
2. B. lata (Vanuxem & Hall), Pl. III. figs. 1-3. Upper
Silurian. New-York State.

VII. Kra@pen1a. An Upper-Silurian Genus.

1, Kl. notata (Hall). Pl. IV. figs. 22, 23. Upper Silurian.
New-York State.
1*, Ki. notata, var. ventricosa (Hall). Pl. I. fig. 1; Pl. IV.
fig. 24, Upper Silurian, New-York State.
B2

4 PROF. T. R. JONES ON SOME PALAOZOIC OSTRACODA

' VIII. Beyricnia. Ranging from the Lower Silurian .to the Car-
boniferous.

. B. trisulcata, Hall, Pl. I. fig. 2. Upper Silurian. New-_
York State.

=

2. B. Halli, sp.nov. Pl. IV. fig.21. Upper Silurian. New-
York State.
3. B. granulata, Hall. Pl. I. fig. 3. Upper Silurian. New-
_ York State.
4, B. oculina, Hall. Pl. I. fig. 4. Upper Silurian. New-
York State.
5. B. Buchiana?, Jones. Pl, IIL. fig. 25. Lower Silurian.
Cincinnati.

6. B. parasitica (Hall). Woodcut, fig. 1, p. 17. Upper
Silurian. New-York State.
7. B. Clarkei, sp. nov. Woodcut, fig. 2, po 17. Wiper
Silurian. New-York State.
8. B. equilatera, Hall. Pl. IL. fig. 6. Upper Silurian. Nova
Scotia.
9. B. tuberculata, Boll, var. pustulosa, Hall. Pl. II. fig. 1.
Upper Silurian.- Nova Scotia. :
10. B. hamiltonensis, sp. nov. Pl. II. fig. 8. Hamilton Group.
New-York State.
11. B. ehata, Kmmons. Pl. 111. figs, 12-16, and ie ive
. figs. 16-18. Lower Silurian. Cincinnati.
12. B. ocultfera, Hall. Pl. IV. figs. 19,20. Lower Silurian.
; Cincinnati.

IX. Isocurtina. From the Lower Silurian to the Devonian.

1. J. lineata, sp.nov. Pl. 11. figs. 5 & 8. Hamilton Group.
New-York State.

2. I. (2?) fabacea, sp. nov. Pl. Il. fig. 11. Hamilton Group.
New-York State.

3. I. Seelyi (Whitfield), Pl. I. fig. 7. Lower Silurian. Lake
Champlain.

4, I. gregaria (Whitfield). Pl. I. figs.9,10. Lower Silurian.
Lake Champlain.

5. I. cristata (Whitfield). Pl. I. fig. 8. Lower Silurian. Lake
Champlain. 7

6. Isochilina?, sp. Pl. I. fig. 15. Lower Silurian. Take
Champlain. - |

X. LeperpitiA. From the Lower Silurian to the Carboniferous.

1. L.(?) seneca, Hall. Pl. I. figs. 13,14. Hamilton Group.
New-York State.

2. L.(?) sinuata, Hall. Pl. I. fig. 12. Upper Silurian. Nova
Scotia.

3. L. hudsowca, Hall. Pl. 1. figs. 5 &11. Hamilton Group.
New-York State.

3*. L. hudsonica? Pl. III. fig. 20. Lower Silurian. Cin-
cinnati.

FROM NORTIT AMERICA, WALES, AND IRELAND. 5

A, L. Claypolei, sp. nov. Pl. III. fig. 17. Lower Silurian.
Cincinnati,

5&6. L. alta (Conrad) et LZ. Jonesi, Hall. (L. alta, var.,
Pl. I. fiz. 6.) Upper-Silurian. New-York State.

7. Leperditia nana?, Jones. PI. IV. fig.4. Lower Silurian.

Wales.
XI. Xxsroteserts. Lower and Upper Silurian, Carboniferous, and
Recent.
1. X. Wrightii, sp.nov. PI. IV. figs. 14,15. Lower Silurian.
Ireland.

I. Genus Primirra, Jones and Holl, 1865.

Primitia, J. & H.‘ Ann. & Mag. Nat. Hist.’ ser. 3, vol. xvi. p. 415.
1. Priwitra mMunDULA, Jones, var. caMBRIcA, nov. (Pl. IV. fig. 7.)

Size: length ‘86 mm., height 5 mm.

This is a true Primitia, related to P. mundula, Jones, especially
fey ol, pl, vi. ‘A. M. N. HY ser. 2, vol. xvi. 1855, although the
valve is not quite so regular in outline, and the sides of the sulcus
are not so stiffly tubercled. We may call it var. camBrica.

From the Bala beds, near Welshpool, Montgomeryshire *.

Primitia mundulu, with its varieties, is a very wide-spread species.

2. PrimitIA HuMILIs, Jones & Holl; var. HumizLior, nov. (PI. IV.
fig. 5.)

Size: length ‘85 mm., height ‘5 mm.

Fig. 5 is a simple suboblong Primi.ia, of the same type as P.
humilis, J. & H., ‘Ann. & Mag. Nat. H'st.’ ser. 5, vol. xvii. 1826,
p. 409, pl. xiv. figs. 6 & 9, but is longer, higher behind, and has a
much fainter sulcus.

From the Bala beds near Welshpool.

3. PRIMITIA SEMINULUM, Jones. (Pl. II. fig. 2.)

Primitia sem'nulum, Jones, ‘Ann. & Mag. Nat. Hist.’ ser. 5,
vol. xvii. 1886, p. 413, pl. xiv. fig. 14.

Size: fig. 2, length 1-2 mm., height ‘8 mm.

Fig. 2 is a characteristic specimen, but the valve is broken away
below and behind the centre. The meshes of the ornament are spe-
cialized at the sulcus. ,

In a limestone consisting of Crinoidal joints, Brachiopods, &c.,
belonging to the Hamilton Group, from Eighteen-mile Creek, Lake
Erie Shore, N. Y. |

P. seminulum is known in the Upper Silurian of Wales, Shrop-
shire, and Scandinavia.

4, Primi, Moreant, sp. nov. (PI. IV. figs. 6a, 0.)
Size: length ‘5 mm., height ‘3 mm.
A small, semicircular, bituberculate, punctate Primitia (the in-

* Figs. 4-13 of Pl. IV. were sent to me by Mr. J. Bickerton Morgan, F.G.S.,
of Welshpool, by whom they were collected fromedark shales of Bala age
at Gwernybrain, near Welshpool, Montgomeryshire, North Wales.

6 PROF. T. R. JONES ON SOME PALAZOZOIC OSTRACODA

terval between the two little knobs representing the generic sulcus).
The tubercles are relatively larger than in J. equalis, J. & H.,
‘A. M. N. H.’ ser. 5, vol. xvii. 1886, p. 412, pl. xiv: fig. 11, andiahe
valve differs very much from P. bicornis, Jones, op. cit. 1855, p.173,
plo vit tie. 23:

From the Bala beds near Welshpool, North Wales. Collected by
Mr. J. Bickerton Morgan, F.G.S., to whom we are indebted for this
and other Lower-Silurian (Ordovician) species.

po. Primi Unerenr, sp.nov. (Pl. LV. figs. 1a; 6) ¢% eiewae
figs. 2 & 3.)

Length. Height.
mim, mim.
Le rnte: Sa 8 "46
Size OP EU ca tate ‘73 “4
D: sek ead we 78 46

Suboblong, straight above, elliptically curved below ; hinder end
semicircular; front part compressed and narrower, with a nearly
straight slope, which makes a blunt antero-ventral angle with the
lower edge. A small but well-marked tubercle rises on the posterior
quarter; there is a slight subcentral swelling, with a very faint
oblique hollow between it and another but faint tubercle in the
antero-ventral region. The valve has a slight convexity, and the
hinder tubercle gives a blunt profile to that end of the valve (fig. 1 ¢).
The surface is ornamented with a minute reticulation, which has
elongate meshes, and passes into striz along the ventral region.

Primitia diversa, J. & H. ‘Ann. & Mag. Nat. Hist.’ ser. 5, vol.
xvii. (1886), p. 412, pl. xiv. fig. 10, may be said to be a relative of
the species under notice, but the differences of shape and surface
are sufficiently distinctive.

Fig. 2 is a variety of P. Ulrich. It has the central swelling
and two little tubercles; but the anterior tubercle is higher up
than in figs. la, 6,,and the outline of the valve is more Leper-
ditioid, and its convexity is more uniform. Except as to the
outline of the valve, this shows a striking analogy to the subrhom-
boidal and Upper-Silurian Primitia armata (Richter), described and
figured in the ‘ Geol. Mag.’ 1881, p. 341, pl. ix. fig. 11.

In fig. 3 the central swelling only is visible. Without this fea-
ture it would probably pass for some of the forms that have been
grouped as “ Leperditia (Isochilina) cylindrica,” Hall; but with it
the ‘valve approximates to the Devonian Primitia Dagon (J. M.
Clafke), ‘Bullet. U.S. Geol. Survey,’ no. 16, 1885, p. 29, ply 2,
figs. 5, 6,'7.. The species is here named after Mr. K. O. Ulrich, of
Newport, Ky., who, having worked assiduously on the Paleozoic
Entomostraca, has favoured me with much information.

The specimens, figs. 1-3, given to me by Mr. John Young,
F.G.S., of Glasgow, are in a slab of Lower-Silurian bituminous shale
(‘‘ Utica Slate”), full of the remains of Asaphus canadensis, Chapm.,
Triarthrus Becki, Green, Lingula curta, Conrad, and Orthoceras, sp.,
brought from Collingwood Oil-springs, Lake Huron, Ontario, by
Mr. D. C. Glen, F.G.8., of Glasgow.

FROM NORTH AMERICA, WALES, AND IRELAND, 7

6. Priwiria untcornis (Ulrich). (PI. IV. figs. 8-13.)

Leperditia unicornis, Ulrich, ‘Journ. Cincinn. Soc. Nat. Hist.’
vol. ii. 1879, p. 10, pl. vii. fig. 4.

Length. Height
mm. mm
(UTE: ee 1:23 8
| eae ge ee 1:3 76
Wists Faget « 1°3 8
i tie 14 66
Oar: eae 16 76
Ai Bes. 35 16 76

Figs. 8-13 would come under Aparchites, were all Primitian
characters absent; but fig. 9 has not quite lost all trace of the
Primitian sulcus, and fig. 13 has a shallow residual pit near the
middle. Figs. 8-13 are varieties evidently of one species—namely,
Ulrich’s “Leperditia unicornis.” The varying extent of submedial or
mid-dorsal depression, the modification of outline and of the posterior
tubercle (almost obsolete in fig. 11, which takes on two subcentral
tubercles) make the individuals disagree to some extent among them-
selves; and the very numerous specimens in the shale show many
modifications of these features.

Bala Beds, near Welshpool, Montgomeryshire. From Mr. J. B.
Morgan’s collection.

Mr. Ulrich’s specimens were from the Lower Silurian of Cincin-
nati, Ohio.

7. Prritia minuta (Hichwald). (Pl. III. figs. 18 & 19, Cincin-
nati; figs. 21, 22, 23, Russia.)

Length. Height.
mm. mm.
Pile 18 vet, 1-0 46
dS eta er eae °8 “435
Size | ASE ae Ikos 73
| Bar wy ies 1°26 ‘73
L ES teres oe 6 3

Cypridina minuta, Hichwald. ‘ Bulletin Imp. Soc. Nat. Moscou,’
vol. xxvii. part 1, 1854, p. 99, pl. ii. figs: 6a, 6; ‘ Beitrige zur
Geologie und Paleontologie Russlands,’ 8vo, Moscau (aud Moskwa),
1854, p. 123, pl. ii. figs. 6a, b.

Leperditia minuta, Kichwald, ‘ Lethea Rossica,’ vol. i. livr. 7,
1860, p. 1335, pl. li. figs. 2 a, 6.

Cytheropsis concinna*, Jones, ‘Ann. & Mag. Nat. Hist.’ April
1858, p. 249, pl. x. figs. 3, 4; Pramitia concinna, op. cit. December
1865, p. 424.

* At one time (op. cit. June 1888, p. 398) I thought that this might be looked
upon as Bythocypris figured upside-down ; but I have strong doubts on that
pant, and prefer to keep it among the almost furrowless, but not quile even,

rimitie, there being “a faint dorsal hollow in the original, which may stand
for the suleus” (tbid. 1865, p. 424). Such a feature characterizes some Pri-
mitié in which the sulcus is becoming obsulete.

8 PROF, T. R. JONES ON SOME PALZOZOIC OSTRACODA

Leperditia (Isochilina) cylindrica (?)*, Hall, ‘ Twenty-fourth
Report State Cab. N. Y.’ 1871-72, p. 231, pl. vil. fig. 12; and
‘Geol. Surv. of Ohio, Paleontology,’ vol. ii. part 2, 1875, p. 1v1,
pl. iv. fig. 5.

The figures given by d’Eichwald in 1854 (and 1860) differ much
one from another f; but the author makes them synonymous. The
specimens shown in Pl, JII. figs. 21, 22, 23, were sent to me by
M. d’Eichwald some years ago, labelled ““Leperditia minuta, from
Talkof” ¢, where his figured specimens were also obtained; and I
take fig. 21 to represent the type, putting aside the author’s bad
drawings referred to above. Figs. 22 and 23 may be varieties or
closely allied forms, or, indeed, valves not quite free from the
matrix.

Among the fossil Ostracoda from Cincinnati there are many
specimens similar to fig. 21, and with even a more strongly pro-
nounced subecentral depression, reaching to the dorsal border. For
instance, in No. 59722, British Museum, which is a seam of solid
dark-grey limestone (15 mm. thick), shaly on two faces, rusty at the
edge, and composed of small organisms, chiefly P. minuta, with
Leperditia? minutissima, and some other, but obscure, Ostracods, as
well as Encrinites, Polyzoans, Brachiopods, and Gasteropods, from
Covington, Kentucky. Also No. 59723 and No. 59725, Brit. Mus. ;
in the latter the valves of P. minuta are of a red colour.

Figs. 18 and 19 are from the piece of Cincinnati Limestone con-
taining Aich. Byrnest and L. hudsonica (?), given me some years
ago by Dr..K. W. Claypole, F.G.S.

If, then, we regard the sulcus as a variable feature, both the
concinna and cylindrica above mentioned fall under P. minuta, as
defined above. If the sulcus be definitely absent throughout a
series, we have Aparchites (Ann. & Mag. Nat. Hist., May 1889,
p- 384). It is quite probable, however, that there are in the
Cincinnati Limestones more than one or two kinds of little Ostracods
haying nearly the shape and aspect of the P. minuta here noticed,
but furnished with other special characteristics. Among the many
associated little valves, exhibiting only their interiors, some evi-
dently differ from the above in their outlines; others, showing

exteriors, have an undulating surface, emphasized in many by one —

or both of their terminal fourths being elevated, and even produced
into short spines or tubercles. These, corresponding with the Welsh

* Hall’s Cytherina cylindrica, ‘Paleont. N.Y.’ vol. ii. 1852, p. 14, pl. iv.
figs. 8a, 8b, from the Medina Sandstone, of Medina, Orleans Co.,, is really a
Leperditia, See ‘ Ann. & Mag. Nat. Hist.’ November 1884, p. 344.

t Figs. 64, 6, are subreniform, with the convex edge upwards ; and figs. 2 a, d,
show a parallelogram with rounded ends, Drawings made from partly im-
bedded specimens might give such results, Primitia tenera, J. G. O. Linnarsson,
‘ Kong]. Svenska Vet.-Akad. Handl.’ vol. viii. no. 2, 1869, pl. ii. fig. 70, also has
a long oblong shape with rounded ends, and was regarded by Linnarsson as being
near P. concinna.

{ L. minuta, Eichw., from Talkof, was referred to as a Primitia by Magister
Fr. Schmidt, ‘Mém. Acad. Imp. Sciences St.-Pétersbourg,’ sér. 7, vol. xxi. no. 2,
Is7o, p. =.

ee = =

FROM NORTH AMERICA, WALES, AND IRELAND. 9

specimens figured in Pl. IV. figs. 8-13, appear to be Primztia uni-
cornis (Ulrich), ‘Journ. Cincinn. Soc. N. H.’ vol. ii. 1879, p. 10,
pl. vii. fig. 4.

“ Leperditia cylindrica, Hall,” is mentioned by H. M. Ami as
occurring, with Beyrichia oculifera, in the Siphonotreta-limestone
(‘Ottawa Naturalist,’ December 1887, p. 3 of separate copy); also
by C. D. Walcott (‘ Albany Instit. Trans.’ 1879, pp. 23 & 37 of
separate copy), with B. oculifera and B. cincinnatensis, in the ** Utica
Slate” of Oneida Co., N. Y.

Small casts of a similar species occur in the hard black shale
(“ Utica Slate”) of Ottawa, with Trilobites, Encrinital joints, &c.

8. Pruwrrra Wuirrierpr, sp. nov. (PI. IIT. figs. 24 a, 24 b.)

Size: length -8 mm., height °33 mm.

Elongate-oblong, convex, with a wide shallow dorsal depression ;
ends rounded unequally, the posterior having a cardinal angle,
whilst the anterior end is neatly rounded. ‘The surface is orna-
mented with a very delicate reticulation of long, oblique, minute
meshes (fig. 24 6).

This specimen is in the British Museum, marked 59723, from
Cincinnati, Ohio. It isin a thin piece of grey limestone, split off a
mass along the bedding ; made up of small organisms, shaly on one
face, and rusty at the edge. On it are“ Leperditia cylindrica, Hall,”
very abundant, with Leperditia? minutissima, Primitia Whaitfieldi,
and Beyrichia Buchiana ? (fig. 25). The last two are very rare;
the Beyrichia is in the cast of a small ripple-mark on the bed-plane.

II. Genus Prmoutropsis, Jones, 1887.
Primitiopsis, Jones, ‘Silur. Ostrac. Gothland,’ 1887, p. 5; and
‘Ann. & Mag. Nat. Hist.’ ser. 6, vol. ii. 1888, p. 406.

), Primirropsis PunctuLiIreRA (Hall). (PI. II. figs. 7 a, 6; 12a, b;
13a, b.)
Leperditia punctulifera, Hall, ‘Thirteenth Annual Report of the
Regents of the University of New York,’ 1860, p. 92.

Length. Height. Thickness *.

mm. mm. mm.

|S oe 1:08 ‘6 ‘48
Size en ees I35 84 8
hae eet oak 1:48 "84 8

_ Figs. 7 a, b, fairly correspond with Dr. James’ Hall’s description
referred to above, but there are more than one little tubercle on the
valve, | and the ventral margin is not so distinctly thickened.
(lig. 7 a has had its postero-dorsal edge partly broken away.)

Taking fig. 7 as a young form, and figs: 12 and 13 as adults, we
find in the latter a stibovate carapace, full in the middle, contracted
at the ends, not quite equally; and more strongly compressed in

* “Thickness” refers throughout to the thickness of the carapace (closed
valves).

10 PROF. T. R. JONES ON SOME PALZOZOIC OSTRACODA

front than behind, the anterior third sloping gently, and the
posterior more suddenly to the margin (figs. 12 6 and 13 5); a
reticulate surface-ornament supplies the ‘‘ minute puncta or pits”
of the original description, but dies out at each end (in the Scandi-
navian Primitiopsis only in front), and there are three small, smooth
tubercles, one central and two on the posterior region; the meshes
are more distinct just round the middle tubercle. Fig. 7 is more
oblong and flatter, but the features may have been produced by
pressure, as the outline of the united valves (fig. 75) is not sym-
metrical, and the postero-dorsal edge has been damaged; the reti-
culation, not so strongly pronounced, reaches to the end-margins,
though weak just there; the central tubercle is represented by a
spot of stronger meshes a little in advance of the centre, and the
two posteiior tubercles are present.

The original specimens were from the Hamilton Group (often
abundant on the shaly laminze), from the shores of Lake Erie to
Canandaigua Lake, N.Y. The specimens here figured are: fig. 7
from the Hamilton Group, at Seneca Lake, N.Y.; fig. 12, in a dark
argillaceous schistose rock, with calcareous organisms, from Darien,
N.Y.; fig. 13, also from the Hamilton Group, at Eighteen-mile
Creek, Lake Erie.

III. Genus Entomis, Jones.

Entomis, Jones, ‘ Ann. & Mag. Nat. Hist.’ ser, 4, vol. xi. 1878,
p. 413.

1. Ewromis RHOMBOIDEA, sp. nov. (Pl. II. figs. 9, 104, 6.)

Length. Breadth. Thickness.

mm. min, mm,
oe 1) a ae 88 38
4 DO er cianraitinae Ie “46 "48

Both of these specimens have probably suffered from pressure ;
but fig. 10, having the sulcus in its normal vertical position, has
apparently best preserved the original shape. Rhomboidal, straight
above and below, with the ends obliquely rounded, unequally in
fig. 10a. Surface flattish and sloping rapidly down at the free
margins, especially posteriorly (fig. 106); impressed with a definite
dorsal suleus; ornamented with numerous strong, longitudinal,
but inosculating raised strive, or thin wrinkles, with a tendency to
become concentric, as more fully expressed in L. concentrica (De
Koninck) and . biconcentrica, Jones.

In fig. 9 the valve is more truly rhomboidal, with the sulcus
oblique (probably by pressure), and parallel to the truncated sloping
ends, which are equal, and have their angles rounded, with one pair
of the alternate angles less rounded than the other.

Oblong and subrhomboidal forms of Hntomis are indicated by
figs. 19, 20, 21, pl. iv. ‘ Monogr. Carbonif. Cypridinadee, Pal. Soc.’
1874; and by fig. 7 (oblique by pressure), pl. xi. ‘A. M. N. HY
September 1879.

FROM NORTH AMERICA, WALES, AND IRELAND. om

Both specimens are from the Hamilton Group: fig. 9 from Seneca
Lake, N.Y.; fig. 10 from Eighteen-mile Creek, Lake Erie Shore,
N.Y.

IV. Genus Srrervura, Jones and Holl.

Strepula, J. & H. ‘Ann. & Mag. Nat. Hist.’ ser. 5, vol. xvii. 1886,

p. 403. .

L. SrREPULA sIGMOIDALTS, sp. nov. (Pl. II. fig. 4.)

Size: length °8 mm., height -44 mm.

A left valve, small, acute-subovate, straight on the back ; posterior
edge broadly and obliquely curved to join the ventral margin, which
slopes upwards to the sharp antero-dorsal extremity. On the
posterior third, and parallel with the hinder margin, is a raised
sharp ridge, bifurcating forwards as two feebler ridges, one of which
curves back in the antero-dorsal region to form a sigmoid flexure
about the middle of the valve and within the larger ridge. There
is no published Strepula having these characteristics.

From the Hamilton Group, at Eighteen-mile Creek, Lake Erie
Shore. N.Y.

V. Genus AXcumina, Jones and Holl.

Aichmina, J. & H. ‘Ann. & Mag. Nat. Hist.’ ser. 4, vol. ii. 1869,
Pp; 217.

1. AXcuMina spinosa (Hall). (Pl. IIL. figs. 4-8.)

Beyrichia spinosa, Hall, ‘Natural History of New York, Geol.
Survey; Paleont. New York,’ vol. ii. 1852, p. 317, pl. a lxvi. figs.
17-21.

Length. Height. Length of

Spine.
mm. mm. mim.
(Co aa 8 “46
| 5 ogee Saar 86 46 26
Size < Re sae rast 86 "D0 66
| gs a NP Nae 8 73
L Site wauce 1:26 *86 ‘73

Valves somewhat Beyrichian in appearance, but the central lobe
is replaced by a strong, oblique spine, thick and hollow at the base,
either elongate or short, pointing upwards, outwards, and forwards,
and sometimes slightly bent. ach valve is thickened on its free
borders with a raised, rounded, but irregular margin. The area at
the base of the spine is hollow and smooth. Sometimes the raised
margin is punctate (fig. 8). Fig. 4 is much like Dr. Hall’s fig. 21 ;
and fig. 5 is like his fig. 20.

In a thin limestone-seam made up largely of Achmina spinosa,
with Bollia lata (rare), Encrinital joints, Tentaculites, fragments of
Trilobites, &c. From Lockport, State of New York. Given to me
by Prof. R. P. Whitfield in 1884. |

Also in a dark-grey limestone, composed of Encrinital remains,
Tentaculites, small Brachiopods, fragments of ‘Trilobites, and
numerous small Ostracods, dihmina spinosa (very numerous),

12 PROF. T. R. JONES ON SOME PALHOZOIC OSTRACODA

Bolla symmetrico (rare). From the Niagara Group, Lockport, New.
York State. Given to me by Dr. James “Hall, F.M.G.S.
2. AicuminA Byrnesi (Miller). (Pl. ILI. figs. 9-11.)

Leperditia Byrnesi, A. 8. Miller, ‘Cincinnati Quart. Journ. of
Science, vol. 1. 1874, p. 123, fig. 10.

Length. Height. Thickness.

: Imm, min. mm.
Size WIGAN iv a 1:06 Sih
; Fics. INO ela 1:06 oh ‘3 (-43 with the spine).

This species has eae valves, unequally rounded at the ends,
and each valve bears a short oblique spine, with a short angular

sulcus or notch behind it, and this is succeeded by a swelling or |

knob at the postero-dorsal angle. The rest of the valve is smooth
and moderately convex, sloping gently to the free border, which has
a very shght, unequal, marginal rim.

The individuals are numerous, constituting a considerable portion
of a thin layer of small organisms (Leperditia hudsonica (?), rare,
Enerinites, Brachiopods, Polyzoa, Annelid jaws, &c.), on a compact,
blue-grey limestone from the Cincinnati Group (Lower Silurian),
Cincinnati, Ohio. Given to me by Prof. EH. W. Claypole some years
ago.

VI. Genus Borzta, Jones and Holl.

Bollia, J. & H. ‘Ann. & Mag. Nat. Hist.’ ser. 5, vol. xvii. 1886,

p. 360.

1. Borrra symuetrica (Hall). (Not figured here.)

Beyrichia symmetrica, Hall, ‘ Paleont. New York,’ vol. 11. 1852,
p- 317, pl. xvi. fig. 16 (containing four figures not separately
numbered); Dana, ‘ Manual of Geology,’ 8rd edit. 1874, p. 227,
fig. 452.

Size: length about 1 mm.

This is closely allied to Bollia lata, but the curved or horse-shoe
ridge is thinner, with a somewhat sharp ventral bend, and encloses
a much larger and wider subtriangular depression or sulcus than in
B. lata. The two other ridges, at the ends of the valves, curve
down to the ventral border. In the lower left-hand figure they are
thicker than the horse-shoe ridge ; and one appears to overhang the
margin, the other being distinct from the edge. In another (lower
right-hand) of the enlarged views, one barely touches the margin,
while the other is divided off from its end of the valve by a distinct
curved furrow.

From the Niagara Shale of Lockport, N.Y.

2. Bornia Lata (Vanuxem and Hall). (Pl. III. figs. 1, 2, 33
Agnostisis| us| latus, Vanuxem, ‘ Nat. Hist. New York ; Geology,’
pt. ii. 1842, pp. 80, 83 (the species is mentioned here).
Beyrichia lata, Hall *, ‘Paleont. New York,’ vol. ii. 1852, p. 301,
pl. a lxvi. figs. 10, 10 a, 6 and 10d (not figs. 10¢, 10).

* The species is here referred to ‘Conrad in Vanuxem,”

FROM NORTH AMERICA, WALES, AND IRELAND. 13

Beyrichia regularis, Emmons, ‘ American Geology,’ vol. i. pt. i.
1855, p. 219, fig. 746; ‘ Manual of Geology,’ 2nd ed. 1860, p. 100.
Beyrichia lata, Jones, ‘Ann, & Mag, Nat. Hist.’ ser. 2, vol. xvi.

1855, p. 168, pl. vi. fig. 13 *.

; Length. Height.
mu. mn.
Fig. 1 : 8 “46
Size isis late) « «et "Te "46
= lees ba og A 1:0 66

Valves having a Beyrichian aspect, but bearing centrally a bent
ridge, somewhat like a horse-shoe, with the curvature downwards,
in the ventral region, and variable in thickness. The ends of the
valves have raised margins, sometimes much thickened (fig. 2) and
even doubled (fig. 3). Thus usually the valve bears a short, but
broad and strong sulcus in the middle of the dorsal region ( ‘“ Sub-
central depression,” Hall, 7. ¢.), and two longer, curved furrows
across the valve near each end. The surface sometimes shows a
delicate reticulation.

The B. ungula of ron Betti) in Dr. Claypole’s collection, is a
close ally of B. lata.

This species has evidently Been confused with another form at
p- 801 and in pl. a Ixvi. figs. 10 a-e; ¢ and e being atrue Beyrichia,
near to B. Kledeni. Prof. Hall’s specimens were from the Clinton
Group of Oneida County, N.Y. Prof. Emmons mentions the Blue
Limestone of =. and the Trenton Limestone, as the source of his
Beyrichia.

Our figured specimens are in a thin limestone seam, largely made
up of small Ostracoda (Bolla lata, Aichmina spinosa, Primitia
cylindrica), with Brachiopods, Encrinites, Tentaculites, and frag-
ments of Trilobites. From Lockport, State of New York. Given
to me by Prof. Whitfield in 1884.

VII. Genus Kra@pensa, Jones and Holl.
Kledenia, J.& H. ‘Ann. & Mag. Nat. Hist.,’ ser. 5, vol. xvii. 1886,
p. 347.
1, Kiapenza norata (Hall). (Pl. IV. figs. 22, 23.)
Beyrichia notata, Hall, ‘ Paleont. New York,’ vol. iii. p. 379
(pl. lxxix. n, figs. 8a—c; not published).

Length. Height.
r 9 mm. mim.
Fe ree wedi aia 5 ae LG 86
ik 2 18 11

This is a Kledenia closely allied to Al. Wilckensiana, Jones +,
but the subcentral lobe and its lateral sulci are feebly developed,

* The ventral curve of the horse-shoe ridge is not sufficiently distinct from
the subsidiary ridge in this figure.

t Ann. & Mag. Nat. Hist. ser, 2, vol. xvi. 1855, p. 90, pl. v. figs. 17-19; and
ser. 5, vol. xvil. 1886, pp. 347, 363 ; and ser. 6, vol. i. 1883, p. 398, nole.

14 PROF. T. R. JONES ON SOME PALOZOIC OSTRACODA

not reaching the dorsal line; and very variable in expression, as
indicated in the figures. In some instances the valves are more
oblong than in Al. Wilckensiana, but in others they are much less
so, the posterior moiety being contracted below, with a strong
postero-ventral slope, giving rise to Prof. Hall’s variety ventricosa. .
Here also the middle lobe is variable in development. Prof. Hall
notes that the surface is delicately granulose (p. 379) in this species.

It is represented by Al. pennsylvanica in Dr. K. W. Claypole’s
collection.

Kl. notata and its variety are abundant in the Tentaculite-lime-
stone (Lower Helderberg), Herkimer Co., N.Y. (Hall, J. c.).

They abound also in a limestone of the Waterlime Group from
near Utica, N. Y. State (British Museum). Beyrichia Hallii ac-
companies them.

1*, Ki@penia norata (Hall), var. venrricosa, Hall. (PI.I. figs. 1a,
1 6 [after the original drawings]; PI. IV. fig. 24.)
Beyrichia notata, var. ventricosa, Hall, ‘ Paleont. N. Y.’ vol. iii.
p. 380 (pl. lxxix. 8, figs. 4 a—c; not published).

Length. Height.
mm. mm. ©
Bio Ge fen iver pce nkd. 2°5 ie2
Size MBit sake as 2:7) I?
Play, BE hs Sek As 1:8 1:03 ‘

This variety is noticed above, under KI. notata.

Tentaculite-limestone from Coeymans, Albany Co., N.Y., collected
and given by Mr. J. M. Clarke, of Albany, N.Y., consists of thin
slabs of compact grey limestone showing on the bed-planes Polyzoa,
small Brachiopods, numerous Tentaculites, and small obscure
Ostracods, such as Primitia minuta(?), a larger oblong form, and
many small Kledenie notate. Among them are some much larger
individuals of this last species, attaining a length of more than 3

and of even 4 mm.

Mr. Clarke has also favonred me with some Paleozoic Ostracoda,
mostly of new species, (1) from the decomposed chert of the Corn-
iferous Limestone of Ontario Co., N.Y., and (2) from the Hamilton
Group in Clarke Co., Indiana.

[From no. 1. Primitia near P. fabulina, J. & H.; Eurychilina
reticulata, Ulrich (? a frilled Primitia near “ Beyrichia reticulata,”
Bornemann); Beyrichie, Strepula, and Moorea.—December 16,

1889. |
VIII. Genus Brrricnia, M‘Coy, 1846.

1. Breyricu1a tRisutcaTa, Hall. (Pl. I. fig. 2, after the original
drawing.)
Beyrichia trisulcata, Hall, ‘ Paleont. N. Y.’ vol. iii. 1859, p. 381
(pl. Ixxix. B, figs. 5 a, b; not published).
Size: length 1:3 mm., height ‘75 mm.

FROM NORTH AMERICA, WALES, AND IRELAND. 15

Fig. 2 looks like a small Kledenia with three short and nearly
equal sulci dividing the dorsal region into four almost equal lobes.
Kl. plicata has even four furrows, but the subcentral prominent
lobe is always distinct in this genus, and I would rather regard the
form under notice as a Beyrichia, because if the three sulci were
more distinct, more unequal, and reached to the ventral region, the
valve would approximate to that of Beyr whia digitata, “Krause,
Wertsehr. d. 1). g. Ges. 1889, p. 20, pl. ii. fig. 12.

The lobe at one end is the smallest of the series. The surface is
stated to be finely granulose.

From the Lower-Helderberg group, State of New York.

2. Beyricuta Haxtit, sp. nov. (PI. IV. fig. 21.)

Size: length 1:3 mm., height ‘76 mm.

A trisuleate Beyrichian form, but not B. trisuleata, Hall. The
three furrows are broad and shallow, reaching a little more than
two thirds across the valve. The two sulci near the ends are
curved nearly parallel to their respective margins, but at some
distance from them; the middle sulcus has an elongate oval outline.
The lobes or ridges are moderately convex, and vary, but not
very much, in size. Two lobes in the middle form a curved, nearly
semicircular ridge, not free in the ventral region, as is the horse-
shoe ridge in Bollza, but coalescing with the two end lobes along
that region ; and the surface of the valve slopes smoothly and gently
down to the margin, all along the free border.

The valve is suboblong; straight on the back, with a cardinal
angle at the posterior end, and rounded off anteriorly. Ends un-
equally rounded; ventral margin slightly incurved.

British Museum. Rare, in a piece of limestone of the Waterlime
Group, from near Utica, N.-Y. State. This limestone is compact and
dark-grey, weathering brownish-grey. Largely composed of small
organisms, especially Kledenia notata, with small Brachiopods, &e.

3. Breyricu1a e@RanuLaTa, Hall. (Pl. I. fig. 3, after the original
drawing. )

Beyrichia granulata, Hall, ‘ Paleont. N. Y.’ vol. iii. 1859, p. 377
(pl. lxxix. B, figs. 1a—d ; not published),

Size: length 3°5 mm., height 2-0 mm.

Fig. 3 represents a Beyrichia much like B, Kladeni, var. tuber-
culate *, Salter, but its dorsal line is straight, and its tree border
is thickened with a broad marginal rim. Of the three the posterior
lobe is the targest, and it unites with the front lobe below the
well-marked, oval, middle lobe.

From the Pentamerus-limestone of the Lower-Helderberg Group,
Schoharie Co., N.Y.

* Geol. Mag. 1881, p. 345, pl. x. fig. 13; Ann. & Mag. Nat. Hist., ser. 5,
vol. xvii. 1886, p. 354, pl. xii. fig. 8.

16 PROF. T. R. JONES ON SOME PALAHOZOIC OSTRACODA

4, Beyricuta ocunina, Hall. (PI. I. fig. 4, after the original
drawing. )

Beyrichia oculina, Hall, ‘ Paleont. New York,’ vol. iii, 1859,
p. 378 (pl. lxxix. B, figs. 2 a—-e; not published),

Size: length 2°3 mm., height 1°38 mm.

This little Beyrichia to a considerable extent resembles B. Saltz-
riana *, Jones, having a neat symmetrical form, with a central and
two other lohes ; but the latter coalesce ventrally, and, according to
Dr. Hall’s description, the posterior (largest) lobe is sometimes
crossed by a slight depression, and projects upwards above the
hinge-line.

From the Pentamerus-limestone, Schoharie Co., N.-Y. State.

5. Bryricura Bucutana (?), Jones. (PI. III. fig. 25.)

Size: length -43 mm., height *3 mm.

This is a very small, not well-preserved, three-lobed Beyrichia.
The front lobe or ridge is free; the middle lobe, curving ventrally,
probably joined the hinder ridge, which is divided into two unequal
parts, its upper (smaller) portion being round, and the lower part
pyriform.

Reuter’s Beyrichia tuberculato-Kochianu + has a somewhat similar
valve, but its middle lobe is short, and the hinder ridge is much too
large and tuberculate. Some varieties, however, of B. Buchiana,
Jones, figured and described by Kiesow as var. nutans t, on account
of the strangulation of the top of the posterior ridge, supply a near
equivalent to the little form under notice. Hall’s B. equilatera,
from Arisaig, Nova Scotia (as figured, Canad. Nat. Geol. vol. v. 1860,
p. 158, fig. 20), is like this, but the’free ridge is larger, and the central
lobe is very much smaller.

Another form near to this is Ulrich’s Beyrichia persulcata (Journ.
Cincinn. Soc. N. H. vol. vii. no. 1, 1879, p. 12, pl. vii. fig. 6); but the
latter has a ridge or lobe between the divided ridge and the margin.

In the specimen, Brit. Mus. 59723; a thin limestone, largely
made up of “ ZL. cylindrica, Hail,” obscure and imbedded, chiefly on
one plane; L. minutissima, Hall, and Primitia Whitfield2, nov., are
also present. On one plane is the cast of a little ripple-mark, and
this small Beyrichia lies in it.—Cincinnati, Ohio.

6. Bryricuia parasitica (Hall). (Woodcut, fig. 1.)

Size: length 1:15 mm., height ‘625 mm.

Mr. J. M. Clarke, of Albany, has kindly sent me a sketch of what
was probably intended for “ Leperditia parasitica,” Hall, Paleont.
New York, vol. i1i. 1859, p. 376 (pl. lxxix. a, figs. 8a,b; notpublished).

* Ann. & Mag. Nat. Hist., August 1855, p. 89, pl. v. figs. 15, 16; Krause,
Zeitschr. d. D. g. Ges. 1877, p. 35, pl. i. fig. 174; Reuter, op. cit. 1885, p. 645,
pl. xxvi. fig. 19 4 a.

+ Zeitschr. d. D. g. Ges. 1885, p. 643, pl. xxvi. fig. 14; in this and in some of
his varieties of B. Buchiana it is the anterior lobe that is shown to be divided

into two parts.
t Op. cit. 1888, p. 7, pl. i. figs. 11 and 14.

Quart.ourn.Geol. Soe. Vol. XLVI PL. 1,

emesis
oe

i

E C.Kmight del.et hth. West, Newnan &Co.1mp.

NORTH-AME RICAN OSTRACODA.

| Quart.Journ Geol.Soc Vol XLv1 PI. i].

10.0

Pie PORE ee ea ca Fe inte he eto oir AE

r \
A cosmuaan
ene dha eS E 0 cee hs te et i ne a
‘ /
j
Ae /
\ /

ee pes
NS ok Be

EC Knight del.etlith. West, Newman & Co. rmp

NORTH-AMERIGAN OSTRACODA

Quart Journ.Geol. Soc Vol. XLVI.P1 IL.

13.0 13

14,0 14

aad “/ 4s 16

Geo Weat & Sone del lith et imp

SILURIAN OSTRACODA

. a

Quart.Journ.Geol. Soc Vol. XLVI.P1 IV.

St MAretente meena

Geo West & Sone del lith et imp

SILURIAN OSTRACODA.

FROM NORTH AMERICA, WALES, AND IRELAND. h7

The specimen is from the Tentaculite-limestone of Herkimer Co.,
N.Y. It is about 1:15 mm. in length, and belongs to the B.
Kledeni-clausa group, passing almost into Kledenia, by the full
ventral coalescence of the fore and aft lobes and the feeble develop-
ment of the anterior sulcus.

Fig. 1.—Beyrichia parasitica (Hall).
(Magnified 20 diameters.)

This drawing (fig. 1) is remarkably similar to the specimen from
New Brunswick, described and figured in the Ann. & Mag. Nat.
Hist. ser. 6, vol. iii. 1889, p. 381, pl. xvii. fig. 7 a, as being probably
the same as Beyrichia arcuata (Bean).

Fig. 2.—Beyrichia Clarket, sp. nov.
(Magnified 20 diameters. )

7. Beyricuia CLaRKEI, sp. nov. (Woodcut, fig. 2.)

Size: length 1°45 mm., height ‘9 mm.

Mr. Clarke has also courteously supplied me with a drawing of a
small Ostracod (fig. 2) which is associated with Beyrichia oculina
and B. notata-ventricosa in the Lower-Helderberg Group of Herkimer
Go., N.Y. |

Subquadrate and deeply sulcate, this appears to be intermediate to
Bollia lata (Pl. III. fig. 3) and Beyrichia Halli (Pl. IV. fig. 21),
see above, pages 12 and 15. The middle or horse-shoe ridge not
being free below, and the two lateral sulci not quite reaching the
ventral margin, place it nearer to the quadrijugate B. Hallit than
to Bollia. In this we can see a passage-form between the two
genera.

I propose to distinguish this interesting form as Beyrichia Clar’ei,
naming it after my obliging friend, Mr. J. M. Clarke, Prof. Hall’s
accomplished paleontological assistant in the State Museum at

Albany, N.Y.
Q.J.G.8. No. 181. C

18 PROF, T. R. JONES ON SOME PALAIOZOIC OSTRACODA

8. Bryricu1a mquitateRA, Hall. (PI. II. fig. 6.)

Beyrichia equilatera, Hall, ‘ Canadian Nat. & Geol.’ vol. v. 1860,
p. 158, fig. 20.

Beyrichia equilatera, Dawson, ‘Acadian Geology,’ 3rd edit. 1878,
p. OOO, wie aN 7

Size: length ‘8 mm., height °52 mm.

The specimen shown by fig. 6 is a poor cast of a Beyrichia, related
to Beyrichia Kledent. It is from Arisaig, Nova Scotia, in the
same kind of sandstone as that containing B. pustulosa (see below).
Tt is labelled B. equilatera, but is not much like the figure published
in the ‘Canadian Naturalist and Geologist,’ 1860, which seems to
have one strong curved ridge, a small central lobe, and two little
lobes (net mentioned in the description) representing a third ridge.
Our figured specimen has the third lobe slightly modified by a faint
oblique sulcus, but is not actually divided. The anterior ridge at
the other end rises high up dorsally, and curves well down to join
the middle lobe.

9. BEYRICHIA TUBERCULATA, Boll, var. pustunosa, Hall. (Pl. IL.
figs. 1 a, 6, ¢.)

Beyrichia pustulosa, Hall,‘ Canad. Nat. & Geol.’ vol. v. 1860, p. 157,
fig. 19; Dawson, ‘Acad. Geol.’ 2nd edit. 1868, & 8rd edit. 1878,
pp. 608, 609, fig. 216.

Beyrichia tuberculata, Jones, ‘ Quart. Journ. Geol. Soc.’ vol. xxvi.
1870, p. 492; ‘Geol. Mag.’ 1881, p. 344, pl. x. figs. 8, 9, & 10.

Size: length 5 (?) mm., height 2°8 mm., thickness of carapace
2 mm.

Our fig. 1 is one of the forms of this Nova-Scotian Beyrichia, and
being an internal cast is comparable with fig. 8, pl.x. Geol. Mag. 1881;
but it has lost its anterior fourth by fracture, and the hypertrophy
of the antero-ventral lobe makes a difference. Although the hinder
lobe in fig. 8 (Geol. Mag.) is partly broken away, the two specimens
may have agreed in this region. As for the valve itself, fig. 9
(Geol. Mag.) is quite equivalent to the cast shown in fig. 8 and to
our specimen, except that the latter has the hypertrophied lobe,
which, however, is not at all an essential or specific feature *.

Our fig. 1, if restored with its valve complete, may be regarded
as equivalent to Boll’s B. tuberculata, having the large lobe, fig. 1 a
(Archiv Ver. Fr. Nat. Meklenburg, 16 Jahrg., 1862, p. 119). This
form, and the same without the big lobe, are described and figured
by G. Reuter (Zeitschr. d. D. g. Ges. vol. xxxvii. 1885, p. 634,
pl. xxv. figs. 24 & 238) as B. tuberculata-qibbosa. Fig. 10 (Geol.
Mag.) is not quite perfect along the antero-dorsal margin; but may
be regarded as a large growth of B. tuberculata, with the lower
portion (preserved) of the anterior lobe proportionally and normally
large.

* Ann. & Mag. N. H., April 1886, pp. 339-342.

FROM NORTH AMERICA, WALES, AND IRELAND. 19

These slightly differing forms may require a varietal name; Dr.
Hall’s “ pusrutosa” precedes that given by Herr Reuter, and can
be retained. |

Our specimen, labelled “ Beyrichia pustulosa: Arisaig, Nova
Scotia,” is a sandstone cast of the inside of a right valve, coated
with hematite. It lies on a small piece of fine-grained micaceous
sandstone, almost wholly stained red, but whitish here and there.

10. BryricHIa HAMILTONENSIS, sp. nov. (Pl. IT. fig. 3.)

Size: length 1:66 mm., height -93 mm.

Suboblong, straight on the back, elliptically rounded below ;
multilobed, the middle lobe isolated and oblique; anterior lobe
forked by a vertical suleus; posterior lobe similarly furcate, but
not so deeply, and passing downwards and forwards (broken) to a
swollen portion just at the middle of the ventral region. All the
surface is pimpled, some of the granulation becoming sharp and
prickly at the dorsal region. This is distantly allied to B. dubia,
Reuter, Zeitschr. D. g. Ges. vol. xxxvii. p. 648, pl. xxvi. fig. 22,
and remotely to B. tuberculata, Boll, which may be taken as the
central form of a large group of these Ostracoda.

B. hamiltonensis is so-called from its belonging to the Hamilton
Division of the Devonian Series in the United States. It came
from Kighteen-mile Creek, Lake Erie Shore, N.Y.

11. Beyrtcnia* crntata, Emmons, (PI. IIT. figs. 12 a, 6, 13 a, 6,
iO, 450, b, 163° Pl. LY. figs. 16a, 6, 17 a, 6, 18a, 6.)
Beyrichia ciliata, KH. Emmons, ‘ American Geology,’ vol. i.’pt. 2,
1855, p. 219, fig. 74¢ (right valve); ‘Manual of Geology,’ 2nd
edit. 1860, p. 100, fig. 90.
B. twmifrons, Hall, ‘ Twenty-fourth Report State N.Y. Mus. N. H”’
1871-72, p. 231, pl. viii. fig. 11 (right valve) ; Report Geol. Survey
Ohio, vol. ii. pt. 2, 1875, p. 102, pl. iv. fig. 8 (right valve).

Length. Height. aoe
mm. mm. mm.
me, Wy fie 12; Pl. LY. fig. 16... 1-53 36 6
ne. 13 ; aa RS at 1:06 (with flange) 66
Size < fig. 14 ; Hels 2/16 1:0 do. 6
| Bema) tai. Be sf dase 1:56 ‘93 do. O3
g TSO RMS ole WiRTssaleca’« « 1°6 ‘86 (no flange)

Valves suboblong, ends rounded unequally, but almost parallel ;
in some cases upright or nearly so (PI. ILL. figs. 18a and 15a);
sometimes oblique from above downwards and backwards (PI. ILI.
fig. 14a); dorsal edge straight, with a long hinge-line; ventral

* Mr. E. O. Ulrich proposes to find a more convenient generic group for
this and some allied forms.
c2

20 PROF. T. R. JONES ON SOME PALZZOZOIC OSTRACODA

border gently curved and ciliated (PI. III. figs. 12 a, 16, and PL IV.
fig. 16a, b), and in many instances provided with a broad, thin,
smooth, outstanding lip above the ciliated border, and hiding it
(Pl. ILI. figs. 134,144, 15a, b, and Pl. IV. figs. 17 a, b, 18a, 6).
This flange-like lip varies in breadth with different individuals, and
in its distance from the ciliated edge (see Pl. III. fig. 15 6, and
Pl. IV. figs. 17, 18). The surface of the valves is crossed by two
strong, and more or less curved or even sigmoidal furrows, varying
in width and intensity, as seen in Pl. III. figs. 12 a, 13 a, 14 a, and
15a. There are consequently three unequal, obliquely transverse
lobes. The curve of the hindermost furrow encloses the highest
and roundest of the lobes. The middle lobe sometimes curves
round ventrally to join the hindermost (as in figs. 13a and 15a);
but sometimes it ends ventrally in an isolated hollow process or
spine (broken in figs. 12a@ and 14a). Another difference among
the specimens is to be seen in the flange and prickles of the ventral
margin, These may both be present (as in Pl, III. figs. 13a, l4a,
15 a, 6, and Pl. LV, figs. 17 and‘18). In Pl 111, fies’ 12 @ ana
and Pl. IV. fig. 16, the fringe only appears. This feature gave
origin to Dr. Emmons’s name for the species. The swollen lobe
not being in front, but behind, vitiates the name given afterwards
by Dr. Hall.

The surface of the valves is always granulose, the granules having
different degrees of coarseness, according to age apparently (see figs.
12,13, 14; in figs. 14a and 154 this feature was inadvertently
neglected owing to the granules becoming lower, broader, and
coalescent).

The figure given by Prof. Hall resembles Pl. III. fig. 15 a, except
that the outstanding flange is not defined. Prof. Emmons’s figure
(except that it is a right instead of a left valve) is comparable with
Pl. ILI. fig. 12a, but without the ventral process. The interior of
a left valve (Pl. III. fig. 16) shows the reverse aspect.

This well-marked species occurs in two picces of stone (marked
59725) in the British Museum :—1. A thin, light brown (weathered)
limestone, consisting of small organisms, such as Encrinital joints,
Brachiopods, and Polyzoans, with B. ciliata and Primitia minuta
(red in colour), standing out more freely on one face than the other.
2. A dark grey, thin, similar limestone, with light grey shaly
faces. Both from Cincinnati, Ohio.

Also in specimen I. 512, Brit. Museum; a grey limestone seam, ~
weathering brownish grey, made up of small organisms (Encrinital
joints, Brachiopods, Polyzoans, &c., with Ostracoda, chiefly B.
ciliata), From the Hudson-River Group, Cincinnati, Ohio.

Figs. 15 and 16, Pl. ILIL., are ina bluish-grey limestone (weathering
brownish) consisting of small organisms, such as Polyzoa, Encrinital
joints, fragments of Trilobites, &c., with B. ciliata. Cincinnati
Group, Lower Silurian, Cincinnati, Ohio. Given to me some years
ago by Dr. E. W. Claypole, F.G.S. |

The edge views in Pl. [V., figs. 16-18, correspond to the valves
in Pl, ILI. figs. 12-14 respectively.

FROM NORTH AMERICA, WALES, AND IRELAND. 21

12. Beyricata ocurirera, Hall. (PI. IV. figs. 19 a, 6, 20.)

Beyrichia oculifera, Hall, ‘ Twenty-fourth Report N.Y. State Mus.
N. H.’ 1871-72, p. 232, pl. viii. figs. 9, 10; Report ‘Geol. Surv.
Ohio, vol. 11. pt. 2, 1875, p. 103, pl. iv. figs. 9, 10.

Length. Height. Thickness.

f mm, mm. mm.
Size 50S Sa a a tL °66 (without the boss).
BO Ro 0 LAF 1:0 ;

This interesting species is related to B. ciliata, Emmons (B. twmi-
frons, Hall), having the two curved parallel furrows and three
curved lobes ; but the latter, more uniform and thinner than in B.
ciliata, are not separated one from another ventrally, and the
hindermost is developed in the dorsal region into a remarkable pro-
cess, like a small thick-stemmed mushroom, smooth (?) on the top *,
and delicately beaded round its edge. This is directed backwards,
and projects so high, that it is not usually preserved, as it is in
fig. 19 a, 6, but worn away, as in fig.20. This projecting ornament
is on the hindermost (highest and thickest) third of the valve, and
has no relation to an eye f.

The valve has a neat, smooth, ventral flange,

_ British Museum (no. 59719). Light bluish grey, thin, argillaceous

limestone, containing on the bed-planes Ostracoda (B. oculifera
chiefly), Polyzoa, Brachiopoda, and fragments of Trilobites, all
abundant, and some Encrinital joints, Cincinnati, Ohio.

. IX. Isocrrtma, Jones, 1858 & 1870.

1. Isocuinina tinEaTa, sp. nov. (PI. II. figs. 5a, b, and 84a, b.)

Length. Height. Phickness.
mm. mm. mm,
RE) oise.4 nt 1-04 64 4
= oe 1:0 D2 "48

Fig. 8 indicates a young individual; oblong, straight above and
below; ends unequally rounded; surface undulate, steep at the
free edges, and particularly abrupt at the ends; ornamented with
very delicate longitudinal striae.

The adult form in fig. 5 is oblong, with nearly equal rounded
ends; surface gently and almost equably convex, but undulate ;
broader and sloping more gently at one end(anterior), and margined
with a weak rim or lip on the free edges ; smooth, but faintly lineate
near the posterior end.

This differs from J. lineata in its young state (fig. 8) in being
larger, convex without abrupt ends, more distinctly lipped, and only
feebly striate.

* Tn our specimens the facet-like marks figured by Prof. Hall are not visible,
and the edge is not fringed but beaded.

| This fact has already been alluded to in the Ann. & Mag. N. H., April 1886,
p. ddl.

22 PROF. T. R. JONES ON SOME PALZOZOIC OSTRACODA

Both specimens are from the Hamilton Group, at Monteith’s
Point, Canandaigua, State of New York. .

2. Isocnrzina (?) FaABACEA, sp. nov. (PI. II. fig. 11.)

Size: length :92 mm., height -44 mm.

Narrow-oblong, bean-shaped, straight above, gently curved below,
semicircular in front, obliquely rounded behind, faintly impressed
in the middle of the dorsal region; sloping gently dorsally, and
more abruptly on the free margins. Surface apparently punctate,
but in reality delicately reticulate all over.

From the Hamilton Group, at Eighteen-mile Creek, Lake Erie
Shore, N.Y. .

3. Isocninina Sextyr (Whitfield). (Pl. I. fig. 7.)

Primitia Seelyi, Whitfield, ‘ Bulletin American Mus. Nat. Hist.
Vol. 113 no. 2, 1889; p60; pl. xi figs, 6) 7.

Size: length 5°0 mm., height 3-2 mm.

The specimen here figured differs somewhat from Prof. Whitfield’s
illustration in being less Leperditioid, that is, more oblong, being as
high in front as behind, in having a more developed posterior
cardinal angle, in not showing a smooth space in the antero-dorsal
region, and in having a slight swelling (with a faint depression) on
the median line behind the centre. Its ventral margin is that of
an Isochilina. I cannot refer it to Primitia. One of its nearest
allies is Isochilina labrosa, Jones, Ann. & Mag. N. H., May 1889,
pp. 383, 384, figs. 3 and 4, and pl. xvii. fig. 11; and another, but
not so near, is Jsochilina Jonest, Wetherby, ‘Journ. Cincinn. Soc.
Nat. Hist.’ vol. iv. 1881, p. 4 (separate), pl. il. figs. 7, 7a.

From a dark blue limestone, Shoreham, Vermont, and waterworn
fragments of a granular limestone, Providence Island, Lake Champ-
lain; probably Birds-eye Limestone. Our figured specimen is in
grey limestone largely composed of Jsochiline (Providence Island).

4, Isocutnina erEcanrta (Whitfield). (Pl. L. figs. 9, 10.)

Primitia gregaria, Whitfield, ‘ Bulletin N. H. Mus. N. Y.’ vol. ii.
no. 2, 1889, p. 58, pl. xin. figs. 3-5.

Length. Height.
mim. mm.
gi ah Bigs) 9 uage 2-9 - 2-06
, LOiu oer 2:6 1:8

This species is variable in outline and features, as noticed by
Prof. Whitfield. Fig. 10 agrees in outline with Prof. Whitfield’s
fig. 5, but the aspect of the nuchal notch and its tubercles approaches
that of his fig. 3. Our fig. 9 differs from all in outline and notch ;
but, as to the latter feature, it approaches fig. 5, one tubercle lying
in a broad notch. The furrowed sides of the notch in our fig. 10
remind us of a complex furrow on the front slope of a Carboniferous
Cyclus, sp., having lumpy margins, and of the ocular spot and its

FROM NORTH AMERICA, WALES, AND IRELAND. 23

broad furrowed notch in the Devonian Kyamodes Whidbornei, Ann.
& Mag. N. H. ser. 6, vol. 1. 1888, p. 296, pl. xi.

The valves have a bright surface; they are in the same black
rock as that containing Jsochilina cristata. These two have their
representatives in the Lower-Silurian rocks of Canada, which supplied
Isochilina gracilis and I, Ottawa, Ann. & Mag. N. H. ser. 3, vol. i.
1858, p. 248.

Isochilina gregaria is closely allied to Isochilina grandis, Jones,
Ann, & Mag. N. H. ser. 2, vol. xvii. 1856, pl. vi. fig. 14, and
Ope eu. ser, O, vol. ix. 1882, p. 171.

In hard black calcareous shale, Cave Island, Ball’s Bay, Lake
Champlain, Vermont. Probably from the Calciferous-Sandstone
Formation.

5. Isocnirina cristata (Whitfield). (Pl. I. fig. 8.)

Primitia? cristata, Whitfield, ‘ Bulletin Amer. Mus. N. H.’ vol. ii.
no. 2, 1889, p. 59, pl. xii. figs. 1 & 2.

Size: length 2°3 mm., height 1:8 mm.

The specimen here figured differs somewhat in outline from either
fig. 1 or fig. 2 of Prof. Whitfield’s memoir; it has a more simple
nuchal depression without any tubercles, and shows a non-punctate
surface. The nuchal mark varies in intensity in different specimens.
The short, oblique ridge below the centre is always present. ‘

This also is an Jsochilina, there being no ventral overlap; other-
wise it might well be a Leperditia. From Cave Island, as above.

For the three foregoing species of Jsochilina, characteristic speci-
mens were chosen and drawn betore the Memoir by Prof. k. P.
Whitfield came to hand. |

6. Isocninina?, sp. (PI. I. fig. 15.)

Size: length 4:1 (?) mm., height 2°3 (?) mm.

In fig. 15 we have indications of a Leperditioid valve with a
nuchal depression asin tig. 8, and a broken, hollow, subcentral
process, analogous to the oblique ridge in fig. 8, but apparently
stronger and more limited in area. It may, however, have been
more like the sharp process in Kolmodin’s Leperditia tuberculata,
(itvers. k. Vet.-Akad. Forh, (1879), 1880, p. 135, pl. xix. figs. 1a,
16; and Walcott’s Leperditia (Lsochilina) armata, ‘ Thirty-fifth
Report N.Y. State Mus. N. H.’ 1883, p. 213, pl. xvii. fig. 10.

From Cave Island, as above.

X. Genus Leprrpirra, Rouault, 1851.

1, Leperpitia (?) seneca, Hall. (PI. I. figs. 13, 14.)

Leperditia seneca, Hall, ‘ Fifteenth Annual Report, University of
the State of New York,’ 1862, p. 112.
Length. Height.

mm. mm.

Sine Die Mey sad 6 62 “44
- 1 ‘56 36

24 PROF. T. R. JONES ON SOME PALZOZOIC OSTRACODA

Small, subtriangular, with the back straight, the ventral margin
strongly curved, giving treat relative height to the valve.

In a fine- grained sandstone, caleareous and finely micaceous ;
from the Hamilton € ~ yp, Ontario Co., New-York State.

2, Leprrprita (?) stnvata, Hall. (PI. I. figs. 12 a, 6, c.)

Leperditia sinuata, Hail, ‘Canad. Nat. & Geol.’ vol. v. 1860,
p. 158; and Dawson, ‘ Acadian Geology,’ 3rd edit., 1878, pp. 609,
610.

Size: length -99 mm., height ‘60 mm., thickness -48 mm.

This is a small, black, shining Leperditia (?), subovate in outline,
being straight on the back and without distinct cardinal angles ;
semicircular behind; boldly curved below, but rising with a less
bold curvature to the limited curve in front. Our specimen does
not show the minute tubercle, but the sinuous mark or little fold
on the postero-ventral border is present, and reminds us of a some-

hat similar feature in Beyrichia hians, Boll, 1856.

¢ In a grey limestone with Brachiopods &c. from Arisaig, Nova
Scotia.

3. Leperpitra Hupsonica, Hall. (PI. I. figs. 5a, b,c (after the
original drawings), and figs. 11 a, 6, c; and Pl. III. fig. 20 ?.)

Leperditia hudsonica, Hall, ‘ Paleeont. New York,’ vol. iii. 1859,
p- 375 (pl. Ixxix. 4, figs. 7 a, b, ¢; not published).

Length. Height. Thickness.

‘ mm. Inm, mm,
Pts sie 5, epee 5°0 3°50 3°0
Size dD ie cal ecient 48 36 32
TLE he. 20 nc Samar (?)°46 26

Carapace small, symmetrical and very convex (subglobular), being

almost as thick as it is high, straight on the back, with the anterior

_ cardinal angle more developed than the other ; free margin (ventral
edge and two ends) well rounded, rather more than semicircular ;
anterior extremity less truly rounded than the other. Further
exact description is given by Prof. Hall (J. ¢.), especially that the
right overlaps the left valve. His specimen came from the base of
the Lower-Helderberg Group, at Becraft’s Mountain, near the
Hudson.

A very similar, if not identical, form has been sent to me by
Prof. Whitfield for examination. This, of very much smaller size,
is shown by figs. 11 a, 6, c, taken from two little subglobose valves,
somewhat pustulose towards the curved edge. Excepting the granu-
lation there is apparently nothing to separate them from L. hud-
sonica. They occur on a piece of limestone (‘ 500 d’’), consisting
of Crinoidal joints, Brachiopods, Polyzoans, &c., and belonging to
the Hamilton Group (Devonian); at Eighteen-mile Creek, Lake
Erie Shore, New-York State.

FROM NORTH AMERICA, WALES, AND IRELAND. 25

Fig. 20, in Pl. III., is a minute Leperditian valve of the same
shape as L. hudsonica, but not quite so high in proportion. Its
cardinal angles are too strong for Leperdinia (Isochilina) minutis-
sima, Hall; and it is less Leperditioid in sk }, having more equal
ends, thus approaching Leperditia anna, Jo. es (1858), in outline.
It is from one of the Cincinnati limestones, associated with Primitia
minuta (Pl. III. figs. 18, 19) and dAtchmina Byrnesi (Pl. IIL.
figs. 9-11).. Given to me long ago by Dr. E. W. Claypole, F.G.S.

L. subquadrata of Pennsylvania (Claypole Collection) is a true
Leperditia, and nearly allied to L. hudsonica.

4, Leprrpitta Craypotet, sp. nov. (Pl, III. figs. 17 a, 4, ¢.)

Size: length ‘66 mm., height :45 mm., thickness ‘2 mm.

Minute, suboval, cardinal angles not being developed at the ends
of the nearly straight back ; ends nearly semicircular, ventral border
elliptically curved ; compressed, especially at one end (anterior) and
along the dorsalregion. This is less Leperditioid in shape and much
less convex than Hall’s Leperditia (Lsochilina) minutissima, ‘Twenty-
fourth Report N.-Y. State Museum Nat. Hist.’ 1871-72, p. 231,
pl. viii. fig. 13 [right valve]; ‘Geol. Surv. Ohio,’ vol. ii. pt. 2, 1875,
p- 102, pl. iv. fig. 4 [right valve]. The ventral border having a
slight flange (not shown in the figure), allowing an overlap, we can
regard this little valve as belonging to a true Leperditia.

It occurs in one of the Cincinnati limestones with Beyrichia ciliata,
collected years ago by Prof. E. W. Claypole, D.Sc., F.G.S., whose
energetic geological work in the United States has supplied me with
numerous specimens of Paleozoic Ostracoda, and after whom it
is here named.

5 & 6. Leprrpitra atta (Conrad), and L. Jonxsr, Hall. (L. alta,
var., Pl. I. figs. 6a, b; after the original drawings.)

Oytherina alta, Conrad *, ‘ Third Annual Report on the Paleontol.
Departm. of the Survey, N.Y., 1840, p. 204.

Cytherina alta, Vanuxem, ‘Natural History of New York,
Geology, Part III. Survey of the Third Geological District, 1842,
p. 112, fig. 23, no. 6 (bad drawing); copied in Emmons’s ‘ Manual
of Geology,’ 2nd edit. 1860, p. 113, fig. 162, no.6; and in L.
Lincklaen’s ‘‘ Guide to the Geology of New York,” in the ‘ Four-
teenth Annual Report of the Regents of the University, State N. Y.’
1861, p. 58, fig. 19, no. 6 (pl. ix. fig. 6).

Cytherina alta (?), Hall, ‘Paleeont. New York,’ vol. ii. 1852, p. 338,
pl. Ixxviii. figs. 2a, b, c, d [figs. a & b, alta; ¢(?) & d, Jones? }.

Leperditia alta (?), Jones, ‘Ann. & Mag. N. H.’ ser. 2, vol. xvii.
1856, p. 88, pl. vii. figs. 6 & 7 [fig. 6, Jonesi; fig. 7, alta].

Leperditia alta, Jones, ‘Ann. & Mag. N. H.’ ser. 3, vol. i. 1858,
p. 250, pl. x. figs. 8 & 9.

Leperditia. alta, Hall, ‘Paleont. N. Y.’ vol. iii. pt. i. 1859, p. 37:

* See Dr. James Hall’s Preface to the ‘ Paleont. New York,’ vol. i. 1846,
Ppp. X, Xle

26 _ PROF. T. R. JONES ON SOME PALZOZOIC OSTRACODA

(pl. Ixxix. a, figs. 6 a—e, not published); and Leperditia Jonesi, p. 372
(figs. 7 a—e, not published).

Leperditia alta [var.], Dana, ‘ Text-book of Geology,’ 1870, p. 98,
fig. 175 (reversed); ‘Manual of Geology,’ 3rd edit. 1874, p. 239,
fig. 473.

Leperditia alta, Meek, ‘ Geol. Survey Ohio,’ 1873, p. 187, pl. xvii.
figs. 2a [ Jonesv], 2 b [alta].

Leperditia alta, Jones, ‘Ann, & Mag. N. H.’ ser. 5, vol. viii. 1881,
pp. 345, 346.

Leperditia alia, Whitfield, ‘Geology of Wisconsin,’ vol. i. 1883,
p. 198, fig. e [alta, var.]; vol. iv. 1882, p.323, pl. xxv.figs. 8 & 9 [alta].

Leperditia alta, Jones, * Ann. & Mag. N. H.’ ser. 5, vol. xiv. 1384,
pp. 342-344,

Size :—
Length. Height, Thickness.
mmm. mm, mm.

EP sh netorrecith ec Se 9 6 (L, alta, var.).
Pal NX: vol. ipl. eva, :

TONG oe iakces cg, by Ge 18 11s (L. Jones: ?).

Tag rg Cea a Ne 12 ‘

ene oe 5 24 } (Lgialta),

These are described as ‘‘individuals of different size”; and
therefore are figured probably of the natural size.

A. & M. N. H. 1856, pl. vii:

HR SO ga AA sites bce os 6 5 (L. Jonesi) \ Arctic
BUS AE Sui ahs oR ain’ oye es Yop 5 3 2(L, alta) Regions.
Ave MN. 1858,*pl. sa
o BS Rm:
aS : te ee iki, ones 6 a } (L. alta) Pennsylvania.
oh a Oat OCC) aCe er Ps
Geol. Surv. Ohio, 1878, pl. xvii.
‘ZA Ry ee ae 103 74 (L. Jonesi?) Ohio
| eC geen en Alef 113 64 (L. alta) ;

Some confusion exists in the definition and nomenclature of these
species. The drawing in Vanuxem’s work is very bad, but Prof.
Hall retained the specific name (with some doubt) for the four spe-
cimens which he described and figured in the ‘Palzontol. New York,’
vol, ii. 1852, p. 338, pl. Ixxviil. figs. 2 a, b, ¢, d.

1. In 1859, ‘ Pal. N. Y.’ vol. iii. p. 372, one of the forms usually
associated with ZL. alta was separated by Prof. Hall as Leperditia
Jonesi, being of larger size and greater proportional height, more
convex centrally, and becoming papillose (part of a valve, fig. 2 d)
on the surface when weathered. If we take fig. 2c for this species,
it is obliquely subovate, well rounded behind, and curving obliquely
upwards and forwards in front; the valve is therefore higher
behind than in front. It is. straight on the back, with its hinge-
line much shorter than the fuli length of the valve (proportion ;

FROM NORTH AMERICA, WALES, AND IRELAND. 27

11 to 184, with 12 for the height); cardinal angles distinct, but
blunt ; the front end slopes downwards suddenly to meet the antero-
ventral curve. With this species, Jones’s fig. 6 of pl. vii. 1856, and
Meek’s fig. 2a, pl. xvii. 1873, more or less conform, but the former
is much rounder, and the.latter is more subovate.

2. The two smallest of the three whole valves above mentioned
remain for Z. alta. Fig. 36 is suboblong, with a straight dorsal
and slightly arched ventral border; the posterior extremity is semi-
circular, and the anterior has rather less height and curvature; the
antero-dorsal angle and slope are less pronounced than in fig. 2 ¢;
the hinge-line is also proportionally longer (8 to 12, the height
being 7). Fig. 2a is evidently badly drawn. Jones’s fig. 7, pl. vil.
1856, is equivalent ; and his figs. 8, 9, pl..x. 1858, Meek’s fig. 2 a,
pl. xvii. 1873, and Whitfield’s fig. 8, pl. xxv. (Wisconsin), 1883,
are also probable equivalents, though their outlines taper somewhat
anteriorly.

3. The published illustrations resembling the drawing sent from
Albany and here reproduced (Pl. I. fig. 6) are Prof. Whitfield’s
fig. e (Lower Helderberg), p. 198, ‘ Geol. Wisconsin,’ vol. i., and a
small woodcut in Dana’s ‘Manual’ and‘ Text-book of Geology.’
The great depth and elliptic curvature of the postero-ventral, and
the narrowness of the antero-ventral region, give a subtriangular
outline to the valve. It is probably a variety.

4, Prof. Hall found Z. alta abundant in the Tentaculite-limestone
(Waterlime Group) of Albany, Schoharie, Greene, Herkimer, Oneida,
and Cayuga Counties in the State of New York (‘ Pal. N. Y.’ iii.
p. 374); and Z. Jones in the Coralline Limestone (Niagara Lime-
stone) of Schoharie and Herkimer Counties (op. cit. p. 372); both
limestones belong to the Lower-Helderberg group. Meek’s speci-
mens were from Greenfield, Ohio; Whitfield’s from Waubakee,
Wisconsin ; Jones’s from Schoharie and from Pennsylvania (all of
these being from the ]ower-Helderberg Group), and some from the
Upper Silurian of Wellington Channel in the Arctic Regions.

In the British Museum a specimen (I. 511) of black limestone,
with Brachiopods, from the Lower-Helderberg Group, of the Hel-
derberg Mountain, New-York State, contains several individuals of
two forms of L. alta, Hall; but the edges of the valves cannot be
satisfactorily examined, being, as usual, more or less imbedded in
the matrix.

7. Luperpitia NANA ?, Jones. (PI. IV. fig. 4.)

Size: length ‘73 mm., height 53 mm.
_ PL IV. fig. 4 would be very much like Leperditia (Isochilina)
minutissima, Hall, were its ventral border more elliptically curved
and not so semicircular; nor are the dorsal angles of Hall’s species
so acute as in our fig. 4, which is probably equivalent to the Lower-
Silurian Leperditia(?) nana, Jones, of Canada, Ann. & Mag. Nat.
Hist. ser. 3, vol. 1. 1858, p. 245, pl. ix. fig. 17.

From the Bala Beds near Welshpool, Montgomeryshire, North
Wales, collected by Mr. J. B. Morgan, F.G.8.

28 PROF. T. R. JONES ON SOME PALZOZOIC OSTRACODA

XI. XxEsToLEBERIS, Sars, 1865.
1. XesroLeBeRis WricHtr, sp. nov. (Pl. IV. figs. 14 & 15a, 6, ¢.)

Length. Height. Thickness.
min. mim, mm,
Ric-<ltrke ces ite 1:2 ‘76
Suns | it CaN 12 7 8

A Cytheroid Ostracod probably allied to the recent Xestoleberis,
see Ann. & Mag. Nat. Hist. ser. 5, vol. xviii. 1886, p. 264, pl. ix.
fig. 8.

Carapace tumid, oviform, but more convex on one edge than the
other, and one valve much larger than the other; both smooth. .

Named after Joseph Wright, Esq., F.G.S., of Belfast, who has
added much to our knowledge of fossil and recent Entomostraca. It
was obtained by him from the Lower-Silurian beds of the Chair of
Kildare, Leinster, Ireland, some years since. For some Cytheroid
and other Ostracoda sent from this locality by Mr. Baily and Mr.
Wright, see Ann. & Mag. N. H. ser. 4, vol. ii. 1868, pp. 54-62, pl. vii.

[ ADDENDUM, December 18, 1889.—Since this paper was read the
following interesting specimens from North America, and collected
by himself, have been shown to me by Dr. G. J. Hinde, F.G.S. :—

1. Several individuals of Prinitiopsis punctulifera (Hall), various
in their development and in the intensity of the reticulate surface-
ornament, from the Hamilton Group, at Thedford, Ontario. Also,
from the same formation at Eighteen-mile Creek, a small Strepu/a,
sp. nov. (?), and a small Bolla, near to, if not identical with,
B. bicollina, J. & H.

2. Schoharie, N. Y., Lower-Helderberg group:—Leperditia alta
(Conrad) and L. Jonesi(?), Hall; together with Kladenia notata

Hall).

3. acti, Nova Scotia, Lower-Helderberg group (C to D groups
of Honeyman) :—Beyrichia pustulosa, Hall (casts), scarcely distin-
guishable from B. tuberculata, Boll; and B. equilatera, Hall (casts),
scarcely separable from B. Kledeni.

4, Niagara Formation, Dundas, Ontario; small, simple Primitie,
flattened ; one has a minute tubercle at its sulcus.

5. Cincinnati Formation (Div. G of Billings), English Head,
Anticosti:—Numerous Ostracoda on thin limestone, some like
Bairdia, probably sp. nov.

6. Clinton or Niagara Formation, Division 2 of Anticosti Group,
W. of Jupiter River, Anticosti :—a fringed Primitia, sp. nov. ?

7. Cincinnati Formation, Group 1 of Billings, 8. of Junction Cliff,
Anticosti :—several minute Ostracoda attached to small fossils ; some
probably spp. nov. |

FROM NORTH AMERICA, WALES, AND IRELAND. 29

EXPLANATION OF PLATES I-IV.
Puate I.
North-American Ostracoda.

Fig. 1. Kledenita notata (Hall), var. ventricosa, Hall. a, left; 0, right valve.
(Magnified 4 diam.)
. Beyrichia trisulcata, Hall. Left valve. (Magn. 8 diam.)
. Beyrichia granulata, Hall. a, left valve (magn. 4 diam.); 0b, part of
surface (highly magnified).
. Beyrichia oculina, Hall. Left valve. (Magn. 4 diam.)
. Leperditia hudsonica, Hall. a, carapace (nat. size); b, right valve,
side view, and ¢, edge view (magn. 2 diam.).
. Leperditia alta (Conrad), var. a, right valve (nat. size); 0, inside view
(magn. 2 diam.).
[Figs. 1-6 are copied from the original drawings intended for
publication in 1859. ]
7. Isochitina Seelyi (Whitfield). Left valve. (Magn. 10 diam.)
8. Isochilina cristata (Whitfield). Right valve. (Magn. 15 diam.)
9 & 10. Isochilina gregaria (Whitfield). Right valves. (Magn. 15 diam.)
ll. Leperditia hudsonica, Hall. a, right valve; b, edge view; c, end
view. (Magn. 25 diam.)
12. Leperditia sinuata, Hall. a, right valve; 6, edge view; ¢, end view.
(Magn. 25 diam.)
13 & 14. Leperditia seneca, Hall. Right valves. (Magn. 25 diam.)
15. Lsochilina ?, sp. Right valve. (Magn. 6 diam.)

oOo Of Con

Puare II.

North-American Ostracoda.
[Figs. 1 a, 5, c, are magnified 10 diameters ; all the other figures 25 diameters. |

Fig. 1. Beyrichia tuberculata, Boll, var. pustulosa, Hall. Cast. a, right valve,
broken in front; 0, edge view ; ¢, end view.
2. Primitia seminulum, Jones. Left valve, broken in the middle.
3. Beyrichia hamiltonensis, sp. nov. Left valve.
4, Strepula sigmoidalis, Jones. Left valve.
5. Isochilina lineata, sp.nov. Adult. a, right valve; 0, edge view.
6, Beyrichia equilatera, Hall. Cast. Right valve,
7. Primitiopsis punctulifera (Hall). Young. a, left valve; 6, edge
view.
8. Isochilina lineata, sp.nov. Young. a, left valve; b, edge view.
9. Entomis rhomboidea, sp.nov. Left ? valve, altered in shape.
10. Entomis rhomboidea, sp. nov. a, lett? valve, less altered; 0, edge
view.
11. Jsochilina fabacea, sp.nov. Left valve.
12. Primitiopsis punctulifera (Hall). a, left valve; b, edge view.
13. Primitiopsis punctulifera (Hall). a, left valve; b, edge view of cara-
pace.
Puate III.

Silurian Ostracoda,

[All the figures are magnified 15 diameters, except figs. 125, 13}, 144, and
246, which are X70 diameters. |

Figs. 1, 2,3. Bollia lata (Vanuxem & Hall). Separate valves.
4-8. AMchmina spinosa (Hall). 4, inside of left valve; 5-8, right
valves,
9-11. Aehmina Byrnesi (Miller). 9, right valve; 10, left valve; 11
edge view of fig, 10.

30 PROF, T. R. JONES ON SOME PALAOZOIC OSTRACODA

Figs. 12-16. Beyrichia ciliata, Emmons. 12a, left valve; b, ornament, X 70
diam.: 18a, left valve; 6, ornament, x70 diam.: 14 a, left.
valve; b, ornament, X70 diam.: 15 a, right valve ; 5, end view:
16, inside of left. valve.

17. Leperditia Claypolei, sp.nov. a, left valve; 0, end view; ¢, edge
view.
18,19. Primitia minuta (Kichwald). Left valves; 18, inside; 19, out-
side of a poor specimen.
20. Leperditia hudsonica (?), Hall. Inside of valve.
21-23. Primitia minuta (Kichwald). 21, left valve (true shape); 22,
right valve ; 23, right valve. (These are from Talkof, Russia.)
24. Primitia Whitfeldi, sp. nov. a, right valve; 6, ornament, X
70 diam.
25. Beyrichia Buchiana (?), Jones. Left valve, not well preserved.

Puate IV.
Silurian Ostracoda.

[All the figures are magnified 15 diameters, except figs. 1 a and 6 a, which
are X40 diameters. ]

Figs. 1-3. Primitia Ulrichi, sp. nov. 1a, right valve, x40 diam.; 4, outline
of the same; ¢, edge view: 2, left. valve of a variety; 3, right
valve of another var. (All these are from the ‘‘ Utica Slate”
of Canada.)

4. Leperditia nana (?), Jones. Right valve.

5. Primitia humilis, J. & H., var. humilior, nov. Right valve.

6. Primitia Morgani, sp.nov. a, left valve, X40 diam. ; 6, the same,
x15 diam.

7. Primitia mundula, Jones, var. cambrica, nov. Right valve.

3. Primitia unicornis (Ulrich), and varieties. Fig. 10 is a right
valve; the other figures are left valves.

(Figs. 4-13 are from the Bala Beds near Welshpool, Mont-
gomeryshire.)

14,15. Xestoleheris Wrightit, sp.nov. 14, carapace, with the left valve
outwards: 15 a, carapace, right valve seen; 0, edge view;
c,end view. (From the Chair of Kildare, Ireland.)

16-18. Beyrichia ciliata, Emmons. 16a and 0, edge and end views of
fig. 12, Pl. III.; 17a and 3, of fig. 13; and 18a and 3, of
fig. 14.

19,20. Beyrichia oculifera, Hall. 19a, left valve; 0, edge view of the
same: 20, inside of a right valve (the boss injured),

21. Beyrichia Halli, sp. nov. Right valve.

22,23. Kledenia notata (Hall). 22, right valve; 23, left valve.

24, Kladenia notata, var. ventricosa, Hall. Left valve.

(Figs. 16-24 are from the United States.)

Discussion.

The Presmpent asked whether the Author had seen the originals
of the specimens from which the American drawings had been
made. He cited several instances showing the errors which had
arisen from describing forms from drawings onlv.

Dr. Woopwarpd commented upon the care the Author had taken
in describing these Ostracods, and the long time he had held his
work over whenever he felt any hesitation concerning his conclu-
sions. He felt sure that the Author had not described his new
forms without the greatest care having been taken to exclude the
possibility of error.

FROM NORTH AMERICA, WALES, AND IRELAND. 31

Mr. J. S. Crawrorp said that he had collected many American
specimens, which he would be happy to lend to the Author, or to
place in the Society’s Museum.

Dr. Hiypk said that although the Entomostraca of the Hamilton
group closely resembled those from the Silurian, the fauna of this
group generally was unmistakably Middle Devonian.

The AurHor, in reply, assented to Dr. Woodward’s remarks
concerning the upward passage of Lower-Silurian forms to recent
times, and said that he would examine Mr. Crawford’s specimens
with pleasure.

oe MONS. F. M. CORPI ON THE

2. The CatastroPHE of Kanrzor1K, ARMENIA.
By Mons. F. M. Corpr. (Read November 20, 1889.)

(Communicated by W. H. Hupuzston, Esq., F.R.S., Sec. G.S.)

Kantzorix, a small village of 215 inhabitants in the Caza de Tor-
toum, a dependency of the vilayet of Erzeroum, was situated in a
narrow valley at an altitude of about 1600 metres. It was ata
distance of 60 kilometres from Erzeroum, and of 10 kilometres from
Nikhah, the seat of the ‘*‘ Katmakamlik.”

The inhabitants of Kantzorik having noticed certain subterraneous
noises, and that the springs of a great mountain situated at the
western opening of their valley had dried up, were alarmed at these
phenomena and gave notice to the local authorities, who directed
them at once to evacuate their village ; but before they had time to

execute this project, towards noon on the 2nd of August, 1889, a —

frightful noise was heard, a part of the Kastern Mountain burst
open, the village was buried under a great muddy mass, and 136
villagers perished in it. Such is the account given by the survivors
of this terrible catastrophe, who affirm that they saw a red torrent,
which would lead one to think that this fluid mud was in a state of
ignition. 7

His Excellency Samit Pacha, Governor General of the vilayet of
Erzeroum, moved by the great misfortune which had happened at
Kantzorik, hastened to send assistance to the sufferers ; and to pre-
vent fresh disasters to the other villages which seemed to be men-
aced with the same fate, he took prompt and intelhgent measures,
placing their inhabitants in safe places, and did me the honour of
entrusting to me the task of going to investigate this phenomenon
on the spot from a geological point of view.

On the 9th August I proceeded to the locality of the disaster and
visited this region, which is so excessively hilly as tu present an
Alpine configuration.

In fact, the whole of this part of the Caza de Tortoum had been
formed in the Secondary period of Triassic, Jurassic, and Cre-
taceous strata, which, in consequence of a Plutonic movement, were
broken up and torn by granitic, trachytic, and especially basaltic
rocks, now forming great mountains, cones, and lofty peaks without
any system, and still presenting numerous traces of the former con-
stitution which they overtop, or to which they serve as a base accord-
ing to the nature of the dislocation.

In going from Nikhah towards Kantzorik, I was surprised by the
great number of balls of mud which occurred among the rolled peb-
bles of the ravine forming the continuation of the great valley of
Kantzorik. These balls, varying in diameter between 10 and 40
centimetres, and formed of sand and calcareous fragments of very
close grain cemented by an ashy material, did not appear until after
the disaster of Kantzo1ik.

CATASTROPHE OF KANTZORIK, ARMENIA. 33

_ After walking for half an hour I arrived at the western opening
of the valley and the terminal point of the flow. There I ‘could
see at once the complete boulcversement which had been produced a
week before. From this point to the foot of the great Eastern
Mountain (which is situated at the other extremity of the valley in

Sketch-plan of the district of Tortoum, where the catastrophe occurred
im August 1889*.

Vit, nase ; vag A Wa: Yf Hi Myers “a 2 a
eo Coe. %e {iL ws
Oj 00r 45 6H F; “Wire, je =:

bgcir’ 4 bie 5
a My My & 2

Oi)
Desks

rN Oat Ga

g(t hy
AS Re “Riise

lis 1a Nie Ae

\

iy ie ¢

hen

By FZ
a! yh he, %, i is" We. ds é Pah iat Beau, ih ” Mn, ? a E
Kus! 2) ah iy [., ii y, & JNM, 2 a
cs is fae t f willl he Me a, 2
i ue ‘on \ K eK duty uae
My wc Hw crcadyt® 4 iO sae LLY, OH We Z
- Vln g gh i ‘ae “i ‘gee nave 4 i ih iN p oh h a YS on.
Se ava Os agi S an Ha ret het if
‘ ; og Ee ie be fy ay Hay, AD Fi) iF
‘ong ta ao Vas Sy a wt on 2 hi we Z

Es yi in He

2S ane e Y ie i a, ys ree att Gu ae M fe iit
ae segs NY i

fw
“yy, tt
fy add
iif arrat til

if a
Cy a foe utanc ef i ve f, yl (it ff), “ial Ss sf
we 4 4 tat 4, | 4 tg” WU, 4 , tan
cia fe eG Se Gy { AMY TT
he Mal tCAat GZ 3 Pace dat Ue ye, Mi, i!

1. Eastern Mountain. 2. Kantzorik. 3. Nikhah.
4. Tortoum Kalé. 5. Sagher.

the direction from east to west), for a distance of about 7 or 8 kilo-
metres, and for a width varying between 100 and 500 metres,
according to the configuration of the ground, stretched, like a vast
motionless river, a mass of solidified marly mud, the greater part of
which was of a bluish-grey colour, and the remainder of various
other tints.

This material, which, taking account of its superficies and of the
inclination of the flanks of the mountains and hills forming the
valley, may be estimated approximately at more than 50,000,000
cubic metres, has the appearance of an undulating sheet, some
asperities of which attain a height of as much as 10 metres, and
sufficiently demonstrate that, after having been thrown out in the
fluid state, by contact with the cold air and the rapid volatilization
of the gases which it contained, it became solidified, and retained
upon its outer surface the character produced by its undulatory
movement, and the contraction which it underwent more or less
rapidly, which enabled it, even at its margins, to remain, like a talus,
above the level which it must have taken, had it spread further, in
extending. Of course the solidification of this fluid mass could only
take place from above downwards; and while the upper part acquired
consistence, the lower part still allowed of the passage of more
liquid materials, carrying with them the balls of which I have already

* This is a photographic reproduction of a sketch sent by the Author,

@.1.6..8. No, 181. D

34 MONS. F. M. CORPI ON THE

spoken—that is to say, unless they were thrown out first of all,
which is also very possible.

I ascended the whole of the valley to the spot where the “llogs
of Kantzorik was situated, which is indicated by a much more
strongly marked elevation of the muddy mass, in consequence,
apparently, of the obstacle which it presented to the surging stream,
although débris of houses and enclosures were carried on in great
quantities even to the extremity of the gigantic flow, where they
are still lying.

Continuing my progress, I arrived at the foot of the hill abutting
on the northern slope of the great mountain, but there in consequence
of the numerous deep crevasses, sinkings in and landslips (éhoule-
ments du terrain), I could not reach the summit without much
difficulty and fatigue. Finally, after all the trouble of ascending
this basaltic cone, I was repaid by the near view of a mountain in
full course of demolition.

The great Eastern Mountain, crevassed in all directions, presented,
for an extent of over 400 metres in width, an enormous vacuity
produced by the sinking in of a great part of its western flank, and
showed a gigantic trench between this part and its base. This
trench, this rupture of the mountain, the bottom of which could
not be seen in consequence of a fold of the strata, certainly served as
the orifice for the issue of the enormous quantity of mud which
spread over the valley, exhaling, they said, a strong odour, and bring-
ing death and desolation where an instant before there was life and
tranquillity, and transforming a smiling and fertile region into a
lugubrious cemetery.

The violent projection of this nearly liquid and incandescent (?)
mass tore from the mountain large blocks, which, by their displace-
ment, dislocating and affecting the equilibrium of the superior parts,
occasioned their fall also. And in fact an enormous portion of the
mountain has been carried away by the bluish-grey muddy material,
upon which it may be recognized by its yellow colour, arranged
in bands of different dimensions over a very great extent of the
flow. .

A noise comparable to that produced by the passage of a railway
train over a long iron bridge continued to be heard at short inter-
vals, and great slips (éboulements) take place, throwing up a fine
powder, which rises into the air like a band of smoke. However, it
is impossible to make out whether these noises are produced by the
sinking in of the mountain, or whether they are the result of the
work of an internal commotion which conjointly provokes these falls.

I have also ascertained the presence of distinct fissures and of
depressions of the ground upon the granitic mountain at the foot of
which is situated the village of Nikhah, 10 kilometres from Kantz-
orik; and I have been told that crevasses of the same nature were
also produced at another point 2 or 5 kilometres further on.

By this cataclysm we certainly recognize the action of an interior
fire, but we can only ascertain the result produced. Will this vol-
canic¢ action stop at the point it has now attained? Will this region

CATASTROPHE OF KANTZORIK, ARMENIA, 30

be transformed and modified by the continuation of the actual dis-
turbance? or, again, should a volcano be established, will it allow of
the expansion of the gases which appear to exert so strong a pres-
sure upon the crust of the earth inthis region? No one can foresee.

Discussion.

The PresipENT, in commenting on the remarkable nature of the
phenomenon, regarded the offer of the paper on the part of the
Author as a compliment to the Society. It was not a volcanic
eruption, but more of the nature of a mud-flow produced by a big
landslip—possibly connected with the stoppage of the springs. Still
it was on a very large scale, though clearly the effect of water and
not of fire.

Dr. Eyans agreed with the President. It was difficult to recon-
cile the alleged incandescence with the other phenomena. Infiltra-
tion of water probably had something to do with the outburst. It
Was not even a mud-volcano. The falling in of the mountain, he
thought, might have been due to soft beds covered by harder mate-
rial having oozed out. It would be interesting to know if there had
been an increased rainfall prior to the occurrence. There was
nothing ofa truly volcanic nature mentioned in the paper. He should
like to have further information about the incandescence.

Mr. Dattas (who translated the paper) said that the “‘ redness ”
was reported by the people to the Author.

Rey. Epwin Hitx thought that the mud-balls could in no way be
explained by igneous agency. ‘The photographs gave no indication
of the presence of steam. As a landslip the amount was very
great, and possibly the phenomenon might be something similar to
the overflow of peat-bogs.

Mr. Huprestron recalled the statement of the Author regarding
the geological constitution of the district, where masses of Secon-
dary rocks are folded within igneous ones, probably of Tertiary age.
It was likely, therefore, that some of the softer Secondary marls,
pressed in more than one direction by harder rocks and soaked by
water, might at last have given way. The immediate cause of the
catastrophe could scarcely be indicated without a knowledge of the
district. Such events occurred from time to time elsewhere. The
Russian topographers, if his memory served him right, had described
the bursting of a mountain-side, with fatal results, in one of the
valleys near Lake Issyk Kul. The smoke-like powder, resulting
from the continued falls of rock, had often given rise to the notion
of volcanic action. There could be no better instance of this than
the case of Mount St. Ehas, the highest mountain in North Ame-
rica. In geography-books this mountain has almost invariably been
described as a volcano, and a portion has actually been designated
as the crater. This illusion had been occasioned by the dust of
rock-falls resembling smoke. We might well pardon the Author
for speculating on the probability of a return to volcanic activity in
a region which bears so many traces of it as this part of Armenia.

p2

36 MR. R, LYDEKKER ON DINOSAURS OF THE WEALDEN

3. Contributions to owr Knowledge of the Dinosaurs of the WEALDEN
and the SAUROPTERYGIANS of the Purbeck and OxrorD CLAY.
By R. Lyprexxer, Esq., B.A., F.G.S., &&. (Read November 6,
1889.)
[PuatE V.]

THe present communication is divided into four sections—the first
giving an account of [guanodont remains obtained from the Wad-
hurst Clay near Hastings subsequently to the writer's previous
paper on this group; the second devoted to the description of a
metatarsus of a Megalosaurian from the same deposits; the third
recording some vertebre of a Sauropterygian from the Purbeck of the
Isle of Portland; while the fourth gives a description of an associ-

ated series of remains of a Pliosaur from the Oxford Clay near
Peterborough.

I. The Iquanodonts of the Wadhurst Olay.

Two years ago I brought under the notice of the Society * certain
remains of large Iguanodonts collected by Mr. C. Dawson, F.G.8.,
from the Wadhurst Clay (Lower Wealden) in the neighbourhood of
Hastings, and now preserved in the British Museum. Among these
a left ilium and some associated vertebrae presented such differences
from the corresponding bones of Jguanodon Mantelli and I. bernis-
sartensis, that I felt justified in regarding them as the types of a
distinct species, for which the name J. Dawsont was proposed. I
was careful at that time to mention that these specimens only were
taken as the types, and it is fortunate that this was done, since it
now appears that the sacrum and ischium which, in the absence of
any evidence to the contrary, were referred to the same species,
belong to a distinct form.

Since the publication of that paper Mr. Dawson has assiduously
continued his collecting in the quarries of the Wadhurst Clay, the
result of which has been the acquisition of a very large series of new
specimens—many of them being associated—although, unfortu-
nately, he has not yet succeeded in obtaining a skull. These speci-
mens, all of which are preserved in the British Museum, indicate
the existence in the Lower Wealden of two Iguanodonts which '
appear to be distinct from J. Dawsoni, and of which I have given a
preliminary notice in the ‘ Geological Magazine’, under the names
of I. Fitiona and J. hollingtoniensis. Before, however, proceeding to
give a fuller account of some of the specimens on which these species
are founded, it will save trouble to formulate a brief summary of the
chief characters of I. Dawsoni, as derived from the type specimens,
supplemented by others taken from an imperfect skeleton recently
acquired by the British Museum.

* Quart. Journ. Geol. Soe. vol. xliv. pp. 46-52 (1888).
t Decade 3, vol. vi. pp. 354, 355 (1889).

+

Quart. Journ. Geol. Sec. Vol. XLVI. Bieeve

Mintern Bros del. et lith

PLIOSAURUS/FEROX.

AND SAUROPTERYGIANS OF THE PURBECK ETC. ol

Fig. 1.—Left llia of Wealden Species of Iguanodon.
(About ,}, nat. size.)

A. I. bernissartensis, B. I. Dawsoni. O. I. Fittont D. 2. Mantelli. E. J. hol-
lingtoniensis (?). E is reversed from the right ilium. In C and D the
veutral, as well as the outer, surface is shown.

38 MR. R. LYDEKKER ON DINOSAURS OF THE WEALDEN

Iquanodon Dawsoni was a species intermediate in size between
I. bernissartensis and J. Mantelli, the middle dorsal vertebrae *
having but slightly compressed centra, with the rib-facet rising to
the level of the neural platform. The ilium, of which a greatly
reduced representation is given in fig. 1 B, is characterized by its
great vertical depth, and the absence of that reflection of the supe-
rior border which is so marked in J. bernissartensis (fig. 1 A) and
I, Mantelli (fig. 1 D); and also by the contour of its postacetabular
portion, which forms a long and deep plate with a rounded termi-
nation, in which there is only a very slight inflection of the inferior
moiety. Lqually characteristic is its preacetabular process, which
is long and comparatively shallow, with a broad horizontal roof-like
inward extension at its point of origin from the preacetabular notch,
and an outward inclination of its lower border as it approaches
the extremity. The pubic processis mainly directed forwards. An
imperfect skeleton in the British Museum (No. R. 1627) from the
Wadhurst Clay of Brede, near Hastings, may be referred to this
species, since the portion of the right ium which now remains
agrees exactly with the type specimen. The femur of this skeleton
has a length of about 37 inches, and the head placed approximately
at right angles to the shaft; but the form of the inner trochanter
cannot be determined owing to the imperfection of this part of the
bone.

Having now indicated the chief characters of Jguanodon Dawson,
we may proceed to notice the chief specimens of tbe other forms
from the same deposits.

Iguanodon Fitton t.—The type specimen of this species is the
ilium represented in fig. 1 C (B.M. No. R.1635), which was ob-
tained from Shornden Quarry near Hastings, from a three-foot bed
of ferruginous sand, which is separated by a stone band of two feet
in thickness from the underlying clay bed, four feet thick, which
yielded the type specimens of J. Dawsont. At a distance of some
25 yards to the westward in the same stratum an imperfect caudal
vertebra and the proximal extremity of a left ischium were obtained ;
while 25 yards still more to the west was found the undermentioned
sacrum, also in the same bed. It might be considered that an in-
terval of 50 yards between two specimens would show that they
were not referable to the same individual. In this case, however,
no other bones have been found in the same part of the quarry, and
the position of the ischium serves to connect the ilium with the
sacrum. Moreover all these bones belong to the same region of the
body, while the ischium and ilium are both of the left side. That
different bones of a single individual in these deposits do become
widely separated horizontally is proved by the metatarsals of Mega-
losaurus described in the second section of this paper, one of which
was obtained in 1884, while the other was found in 1889 at a
distance of about 180 yards from the spot where the first occurred,
It seems, therefore, to be most probable that the four above-men-

* Quart. Journ. Geol. Soc. vol. xliv. p. 48, fig. 1.
t Geol. Mag. decade 3, vol. vi. p. 354.

;
.

AND SAUROPTERYGIANS OF THE PURBECK ETC. 39

tioned specimens belong to one and the same individual. The
type ilium is fortunately the left one, and is therefore strictly
comparable with the type of I. Dawsont. ‘This specimen, although
it has been fractured, is nearly entire, but unfortunately the pre-
acetabular process is broken, and a fragment is missing near its
origin, so that its exact length cannot be determined. ‘The ex-
tremity of the pubic process is also missing. Compared with the
ilium of J. Dawsona (fig. 1 B), this specimen appears to indicate a
somewhat smaller form, and is of a relatively deeper type, with a
highly convex superior border, a more concave external surface,
and a less defined acetabulum and ischial tuberosity. The pre-
acetabular process is deeper and apparently shorter, and has no
roof-like inner extension at its origin from the preacetabular notch,
nor any tendency to an outward inclination of its inferior border.
Posteriorly the difference from J. Dawsoni is still more decidedly
marked. Thus the lateral surface of the postacetabular portion
terminates in a comparatively sharp point; while inferiorly this
portion gives off a shelf-like projection standing out almost at right
angles to the vertical plate. As minor features of this ilium, it
may be observed that the preacetabular notch is very shallow from
above downwards, the prepubic process is deflected downwards,
the interval between the pre- and postacetabular notches is compa-
ratively short, and in the preacetabular notch the surface of the
bone is rounded off. The vertical height of this specimen from the
inferior border of the middle of the acetabulum is 11°3 inches, and
the approximate total length (allowing one inch for the missing
fragment of the preacetabular process) 32 inches.

The associated ischium has the hammer-shaped head character-
istic of the one I have figured in association with the ilium of J.
Dawsom in my previous paper.

The sacrum, which is imperfect, is characterized by the lateral
compression of the component vertebrae, and thereby agrees with
the somewhat smaller sacrum from the Weald Clay referred, and I
believe rightly, by Sir R. Owen to J. Mantelli. The vertebral
centra are completely anchylosed together.

That the present form, as typified by the ilium, is perfectly distinct
from J. bernissartensis and J. Mantelli of the Upper Wealden is quite
evident ; the great development of the inwardly directed horizontal
shelf of the postacetabular portion of the ilium being of itself a
sufficient distinction. The vertebre from the Upper Wealden on
which Sphenospondylus gracilis is founded appear to be much too
small to have belonged to this form; while since its distinctness
from J, Dawsoni has been already sufficiently indicated, there ap-
pears no doubt as to the right of Jyuanodon Fittoni to rank as a
distinct species.

In referring this species to the genus Jgwanodon rather than to
the allied Camptosaurus (Canptonotus) I have been mainly guided
by the characters of the sacral vertebra, which are those of one of
the typical group of Iguanodon, and also by the large size of the
present species—Camptosaurus being typically of comparatively

40 MR, R. LYDEKKER ON DINOSAURS OF THE WEALDEN

small dimensions. So far, however, as I can judge from the figure
given by Prof. Marsh*, the ilium of the present form appears to
present a considerable resemblance to that of the type species of
Camptosaurus. This is especially shown in the great vertical depth,
in the form of the postacetabular portion, in the deflection of
the pubic process, and the shallowness of the preacetabular notch.
The preacetabular process is also of great depth in both, although it
is much shorter in the American form. I am not, however, dis-
posed to attach much importance to the latter difference, more
especially since there is a comparatively long preacetabular process
in the ilium of the so-called Jguanodon Prestwichi, which I am
unable to separate from Camptosaurus. In the compressed sacral
vertebrae J. Fittona differs, however, very widely from Camptosaurus ;
and I am accordingly disposed to consider this species as one which
while retaining an ilium approximating to that of the less specialized
Camptosaurus type, has acquired the sacrum of a typical [guanodon.

Iguanodon hollingtonrensis +.—Of this form there is untortunately
no complete example of the ilium among the specimens collected by
Mr. Dawson, so that its diagnosis cannot at present be given so con-
cisely as is desirable. The specimens which I take as the type of
this species are a large number of associated bones from the Wad-
hurst Clay of the Hollington quarry near Hastings, one moiety of
which (B.M. No. R.i148) was obtained in 1887, while the others
(B.M. No. R. 1629) were collected in 1889. The former moiety
comprises the right femur (fig. 2), part of the tibia of the same side,
a metatarsal, and two imperfect dorsal vertebra; and these speci-
mens were provisionally entered on p. 217 of part i. of the writer's
‘Catalogue of Fossil Reptilia and Amphibia in the British Museum ’
under the heading of J. bernissartensis, it being suggested that
they might belong to an immature individual of that; species, although
it was also pointed out that they might perhaps be referable to
I. Dawsoni. 'The second moiety imeludes the two seapule, the lett
radius and ulna, a phalangeal spine of the pollex, the left femur,
parts of the left tibia and fibula, a metatarsal, &c. It is further
believed that an associated series of sacral and caudal vertebre
(B.M. No. R. 1632) from the same quarry are-referable to the
same individual.

The right femur of the type skeleton is represented in woodcut
fig. 2, and, with the exception of the lesser trochanter and part of
the adjacent region, is practically entire, aithough it has been much
crushed and broken. It has a length of some 32 inches (or ap-
proximately the same as the corresponding bone of Jguanodon
Mantelli), and is characterized by the marked convexity of the
anterior profile of the shaft, by the ‘‘ pendent” form of the large inner
trochanter, which is situated in the lower half of the shaft, and by
the obliquity of the setting-on of the head to the shaft. Now both
the form and the position of the inner trochanter distinguish this
bone from the femur: of J. Mantelli, in which this trochanter is of

* Amer. Journ. ser. 3, vol. xviii. pl. iii. (1879). :

Tt Geol. Mag. decade 3, vol. vi. p. 855 (1889).

» AND SAUROPTERYGIANS OF THE PURBECK ETC.

/

4]

Fig. 2.—The Right Femur of Iguanodon hollingtoniensis, 1 nat. size;

from the Wadhurst Clay near Hastings.

ect Did ie

a, head ; 0, lesser trochanter; ¢, inner ditto; d, ectocondyle; e¢, entocondlyle.

492 MR. R. LYDEKKER ON DINOSAURS OF THE WEALDEN

the “crested ” type*. The position of this inner trochanter is,
indeed, very similar to that obtaining in the larger femur of J. ber-
nissartensis T ; but in the latter the trochanter is decidedly of the
“crested” type. There is accordingly evidence as to the specific
distinctness of the form under consideration from the two species
mentioned above. With regard to J. Dawsoni, the femur already
alluded to (p. 38) as referable to that species is somewhat larger
than the present one, and, so far as its imperfect condition admits
of comparison, appears to present structural differences, its shaft
being much less curved. The two dorsal vertebre associated with
the femur of the present form are much smaller than those of
I, Dawson. Other collateral evidence will be adduced as to the
distinctness of the form under consideration from the latter species ;
but in the meantime it may be observed that in its curved shaft
and pendent trochanter the femur before us approximates to that of
Camptosaurus t, although these features are not so strongly marked
as in the latter.

Turning now to the sacral and caudal vertebre from the Hollington
quarry (No. R. 1632), which are believed to have been associated with
the type specimens, it may be observed that the sacrals are character-
ized by the absence of anchylosis between their centra, and also by
the flattened heemal surfaces of the latter ; in both of which respects
they resemble Camptosaurus. Now these sacrals are of the same
type as those (No. R. 811) which I have previously referred to J.
Dawsoni; the latter (which likewise came from the Hollington quarry)
being associated with dorsal vertebra (No. R. 604) of the same form as
those of the type skeleton. There is accordingly every probability
that these sacral vertebre are referable to the present form. There
is, however, associated with the sacrals (No. R.811) an imperfect
left ilium (No. R. 811 6), which although much broken and flattened
affords important evidence. This specimen is represented in fig. 1 E.
Its preacetabular portion differs from that of J. Dawsonz by the
absence of an inner roof-like extension, and the whole bone is of a
much less massive build. Compared with the ilium of J. Fittoni
(fig. 1C), the present one differs by the shallower preacetabular
process, the longer interval between the pre- and postacetabular
notches, the greater depth of the preacetabular notch, and apparently
also by the more forward direction of the pubic process. Precisely
similar characters are found in the imperfect right ilium, belonging
to another imperfect skeleton collected by Mr. Dawson (No. R. 1636),
which I am accordingly disposed to refer to the present form.

We are now in a position to sum up the evidence of the specific
distinctness of the Hollington Jyuanodon from the other species.
The evidence of the femur justifies its separation from J. Mantelli
and J. bernissartensis. The same evidence, so far as it goes, is in

* See Dollo, Bull. Sci. France et Belg. 1888, pp. 215-224.

+ Dollo, op. cit. p. 216, fig. 1. When suggesting in the work cited that the
present specimen might belong to a young individual of JZ. bernissartensis, my
attention had not been directed to the difference in the contour of the inner
trochanter.

~ Compare Dollo, op. cit. p. 216, fig. 2.

AND SAUROPTERYGIANS OF THE PURBECK ETC, 43

favour of its distinctness from J. Dawsoni. This is supplemented
by the evidence of the sacral vertebre and ilium. Thus it has been
shown that the dorsals associated with the sacrals are similar to
those associated with the types of J. hollingtoniensis, and that the
sacrals and ilium are not referable to J. Dawsoni; and there is
accordingly, apart from the apparent association of some of these
sacrals with the above-mentioned types, every reason for regarding
this form of sacrum and ilium as referable to J. hollingtomiensis.
If I am right in this respect there will be equally good evidence as
to the distinctness of the Jguanodon to which I have applied the
name last mentioned from J. Fittoni. :

The skeleton, No. R. 1636, is remarkable for the great relative
length and slenderness of its scapula, and the same feature is
apparently shown in an imperfect skeleton from the Hollington
quarry (B.M. No. 33), which I believe to be also referable to
I. hollingtoniensis.

In the characters of the sacrum and femur J. hollingtoniensis
approximates to Camptosaurus, although, as I have already observed,
the ‘‘ pendent” character of the inner trochanter is less strongly
marked than in the type of the latter. My reason for referring this
species to Jguanodon rather than to Camptosaurus is the modifica-
tion of the one phalangeal of the pollex into the conical spine
characteristic of the former; but the species must be regarded as
connecting the typical forms of ZJguwanodon with the less specialized
genus Camptosaurus.

[Since the above was written, Mr. 8. H. Beckles, of Hastings, has
been good enough to send to the British Museum part of the skeleton
of a small Jguanodon from the Wadhurst Clay of that neighbour-
hood, which affords important evidence as to the characters of
I, Fittoni. These associated specimens include the right ilium, a
pubis, the left femur, and several more or less imperfect vertebree.
The ilium accords in contour with the type of J. /ttoni, but in its
smaller dimensions agrees with the corresponding bone of J. Mantell: ;
this smaller size may be indicative either of immaturity or of sexual
difference from the type.

This ilium shows the peculiar outward curvature of the preace-
tabular process, which is obscured through fracture in the type; it
has the same inflection of the inferior surface of the postacetabular
as in the latter; and also the rounded surface of the bone in the
preacetabular notch. The difference in the contour of this ilium
f-om that of the figured ilium of J. Mantelli (B.M. No. R. 1138) is
well seen if the two are put side by side and viewed from the ventral
aspect, when a difference similar to that seen between fig. 1 C and D
is observable. In J. Mantelli the surface of the bone forming the
preacetabular notch has a sharp edge, while the inner inflection of
the postacetabular process is much less marked, and does not com-
mence till much nearer the posterior extremity. The whole bone is
also less deep and less curved from above downwards in J. Mantelli,

The femur of Mr. Beckles’s specimen is very important, since it
shows that the inner trochanter was of the “crested” type of

44 MR, R. LYDEKKER ON DINOSAURS OF THE WEALDEN

I. Mantelli, and quite different from the “ pendent” type of that of
I, hollingtonensis (fig. 2); so that we have now decisive evidence
of the distinctness of the latter from J. Fitton’. The inner tro-
chanter of the femur of the latter 1s placed lower down than in
I. Mantellr.

It may be added that some of the caudal vertebrae of Mr. Beckles’s
specimen present the peculiarity of being anchylosed together, while
some of them have also become proccelous. All these peculiarities
must, however, be regarded as quite abnormal, and it is not
improbable that they are due to an injury received during the
lifetime of their owner. |

Fig. 3.— Posterior aspect of a late Cervical Vertebra of an Iguanodon ;
from the Wealden, near Hastings. (% nat. size.)

—

pt.z, postzygapophysis ; tp, transverse process.

Cervical Vertebra.—Quite recently Mr. C. Dawson has procured
me the loan of a cervical vertebra of a large Zguanodon, which on
account of its remarkable state of preservation is deserving of a brief
notice. This specimen was found by Mr. P. Rufford, of Hastings,
imbedded in a nodule on the beach near that town ; and it has been
extracted from its matrix with scarcely any damage. I am unable
to say from what horizon in the Wealden this fine specimen was
derived, but since it is smaller than the cervicals from the Upper

AND SAUROPTERYGIANS OF THE PURBECK ETC. 45

Wealden referred to J. bernissartensis, and much larger than those
of I. Mantellr, it appears very probable that it may be referable to
the Lower Wealden J. Dawsonz, which is intermediate in size between
these two species. The specimen is represented on a reduced scale
in fig. 3 from the posterior aspect. It will be seen from the
figure that, with the exception of the parts of the edge of the
posterior terminal cup of the centrum, the specimen is practically
entire. The distinct neural spine, long transverse processes, and the
position of the capitular rib-facet high up on the centrum indicate
that the specimen is from that part of the vertebral column where
the cervicals are just acquiring the characters of dorsals ; but since
the centrum is opisthoccelous, and apparently carries the whole of
the capitular facet, I think the specimen should be reckoned as a
cervical. The extreme height of this specimen is 13 inches; the
height from the base of the neural canal to the summit of the neural
spine 7 inches, and the transverse diameter of the posterior cup of
the centrum 6°5 inches.

Il. Metatarsus of Megalosaurus from the Wadhurst Clay.

In 1887 Dr. Ernst von Koken *, of Vienna, described and figured
a Megalosaurian tooth from the Lower Wealden of Germany, which
in 1884 Prof. Dames had made the type of the species Megulosaurus
Dunkert. In the following year, when cataloguing the Dinosaurian
remains in the British Museum 7, finding that the Megalosaurian
teeth from the English Wealden presented no characters by which
they could be specifically distinguished from the type of IZ. Dunkeri,
I referred the whole of them, irrespective of size, to that species ;
under which heading I also included a number of vertebrx and limb-
bones.

Among the limb-bones was the imperfect metatarsus (No, 2559)
figured in Owen’s ‘ Wealden and Purbeck Reptilia’ (Mon. Pal. Soe.
pt. iv. pl. x1.) as Hyle@osaurus, which, as I have indicated in a former
communication to this Society t, appears to be Megalosaurian. In
addition to this specimen there were also entered a dorsal vertebra
(No. R. 604a), an imperfect tibia (R. 604c), and the fourth left
metatarsal (R. 604d), all of which were obtained (as I am now
informed) by Mr. Dawson in 1884 from the Hollington quarry, near
Hastings, in immediate association, and which may be safely regarded
as referable to a single individual. I considered that this metatarsal
agreed with the metatarsal of No. 2559, described by Owen as the
fourth ; the whole of that metatarsus being figured by him as belong-
ing to the left side.

Thus matters stood still till the spring of 1889, when Mr. Dawson
brought another metatarsal of Megalosaurus (B.M. No. R. 1525)
which had recently been obtained from the same quarry, but at

* Pal. Abhandl. vol. iii. p. 316, pl. ii. fig, 2.

+ Cat. Foss. Rept. Amphib. Brit. Mus. pt. i. pp. 163-168. The authority
for the species is thers erroneously given as Koken,

t Quart. Journ, Geol. Soe. vol. xliv. p. 53,

46 MR, R. LYDEKKER ON DINOSAURS OF THE WEALDEN

a distance of some 180 yards to the eastward of the spot where
the other specimens had been discovered in 1884. On putting
this new specimen in its proper relative position to the metatarsal
(No. K. 604 d), there can be no question but that the two belong
to the left foot of the same individual, the new specimen being the
second metatarsal. In woodcut fig. 4 these two metatarsals are
represented in their approximate relative positions.

Fig. 4.—The second and fourth Left Metatarsals of Megalosaurus
Dunkeri ; from the Wadhurst Clay, near Hastings. (About +
nat. s1Ze.)

<R ‘ae Br "
oe Wye

Tis I }

Placed in apposition with the metatarsus No. 2559, it is at once
apparent that the Hollington specimens are specifically distinct from
the former; and they further show that the former belongs to the
right side, and not to the left as in Owen’s figure. This is proved
by the circumstance that in this group it is always the second meta-
tarsal that is longer than the fourth, and it is evident that in
No. 2559 the imperfect metatarsal marked II. in Owen’s figure
would when complete have been longer than the one marked IV.
Further comparison between the Hollington metatarsus and No. 2559

AND SAUROPTERYGIANS OF THE PURBECK ETC. 47

shows that the former bones are characterized not only by their
larger size, but also by their relative length and the great excess in
the length of the second over the fourth. Moreover, both these
bones have their antero-internal borders rounded, while the distal
surface of the fourth is comparatively narrow. In No. 2559, on
the other hand, the bones are absolutely smaller and apparently
relatively shorter, the second being but slightly longer than the
fourth ; while both these bones have sharp antero-internal borders
and the distal surface of the fourth metatarsal is broad and squared.

Seeing, therefore, that there is clear evidence of the existence of
two species of Megalosaurians in the English Wealden it remains
to determine which should be referred to WM. Dunkeri; for I have
no hesitation in believing that the British and Continental forms
were specifically identical. Now the type tooth of MW. Dunkeri is of
comparatively large size, and was obtained from the lower division
of the Hastings beds, which must be equivalent either to the Wad-
hurst Clay or the underlying Ashdowns ; while No. 2559 came from
the higher division of the overlying Tunbridge sands at Cuckfield,
The Hollington metatarsus agreeing, therefore, in relative size with
the type tooth and coming from approximately the same geological
horizon, there is every probability that it belongs to the same species,
to which IJ accordingly propose to refer it. It is of course unsatis-
factory to have a species founded upon such an uncharacteristic
portion of the skeleton as a single tooth; but being so, we are bound
to accept and make the best we can of it. So far as it goes, the
circumstance that the Iguanodons of the Wadhurst Clay appear to be
all specifically different from those of the Tunbridge beds and Weald
Clay is in favour of the view that the Hollington metatarsus really
belongs to the species to which I propose to refer it.

Finally, seeing that the Cuckfield metatarsus is decidedly specific-
ally distinct from the latter, | have made it the type of a distinct
species, under the name of Meyalosaurus Owen *.

III. Crvoriosavrvs portianpicus from the Purbeck.

In part IL. of the British Museum ‘ Catalogue of Fossil Reptilia
and Amphibia’ ~ I have referred the vertebrae from the Portlandian
described under the names of Plesiosawrus winspitensis and P. cari-
natus (=P. Phillipsr) to Cumoliosaurus (Pliosaurus) portlandicus
of Owen, on the ground that all the known vertebra from these beds
are of one type, and are therefore almost certainly referable to the
species typically represented by the bones of the pelvic limb.

Hitherto this species has been known solely from the Portlandian,
but I am now able to bring evidence that it ranged upwards into
the Middle Purbeck. This evidence is afforded by the imperfect
centra of two posterior cervical vertebree which I procured during .
the past summer from the quarries at Portland. They were obtained
from the ‘ Cinder-bed’ of the Middle Purbecks, which, as is well

* Geol. Mag. decad. 3, vol. vi: p. 825 (1889).
tT Pp. 227, 228 (1889).

48 MR. R, LYDEKKER ON DINOSAURS OF THE WEALDEN

known, is one of the few marine beds found in that series. The best-
preserved of the two specimens is represented in fig. 5; and it will
be seen therefrom that both the ribs and the neural arch were not
anchylosed to the centrum, from which we may probably infer that
the specimens belong to an individual which had not attained full
maturity. Apart from the fractures which they have sustained in

Fig. 5.— Anterior, right lateral, and ventral aspects of the Centrum of
a Dorsal Vertebra of Cimoliosaurus portlandicus ; from the Pur-
beck of the Isle of Portland. (§.)

co, costal facet.

the process of extraction from their bed, these specimens are beauti-
fully preserved, and are thereby in marked contrast to the posterior
cervicals from the Portlandian in the collection of the British
Museum, all of which have suffered by rolling. The extreme pro-
minence of the carina on the hemal surface at once shows that
these specimens agree with the cervical figured by Phillips * as
Plesiosaurus carinatus. They are, indeed, of somewhat larger dimen-
sions, as is shown by the following table :—

Phillips’s Present

specimen. specimen.
TGR se. 5 sins We Bats 1:63 in. 1-9 in.
TEESE PE TE ifr terete tr 1-60 in. 19 in.
WG ED hrs acare es afe.0.5 1:95 in. 2-4 in.

eRe ok Leas WN Ba te ne Se SE
* Geology of Oxford, p. 375.

AND SAUROPTERYGIANS OF THE PURBECK ETC, 49

This, however, I cannot regard as anything more than a difference
in age or of individual development, seeing that both specimens are
apparently immature.

The two posterior cervicals in the British Museum (Nos. 41238,
45904) are still smaller than Phillips’s specimens, and have the de-
pression on either side of the hema! carina much less strongly marked,
this being partly due to their water-worn condition and partly also
to their immaturity.

In describing those specimens in the Museum Catalogue, I con-
sidered that they would agree in relative size with the femur on
which Cimoliosaurus portlandicus was founded. A subsequent
opportunity of comparing the size of that limb with the entire
skeleton of Cimoliosaurus Richardsoni has, however, convinced me
that the present specimens are more nearly of the size which
accords proportionately with the hind limb ; from which I also infer
that C. portlandicus was of the approximate size of the last-named
species.

Hitherto, so far as I am aware, the only evidence of the occurrence
of a Sauropterygian in the Purbecks is afforded by an imperfect
humerus or femur mentioned on p. 227 of the above-mentioned
‘Catalogue.’ It was then suggested that the specimen in question
might be referable to the Wealden C. limnophilus, but it may equally
well belong to the present form.

The freshwater vertebrates of the Purbecks, judging from the
Chelonia, appear to be closely allied to those of the Wealden, at
least one species ; Hyleochelys latiscutat«) being common to the two
series. It is therefore of considerable interest to find that where
marine conditions obtained there was an equally close alliance, if
we may judge from a single instance, with the vertebrate fauna of
the Portlandian.

IV. A Phosaurian Skeleton from the Oxford Clay of Peterborough.

In a paper read before the Society on the21st of November, 1888,
I described under the name of Peloneustes * the remains of a com-
paratively small Pliosaurian from the Oxford Clay, which I regarded
as a more generalized form than Pliosaurus, although it was doubt-
ful if it could be regarded as the direct ancestor of that genus. My
reasons for separating Peloneustes from Pliosaurus were the great
length of the mandibular symphysis, the attachment of the neural
arches and cervical ribs by suture to the vertebrae, and the relatively
longer epipodial bones, of which the ulna and fibula were subreniform.
I may add that in this description I considered that the pectoral
limb was larger than the pelvic; but from specimens in the collec-
{ion of Mr. Leeds it appears that the reverse condition obtains 7, as
in Pliosaurus.

* Quart. Journ. Geol. Soc. vol. xlv. pp. 48-56 (1889).

t+ The limb figured on p. 54 of the memoir cited will accordingly be the
pelvic instead of the pectoral, as, indeed, I considered to be the case when the
figure was drawn. ‘Lhe tibia (¢) is drawn too small in proportion to the fibula

Q.J.G.S. No. 181. E

50 MR. R. LYDEKKER ON DINOSAURS OF THE WEALDEN

Quite recently Mr. A. N. Leeds of Eyebury, near Peterborough, has
added to his unrivalled collection of Saurian remains from the Oxford
Clay of that neighbourhood a considerable proportion of the skeleton
ofa large Pliosaur, which is important as being not only the first
example (exclusive of Peloneustes) of the association of teeth, vertebra,
and limbs, but also as being a generalized form connecting the
typical Kimeridgian species of Pliosaurus with the smaller forms
described as Peloneustes. Mr. Leeds has been good enough to permit
me to select such portions of the skeleton as appeared best to illus-
trate the alfinities of this form, the description of which I now give.
The specimens collected by Mr. Leeds include the greater part of the
mandible, showing the entire symphysis, a number of detached teeth
in very beautiful preservation, several cervical vertebre, in some
instances with the neural arches and ribs, the greater portion of the
pectoral limb. of one side, and portions of that of the other, and
several bones of the pelvic limbs.

These specimens indicate an individual agreeing approximately
in size with an imperfect skeleton of Pliosaurus brachydirus in the
British Museum, No. 46796 *, the cervical vertebree of both examples
being of nearly the same size, and the mandibular symphysis having
a transverse diameter of about six inches. The humerus measures
neariy 24 inches in length, or slightly more than in the type skeleton
of P. brachydirus from Market-Rasen.

The mandibular symphysis agrees with that of the typical Kim-
eridgian species of Pliosaurus in that it extends back as far as the
seventh tooth. Exceptfor its much larger size the mandible presents
no characters by which it can be distinguished from a probably
immature mandible from the Oxford Clay in the Eyebury collection
which I have referred ¢ to Plhiosaurus ferow.

Of the detached teeth one of the largestis represented in Pl. V.
fig. 1, this and other similar ones being the finest specimens of
Pliosaur tecth that I have ever seen. Whether this tooth belonged
to the upper or lower jaw, there are no means of definitely deter-
mining, but it is evidently either from the premaxillary or the
symphysial region. ‘The pulp-cavity is open and extends the whole
length of the root and some distance into the crown. The crown
of this tooth is almost undistinguishable from that of the smaller type
of teeth belonging to Peloneustes philarchus. It also closely resem-
bles the Pliosaurian teeth commonly occurring in the Oxford Clay of
Peterborough, which are undistinguishable from the Continental
examples described under the name of Lioplewrodon ferox, a name
which I have altered to Pliosaurus ferowt. It is true that in the
present examples the intercarinal space of the teeth of typical
Pliosaurs is scarcely definable, and the ridges are rather more con-
tinuous and closer together than in typical examples of P. ferow;
yet, after careful comparison with a number of specimens, I find
such a transition from the typical form to the present type that it

* Cat. Foss. Rept.and Amphib. Brit. Mus. pt. ii. p. 124 (1889).
t ‘Catalogue,’ op. cit. p. 145. t ‘Catalogue,’ p. 145.

—

AND SAUROPTERYGIANS OF THE PURBECK ETC, 51

appears impossible by the teeth alone todistingnish this Pliosaur
from P. ferow.

Of the cervical vertebre a centrum, with the cervicalribs, from the
hinder region of the neck, is represented of three fourths the natural
size in Pl. V. fig. 2. This vertebra presents all the characters of a
typical Pliosaur. Its terminal faces are subcylindrical, and have
no mamilla round the central depression; the costal facets are
very prominent; and the external surface is highly rugose, The
dimensions are: length 1°75, height 3:6, and width 4:0 inches. The
length is therefore very nearly half the vertical diameter. A. rather
later cervical, in which the terminal faces have become transversely
ellipsoidal, has a height of 3°7 and a width of 4:3 inches, the true
length not being determinable owing to crushing. The neural arch
represented in Pl. V. fig. 3 shows the presence of large and well-
developed zygapophyses. Unfortunately the nature of the cervical
zygapophyses in the Kimeridgian Pliosaurs does not appear to be
known. In the dorsal region, however, the zygapophyses were of
very small size and almost aborted in the Plosaurs of the
Kimeridge Clay ; and an immature vertebra in the Eyebury collection
shows that the same condition obtained in at least one of the
Pliosaurs of the Oxford Clay. There are no signs of any sutural
connexion of the arches and ribs with the centra of the cervical
vertebrae in the specimens under consideration.

If my memory does not fail me, these cervicals closely resemble
an associated series in the Cambridge Museum from the Oxford
Clay of Great Gransden, near St. Neots, Huntingdonshire, to the
owner of which Prof. Seeley has applied the name of Plhosaurus
pachydirus, although without any description to justify the adoption
of that name *, these specimens being noticeable for the prominence
of the costal articulations. The form to which that name was
applied I have provisionally included in the work cited in P. ferow.
On p. 146 of that work an imperfect late cervical vertebra
(No. 47429) trom the Oxford Clay near Peterborough is provision-
ally referred to the same species. On comparison with the present
specimens such a marked resemblance is presented by that vertebra,
that there seems to be every reason for considering both as specitically
the same. It is true, indeed, that in the British-Museum vertebra
the costal facets are less prominent than in Mr. Leeds’s specimens ;
but I think this difference may be partly due to individual
variation, and partly to the edges of these facets in the former
specimen having been chipped.

That the vertebra under consideration indicate a totally different
form from the one to which the name of Pliosawrus Evansi has been
applied, is quite evident. Thus the typical cervical vertebra of
the latter (which through the courtesy of Prof. Hughes I have been
enabled to compare with the specimens under consideration) differ
not only in their much smaller size, but in their proportionately
greater length, which much exceeds half the vertical diameter of

* See ‘Catalogue’ op. cit. p. 145.
tT See ‘Catalogue,’ p. 128.
EZ

52 MR. R. LYDEKKER ON DINOSAURS OF THE WEALDEN

their terminal faces, and in their smooth external surface. Compared,
indeed, with the cervical vertebree of Peloneustes philarchus there is:
such a close resemblance, that I think there is little doubt that Plo-
saurus EHvansi should be transferred to Peloneustes; and from the
agreement in relative size between the cervical vertebra: and the
mandible and paddle from the Oxford Clay in the Eyebury collec-
tion figured by Phillips as Pliosaurus, which I have shown* to be
referable to Peloneustes, it appears probable that those specimens
are likewise referable to P. Evansz.

The only other bones to which it will be necessary to refer are
the epipodials (radius and ulna, and tibia and fibula). A reduced
figure of the tibia and fibula is given in Pl. V. fig. 4, from which
it will be apparent that these bones differ from their homo-
logues in the Kimeridgian species of Pliosawrus in that they are
vertically instead of transversely elongated, in which respect they
agree precisely with the corresponding bones of Peloneustes.

Summing up the result of the foregoing observations, it appears
that we have to do with a large Phosaur which in dental characters
cannot be satisfactorily distinguished from Plosaurus ferow, and
may accordingly be referred to that species, a reference which will
confirm the conclusion that the vertebre named P. pachydirus are
likewise referable to the same species. This Pliosaur, while agreeing
with the typical Kimeridgian forms in the character of the
mandibular symphysis and vertebre, is allied by the teeth and
epipodial bones to the smaller forms known as Peloneustes, and
therefore serves to connect the latter with Pliosaurus, although not
necessarily leading to its abolition.

Further, the available evidence points to the transference of
Pliosaurus Hvansi to Peloneustes, and also indicates that the more
elongated centra of the cervical vertebrae may be added to the dis-
tinctive characters of that genus

The evidence now clearly shows that Peloneustes, which may have
been descended from the Longirostrine group of Plesinsaurus, 1s
the direct ancestral type of Plhiosaurus, which has gradually hecome
more specialized in the characters of the teeth, in the imperfect
articulation between the centra and appendages of the vertebra, in
the shortening and widening of the epipodial bones, in the shorter
mandibular symphysis, and, finally, in the increase in absolute
corporeal bulk.

EXPLANATION OF PLATE V.

Remains of Plinsawrus ferox from the Oxford Clay, near Peterborough.

Fig. 1. A tooth, natural size.

2. Anterior aspect of a late cervical vertebra, with the rib (7) of the right
side, # nat. size.

3. Imperfect neural arch of a cervical vertebra, } nat. size. pt.z, post-
zygapophysis; pr.z, broken base of prezygapophysis.

4. A tibia (Z7.) and fibula (7), 4 nat. size.

* See ‘ Catalogue,’ p. 154.

AND SAUROPIERYGIANS OF THE PURBECK ETC, 53

Discussion.

The Presrpenr regretted the absence of those best acquainted
with the subject, and alluded to the difficulties in the way of
criticism.

Mr. Leens, referring to the fossil from the Oxford Clay, observed
that the jaw is identical with Pliosawrus and the paddle with
Peloneustes. He was in possession of a large jaw of Plosaurus,
measuring 4 ft. 7 in., with which he identified the lower jaw of
this species. The body-bones were much broken up. There was
great difference in the size of the paddles, but he did not know
whether the fore or hind paddles were the larger.

Mr. E. 'T. Newron was satisfied, with regard to the specimens of
Iyuanodon referred to, that the species were distinct.

Dr. Woopwarp spoke cf thanks being due to Mr. Leeds for the
care with which he had worked the clay-pits of the country round
Peterborough. In this country remains of Saurians were too often
fragmentary, whilst in Belgium they were often entire. Mr. Leeds
had secured complete remains of Oxford and Kimeridge Clay marine
reptiles, and had taken care to match the individual bones with the
individual specimens.

He also spoke of the good work of Mr. Dawson amongst the
Wealden Dinosaurs, and of Mr. Rufford as regards the vertebra of
Iywanodon.

Prof. Huaus inquired as to the evidence for the association of
the bones referred to the same individuals.

Mr. Lrrps explained that some of his specimens consisted of the
entire skeleton, whilst others were imperfect. ‘These particular
bones were much broken, but were all found on one level; had it
been otherwise he would not have connected them. He proseeded
to describe the position of the bones, which were certainly those of
one animal, there being none other. :

Dr. Murix, alluding more especially to Jguanodon, spoke of the
difficulty of judging from diagrams in the absence of the specimens.
Looking at the femurs, one might say that the difference was one of
age rather than of species.

Mr. Smita Woopwarp thought that Peloneustes should be rede-
fined or done away with. With regard to the skeletons obtained
by Mr. Leeds, there could be no doubt as to the natural association
of the bones; they rested upon well-defined old floors in the clay,
marked by accumulations of broken shells.

The Avrnor, in reply, stated that he had given his reasons for
regarding the Iguanodont remains as associated; there was no
question whatever as to those of the Plosaurian belonging to a
single individual. He could not admit Dr. Murie’s view that the
differences in the Iguanodont remains were due to age. In reply
to Mr. Smith Woodward, the Author remarked that Peloneustes was
distinguished from Phiosaurus by its cervical vertebrae as well as by
the longer mandibular symphysis. He acknowledged his obligations
to Mr. Leeds and Mr. Dawson.

o4 DR. G. J. HINDE ON A NEW GENUS OF SILICEOUS SPONGES

4. On a new Genus of Stricnous Sponezs from the Lowsr Catca-
rEOuS Grit of Yorxsuire. By Grorex Jenntnes Hinz, Ph.D.,
F.G.S. (Read November 20, 1889.)

[Puate VI]

Nerarty forty years since*, Dr. H. C. Sorby, F.R.S., communi-
cated to this Society a paper on the microscopical structure of
the Calcareous Grit of the Yorkshire coast, in which reference
was made more particularly to the nature of certain microscopic
reniform bodies with which the rock in piaces was largely filled.
In mineral constitution some of these bodies were of calcite, others
of chalcedonic silica, whilst in others both these minerals were
present, and the question as to their original constitution was
decided by Dr. Sorby in favour of the calcite, since it was
thought extremely improbable that, if originally of silica, this
material would have been dissolved and replaced by calcite, whereas
the substitution of silica in place of calcite was a well-known
phenomenon. ‘The definite form and outline of these bodies left no
doubt that they were of organic origin, and Dr. Sorby recognized
their resemblance to the small siliceous globules which form an
outer crust to many existing sponges, but rejected this view on the
ground of their supposed calcareous nature, and he finally concluded
that they were small shells, possibly Foraminiteral, in whose interior
calcareous or siliceous materials had been infiltrated, in the same
manner as in the chambers otf the Ammonites occurring in the same
rock.

Subsequently, in 1876, Prof. J. F. Blake, F.G.S., discovered
similar minute bodies in rocks of nearly the same age in Dorset-
shire and Wiltshire, and noticed that some of them were hollows
enclosed by thin crusts or shells, which dissolved in acid, and further
that their surfaces were ornamented by regular rows of small pits,
which were supposed to indicate minute perforations in the shell.
On these grounds they were described as peculiar forms of Forami-
nifera, and named Renulina Sorbyana. In an incidental reference
in a later ¢ paper, Prof. Blake hints at the possibility that they may
have been originally siliceous,

Mr. W. H. Hudleston §, F.R.S., likewise refers to these same reni-
form bodies in treating of the generally siliceous character of the
Coral Rag at North Grimston, in Yorkshire, and adopts the view
that they were siliceous'spicules, similar to those forming the outer
layer of the recent sponge, Geodia arabica. In this case the author

* Quart. Journ. Geol. Soc. vol. vii. (1851), pp. 1-6. See also ‘ Proceedings
of the Geological and Polytechnic Society of Yorkshire, June 5, 1851, vol. iii.
pp- 197-206, pl. iv.

+ Monthly Microscopical Journal, vol. xv. pp. 262-264.

+ Proc. Geologists’ Assoc. vol. v. (1877), p. 266.

§ Jb. vol. v. p. 443.

Quart. Journ. Geol.Soc.Vol.XLVI.Pl.VI.

A.T.Hollick.del.

) RHAXELLA PERFORATA.

| Rade iaes heen es
; : i ns ae Pyce a8, ae ae
>? Mie ghee, Whe hh tied : ‘ Te

. riAt ¥ mut #9 age. Ft Dy ga C weet S oe

‘ haew me A

vie

i eee ee >
a = HS =

:

”

r

a

ae oe 2
{
‘
f
t 4

=
—s
~

i ene

at

a: 5 ae

y

‘
| “
r + # x
en tr - :
e ‘
*
r ‘
i
D} t i
: i
4%} »
a uF y
i -
ia
- . , 2
Z ‘
- 75
‘
,
j
.
‘i
'
WP,
: ‘
fd
. i
J ¢ f
A. ,
: ' Pe ee
a

FROM THE LOWER CALCAREOUS GRIT OF YORKSHIRE. 5d

remarks that the acerates and the anchor-spicules appertaining to
the same sponges must have been equally abundant, affording a
copious supply of organic silica, which has been one source of ‘the
chalcedonic matter so largely pervading portions of the Rag.

Dr. Sorby again mentions the small reniform shells in his pre-
sidential address to the Society in 1879 *, and states that in the
Peérna-bed in Dorsetshire and in certain beds in Yorkshire they
constitute as large a part of the bulk of the rock as the Forami-
nifera do in all but a very few exceptional specimens of Chalk.

In 1880 7, Prof. Sollas compares these bodies with the globate
spicules of Geodian sponges in the Upper Chalk, and on the suppo-
sition that they belonged to similar sponges, changed Blake’s name
to Geodites Sorbyana.

The view that these detached reniform spicules, or globates as
they have been termed, belonged to the dermal crust of siliceous
sponges like those of the living genus G‘eodia, has been very gener-
ally accepted as correct, though an objection of considerable weight
could be urged against it, namely, that they occurred almost exclu-
sively in these rocks, without admixture with other forms of spicules,
whereas in the existing Geodian sponges the globates of the crust
form but a small proportion of the entire mass of the body-spicules,
and as these latter are larger and more robust than the globates, it
is natural to suppose that they would be present in the same rocks
with them; and, in fact, this 1s the case in the contents of the
Upper Chalk flints of this country and in the Kreidemergel of
Westphalia, where the fusiform acerates and characteristic trifid or
fork-spicules of G'eodia are mingled with the globates. The absence
of the detached larger acerate and fork-spicules in the Calcareous
Grit would tend to show that the globate spicules did not form the
erust of sponges like the recent Geodia, and this is now proved by
the occurrence of several more or less perfect specimens of sponges in
the same rocks with the detached spicules, which seem to be
entirely composed of this one form of globate spicule, and thus
explain its exclusive occurrence in the rock. Sponges with skeletons
thus formed are very distinct from any others yet discovered as
fossil, though there is a living gonus to which they may possibly be
related. Independently of their remarkable structural features,
these sponges are very exceptional instances of the preservation as
fossil of the connected skeleton, although its constituent spicules are
not organically united together, and the fact of their existence in
such great numbers that their microscopic detached spicules con-
tribute no small part of the mass of certain beds of rock, adds
further interest to their description.

I may premise that the sponges in question belong in part to the
Natural History Museum at Scarborough, and in part to that at
York, and [ am indebted to the kindness of Mr. C. Fox Strangw ays,
F.G.S., and to the Trustees of the York Museum, through Mr. H.

* Proc, Geol. Soc. 1879, p. 51.—Appendix, pl. vi. fig. 1.
t Ann, & Mag. Nat. Hist. ser. 5, vol. vi. p. 392.

56 DR. G. J. HINDE ON A NEW GENUS OF SILICLOUS SPONGES

M. Platnauer, F.G.S., for the opportunity of studying them *,
Some of the specimens, from their porous aspect, had been recog-
nized and labelled as sponges; but, so far as I am aware, no
reference to them has ever been published, and the resemblance of
their spicules to the detached bodies in the Calcareous Grit does not
seem to have been noticed.

The specimens are now for the most part weathered out on the
surface of a hard matrix of the Calcareous Grit, consisting principally
of sand-grains and detached spicules like those of the sponge,
cemented together by calcite or silica. In one specimen the matrix
is decayed, so that the sponge has been quite freed from it. The
sponges appear to have been upright, palmate or fan-shaped, and in
the early stage of growth funnel-shaped in some _ instances
(Pl. VI. fig. 1). No specimen is perfect; the largest individual
measures’ 140 millim. in height by 80 millim. in width, and the
walls are about 14 millim. in thickness. The walls consist of
plates or indistinct trabecule, which anastomose to form a laby-
rinthine structure (Pl. VI. fig. 3). The plates are perforated irregu-
larly by ovate apertures or shts of varying dimensions (fig. 2),
ranging from 1 to 9 millim. in width; they vary in thickness from
-5 millim. to 4 millim., and the interspaces between the plates of
the wall correspondingly vary from 1 to about 4 millim. The
outer surface of the wall in some cases is smooth, in others rough
to the touch; occasionally small oysters are attached to it.

These laminate walls appear to be entirely composed of the
small reniform or so-called globate spicules already mentioned,
which are closely aggregated into a solid mass, and now firmly
cemented together by silica resulting from the fossilization. In
a transverse section through the sponge-wall the spievles are seen
in close contact, their individual outlines for the most part being
clearly shown; but in the central portions of some of the lamine,
secondary crystallization has tused them into a mass of fibrous
chalcedony (fig. 4). The nature of these spicules can be more
favourably ascertained from the detached forms, obtained by dis-
solving some of the matrix in acid, than from those in the connected
skeleton, which appear to be more altered. Their mineral charac-
ters have already been carefully described by Dr. Sorby, and no
further reference needs here to be made to the circumstance that
some are at present of crystalline calcite, since it is now well esta-
blished that these are but replacements after silica. Some of the
siliceous spicules retain outlines as smooth and perfect as in recent
forms (figs. 5, 6, 8, & 10), whilst others are corroded in varying
degrees, small concave hollows having been scooped out from their
surfaces, so that they now present a very Jagged appearance (fig. 9).
The central portion in some of the spicules also shows differently
tinted, banded layers of chalcedony, whilst the outer zone is
transparent (fig. 10). Mounted in Canada balsam they are so

* Since my paper was sent into the Society, Mr. W. H. Hudleston has shown

me two specimens of this sponge in his own collection, one from Scarborough
and the other from the Coral Rag of Settrington.

FROM THE LOWER CALCAREOUS GRIT OF YORKSHIRE. 57

transparent that little more than their outlines can be distinguished ;
whereas in glycerine they stand out prominently, and their surface
features are clearly seen. The spicules vary from ellipsoidal to
subspherical in form, with a small notch or hilum which gives
them their characteristic kidney-shaped appearance. In sections
of the sponge-wall they range from ‘11 to ‘15 millim. in diameter,
but some of the detached torms are not more than *08 millim.
in thickness. On the surface of the best-preserved spicules there
is an ornamentation of minute subcireular spots with shaded
borders, apparently regularly quincuncially arranged ; the spots are
very minute, averaging only ‘002 millim. in width (figs. 6 & 7). They
were first noticed by Prof. Blake, and supposed by him to indicate
perforations in a surface-shell. I have also noticed in a few of the
spicules traces of very fine lines or fibres radiating from their centres
to the surface (fig. 8). These and the sarface-markings indubitably
prove the structural similarity of the fossil spicules to the siliceous
globates of the crust of the recent Geodia and other sponges ; for it
has long been known that each of these recent globate spicules is built
up of a great number of minute siliceous radial fibres which extend
from the centre of the spicule and terminate on its outer surface in
nodose or spined ends, and the traces of radiate fibres and the surface-
spots in the fossil spicules are really due to the original structure of
minute fibres like those of the globates of the recent Geoda.
The subcircular spots representing the terminal ends of the fibres
in the fossil globates are, however, much finer than those of recent
forms, but they correspond more nearly in this respect with the
globates of the recent genus Placosponzia, mentioned below.

Hitherto no sponge has been described, either fossil or recent, with
a skeleton entirely composed of globate spicules, as seems to be the
case with this fossil form, and its systematic relations are conse-
quently somewhat uncertain. As a rule, globate spicules, like
those of this fossil, form a firm dermal crust to sponges whose main
skeletal spicules are of quite a different character; thus in G'eodia,
as already mentioned, the mass of the skeleton of the sponge usually
consists of relatively large fusiform acerates and long-shafted forks
and anchor spicules; and in the Jurassic Lecanella paterefornus,
Zittel, whilst the surface is stated by * v. Zittel to be covered with
innumerable globate spicules of precisely the same character and
size as in our fossil, the main skeletal spicules are irregularly
branching Lithistid forms. There is, however, a very remarkable
recent genus, Placospongia, Gray, in which the globate spicules form
a solid interior axis to the sponge, of much the same character as
the anastomosing plates of the interior of the present fossil. In the
type species of this genus, P. melobesioides, Gray f, which I have had
an opportunity of examining in the Natural History Museum,
South Kensington, there is in addition to the solid axis of globate
spicules a deuse dermal crust of the same kind of spicules, and in

* “ Studien iiber fossile Spongien,” Abh. der k. bayer. Akad, der Wiss. Cl. ii.
Bd. xiii. Ab. i. p. 135.

t Proc. Zool. Soc. Jan. 1867, p. 127.

58 DR. G. J. HINDE ON A NEW GENUS OF SILICEOUS SPONGES

the interspace between the axis and the crust a layer with numerous
pin-like spicules, frequently in sheaf-like bundles with their pointed »
ends directed to the exterior, and scattered globates as well. But
for the presence of this layer of skeletal pin-like spicules, of forms
characteristic of an important group of Monactinellid sponges, there
would have been considerable analogy between the present fossil
and Placospongia. The possibility that pin-like spicules may have
been originally present in the interspaces between the anastomosing
wall-plates of this fossil sponge is not altogether excluded; for
judging by their disposition in Placospongia, they would be much
less likely to be preserved in situ than the dense axis of globates,
and some show of probability is given to this supposition by the
occurrence of a few detached pin-like spicules mingled with the
globates in the rock matrix. In the sponges themselves, however,
there is no evidence of an intermediate layer of pin-like or other
spicules ; their walls, as already stated, appear to be entirely com-
posed of the minute globates. As, moreover, we find that the globates
are associated in different sponges with various types of skeletal
spicules, Tetractinellid, Lithistid, and Monactinellid, there is
no antecedent improbability that they may exclusively form the
skeleton in this fossil.

In addition to possessing a solid interior skeleton of globate
spicules, there is another point of resemblance between Placospongia
and this fossil, in the fact that the minute siliceous component
radial fibres of the globates in the two forms are very similar,
whilst they are distinctly smaller than the radial fibres of the
globates in Geodia.

The presence of a distinct zone of pin-shaped spicules in Placo-
spongia and their apparent absence in this fossil indicates, how-
ever, a very marked systematic distinction between these forms; and
they may respectively prove to be types of two distinct families *.

It may be inferred that the detached globate spicules probably
belong to more than a single genus and species, and it is therefore
necessary to propose a special designation for the particular sponge
above described. The generic name fenulina, given by Prof.
Blake to the globates, has moreover been preoccupied +. I propose
therefore to name this fossil genus Ahawellat, and the family
Khaxellid, with the following diagnosis :—

* There is considerable difference of opinion as to the proper systematic
position of Placospongia. By Dr. Gray and others it has been placed near
Geodia on account of the similarity of the globatespicules, whilst Mr. H. J.Carter,
F.R.S., relying on the characteristic pin-like spicules, places the genus in the
Suberitida, that is, with Monactinellid sponges (Ann. & Mag. Nat. Hist. ser. 5,
vol. vi. (1880), p. 477). Dr. Vosmaer states (Bronn’s Klassen u. Ordn. des
Thierreichs, Spongien, p. 405) that it should probably come at the end of the
Geodidz.

+ See Lamarck, Hist. Nat. Anim, s. Vert. vii. p. 605(1822); Blainville, Dict.
Sci. Nat. tome xxxil. (1824).

t pag, a berry, dimin,

FROM THE LOWER CALCAREOUS GRIT OF YORKSHIRE. ag

Genus Ruaxetia, Hinde.

Sponges with walls of anastomosing plates or trabeculae, com-
posed entirely of aggregated masses of globate spicules.

RHAXELLA PERFORATA, sp.n. (Pl. VI.)

Sponges palmate, flabellate, or perhaps funnel-shaped ; the largest
specimen, which is not complete, is 140 millim. in height and 80
millim. in width. Outer surface smooth or faintly ribbed, perforated
irregularly by oval or slit-lke apertures from 1 to 9 millim. in
diameter. The plates of the wall are from ‘5 to 4 millim. in
thickness, usually from 1 to 2 milliim. They interosculate so as
to form labyrinthine interspaces of varying width. The globate
spicules vary from ellipsoidal to nearly spherical in form, with a
_ well-marked depression or hilum. They are mostly from -11 to
-15 millim. in diameter ; very small forms are only ‘08 millim. The
fibres of the globates are very minute; their distal ends are sub-
circular, and average ‘0U2 millim. in diameter.

Distribution. Corallian : Lower Calcareous Grit (Zone of Ammo-
nites perarmatus): Scarborough, Yorkshire. Coral Rag: Settring-
ton, Yorkshire (Huddleston). Detached spicules, some of which
probably belong to this species, also occur in the Coral Rag of North
Grimston, Yorkshire (Hudleston), and on nearly the same horizon
at Sturminster Newton, Dorsetshire, and at Hilmarton, near Colne,
Wiltshire (luke).

SuMMARY AND ConcLUSIONS.

In the Lower Calcareous Grit of Scarborough definite sponges of
somewhat irregular outlines, varying from funnel-shaped to sub-
palmate in form, occur partially weathered out, as a rule on the
surface of the rock. ‘he sponges are siliceous, their walls consist
of irregularly perforated plates or anastomosing trabecule, which
are entirely built up of aggregated masses of minute globate spicules
similar to those of the recent genera Placospongia and Geodia,
without any apparent intermixture of other spicular forms. The
globates show traces of component radial fibres and surface-markings
precisely similar to those of analogous spicules in recent sponges.

Sponges of this type of skeletal structure, with labyrinthic walls
wholly of globate spicules, have not hitherto been known either
fossil or recent; as a rule, spicules of this form are associated with
acerate, trifid or pin-shaped spicules, and in one fossil genus with
lithistid spicules. The recent Placospongia, which has a solid
central axis of globate spicules, presents the nearest analogy to the
fossil Rhawella.

These sponges are very good instances of the preservation of the
entire or nearly entire skeleton of the organism in spite of the fact
that the component spicules are not originally united together or
held in position otherwise than by the soft animal structures, which
necessarily perish after the death of the animal. Such instances are
extremely rare ; for as a rule sponges of this character fall to pieces

60 DR. G. J. HINDE ON A NEW GENUS OF SILLICEOUS SPONGES

and their individual spicules are scattered over the sea-bottom. <A
similar fate undoubtedly befell the great majority of these sponges
in the ocean of the Lower Caleareous Grit; for, whilst the entire
skeletons are very seldom met with, the detached component spicules
form avery notable proportion of the rock-matrix in which they are
imbedded, and the specimens may be considered as the scantiest
relics of an enormous multitude, which by specially favourable cir-
cumstances have escaped disintegration.

These sponges also furnish additional proof of the connexion be-
tween these organisms and beds of chert and silica (other than
quartz). Thus in the Cliff at Scarborough, as Mr. Hudleston has
shown, there isin the Lower Calcareous Grit, from which these sponges
have been obtained, a bed of 3 feet 4 inches (about 1 métre) of
intensely hard chert, and beneath this, 30 feet (9 métres) of a
calcareous grit, largely cemented by silica. There can be little
doubt that most of the silica in this considerable thickness of rock
(not reckoning the sand grains) is due to the siliceous sponges ; for
throughout these beds, not only at Scarborough itself but in the
adjoining areas, Mr. Hudleston has pointed out that where these
minute globates are not themselves now present in the siliceous
strata, they are represented by minute empty moulds, which bear
witness that the spicules themselves have been dissolved and the
resulting silica has been redeposited to form the siliceous cement in
the rock. Mr. Hudleston has given so excellent a description of
the Calcareous Grit which has been thus formed that I venture to
quote the passage*;: —“‘ It is almost entirely devoid of calcic carbonate,
and consists chiefly of a poriferous mass of siliceous matter, which
includes a quantity of extremely fine quartzose sand. The cherty
portions exhibit the pores also, but then they seem further apart
and less connected. Sometimes the pores are empty—pin-hole
structure ; sometimes they contain a white powder, which is either
silica or a silicate—speckled structure. In a greater or less degree,
the above characters may be recognized in very much of these yel-
low sponge-cake cale.-grits, giving rise to the idea of the decompo-
sition of granular bodies of almost microscopic minuteness, which,
during the formation of the rock, had formed no inconsiderable
portions of its mass, but which, subsequent to consolidation, have
in most cases been removed by solution.” Proc. Geologists’ Asso-
ciation, vol. iv. (1875), p. 32, sep. cop.

EXPLANATION OF PLATE VI.
Rhaxella perforata, Hinde, gen. et sp. nov.

Fig. 1. An imperfect subpalmate specimen, showing the irregular mode of
growth and the perforate character of the wall. Natural size. The
specimen is now quite free from the matrix. It comes from Scar-
borough, and now belongs to the Museum at York.

2. A fragment of another specimen in which the wall exhibits a flattened
trabecular structure with slit-like apertures. Natural size. __

3. A transverse section of the above, showing the labyrinthic disposition of
the laminee of the wall. Enlarged two diameters.

* Proceedings of the Geol. Assoc. vol. iv. (1875), p. 44, sep. cop.

FROM THE LOWER CALCAREOUS GRIT OF YORKSHIRE. 61

Fig. 4. A transverse section of a fragment of the wall-plates, enlarged twenty
diameters, showing its structure of globate spicules. In this specimen
the sponge is imbedded in a matrix of transparent granular calcite.

5. Several of the globate spicules, obtained by dissulving in acid the rock-
matrix in which one of the sponges is partially imbedded, showing
variations of form and size. Enlarged sixty diameters.

6. A globate spicule, enlarged two hundred diameters, showing the minute
points on its surface produced by the distal ends of its component
siliceous fibres. The specimen is mounted in glycerine.

7. A portion of the surface of a globate spicule, showing the markings
enlarged to six hundred and sixty diameters.

8. A globate spicule, enlarged two hundred diameters, showing traces of its

. component radial fibres. ‘The specimen is mounted in Canada balsam.

9. A globate spicule, enlarged two hundred diameters, showing the effects
of corrosion on its surface, whilst the imterior has been replaced by
banded chalcedony. Mounted in glycerine.

10. A similar spicule, showing central replacement, whilst the surface
remains unaltered. Mounted in Canada balsam.

Discussion.

The Prestpent said that paleontologists were greatly indebted to
Dr. Hinde for his researches on sponge-structure. They would espe-
cially welcome these details on an entirely new form. He noticed
the apparent anomaly of “ globates” being called “ spicules.”

Mr. Hupieston had been greatly interested in the results of this
particular piece of work, since it helped to clear up some disputed
points in connexion with the Corallian rocks of Yorkshire. These
microscopic globates, though swarming in parts of the Lower Cal-
careous Grit, were far from uncommon in portions of the Coral Rag.
He had been struck with the amount of chalcedonic silica in certain
portions of the Rag, and had egdeavoured to ascertain its source.
The rock-sections prepared for this purpose were full of small
granular bodies, which Prof. Sollas pronounced to be globates of a
siliceous sponge such as Geodia. The difficulty, of course, was to
account for the absence of the elongate spicules, and Mr. Hudleston
admitted that his own remarks on this point at a time when no one
had any suspicion of a sponge whose spicules were all globates,
might be open to correction. But since elongate spicules are
traversed by a canal, where the action of solvents first shows itself,
he still thought it possible that they might disappear as soon, if
not sooner, ‘than the more microscopic globates. The Author
thought otherwise. Anyhow, the problem, which had puzzled
Mr. Sorby and led to so much discussion, was now conclusively solved
by the recognition of the true nature of the Scarborough fossil,—
one of the many results of Dr. Hinde’s intimate acquaintance with
sponge-structure.

The Avror, in reply, said that he agreed with the remarks of
the President as to the anomaly of the term “ globate” spicules, but
the word “spicule ” might be advantageously employed i in a general
sense for the small bodies which compose the skeletons of ee
He did not think that Mr. Hudleston was much to blame for referring
the detached globates to Geodia, as he himself had been quite asto-
nished at the discovery of such a sponge as the one now described.

62 MR. R. LYDEKKER ON THE OCCURRENCE OF THE

5. On the Occurrence of the Srripep Hymna wn the Tertiary of the
Vat p’Arno, By R. Lyprexxesr, Hsq., B.A., F.G.8., &e. (Read
November 20, 1889.)

In cataloguing the remains of fossil Carnivora preserved in the
British Museum *, I entered, under the head of Hycna striata, a por-
tion of the left maxilla of a hyena obtained by the late Mr. Pent-
land from the Tertiary deposits of the Val d’Arno, in Tuscany.
At that time I had no evidence of the existence of this species in
the Pliocene, and the specimen was accordingly provisionally re-
garded as of Pleistocene age, since beds of that epoch are known to
occur in the Val d’Arno. At a later date I again referred to this
specimen in a paper read before the Society on May 12th, 18867,
and concluded that it might be from beds of Upper Pliocene age.
In the same communication I also described and figured a right
upper carnassial of a hysena from the Red Crag, which was likewise
referred to the existing Striped Hyena (H. striata). Following,
however, the lead of Professor A. Gaudry, I was at that time dis-
posed to regard H. arvernensis, of the Upper Phocene of the
Auvergne, as nothing more than a large variety of H. striata. It
was also considered that the premolars from the Red Crag, described
as H. antiqua, were in all probability referable to the same exist-
ing species.

In a recent memoir on the fossil Hyeenas of the Val d’Arno, Dr.
K. A. Weithofer £, who appears to have had the opportunity of ex-
amining actual specimens, concludes that H. arvernensis is entitled
to rank as a valid species. Thus it is much larger than H. striata,
while the inner tubercle of the upper carnassial is directed more
anteriorly, so that the width of this tooth across the tubercle is
much less in proportion to its length than in the Striped Hyena,
and the hind talon and inner cusp of the lower carnassial are rela-
tively smaller than in the latter.

In noticing the carnassial from the Red Crag, figured by myself
in the paper already quoted, and referred to H. striata, Dr.
Weithofer § accepts my determination, although, of course, imply-
ing that its identification with H. arvernensis is erroneous. When,
however, Dr. Weithofcr || comes to speak of the specimen from the
Val d’Arno, which I have referred to H. striata, he states that all
the specimens from the Pliocene beds of that locality which have
come under his notice are more nearly allied to the Crocutine group,

* Cat. Foss. Mamm. Brit. Mus. pt. i. p. 88 (1885).

+ Quart. Journ. Geol. Soc. vol. xlii. p. 864 (1886).

t Denkschr. k. Ak. Wien, vol. lv. p. 341 (1889).

§ Op. cit. p. 844. The words are:—“ Lydekker bildet aus dem Red Crag
einen oberen Reisszahn einer Hyane ab den man allerdings—fiir sich allein—
als mit H. striata identisch erklaren muss.”

|| Op. cit. ps 840.

STRIPED HYNA IN THE TERTIARY OF THE VAL D’ARNO. 63

while in the Pleistocene he finds only ZH. crocuta (spelea#); and
by this he implies that my identification of the British-Museum
specimen with H. strata is incorrect. Since, however, the occurrence
of this species in Southern Europe is of some interest, I have deemed
it advisable to lay the evidence before the Society.

The specimen, of which two views are given in the accompanying
woodcut, comprises a fragment of the left maxilla, containing the
entire carnassial, the imperfect hinder half of the third premolar,
and traces of the inner extremity of the true molar. I give, in the
first place, the dimensions of the carnassial of this specimen (B.M.
No. M. 469) as compared with the corresponding measurements of
two recent examples of H. striata, and also of the above-mentioned
carnassial from the Red Crag. The dimensions of the recent spe-
cimens given in the first column are taken from Dr. Weithofer’s
memoir (p. 341), and those in the second column from a specimen
in my own collection.

Dimensions of Upper Carnassials of H. striata.

Val
Recent. Red Crag. d’Arno,
PIM. 5s oe ek ois oe 0:031-0°031 0:0325 0:0315
Width across inner tubercle .. 0-019 0-018 0:0195
Width of inner tubercle .... 0°009-0-008 0-0075 0-009
ienerh of lst lobe.......... 0009 0-010 0-010
enero 2nd lobe. ........ 0-011 0-015 O-O11
Wereth oi ord lobe ........ 0-011 0-011 0-0105

Lateral (A) and oral (B) views of part of the left maxilla of Hyena striata ;
from the Val d’ Arno. Nat. size. pm.3, third premolar; pm.4, fourth
premolar (carnassial) ; ™.1, true molar.

* Dr. Weithofer’s words are as follows:—‘ Nach dem Material jedoch, das
mir zu Gebote steht, gehdren beide Hyinen, die im Arnothal in plioeanen
Lagern gefunden worden, dem Crocuta-typus an; dasselbe gi!t auch von der
im Pleistocin der Umgebung von Arezzo gefundenen Hyane (= //yena spelea,
Goldf.).”

64 MR. R. LYDEKKER ON THE OCCURRENCE OF THE

The slight differences in these measurements are well within the
limits of individual variation. With regard to the actual contour:
of the fossil and recent teeth, I can find absolutely no difference in
them, whether I compare the Val d’Arno or the Red Crag example
with the recent jaw. ‘Thus in all these teeth the inner tubercle is
very large, and does not extend so far forward as the anterior
border of the first lobe, while the upper border of the crown of the
external surface of the third lobe is characterized by its sharp
downward deflection, thus rendering the enamel on the hinder part
of this surface of very small extent. The outer surface of this third
lobe is also characterized by the distinct median vertical groove.
The true molar in the Val d’Arno specimen is represented only by
a minute fragment, which does not indicate its original contour.
The third premolar is likewise exceedingly imperfect, but the por-
tion remaining accords with the corresponding tooth of H, striata.

In the absence therefore of any difference between the Val
d’Arno specimen and the corresponding portion of the juw of the
Striped Hyzena there appears every reason for referring the fossil
to that species.

Comparing the British-Museum specimen with the upper jaws of
the hyzenas from the Val d’Arno figured by Dr. Weithofer, it will
be at once apparent that it has nothing to do with H. robusta, of
which the upper carnassial is represented in pl. i. fig. 3 and pl. iv.
fig. 1 of the memoir cited, that species being, indeed, as Dr. Weit-
hofer points out, closely allied to the crocutine H. felina of the
Siwaliks. Compared with the upper carnassial of the specimen re-
presented in pl. 11. figs. 1, 2 of Dr. Weithofer’s memoir under the
name of H. topariensis, there is, indeed, a somewhat nearer resem-
blance, although there are well-marked specific differences. Thus
the length of the upper carnassial of H. topuriensis is 0-034, while
its inner tubercle is relatively smaller, and extends as far forward
as the anterior border of the first lobe. Again, in the third lobe of
the carnassial of H. topariensis the upper border of the outer surface
of the crown is not deflected, so that there is a large surface of
enamel in this part of the tooth, while there is not the distinct
vertical groove found in H, striata. Most of these differences are,
indeed, noticed by Dr. Weithofer when he contrasts the carnassial
of H. topariensis with the specimen from the Red Crag above men-
tioned ; and he observes that the two are altogether different.

In describing the specimens figured as H. topariensis, Dr. Weit-
hofer regards them as closely allied to, if not identical with, H.
Perrier of the French Pliocene; and it appears to me that there
can be little doubt that the French and Italian specimens belong
to a single species, for which the latter name should be retained.
If this be so, we have evidence that H. Pervert is markedly distinct
from H. crocuta, with which it has been compared, and is, appa-
rently, more nearly allied to H. brunnea, as Dr. Weithofer suggests
in the description of his specimens. H. Perriert (topariensis) 1s,
indeed, distinguished from H. brunnea by the presence of an an-
terior talon to the last lower premolar, and by the absence of the

STRIPED HY NA IN THE TERTIARY OF THE VAL D’ARNO. 65

inner cusp to the lower carnassial, although one specimen of the
living species in the Museum of the College of Surgeons also shows
the same deficiency. In H. brunnea, however, judging from a single
specimen, the inner tubercle of pm. 4 does not extend forward to
the anterior border of the first lobe of this tooth, in which respect
this species resembles H. striata*.

So far as I can gather, H. arvernensis seems also to be closely
allied to H. brunnea, having an inner cusp to the lower carnassial,
although there is no evidence as to the position of the tubercle in
the upper carnassial. J am, indeed, not very clear how H. arver-
nensis can be even specifically distinguished from H. brunnea, and
I would observe that both these forms seem decidedly nearer to
H. striata than to H. crocuta, while H. Perriert seems to connect
them with the latter.

Finally, I submit that sufficient evidence has now been adduced
to prove beyond reasonable doubt the occurrence of the Striped
Hyzena in the ossiferous deposits of the Val d’Arno, and also that
none of the specimens hitherto figured from these beds are referable
to that species.

Discussion.

The Prestpent called attention to the remarkable geographical
distribution of recent and fossil Hyenas. He remarked that HZ.
crocuta had been found by Mr. Lydekker in some of the Indian
caves, though H. striata was the only form living in that country:
and that at the present day H. striata was not found anywhere
along with H. crocuta, although both, or their ancestors, appear to
have inhabited Europe in late Tertiary times.

* Too much importance must not be attached to the position of this tubercle,
Thus in H. crocuta it usually extends to the anterior border of the first lobe,
but in one recent skull preserved in the Geological Department of the British
Museum it is behind this border, and a considerable variation may be observed
in the series of fossil specimens in that collection.

w.0.G. 5. No. 131. F

66 CAPT. A. W. STIFFE ON THE GLACIATION OF PARTS

6. Nore on the Gractation of Parts of the VatuEys of the JHELAM
and Sinp Rivers in the Himataya Mountains of Kasuuir.
By Capt. A. W. Srirrz, F.G.S. (Read December 4, 1889.)

( Abridged.)

THe extent of the former glaciation of the Himalayas has been
discussed by various authors, and very different views have been
expressed as to its magnitude. Mr. Lyddeker has noticed the
unstratified deposits of boulders in the Jhelam gorge, and the proba-
bility of their being ice-borne * ; Messrs. Theobald and Wynne have
described glacial deposits in the plains of the Punjab, not remote
from the foot of the mountains +; quoting Dr. Verechere’s remarks
on erratic blocks ahout 100 miles 8.W. of the Jhelam valley +, Mr.
Wynne § describes similar blocks near the Indus river southward
of Attock, and enormous moraines and angular blocks in the Eastern
parts of the Salt Range, also others 20 miles southward of Jhelam
City ; Col. Godwin-Austen || also refers to extensive glaciation of
the Jhelam valley.

The Author records his own experience while on a visit to the
valleys of the Jhelam and Sind rivers, stating, in the first place,
his belief in the gigantic scale of the ancient glaciation, and then
giving first a general description of the principal features of the
Sind valley and the existing glaciers near Sonamarg, which are at
present apparently still shrinking. The existence of snow-fields
far below the foot of the glaciers is an unusual feature.

Very perfect and typical older terminal moraines exist at Sona-
marg, some 4 imiles below the present glaciers, at an elevation of
about 10,000 feet, and these, at a not remote period, blocked up the
‘valley of the Sind river, and formed ‘a small lake now replaced by
a smal] Alpine plain; the sections cut by the rivers through these
moraines are remarkable.

The glaciated appearance of the gorge through the mountains just
below Sonamarg is very striking, and the indications reach to great
heights above the present valley-level, and the whole of the Sind
valley is characterized by a succession of moraines, through which
the river has cut gorges, sometimes very deep. The most marked
positions noted were as follows :—One on each side of Gagangair,
one with several concentric curved mounds about 5 miles above
Kongan, and another, just above Gootlibagh, only seen on the south
side of the valley.

But to go much further than this, the hillsides of the valley
generally were observed to be comparatively rounded in outline up to

* Memoirs of the Geological Survey of India, vol. xxii.

+ Records of the Geological Survey of India, ‘November 1880.
+ Journ. Asiat. Soc. Bengal, vol. XXxVi. p. 113.

§ Mem. Geol. Surv. India, vol. xiv.

|| British Association Report, 1880.

OF THE JHELAM AND SIND VALLEYS. 67

a definite height of 2000 feet or more, above which horizon they
were very rugged, suggesting forcibly the idea that the valley
must at one time have been filled with ice even to that greater
depth ; and there is no difficulty in believing this to have been
the case.

The lakes still existing in the Kashmir valley are referred to as
remains of a former extensive lake which has been filled up by
recent alluvium, and the Author describes the outlet of the drainage

of the valley at Baramulla; he then proceeds to notice the present

state of the supposed glacial deposits in the Jhelam valley, and
states that he formed the opinion that the dam or barrier near
Baramulla was partly morainic, and he has since seen that Prof.
Leith Adams considered that some of the gravels at this point were
of glacial origin.

The whole valley or gorge of the Jhelam from this point as far
as Mozufferabad, where it makes a sharp turn back on itself, shows
extensive glacial or morainic deposits. Below this bend, the Author
is not able to speak from observation.

The deposits have here been much modified by the river cutting
through them and depressing the valley, and by the superposition

_of fiuviatile deposits, chiefly from lateral valleys, and of the appear-
ance described as ‘‘ fans” by other writers.

Good sections of both kinds of deposits are seen in many places
where the river has cut through them, and also along the line of the
new road now being carried up the valley.

The two classes of deposits thus seen together are widely different
in appearance: the morainic matter with large and small blocks or
stones scattered at random through the clay, sometimes far apart,
and of mixed materials, partly subangular, and some of the blocks
very large; and the “fans” with closely packed well-rounded
pebbles of comparatively uniform dimensions and with some ap-
pearance of stratification.

In conclusion, the Author mentions the great deposits of travelled
granite blocks near Rampoor, which, on account of their size and
difference of composition from any neighbouring rocks seen in situ,
he thinks can only have been distributed by ice; and, finally, he
refers to the excavation of the valley by fluviatile action, partly
through these glacial beds, since glacial times.

DIscussION.

The Prestmpent had not himself visited Kashmir, but would call
atteution to two points: first, did glaciers come down to a lower
level in the Himalayas in Glacial times than they do now ? this he
thought bad been proved; secondly, what was the origin of the
large stones in the Jhelam valley and of those found in the region
west of Rawul Pindi? Commenting upon the supposition that the
latter had been transported by floating ice, he called attention to the
ereat floods of the Indus. Some of these were owing to the damming

up of tributaries, possibly by ice. In the Glacial period the Jhelaw
F2

68 THE GLACIATION OF PARTS OF THE JHELAM AND SIND VALLEYS.

might have been so dammed. He discussed the former extension
of the ice in other Himalayan regions. :

Mr. Lyprxxer said that there was no question that glacial de-
posits occurred in the Sind valley at Sonamarg and somewhat
lower down the valley. In the Jhelam valley the evidence was
not so satisfactory. The granite boulders never crossed small in-
tervening ridges between one valley and another, but followed
locally the stream-courses. He thought that when the lower parts
of valleys had been filled with detrital material it was difficult
to refer this to the action of glaciers, which should rather have
cleared out the valley-bottoms. The granite boulders disappeared
lower down the river. He referred to the detrital deposits in
Thibet, which certainly were not glacial.

Gen. MacManon was familiar with adjoining parts of the Hima-
layas. He thought there was no doubt that at no very distant period
there was an extension of the ice in the Inner Himalayas. He had
found the usual scratched and polished rocks at considerable dis-
tances from the valley-heads. Kven in the Outer Himalayas he
had found a remarkable moraine at Mamul, 14 miles from Dal-
housie, at an elevation of 4740 feet above the sea, perched upon the
crest of a spur running down from a mountain 9108 feet high,
containing granites and schists resting upon Carboniferous Lime-
stone. Referring to the question of boulders, he did not think
that in the Outer Himalayas these always furnished evidence of
glaciers. Some, he believed, had slipped down upon snow.

Prof. Huenxzs noted that the evidences of glaciation above the
Kashmir plain were unquestioned, whilst further down the origin
of the boulders was disputed. He asked whether the evidence of
glaciation of this part rested upon the boulders alone, suggesting
methods by which these boulders might have been transported by
water.

The Prestpent observed that boulders 20 or 30 feet across were
found many miles away from the Himalayas on the Punjab plains.

The AvuTHor, in reply, said that the blocks below Baramulla were
subangular, and that no rocks of similar character appeared in situ.
The boulders were furthermore imbedded in clay, and though he had
seen no ice-scratches on the blocks, he could not conceive clay and
boulders being deposited together by water. He maintained that
the detrital fans and the deposits which he referred to glacial action
were quite distinct. There were indications that the ice had gone
even higher than he had argued for in his paper.

THE TRIASSIC BRECCIAS AND CONGLOMERATES OF SOUTH DEVON. 69

7. The Iennovus Constituents of the Triassic Bruccras and Con-
GLOMERATES of South Devon. By R. N. Worvru, Esq., F.G.S.
(Read December 4, 1889.)

In the paper on “The Elvans and Volcanic Rocks of Dartmoor”
which I had the honour of laying before this Society on the 3rd of
April last, I mentioned that the examination of a number of
fragments of igneous rocks included in the Triassic breccias and
conglomerates of South Devon had shown that many so-called
“‘porphyritic traps ” among them were really “ elvans ” or felsites,
whilst others presented a near approach to true volcanic types *.

My present purpose is to follow up that remark by giving the
results of a detailed investigation of the igneous constituents of
these beds. The subject is by no means a new one; for the origin
of these fragments has now and again engaged the attention of
geologists, some of great eminence, for nearly seventy years. But
the opinions expressed have been diverse, and the problem can
neither be regarded as settled nor as having approached a definite
solution. So far as I am aware, indeed, no recent attempt has been
made at a general investigation ; and there has certainly been no
such application of modern methods of petrological research.

Under these circumstances it is hoped that the present paper may
prove of service as a record of observed facts affording material for
judgment; and that it will not be thought the attention of the
Society has been needlessly called to a topic in itself perhaps unim-
portant, but which, nevertheless, has weighty bearings on the
physical history of the West of England. There is no occasion, for
example, to enlarge on the proposition that very different conclusions
would have to be drawn with regard to the conditions prevailing
during the formation of these breccias and conglomerates, from the
presence in them of foreign rocks on the one hand or of native rocks
on the other.

, I preface the results of my own inquiries with an outline sketch
of the

History oF THE QUESTION.

The first detailed attempt at a lithological examination of these
rocks was made by the Rey. J. J. Conybeare, F.R.S., and set forth
‘in a letter in the ‘ Annals of Philosophy,’ dated February 15217.
Mr. Conybeare identified “Granite and Porphyritic Rocks” as
forming a “ very considerable portion of the imbedded fragments ;”
and described them under five classes and twelve varieties, in terms
which show that he had before him just such rocks as are com-
monly present now, specially indicating schorlaceous pegmatites and
“ elvans,” and suggesting “that the whole contents of this breccia

* Quart. Journ. Geol. Soc. vol. xlv. p. 399.
+ 2nd ser, vol. i. pp. 254-259,

70 MR. R. N. WORTH ON THE IGNEOUS CONSTITUENTS OF THE

had been furnished by the inferior rocks of its immediate neighbour-
hood.” While, however, Mr. Conybeare names granite, none of the
descriptions given by him apply to genuine granitic rocks. tg"

Sir H. de la Beche, in his well-known ‘Report on the Geology of

Jornwall, Devon, and West Somerset,’ indicates the common local
origin of these clastic beds, but notes the conglomerates of the strip
of Trias trending west from Crediton to Jacobstow as comprising
‘besides rounded fragments of the adjoining carbonaceous sand-
stones and slates, pebbles of porphyritic rocks, and some which
seem rolled fragments of Dartmoor granite”; and the conglo-
merates ‘from the neighbourhood of Exeter to the sea” as made up
*‘ of angular fragments and rolled portions of the various sandstones,
slates, and limestones on which they rest,” with certain igneous
rocks not so identified—most numerous towards the Teign; and
finally he thus sums up the evidence :—

‘“* When the detritus composing the conglomerate occurs in suffi-
ciently large pieces there is little difficulty in perceiving that with
the exception of some fragments of igneous rocks in South Devon, it
is derived from the adjacent and disturbed older beds, or from
igneous rocks associated with the lower part of the series; and we
infer that the finer portions are more comminuted parts of the same
rocks.”

Half a century since, therefore, the only question treated as open,
touching the constituents of these conglomeratic beds, was the origin
of certain of their igneous components, and that has remained the
single point of doubt or controversy, though it may seem strange
that the invariable local character of the sedimentary constituents —
had not almost forced the conclusion that their igneous associates
were local too.

Sir Henry de la Beche failed to detect any granite similar to
that of Dartmoor in the conglomerates south of Exeter to the sea, .
* while fragments of other igneous rocks, chiefly porphyries, a large
proportion of which are not known to occur in place, are extremely
abundant.” His general suggestion with regard to these porphyries
was that they might “readily have formed portions of igneous
masses covered up by the Red Sandstone series, and it is by no ,
means improbable that such masses are thus concealed ”*. |

While Sir Henry had thus accepted the occurrence of coe
resembling “some varieties of Dartmoor Granite” in the conglo-
merates near North Tawton and Sampford Courtenay, Mr. Godwin-
Austen, F.R.S., positively denied in the most absolute terms the
presence of any granite among the materials of the red conglomerates
of Devon. ‘No granite pebbles have been found among the
various materials of which the new conglomerates are composed” 7.
It is no doubt partly due to the uncertainty of one authority and
the overcertainty of the other, that this question has remained so
long in suspense. But the chief hindrance may have been the

* The citations from Sir Henry de la Behe are taken from the chapter in his

Report on the “‘ Red Sandstone Series,” pase‘, pp. 193-220.
t Geol. Trans. 2 ser. vol. vi. p. 478.

TRIASSIC BRECCIAS AND CONGLOMERATES OF SOUTH DEVON. 71

search for Dartmoor granite in particular, instead of Dartmoor rocks
in general.

The presence of indubitable fragments of Dartmoor granite in
the conglomerates of North Tawton and Haldon has, however, long
been recognized. They were found there by Mr. Vicary, F.G.S.,
and somewhat later by Mr. Pengelly, F.R8.S., in company with him,
at least thirty years since.

And so Mr. G. W. Ormerod, F.G.S., in a paper read before this
Society, on ‘“‘ The Murchisonite beds of the Valley of the Exe,” in
1875 *, identified the Murchisonite as clearly of Dartmoor origin,
and mentioned the occurrence of granite pebbles at Teignmouth.

But it is to Mr. Vicary that we owe the most definite pronounce-
ment on this head. In a paper read before the Devonshire Associa-
tion for the Advancement of Science, Literature, and Art in 1867 Tf,
he avers unhesitatingly that ‘‘the masses containing Murchisonite
are but altered portions of the granite of Dartmoor,” the variation
in colour and texture between the Murchisonite pebbles and the
in situ granite being quite paralleled by the changes which have
taken place in fragments of Carboniferous Grit and Devonian Lime-
stone in the same association. Moreover, he remarks that “ they
occur in the Trias in close proximity with pebbles of schorl and
altered rock, a collocation strikingly similar to that met with in
Dartmoor streams.” His final conclusion is (and I have his authority
for saying that it is only strengthened by subsequent investigations),
“Tf the granite was exposed at the surface at the era of the red
rocks, Dartmoor must have furnished a large proportion of the
conglomerated materials. I feel confident that a thorough exami-
nation of these materials will prove that granite is a far more
important constituent than geologists generally suppose.”

More recently it has been suggested that we should look else-
where especially for the origin of the characteristic red felspar
porphyries ; and Mr. W. A. E. Ussher, F.G.S., has suggested that
their source may be in the Channel area ¢.

Mr. Ussher also points out that while the breccias or con-
glomerates frequently contain igneous fragments distinctly referable
to the destruction of such igneous patches as those of Washfield,
Killerton, Silverton, and Spencecombe, “ the porphyritic and Murchi-
sonite fragments are confined to the South-Devon breccia.”

Instead of suggesting that these comparatively unworn fragments
are in any sense “ foreign,”’ such facts seem to me to assign them a
distinctly local character, and to indicate a probable origin in the
direction towards which the area of the beds containing them nar-
rows. We have another valuable hint in the fact that these frag-
ments attain their largest size in the vicinity of Teignmouth, and
that thence both to the north and south they rapidly graduate
downward to very moderate dimensions, and, in fact, into sand. It

* Quart. Journ. Geol. Soe. vol. xxxi. pp. 846-354.

ft Trans. Dev. Assoc. vol. ii. pp. 200-202. =

t Vide Quart. Journ. Geol. Soe. vol. xxxiv. pp. 461-462, vol. xxxv. pp. 240-
2157.

12 MR. R. N. WORTH ON THE IGNEOUS CONSTITUENTS OF THE

is not meant to imply that there is any absolute natural assortment ;
but that the range decreases, from materials varying between boulders
and sand, to materials in which the larger pieces would fairly be called
eravel.
This recital marks out the purport and scope of the present
inquiry.
INVESTIGATION.

In the preparation of this paper special examination has been
made of the breccio-conglomerates near Crediton, Exeter, Heavitree,
Exminster, Dawlish, and Teignmouth, with specimens of the con-
tained rocks collected at other points—to the number, in all, of
several hundreds, indeed thousands.

Generally speaking, the largest fragments occur, as already noted,
at and near Teignmouth ; and many very interesting examples may
be seen there built into walls near the sea. Especially prominent
also are the boulders in the Dawlish valley. Blocks occur ranging
to four and five feet in diameter. Around Teignmouth and Dawlish,
too, the breccias and conglomerates are most varied in their com-
position, and contain the largest proportion of granitoid rocks.

The constituents of the Exminster conglomerates come next in
size, and frequently range up to four or five inches in diameter,
occasionally more. ‘The granitoid character is also well preserved.

At Heavitree the same leading associations are fairly prominent,
but the fragments show a smaller average, and the proportion of
immediately recognizable granitoid examples is smaller also.

In the immediate Crediton district granitoid constituents, though
present, are not prominent, although at points igneous fragments
abound. ‘They are plentiful, however, to the west, in the strip of
Trias ranging along the north of Dartmoor, especially near North
Tawton and Sampford Courtenay.

The igneous fragments in the Torbay conglomerates diminish in
size and importance southward from the Teign. They are less con-
spicuously granitoid, and are frequently better rounded than their
sedimentary associates.

In the Triassic outlier at Slapton, if we may draw any conclusion
from the modern beach, granitoid pebbles must have been fairly
common, since there are plenty of well-characterized examples on
Slapton Sands which could not have been brought thither by any
modern river, but may well be Triassic waste.

The following is a complete list of the various kinds of igneous
and altered rocks noted. Most of them are represented by numerous
examples and occur at different points, and very few can be regarded
as rare,

I. GRANITEs,
1. Coarse-grained granite with porphyritic felspars, partly kaoli-
nized. Differs from ordinary coarse-grained Dartmoor granite
only in its reddish colour, though here, as in the dark-red

porphyries, the kaolinized felspars are white. I am indebted
for this example to Mr. Vicary.

TRIASSIC BRECCIAS AND CONGLOMERATES OF SOUTH DEVON. 73

2. Fine-grained schorlaceous granite from Exminster. This is the

only example which gave rise to doubt. Macroscopically it
seemed a fine-grained granite with a little mica and a fair pro-
portion of schorl. When sliced it suggested a possible clastic
origin, and as I felt unable to satisfy myself I obtained Professor
Bonney’s ever-ready help; and he pronounces it a fine-grained
granite, probably from a vein or small boss. Also precisely
identical with Dartmoor varieties.

3. In a quarry at Exminster there occur small patches of granitic

material, quartz, kaolin, and mica, which are clearly the relics
of decomposed granite fragments ; and very similar looseness of
texture may be observed in granitoid remnants elsewhere.

4, A comparison of sand from the Trias at Heavitree with modern

sand from the bed of the Teign at Chagford (both given me by
Mr. Vicary) shows the following results :—Heavitree: felspar
fragments, including Murchisonite ; quartz-grains, many of the
smaller fairly rounded ; granitoid rock, with schorl; grit, slate,
Lydian stone; felspathic trap (andesite?); colour ruddy.
Chagford: Bulk of the material essentially identical with that
of Heavitree, but less rounded and not iron-stained; quartz;
felspar; felsite; schorlaceous granite; a little slate and grit; »
mica: it chiefly differs from that from Heavitree in the plain
presence of mica and the absence of felspathic trap ; while slates
and grits are naturally more plentiful at Heavitree than at
Chagford.

IJ. Fetstre Grovp.

These rocks afford the widest range of variation, and are far

more plentiful than the true granites. I include under this head all
the granitoid fragments, seeing that most of the varieties pass easily
into each other, but divide them into schorlaceous and non-schor-
laceous.

re ee

A. Non-Schorlaceous.

. Pegmatite, apparently vein. Quartz, with some well-crystallized

felspar. ‘Teignmouth.

. Quartz-felspar vein, with decayed mica and kaolinized felspar.

Exminster.

. Reddish quartz-felspar rock, like a Dartmoor vein-stone. Teign-

mouth.
Glassy quartz-felsite, reddish grey. Undistinguishable from some
Dartmoor elvans. Teignmouth.

. Grey spherulitic felsite, with porphyritic quartz, slightly

vesicular; some cavities lined with crusts, some filled with
kaolin. Under the microscope the spherulitic structure is well
marked. Teignmouth.

Grey quartzose rock of trachytic aspect, of somewhat porous
texture ; base appears like an open granular felsite ; contains

74 MR. R. N. WORTH ON THE IGNEOUS CONSTITUENTS OF THE

remains of decayed porphyritic felspars, quartz-blebs, and little
nests of black mica, the latter a feature of frequent occurrence
in many elvans. Teignmouth.

7. Dark red rock, presenting much the same general characters.
Teignmouth.

8. Reddish-grey granular open-textured rock, with blebs of quartz,
mica-nests, and felspar-cavities lined and partly filled with
kaolin; some red iron-oxide in irregular cavities. Teign-
mouth.

9. Grey granular rock of trachytic aspect, with some porosity ;
cavities with remains of kaolinized felspars; decayed mica; a
little differentiated quartz. Teignmouth.

10. Pinkish-brown felsite, rough texture, slightly vesicular ; por-
phyritic felspars ; fluxion-structure indicated. Teignmouth.

11. Somewhat similar rock with quartz-blebs; cavities with kaoli-
nized matter; some white mica; porous rather than vesicular.
Teignmouth.

12. Yellowish-brown quartz-porphyry, loose-textured subvesicular
base, with quartz-blebs and developing felspars in part kaoli-
nized; matrix very porous in parts, yet heavy. Under the
microscope this rock shows hardly a trace of felsitic reaction,
though it does not suggest a texture between felsitic and
andesitic so closely as some of its associates. There is a little
mica. Dawlish.

13. Greenish rhyolite or liparite with compact base, and large
cavities, elongated in direction of flow; occurs in wall at
Teignmouth ; and is no doubt from conglomerate.

14. Finely vesicular rhyolitic rock with compact semivitreous green-
grey base; porphyritic quartz and felspar, the latter partly
kaolinized; nests of mica; shows distinct fluxion-structure.

15, Harthy-textured red and grey felsite with porphyritic felspars,
nests of mica, and vesicles partially filled with kaolin. Teign-
mouth.

16. Red felsite with porphyritic quartz and felspar, quartz pre-
dominating. Torbay.

17. Vesicular felsite (“‘ horny ” base) with porphyritic quartz, mica,
and felspar; full of irregular cavities. Torbay.

18. Red porphyritic felsite with quartz, kaolinized felspar, a little
mica; somewhat open-textured. Torbay.

19. Reddish coarse-grained porous variety, with mica more promi-
nent ; shows flow-structure.

20. Compact red felsite with porphyritic quartz, felspar, and mica.
Heayitree.

21. Pinkish-grey felsite, subvitreous base, with porphyritic quartz
and felspar, the latter partly kaolinized; has a decidedly
rhyolitic look. Heavitree.

22. Granular red felsite, porphyritic quartz and felspar; some
decayed mica. Heavitree..

23. Pinkish crystalline-granular felsite with porphyritic quartz and
felspar ; small flakes of mica. Crediton.

TRIASSIC BRECCIAS AND CONGLOMERATES OF SOUTH DEVON. 75

24. Porphyritic red and white quartz- and felspar-rock ; apparently
a vein-stone from “‘felspathic trap.” Crediton.

25. Grey-green felsite, finely granular texture, with porphyritic
quartz, kaolinized felspars, and some decayed mica. Crediton.

26. Fine-grained crystalline-granular felsitic rock. Exminster.

27. Reddish-grey quartzose felsite. Exminster.

28. Dull-brown porphyritic rock, felsitic base with kaolinized por-
phyritic felspars, Murchisonite, quartz, and mica. Some has a
brecciated look. Is closely allied to next.

29. Deep-red porphyritic rock, varying to red-brown and purplish-
brown; compact felsitic base with porphyritic quartz and
felspar, some of the latter kaolinized, some Murchisonite ; occa-
sionally but not invariably some mica. This is the so-called
red “ porphyritic trap,” more or less characteristic of the con-
glomerates within our area, from Torbay to the Crediton
valley, and the origin of which has been a special topic of
discussion, Save in colour, however, these fragments are
hardly distinguishable from some Dartmoor elvans.

I have been fortunate enough to trace them home as veins to the
so-called “‘felspathic traps,” in fragments of which I have found
them occur, both at Exminster and Teignmouth. ‘They appear in
some instances to have produced contact-alteration. They are really
what they seem to be (porphyritic elvans), which have traversed
granites and “traps” alike, and are of purely local origin. They
have undergone as much alteration, probably, as any class of rock in
the breccias, ranging in texture from an earthy to a vitreous base,
but can be followed without difficulty trom one phase to another.
One example really differs from the rock it intrudes on more in
structure than anything else, both showing felsitic characters, but
the vein being coarser and distinctively porphyritic.

B. Schorlaceous.

. Granular schorlaceous pegmatite. Exminster, Teignmouth.

. Reddish compact felsite with blebs of quartz, a little mica, and
schorl pseudomorphous after felspar, and in spots. Exminster.

. Variety of same rock, with somewhat granular texture, por-
phyritic quartz, decayed felspars, and veined with schorl.
Exminster.

. Finer variety of same. Exminster.

. Felsite like number one, with mica-aggregates. Exminster.

Granular greyish-drab felsite, with acicular schorl. Exminster,

Fine-grained reddish felsite, with porphyritic quartz and felspar,

base sprinkled with black specks. HKxminster.

. Red felspar- and schorl-rock. Lxminster.

. Quartzo-felspathie rock with blebs of quartz, large porphyritic
felspars, and schorl. ‘Teignmouth.

10. Base black schorl and quartz, with porphyritic quartz and

felspars (kaolinized) ; a little mica. Teignmouth.

© Wwe

STO OU

<& 0O

76 MR. R. N. WORTH ON THE IGNEOUS CONSTITUENTS OF THE

11. Porphyritic vein-stone, with Murchisonite, decayed felspars and
schorl. Exminster. (Possibly associated with andesite.)

12. Fine-grained grey felsitic rock, with quartz-blebs, porphyritic
felspars, kaolinized felspar-granules, fine mica, and acicular
schorl. Exminster.

13. Grey granular felsite, with quartz, mica, and schorl. Exmin-
ster.

14. Quartz-felspar-schorl rock. Heavitree.

15. Schorlaceous felsite. Red compact base with small porphyritic
felspars, quartz-blebs, mica, and patches of blue radiating
schorl—a, beautiful microscopic object. Teignmouth.

16. Reddish felsite with dots and nests of schorl, bluish-grey and
radiating. The microscope reveals the existence of radial
structure in the ground-mass, apart from the schorl. Teign-
mouth.

17. Schorlaceous felstone, with more prominent porphyritic felspars,
nests of schorl-needles, and some porphyritic quartz. Teign-
mouth.

18. Schorlaceous felsite ranging from fairly compact to granular ;
long felspar-crystals, quartz-blebs, decayed mica-clusters, light
spotty schorl. Teignmouth.

19. Rock with an andesitic rather than a felsitic look, but contain-
ing occasional needles of schorl. Teignmouth.

Ill. Anpzsrric Group.

I class under this head the various examples of “ felspathic
traps” which, like those in situ, range between andesites and basalts,
but are chiefly of the former class. They are found in the breccias
and conglomerates more or less plentifully throughout the district
under review, and in many cases present no distinctive characters
from some of the varieties in situ. Nor is the range of variation
greater in the one than in the other. The chief point to notice is
the frequent kaolinization of the felspars in these fragments, which,
in the case of the rocks with felted texture, gives them a curious
speckled mosaic aspect.

1. Fine-grained greyish-red or reddish-grey mica-andesite. Tor-
bay.

2. Ditto, but quartzose and slightly open-textured, suggestive of a
rock intermediate with a felsite. Torbay.

3. Red-grey speckled, felted andesite, with porphyritic vein con-
taining Murchisonite. Teignmouth.

4, Fine-textured andesitic rock, with acicular or felted base; red,
speckled with grey and spotted with black (? iron-oxide) and
containing kaolinized lath-felspars. Traversed by a porphyritic
felsitic vein, having a red compact subvitreous base, with
porphyritic quartz and felspars, and some mica. Exminster.

5. Fine-grained speckled variety, closely resembling sandstone.
Exminster.

TRIASSIC BRECCIAS AND CONGLOMERATES OF SOUTH DEVON. GT

6. Red speckled base, with kaolinized porphyritic felspars. Ex-
minster.

7. Slightly amygdaloidal variety, granular base with quartz-blebs
and porphyritic felspars. Suggests felsitic alliances, and pre-
sent aspect may be in part due to alteration. Exminster.

8. Speckled variety, with blackish patches.

9. Felted andesitic porphyry, red-speckled, lined with white.
Heavitree.

10. Examples resembling rock of Rougemont and of other spots in
the vicinity of Exeter. Heavitree. ?

11. Loose-textured, dark-brown patches occur in the breccia at
Exminster, which appear to be the remains of fragments of
decayed scoriaceous rock, like that of Thorverton or Wash-
field.

12. Rough-textured dark basaltic rock, closely resembling trap of
Yeoton. Teignmouth.

13. Loose-textured micaceous rock, closely resembling trap of
Killerton. Teignmouth.

14. Rock lke vein in trap at Posbury. Teignmouth.

LY. MiscELLANEoUs.

1. Quartz vein-stone. Exminster.

2. Glossy quartz-vein-stone. Yeoton. (Both these are of Dart-

moor character.)

3. Schorl rock. Teignmouth, Exminster, Heavitree—in fact almost

universally distributed.

4. Schorl-vein-stones, some laminated. Exmunster.

5. Felted schorl-rock, with porphyritic felspar. Exminster.

6. Schorl-felspar-rock with scoriaceous aspect. Teignmouth.

7. Reddish-brown altered brecciated rock, with schorl-crystals,

8. Veined schorl- and quartz-rock.

9. Highly altered, consolidated, bluish-grey schist, traversed by
numerous minute veins, some of which suggest cassiterite, now
very hard and compact. Teignmouth, Crediton.

10. Altered slate, baked and partly veined by felsitic matter.
Crediton.

Of these four classes of igneous and associated altered rocks, con-
taining in all 76 species or varieties, two (I. and IV.) can unhesi-
tatingly be assigned a Dartmoor origin in gross, and the same
remark applies to the schorlaceous division of IJ. The remaining
class, III., can with equal certainty be identified with or allied to
the in situ ** felspathic traps ” of the neighbourhood.

We have thus to consider further only the non-schorlaceous
section of No. II., and here we find the same characteristics; the
bulk of the examples differ in no essential particular from Dartmoor
elvans, and in the majority of the cases are practically identical
with them.

Of the residue, with but three exceptions, it may at once be said
that they belong to the same category, the only noteworthy distinc-

“78 MR. R. N. WORTH ON THE IGNEOUS CONSTITUENTS OF THE

tion between them and admitted Dartmoor felsites bemg that they
are of a looser and more open texture, displaying at times a porous
character which approaches an irregular vesicularity. They aro
apparently the more surface portions of felsitic dykes, or, it may
even be, fragments of felsitic lavas; and, at any rate, they may
reasonably be supposed to represent less deeply-seated rocks than
_the ordinary elvans. The very wide range of characters which
elvans assume, even in the same flow, was pointed out in my paper
of April last, and need not be enlarged upon here; and I will only
add that approaches to this trachytic or open texture are by no
means absent i sztu.

The only examples, then, in the whole series that show any
material divergence from existing Devonian rocks of the general
felsitic type are (5) the spherulitic felsite ; (13) the greenish rhyolite
or liparite; and (17) the vesicular felsite with horny base—three
rocks extremely likely to be found in this connexion, and affording
no reason why they should be regarded as an exception to an
otherwise universal rule. :

I do not think the fragments generally can be regarded as having
been altered to the extent frequently imagined. Structural change
has been very slight; and the chief points to note are the very
general modification of colour in sympathy with the ferruginous
surroundings (though this is by no means universal), and the
somewhat exceptional extent to which kaolinization has proceeded,
especially in the andesitic contingents.

ConDITIONS OF FoRMATION.

To complete our inquiry we must consider the conditions under
which these breccias and conglomerates were formed. That the
materials were carried to the places where we now find them by
water is clear. It is evident also that this water must have operated
over a wide area and with varying force. The current which carried
‘the great blocks of Teignmouth and Dawlish was more powerful
than that which distributed the sand and gravel of Heavitree; but
the bulk of the material must have quickly come to rest, or we
_ should have no breccias. At the same time there was enough tri-
turation and travel to reduce the softer sedimentary rocks very
considerably. ‘These conditions would be fulfilled by high land
with short rapid rivers abutting on a shore-line, along which the
material which they brought down would speedily be distributed ;
and in the present instance I suggest that we have a relic of this
high land in what is now Dartmoor. The work done by the existing
Dartmoor rivers, in its degree, strikingly resembles that of these
ancient Triassic streams; but the latter, while unquestionably of
greater volume, had, in all probability, powerful assistants in a
glacial climate on the one hand, and the disturbing effects of vol-
canic activity on the other. Of the existence of volcanic action
there is ample evidence.
Sir Henry de la Beche writes cautiously, but plainly indicates his

TRIASSIC BRECCIAS AND CONGLOMERATES OF SOUTH DEVON. 79

belief in the causal association of igneous action. ‘‘ Near Tiverton
the igneous rocks would seem to have been ejected after a certain
thickness of conglomerate had been accumulated. . . . Near Exeter
igneous action seems to have accompanied the earliest deposit” *.
He also directs attention to the fact that “the igneous rocks asso-
ciated with the lower part of the red sandstone series near Exeter
....occur in the prolonged direction of the granitic bosses and
elvans extending from the Scilly Isles to Dartmoor, themselves
apparently ranging in a line through which trappean matter had
been previously erupted ” +.

Next, discussing the occurrence of fossiliferous Devonian frag-
ments in the Trias of Tiverton, the late Rev. W. Downes, F.G.S.,
was led to postulate the existence of ‘“‘an active volcano upon the
coast of the early Triassic sea” +; and in 1885 Mr. A. Somervail
suggested a volcanic origin for the basal breccias of the Sonth-Devon
Trias §,

The highly interesting group of rocks which have been classed as
‘the felspathic traps of Devonshire are commonly, though not uni-
versally, associated with the South-Devon Trias. They make their
“appearance at or near the junction of the Carboniferous and
Triassic formations, from Washfield, near Tiverton, on the north, to
Haldon on the south. They extend westward along the strip of
Trias which runs from Bradninch to Jacobstow, and occur frequently
along both north and south lines of junction of the two formations
as far as Greenslade near North Tawton ” ||.

To this it must be added that a member of the series occurs
associated with a Triassic outlier at Cawsand on the shore of Ply-
mouth Sound, and that a dyke of mica trap at Roseash, unconnected
‘with Trias, appears to be of similar character 4.

These traps are in part antecedent to, and in part contemporaneous
with, the breccias and conglomerates which we are considering.
They are pre-Triassic, because their fragments are found in these
‘beds. They are continuous into the Triassic era, because at certain
points they overlie and alter the Trias.

They are commonly red or reddish-brown in colour, but by no
means universally so, and appear in this respect to have been
somewhat influenced by the Triassic rocks in situ, as well as in the
breccias and conglomerates, where, indeed, they display this colour-
character more constantly. The trap of Cawsand very well illustrates
this Triassic influence. In contact with the remnants of the Triassic
outlier it is red, but the veins sent off into the Devonian rocks for a
considerable distance become drab and grey. The Roseash rock is
yellowish brown; so is much of the Killerton, where the rock
occurs in mass.

‘One of the most important points connected with the chronology

* Report, p..215. t Report, p. 216.

t+ Trans. Dev. Assoc. xiii. p. 297. § Lbid. xvii. p. 285.

| ‘On the Feldspathic Traps of Devonshire,” W. Vicary, F.G.S., Trans.
Dev. Assoc. i. pt. iv. p. 43.

@ Trans. Dev. Assoc. xvi. p. 498.

80 MR. R. N. WORTH ON THE IGNEOUS CONSTITUENTS OF THE

and stratigraphical relations of these traps remains to be considered.
They are traversed at so many points by felsitic dykes that this
association has a constant and not a merely casual character. Mr.
Vicary noticed these dykes and their strong resemblance to elvan
courses, though, as ‘a matter of convenience,” calling them
sandstone*. Mr. Etheridge, F.R.S., suggested that a “ dike-like
line” in an example submitted to him by Mr. Vicary from Posbury,
‘‘ appeared to be an elvan.”

Sir H. de la Beche remarked, ‘‘the quartziferous porphyry near
Dunchideock closely resembles some elvans in all except colour” 7,
an exception which my experience shows does not hold good.
Mr. Townshend M. Hall, F.G.S., in 1879 ¢ announced the discovery of
a granitoid vein traversing the Triassic outlier at Portledge, which
“appeared to be a true porphyritic granite.” I have myself found
within the past few months fragments of syenitic veinstone closely
associated with the Cawsand trap.

When we add to this the occurrence of veins of porphyritic
felsite traversing fragments of felspathic trap in the breccias and
conglomerates, the chain of evidence seems complete that these
felspathic traps are comprised within the period of igneous activity
represented by the Dartmoor elvans, and that therefore Sir H. de la
Beche was right in suggesting a connexion between the two, though
this connexion was probably much more intimate than he suspected.

It is perfectly clear that there are no rocks to be seen now in
situ which can have yielded the examples of felspathic trap found
in the conglomerates in the neighbourhood of Dawlish and Teign-
mouth and thence to the southward; for these fragments must have
come with their granitoid and schorlaceous associates from the
direction of Dartmoor; and not only are there no exposures of such
rocks between the conglomerates of this district and the Moor, but
no places where they could be hidden from view unless it were by
the deposits of the Bovey basin, which for other reasons may be
dismissed. Lava-flows, it is true, might be wholly removed and
leave no trace in place behind ; but necks and dykes cannot be got
rid of by denudation in any such way, and would still be apparent.

The fact that these fragments came from the direction of Dart-
moor, coupled with the absence of any locality between Teignmouth
and Dawlish and their vicinities and Dartmoor whence they can
have come, thus points directly to Dartmoor itself as their source,
If that great granitic plateau is the base of a volcano, and if the
granites now exposed passed upwards into felsites, rhyolites, and
volcanic rocks, all is perfectly clear; but I cannot see that any other
hypothesis will meet the case.

The great bulk of the igneous fragments of these breccias and
conglomerates is more or less of a volcanic type, and the Plutonic
examples, though present, are comparatively few. The former
represent an enormous amount of degradation and denudation, which

* Op. cit. p. 47. This character is often simulated by elvans,

t Report, p. 217.
+ Trans. Dev. Assoc. xi. pp. 480,431.

TRIASSIC BRECCIAS AND CONGLOMERATES OF SOUTH DEVON, 81

the existing remnants of the felspathic traps by no means indicate a
capacity to supply: and beyond the Dartmoor area we seck in vain
for a source of sufficient magnitude. And it will be borne in mind
that on the most moderate estimate an enormous amount of super-
incumbent matter must have been removed from Dartinoor before
its 300 square miles of granite could have heen exposed as we see
them to-day, and that it is as absolutely certain as any geological
hypothesis can be, that a large proportion of this must have gone to
build up the beds ‘of the adjacent Trias.

ConcLUSIONS.

My conclusions may be summarized as follows :—

1. That the igneous materials of the Triassic breccias and con-
glomerates of South Devon are, as well as the sedimentary, of local
origin.

2. That they consist of granites, felsites, and volcanic types,
ranging from andesites to basalts.

3. That the granites are wholly, the felsites mainly, identifiable
with the granites and elvans of Dartmoor and its borders.

+. That the great bulk of the voleanic rocks are undistinguishable
in character from “felspathic traps” associated in situ with the
South-Devon Trias, but that andesitic features predominate.

5. That schorlaceous and contact-altered rocks occur in the
breccias and conglomerates, which may be referred with absolute
confidence to the outer (or upper) zone of Dartmoor.

6. That the few examples of igneous rocks in the breccias and
conglomerates which, allowing for alteration, cannot be absolutely
assigned to rocks yet existing 7m situ in Devon, are rocks of precisely
similar character, such as it is natural to expect in the same asso-
ciation, and simply phases of the same magma.

7. That the condition under which the “ felspathic traps” of
Devon occur 7m situ, their characteristic association with elvans, and
the part which they bear in the constitution of the Triassic breccias
and conglomerates, are calculated to lead to the inference that they
are volcanic phenomena connected with the igneous activities of the
Dartmoor region, and probably represent its final period, as the epi-
diorites and proterobases of the north and west of Dartmoor may its
earlier stages.

8. That the elevation of Dartmoor and the associated igneous
phenomena, which have been commonly regarded as_post- -Car-
boniferous and pre-Triassic, may in all probability be assigned to
narrower limits, and be regarded as not earlier than Permian times,
and possibly as occupying the Permio-Triassic interval, continuing
into the earlier stages of the Trias. Certainly if the eruptions of
the “ felspathic traps” of Devon and their associated elvans are
related to the great Dartmoor movement (and, as we have seen, these
traps are in part of Triassic date), we cannot well give the origin
of that movement a higher than Permian antiquity.

Q.J.G.8. No. 181. G

82 MR. R. N. WORTH ON THE IGNEOUS CONSTITUENTS OF THE

Discussion.

The PrestpEnt said that the question whence the materials were
derived was one of great interest, and must be worked out by careful
determination of the specimens.

Prof. Bonnry observed that the subject was one difficult to dis-
cuss, requiring great caution. But few specimens were shown, which
added to the difficulty; we required to see those from the breccia
and the en-situ rocks together. He was inclined to think the Author
right in his main contentions, and knew that he was an enthusiastic
worker. There was certainly Dartmoor granite in the breccia: those
rocks also with large crystalsin a more compact matrix might repre-
sent more rapidly consolidated portions of the same material. He
was glad a Devonshire geologist had taken up the subject. The
breccias indicated unmistakably the proximity of high land at the
time of their deposition.

Dr. Grrxre had been over part of the ground, and was unable to
see the connexion between the composition of the breccias and the
supposed occurrence of a Volcano on the site of Dartmoor. The
materials had not come from very far. During Triassic times there
was undoubted volcanic activity from many points of eruption, so
that there was no necessity for bringing the basic volcanic rocks
from Dartmoor; indeed, the presence of Dartmoor granite in the
breccias was unfavourable to the notion of volcanic rocks having
been derived from that source.

Dr. Hicxs had no doubt that some of the fragments had been
derived from rocks such as are known to occur in Dartmoor; but
that need not necessarily indicate more than that there was a pre-
existing ridge of such rocks in that area.

Mr. Hupteston tad arrived at much the same conclusion as Dr.
Geikie, especially as to the source of most of the volcanic fragments.
Tf Dartmoor had been a volcanic pile at the time of the deposition
of the breccias, its bulk ought to have contributed more material in
proportion to the local sedimentary rocks than is the case. There
was no @ priort improbability in the Dartmoor granite having termi-
nated upwards, af one time, in voleanic rocks ; but the period was
probably not later than the close of the Carboniferous when the
ereat earth-movements took place. Most of this material would
have been removed before the accumulation of the Triassic breccias.
Hence he was prepared to accept the theory of a great Devonshire
volcano, but rather doubted the evidence of its existence in the
South-Devon breccias.

Prof. Hugues inquired about the possibility of some of the frag-
ments having been thrown up by volcanic outbursts, from rocks not
then exposed at the surface. He had missed any reference to the
presence of harder volcanic material, such as is more or less seen to
be intercalated in the Devonian.

Prof. Jupp said that the subject could only be attacked by a local
worker. He regretted the absence of the Author and that there

TRIASSIC BRECCIAS AND CONGLOMERATES OF SOUTH DEVON. &3

was not a larger series of rocks exhibited. The Author’s areu-
ment appeared to be that the breccias contained granites, dyke-rocks,
and surface-lavas; that the two former of these came from the
Dartmoor area; and that it was not unreasonable to suppose that
the third class came from the same source.

84 PROF. J. PRESTWICH ON THE RELATION OF THE

8. On the Retation of the Wustteton Bens, or Pessiy Sanps of
SurroLk, to those of NorroxK, and on their Exrenston INLAND ;
with some OBSERVATIONS on the Pertop of the Finan ELevation
and Drnupation of the Wrap and of the Tuamus Vatiny, &e.
By Josepu Prestwicu, D.C.L., F.R.S., F.G.S., &e.—Parr I.*
(Read June 5, 1889.)

PATE te

$1. Introduction.

Iy a paper on the Crag Beds of Norfolk and Suffolk + which I had
the honour of laying before the Society early in 1870, I proposed to
term the great bed of flint-pebbles overlying the Chillesford Beds
and underlying the Boulder-clay in Suffclk, the “ Westleton Sands
and Shingle,” remarking that ‘‘the importance to be attached to
those beds does not arise so much from their exhibition here [Suf-
folk], as from the circumstance that they will serve to determine
the position and age of some beds of sand and gravel, generally
without fossils, which have a wide range in the south-east of
England, and the exact [geological] position of which it is impor-
tant to know in consequence of their bearing on many interesting
problems connected with the denudation of the country.” I further
mentioned that these marine sands and shingle had a much greater
extension than had their associated beds on the Norfolk coast, that
they ranged through Suffolk, Essex, and far up the Thames Basin,
and that the main character by which they were to be recognized
was the great preponderance of well-worn rounded pebbles of
flint and of white quartz, with smaller variable proportions of
angular or subangular chalk-flints, and of Lower-Greensand chert
and ragstone, mixed with a few pebbles of quartzite, sandstones,
slates, and lydian stone, the whole indicating the action of
currents or streams, not from the north as with the Glacial Drifts,
but from the south and south-east.

For some years afterwards various circumstances hindered me from
resuming my notes, many of which were made in 1845-1855 during
the construction of the Great Eastern Railway and its branches,
where the sections are no longer visible. At the meeting of the
British Association in 1881, however, I gave a short account of the
extension inland of these beds, and mentioned their occurrence on
some of the hills in Essex, Hertfordshire, Buckinghamshire, Berk-

* Part I. only of this paper, dealing with the coast sections, is here printed.
Parts II. and IIT. will deal with the relation of the beds here described to the
Glacial Beds in the Thames Valley, and with some other questions.

t Quart. Journ. Geol. Soc. vol. xxvii. p. 461.

WESTLEION BEDS TO THOSE OF NORFOLK, ETC. 85

shire, Kent, and Surrey. But that paper was only published in
abstract, and without tables or sections.

In the meantime the significance of these beds had not escaped
the attention of Mr. Whitaker, who adopted the name of the
** Pebbly Series ;” but as there are very similar pebbly beds of
Tertiary age in the Blackheath, Addington, and Bagshot districts, I
think the local name of Westleton, where their typical characters
can be best seen, preferable. In 1880* Mr. Whitaker came inde-
pendently very much to the same conclusion as myself with respect
to certain Pebble-beds on some of the hills around London, as
likewise did Mr. 8. V. Wood, who gave in his paper of 1880 7
a plate of sections and a map showing a number of outliers in
the London and Hampshire Basins, but with the drift-cappings
marked in many instances doubtfully, and mostly without local de-
scriptions or proofs. I shall have occasion to refer to both these
papers at greater length presently.

As regards classification, Mr. 8. V. Wood, in his several papers
(1866--1372), places the Pebbly Sands of the Bure Valley at the
base of the Glacial Series (or of his ‘“‘ Lower Glacial”); whereas
Mr. H. B. Woodward, in his Survey Memoir, classes them with the
Upper Crag. It is true that in Norfolk they succeed immediately,
and in many cases conformably to the Norwich Crag and Chillesfoid
Beds; but, as pointed out by Mr. Wood, there is also often a line ot
erosion between the two, and although the marine fauna contains
similar species, it is poorer and more purely northern than that of
the Crag Series. Further the Pebble-beds extend far beyond the
area of the Crag, and afford evidence, as I shall endeavour to prove
presently, of great physiographical changes having intervened be-
tween these two groups. ‘There is evidence also of an equally
important, if not a still stronger, break between the “ Pebbly
Series” aud the Glacial Beds. I would therefore assign to the
Westleton Beds a position apart, whether in relation to the Crag or to
the Glacial Series. They mark a great change not only in the
physical geography, but also in the life of the times, for it was then
that the existing Mammalian fauna began to supersede the extinct
species, and the Molluscan fauna to resolve itself almost entirely
into species now common in this country, with a few others, which
although still living are, hke some of the land animals, relegated
to colder climates. ‘This applies also to the flora.

For these reasons and also because this period is one of those coin-
cident, as I hope to show in the second part of this paper, with the
time of the final elevation of the Weald and of the genesis of the
Thames (the main excavation of the valleys and the great denudation
of the Weald being referable to subsequent Glacial and Post-Glacial
times), much importance attaches to this geological horizon. Lalso
look upon these beds as the base of the Quaternary Series,

Since 1870 a number of important papers, including several

* Mem. Geol. Survey, ‘‘ Guide to the Geology of London and the Neighbour-
hood,” pp. 55-57.

t Quart. Journ. Geol. Soe. vol. xxxvi. p. 457.

86 PROF. J. PRESTWICH ON THE RELATION OF THE

Memoirs by the officers of the Geological Survey, on different: parts
of the Eastern Counties, have appeared, and various opinions have
been expressed respecting the age, and the correlation, as well as the
classification of these beds. It may be desirable therefore, before pro-
ceeding to the second part of this paper, to give my reasons for ditter-
ing from some of these conclusions. ‘lhe Memoirs of the Survey, to
which I shall have frequent occasion to refer, now supply a mass of
valuable details, which greatly facilitate the task and do away with
the necessity of much local description. I shall confine myself
therefore to my own notes and a few typical sections, and to ques-
tions of synchronism and classification.

§ 2. Historical Remew.

In my notice of the Westleton Beds, I referred, but very briefly,
to the Bure-Valley Crag of Messrs. 8. V. Wood and Harmer, as I
touched only incidentally on the beds of north Nortolk*. At the
same time, I felt justified in expressing my own views with respect to
their general bearing, not only because they differed in many material
points from those of Mr. Wood, but likewise on the ground that my
paper was the result of independent observations made during the
preceding quarter of a century, and our conclusions differed on
many material points. It would appear that we were both work-
ing independently at the same subject, and the difference of views
may have arisen in a great measure, as suggested by Mr.
Whitaker, from the fact that whilst Mr. Wood was working
from north to south and chiefly inland, I had been working trom
south to north and chiefly on the coast-line.

That I was not singular in hesitating to accept Mr. Wood’s views
will be evident from the remarks of Mr. I. B. Woodward, Mr. Clement
Reid, and others, who have since surveyed the district.

In 1866 Mr. Wood stated briefly, in the supplement to a paper
by his father on the Crag Mollusca 7, that in the Bure Valley there
was a fossiliferous Crag consisting of sands and shingle with shells
(Tellina obliqua, Cyprina aslandica, Cardium edule, &e.) in patches,
and that this Crag was newer than the Norwich Crag. As these
beds in the Bure Valley rest, however, directly on the Chalk,
and as the diagrams were only generalized ones, we were, in the
absence of detailed local sections, left without the necessary strati-

* Tregret that Messrs. Wood and Harmer should have thought that my state-
ment was a misrepreseniation of their views, J mentioned, ] believe correctly,
that they had’ placed the Bure-Valley Beds on a higher level than the Norwich
Crag, though Imay have misunderstood, with reference to the Weybourn Crag, the
meaning they attached to the term “ Lower Glacial,” with which they associated
these beds. In the absence of more detailed sections and definitions, it was
difficult to follow the exact meaning of Mr. Wood’s earlier papers. Whether
there was anything new in my views, T must leave the reader tojudge. There are
certainly material ‘differences in our inter pretation of the phenomena.

+ Quart. Journ. Geol. Soe. vol. xxii. p. 547.

-WESTLEION BEDS TO THOSE OF NORFOLK, ETC. 87

graphical evidence in proof of their exact relationship to the associ-
ated strata.

In the following year Mr. F. W. Harmer gave a section oi the
Yare Valley *, confirming the views of Mr. Wood; and in 1868
these gentlemen read at the Meeting of the British Association in
Norwich a. joint paper, illustrated with a large map and _ local
sections, but of which an abstract only was published in that year 7.
In this it was stated that the Pebbly Beds or Crag of Belaugh in the
Bure Valley, and the Crag of Weybourn and Cromer, were newer
than the Chillesford Beds, and that ‘‘ the ‘sands with pebbles’ occupy
in the south of Norfolk and the north of Suffolk, the same place
relatively to the ‘ contorted Drift’ as is occupied on the Cromer coast
by the Weybourn Sand (or so-called ‘ Crag’ of the Cromer coast),
the Cromer Till, and the indenting sand (or bed C). These pebble-
beds may thus represent in time either the whole or any one of the
formations A, B, and C; or they may form merely the closing bed
of the true Crag Series, in which case the Weybourn sand, the
Cromer Till, and bed C are entirely unrepresented in the south of
Norfolk and north of Suffolk.” On the next page A is stated to
represent the Weybourn Sand with shell patches resting on the
Chalk, aud “passing up by interbedding into B, the Cromer
Till or Lower Boulder-clay,” and C the sands which indented into
‘‘ a deeply-eroded surface of the Till.”

In 1869 a paper was communicated to the Norwich Geological
Society by Mr. Harmer {, which gives a clearer exposition of
Mr. Wood’s views, and is accompanied by a list of the Belaugh shelks,
including these of Weybourn (postea, p.93)§$. In this Mr. Harmer
says that “ the only doubt felt by Mr. Wood and himself in con-
nexion with the beds of the Crag Series in Norfolk is, whether or
not the pebbly sands of Belaugh and Weybourn are identical with
the Pebbly Sands and Pebble-beds which overlie the Chillesford Clay
in the neighbourhood of Norwich, of Ladden, of Halesworth, and
of Beccles, or whether they do not form astill later deposit,” . . . ‘* so
that for the present they do not express any opinion on the identity
of the Pebble-beds in these two areas.”

In other papers published in 1869 || those gentlemen again give
the succession of beds about Norwich, and state that the Pebbly
Sands and Pebble-beds (a name which they were the first to adopt),
which succeed to the Chillesford Clay, ‘expand northwards into the
Weybourn Sand and Boulder Till of the Cromer-Cliff section ; this
bed is unconformable to the Crag and Chillesford beds, is paleeonto-

* Quart. Journ. Geol. Soc. vol. xxiii. p. 89.

t Geol. Mag. Oct. 1868, vol. v. p. 452. The map and sections were not
published until 1872, when they appeared in the ‘Supplement to the Crag
Mollusca,’

t Geol. Mag. vol. vi. p. 231.

§ Mr. H. B. Woodward's list of these fossils given at p. 93 is corrected by
Mr. Wood up to 1881.

|| Quart. Journ. Geol. Soe. vol. xxv. p. 446.

88 PROF. J, PRESTWICH ON THE RELATION OF THE

logically distinct from them, and is characterized by the first
appearance in England of Z'ellina balthica.”

Ini1e70* Wir. Wood reiterates his opinion that the Pebbly Sands
of Belaugh, from which he had then obtained 35 species of Mollusca,
are “continuous with the pebbly sand underlying and baka
with the Till along the Cromer coast and yielding similar shells,”
and he groups these together with the Contorted Dritt, as ‘ Dower
Glacial” (the italics are mine).

In January 1870 my paper on the Norwich Crag and Westleton
Beis was read +, although it was not published until 1871,
owing to difficulties connected with the lists of fossils. The main
object of that paper was to correlate the Westleton with the Mun-
desley Fluvio-marine Beds, and to show that they passed uncon-
formably under the Till of Cromer, with which they have no con-
nexion, and overlay the Norwich Crag.

It was not until 1872 that Mr. Wood published the detailed
sections upon which his conclusions were founded, and gave a full
list of the fossils of the ‘‘ Lower Glacial” beds, including the Bure-
Valley and Weybourn Crags. This showed that although we had
both arrived independently at the conclusion that the Pebble-beds
of both counties were newer than the Chillestord Beds, there were
many points, such as in the correlation of the Weybourn Beds, the
passage upwards of the Pebbly Sands into the Glacial Beds, the
construction to be put on many of the Suffolk Beds, and other
points, which I shall have occasion to notice as we proceed, that
constituted radical differences.

We hare in 1880 § the last expression of Mr. Wood’s views with
reference to the Pliocene, Glacial, and Postglacial deposits. In this
paper he deals with the many theoretical considerations connected with
the changes of level and conditicns, and the range of the several de-
posits. He also alters some of his previous determinatiuns in the Suf-
folk area, and explains his views of the “ origin and mode of accumu-
ration of the Pebbly Sand and Cromer Till as one formation.” But
to obtain a correct knowledge of Mr. Wood’s range of work, the
reader should consult the several papers here referred to. It is
difficult to epitomize them owing to the frequent introduction of
theoretical considerations among the questions of fact, and the re-
peated subordination of the latter to the former.

In 1881 || Mr, H. B. Woodward came to the conclusion that in
Norfolk the beds between the Glacial Drift and the Chalk formed an
indivisible group—‘ the Upper Crag or Norwich Crag Series ”—
composed of a variable group of sands, Pebble-beds, and laminated

* Geol. Mag. vol. vii. p. 17.

t Quart. Journ. Geol. Soe. vol. xxvii. p. 452.

t ‘Intreduction to the Supplement to the Monograph of the Crag Mollusca,’
Paleontographical Society, 1872-1874, pp. xv—xviii.

§ Quart. Journ. Geol. Soe. vol. xxxvi. pp: 457-527.

|| ‘The Geology of the Country around Norwich,’ Mem. Geol. Survey Expl.
of Sheet 66 N E., 8.E. pp. 31-41.

WESTLETON BEDS TO THOSE OF NOKFOLK, ETC. 89

clays, with occasional seams or patches of shells. In this he in-
cludes the Pebbly Sands, the Bure-Valley (or Westleton) Beds, the
Chillesford Clay, and the lower Fluvio-marine Crag. The Wey-
bourn Crag he considers, with Mr. Wood, to belong to the upper
or Pebbly-sands division. He remarks on the importance of the Mol-
luscan fauna and on the fact that the shells are, with few exceptions,
of the same species throughout, but varying, though on the same
horizon, ‘in the abundance of particular forms ” and “in the number
of different species.” He dwells on the fact that in the Bure-Valley
Crag of Belaugh there are “only two species not positively known
to occur in the Crag near Norwich, namely Tellina balthica and Palu-
_ dina viripara,” and states that 2 is nowhere seen im ‘section in its
fossiliferous form above the other * zones” of the Crag * (p. 36). He
also considers that the Haddiscoe gravels, ‘‘ with which the pebble-
beds of Halesworth, Henham, and Westleton are correlated, are
distinct from the Pliocene Bure-Valley Beds, which I (H. B. W.)
group with the Upper Crag” (p. 85).

In Mr. Clement Reid's memoir ‘“ On the Country around Cromer,”
1882 7, he expressed an opinion that my divisions of the Crag on
that coast will not hold good, in that I have placed the Chillesford
Clay at different horizons; but as he does not say to which of my
sections this observation applies, | am unable to answer the objection.
This stratigraphical olsjection will, however, be met further on in this
paper.

In a later paper t Mr. Woodward expresses his belief that the
Westleton and Mundesley Beds on the Cromer coast “ are not the
same as the Bure-Valley beds inland,’ and he gives an amusing
avcount of ‘the confused and deplorable condition that the nomen-
clature of the Pliocene and Post-Pliocene deposits is in.” He fears
“that the introduction of the words ‘ Chillesford Clay’ had been at
the root of nearly all the evil in the shape of confused or compli-
cated classification,” but he confesses “ that coming from a county
where some of the rocks are measured by thousands of feet, he may
have contemplated with too little respect divisions that dwindle into
inches,” no less than five subdivisions having been introduced into
30 feet of strata, and “of these nearly all had two or three names.
But most distressing of all has been the indiscriminate identification
by some observers of the Chillesford Clay with any micaceous and
laminated clay-seam ’’$.

It may be thought that Mr. Woodward somewhat magnifies the

* The italics are mine.—J. P.

t Mem. Geol. Survey, Explan. of Sheet 68 E.

t ‘Notes on the Bure-Valley and the Westleton Beds,” Geol. Mag. dee. ii.
vol. ix. p. 452 (1882) ; and ‘Geology of England and W ales, 2nd edit. pp. 460-
508.

§ Laminated clays are common in the Westleton and Mundesley, as well as
in the Norfolk Glacial Series. To be sure of the Chillesford Clay, it is neces-
sary to determine it either by superposition or by its fossils, when present,
or by following its range on a given horizon. Mr. Gunn named the upper
divisions of the Mundesley group “ Preglacial Laminated Series,”

90 PROF, J. PRESTWICH ON THE RELATION OF THE

risk incurred by the adoption of such meagre divisions; but in the
absence of more important masses of strata, we have unavoidably to
depend on these smaller beds, although it must be with the qualifi-
cations he names. :

Mr. Woodward states that his conclusions differ from mine in
some important particulars, chiefly in the correlation of the beds in
several localities. He bases much on the fact that in the general
sections I have coloured the Dunwich Cliffs as Glacial Sands *.
That, however, in no way affects the special question. Whether
the Dunwich Cliffs, which are much obscured, belong to one division
or the other is unimportant. Mr. Woodward satisfied himself that
they belong to the Westleton Beds, but Mr. Whitaker has since
shown reason to believe that the lower part at all events belongs to
the unfossiliferous sands of the Crag. At one spot they are capped
by a small patch of Westleton pebbles with an overlier of Boulder-
clay ; while the lower part of the cliff, consisting of sands without
fossils, may very probably, as Mr. Whitaker supposes, belong to the
Crag tf.

Mr. Woodward objects to Messrs. Wood and Harmer grouping the
Bure-Valley Beds as Lower Glacial, and sees no satisfactory palee-
ontological reason for separating them from the Norwich Crag, with
which he unites them under the name of the “ Norwich-Crag Series.”
He states that “the grounds on which Messrs. Wood and Harmer
separated the Bure-Valley Crag from the Norwich Crag have proved
to be unsound. The Bure-Valley Crag is paleontologically identical
with the Weybourn Crag, as they originally pointed out. Both
beds contain the Vellina balthica. But as my colleague Mr. C. Reid
has shown, the Weybourn zone is to be traced at the base of the
Forest-Bed Series, at Sherringham and other places; whereas
another bed, at a higher horizon, since called the ‘ Leda-myalis
bed’ by Mr. Reid, was also correlated by Messrs. Wood and Harmer
with the Bure-Valley Beds. ‘Thus we have a fossiliferous zone at
the top and another at the base of the ‘ Forest-Bed Series,’ both of
which have been called the Bure-Valley Beds; and this is the reason
why some observers have stated that the Norwich Crag overlies the
Forest Bed of Cromer, while others have maintained that the Crag
underhes it. The true fossiliferous Bure-Valley Zone, however, as
just stated, occurs at the base of the Forest-Bed Series, and is
represented by the Weybourn Crag. The Tellina balthica thus
occurs. beneath beds which Messrs. Wood and Harmer have grouped
as ‘ Pre-glacial,’ and their argument that this shell is confined to
Glacial aad more recent deposits loses all weight.” ‘ Hor the same

* T find that I overlooked one of my early note-books, in which I had noted
Boulder-clay and Westleton Shingle at one point on the top of the cliff, as
described by Mr. Whitaker in his ‘ Geology of the Suffolk Coast,’ pp. 52-89.

t In 1871 Messrs. E. T. Dowson and W. M. Crowfoot, of Beccles, found a
fossiliferous bed quite at the base of this cliff, from which they procured 44
species of shells with a few Mammalian remains. They refer this bed to the
Fluvio-marine Crag.

WESILETON BEDS TO THOSE OF NORFOLK, ETC. gt

reason, also, the Mundesley and Westleton Beds, identified by Prof.
Prestwich on the Cromer coast, are not the same as the Bure-
Valley Beds inland.”

Mr. Woodward further states that under the term “ Lower Glacial
Dritt” he would include not only the Cromer Till and Contorted
Drift, but also the *‘ Middle Glacial,’’ as he regards them as inti-
mately connected; ‘hence the Westleton Beds would be Lower
Glacial, the Mundesley Beds would come in the debatable ground
called Preglacial, the Bure-Valley Beds are Pliocene.”

In a subsequent paper * Mr. Woodward, in speaking of the Crag
and Pebbly Gravel, says ‘“‘ In their notes on the pebbly gravel and
its relation to beds above and below, Messrs Wood and Harmer
have expressed their opinion that on the coast the Weybourn Sand
(=Bure-Valley Beds) passes up by interbedding into the Cromer
Till, while the pebbly gravels around Norwich that immediately
underlie the Lower Glacial brickearth, were considered by them to
be, to some extent, the equivalents of the Cromer Till.”

He then observes, ‘“‘ Neither my colleague Mr. Reid nor myself
have seen any evidence to corroborate this opinion ; on the contrary,
the line between the undoubted pebbly gravels (which are grouped
by us as Pre-glacial) and the overlying Glacial Drift is generally
sharply defined,’—a conclusion in which I quite agree.

I quote these remarks of Mr. Woodward (the bearer of a name so
long and honourably connected with the investigation of the Crag and
Glacial series of Norfolk) to show how complicated the question has
become, and how diverse the opinions on the subject still are. The
classificatory objections to Messrs. Wood’s and Harmer’s Bure-
Valley Crag do not, however, affect the question of superposition,
on which their main contention on this point is founded.

In 1887, Messrs. W. Whitaker and W. H. Dalton, in their
memoir ‘ On the Geology of the Country around Halesworth and Har-
leston’ 7, state that in the area they describe, the beds of the Pebbly
Series vary, and “to the west and north-west they change into fine
sands and loams, each exposure showing different peculiarities.”
They express a preference for the use of the lithological name
instead of the geographical ones of Mr. Wood and myself, and leave
the question of the relation of the Pebbly Series to the Glacial Drift
and Chillesford Clay or to the Pliocene below an open question.

The reasons for not pledging himself to the question of classifica-
tion are given by Mr. Whitaker in a later memoirt. In this he
makes some pertinent remarks on the “ Pebbly Series” and its
literature. In explanation of the various names and classifications
that have been proposed for these beds by diflerent writers, he
suggests that “It seems possible that anyone working southward
from the northern part of Norfolk might get into a somewhat dif-

* Mem. Geol. Survey Expl. Qt. Sheet, 68 N.W. and S.W. pp. 11-14 (1884).

t Mem. Geol. Survey Expl. Qt. Sheet 50 N.E. pp. 11-17.

t “The Geology of Southwold and of the Suffolk Coast, from Dunwich to
Covehithe,” Mem. Geol. Survey, Explanation of Sheet 49 N., 1887, p. 22.

92 PROF. J. PRESTWICH ON THE RELATION OF THE

ferent mental groove from anyone working northward from the
southern part of Suffolk. Both may be locaily right; but it does’
not follow that either must be right generally; at all events the
variety of opinion that has been evolved is rather bewildering.”
This must be my apology for the present digression.

In his memoir of 1884 Mr. Whitaker records the occurrence in the
highest part of the Westleton shingle at Henham of a band of iron-
stone with casts and impressions of shells; but the species are
not named. He likewise announces the discovery of fussils—in the
Southwold area—of this age, in one case in a pit on the Lowestoft
Road, two thirds of a mile N.N.W. of Southwold Church, and in
another in the railway-cutting near the station (p. 29), and gives
lists (p. 85) of the species, on the authority of Mr. W. M. Crowfoot
and of Mr. 8. V. Wood. I am not, however, quite satisfied that
these shells, or at least all of them, belong to the Westleton beds.
As this is a point of considerable interest, I give the species in
the Table at p. 93 for the purpose of comparison with those of other
localities.

In the first-named locality casts and impressions of shells were
found im an iron-concreted portion of the shingle, whilst at the
bottom of the pit actual shells were found. In the second locality
the shells occurred in a Jenticular mass, 6 inches thick and about
5 feet deep, in a cutting 7 feet in depth, and in another small patch
about 12 yards northward. It appears to me, however, possible that
some of these shells may belong to the Upper Crag (the Chilles-
ford Sands); for the Chillesford Clay has been much denuded*, so
that the Pebble Beds often come into juxtaposition with the Upper
or Fluvio-marine Crag. A little north of Southwold, the cliff section,
in fact, shows the pebbly (Westleton) beds in contact with yellow
sands of this age, owing to the removal of the Chillesford Clay. It
may be therefore that the lower part of the sections belongs to the
Crag, or that the shells are derived from it.

The following are the species mentioned by Mr. Whitaker as
occurring in the above-named places. To these I have added a
column tor the species enumerated by Mr. H. B. Woodward from
the typical Bure-Crag localities of Belaugh and Wroxham, although
even there, I think, there is some uncertainty whether the latter
beds are free from intermixture with the Fluvio-marine Crag. It
must, however, be borne in mind that the range and location of
specics in the Crag are extremely variable.

* Mr. Whitaker mentions that the Chillesford Clay is wanting in places near
Southwold, probably having been cut off by the Pebbly Beds (op. cit. p. 62).
It was wanting also in the Southwold well, where the underlying Crag was
tossiliferous.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 93

Mr. Whitaker’s Mollusca of Southwold beds and of the Bure-Valley
beds of Norfolk, compiled from the lists of Mr. W. Whitaker *

and Mr. H. B. Woodward f.

The third column shows the species that occur also in the Upper or Fluvio-
marine Crag of the adjacent localities of Haston Bavant (near Southwold) and

of Norwich (near the Bure Valley).

ADOMA/EPHIPPIUM 2.220... .c.c00e0-
PANAMA ISURTALA 6a cinneediccssavecscscees
PURPATHS DORGAITS ” iccecevercscscscacses
Aatarte cOMpressa .............0000:
Gari CUS oie: .. cacsccescsscceses
Cardium greenlandicum ............
Cardium islandicum.................-
SOT BETIAUR) Gen pov cendemedieveadess
Cyprina islandica ..........6...csce0ee
POA WICTALUS ..c.cdee eceudecdeccsees
Leda oblongoides .......4. sesseeeeee
Hane@ins, WOTEALIS 0.0.0. <ss0d+eacaceesses
IP EHEETIOVAIES | iooacciscevsscidartenwes es
MTC SOUR “sche ccsedetacacaresess

PAR PEOMATIAN | 8. fees cededatles Wwedess
PANG BOULIS\), . 2eiiond ocesdavacdasses
Nucula Cobboldiv .....0..6.....-0
Pecten tigrinus, var. levis .........
EUW OMAS CVIBSPALA. (icscoccssecctsssceeoe-
Saxicava arctica, var. rugosa ......
Serobicularia plana ..........0.0:.0+
PMA ANGICH) ( s6cisie ed co dsecs'er sos
SUSUR IAbA | cas duge aden aes-iacs secee-
SPE MGAVODIGUE {0 cccccssancassacseeses
Tellina pratenuis ..............cs0008
Thracia papyracea ..........0....04.
PSC UNGALUIA 6..6.02...c.c000-
Cerithium tricinctum. ...............
MGPOPUANCLOTOR, foecasscvsbsecscceses
PUBORIGS PUCIS iioic.scdecesecdeeees.
Melampus pyramidalis

PUGRIGH CALCD, Fonscneevasensseescncces
Natica helicoides ............2-sss0.s
PONCE, MGCIA | Sec sccsescsccsvescaes
Paludina? glacialis ..................
feuepura lapillus: ..i.0i.vste..scess..
Scalaria proenlandica ...............
COPAGMANCIGUMS srisececicecaecig’s
Trophon antiquus, var. contrarius.
Mtritella/ towebwiitss..sseastiesst sce.

Southwold
Pp. Bite
Station

8.

eorteos

sarees

eeecee

eeeeee

eeseee

eeesee

eeseee

ser eee

eeeeee

|

a0.
£8
; ene
ay. sey a ¢
Bes | 235
a5 | see
o iS
ome | 246
Bae wihas ae
Flas
W. N.
N.
B., W. Hoan
B., W. E., N.
B., W EN;
es E., N.
B. fragts.
ig E., N.
B., W. BS, We
B. *?
B., W. N.
B., W. E., N.
B. E., N.
W. N.
W. E., N.
B., W. E., N.
B., W. E., N.
B,, W. H., N.
W.
B. N.
B. N.
B. x N,
B., W.
B., W. H., N.
B., W. BN:
B., W. Bs Bs
B. N.
B. E., N.
ask ¥N,
5. WW. E., N.
Bi w,N.
Ru iver H., N.
Ena ene be i Evy ING
B. E., N.
oe Oe E., N.
in)
iB} H., N
B., W. E., N.
B., W. E., N.
B., W N.
wees K., N.

The specimens in the third column marked with an asterisk are also found
in the Crag near Southwold ; w in the Southwold well.

* Mem. Geol. Surv. 1887, pp. 82-84.

t Ibid, 1881, pp. 42-53.

94 PROF. J. PRESTWICH ON THE RELATION OF THE

It thus appears that of the 18 species from the Southwold sections
13 are recorded in the Bure Valley; whilst of the other species,
three (Melampus pyramidalis, Cerithium tricinctum, and Paludina
media), which are characteristic of the Fluvio-marine Crag, have
not been met with in the Bure-Valley Crag. The other two are
also Norwich species, but have a wider range. On the other hand,
of the 36 species quoted from the Bure Valley, 16 are wanting at
Southwold, amongst which is the only characteristic shell of that
Crag, Tellina balihica, while other such common Westleton and
Bure-Valley shells as Scalaria grenlandica, Nutica helicoides, Asturte
compressa, Leda oblongoides, and Mytilus edulis are also wanting.

§ 3. Choice of Terms.

The main objection, however, to the adoption of the ‘ Bure-
Valley Crag or Pebble-beds”’ as terms for these geological zones, is
that neither their paleontological value nor their stratigraphical
relations are in that district free from uncertainty. Where the
Chillesford Clay intervenes, there is no doubt of their distinctness ;
but where this bed is wanting, as is commonly the case in Norfolk,
it is almost impossible to distinguish between the beds above and
the beds beneath that zone; and as, in consequence of the Pebbly
Beds resting upon an eroded surface of the Chillesford Beds, the
juxtaposition of the two shell-beds is of frequent occurrence*, their
duality then is lost. At Norwich this distinction still exists; but
further northward, in the Bure Valley, the Chillesford Clay is
either wanting or else exists in a very fragmentary form; so that,
in such cases, owing to their having many characters in common,
the distinction between the Bure-Valley and Norwich-Crag beds
might pass unnoticed.

It may, in fact, be a question whether the thin seam of clay
which in Mr. Wood’s typical sections of Belaugh and Wroxham is
intercalated near their base (see Mr. Woodward’s memoir, pp. 60
and 62) does not represent the Chillesford Clay, and whether in the
same way the thin occasioual bed of clay a foot or two above the
Chalk in the coast-section is not also of the same age, and whether
the lower shell-bed in these several localities should not be referred
to the Norwich Crag instead of grouping it with the overlying beds
under the term of the ‘‘ Weybourn Crag,” or as the “ Lower Glacial ”
of Mr. Wood. (See Supplement to the Crag Mollusca, pp. 203 -219.)
To test the point, I would keep the fossils from these beds separate
until their exact relationship is ascertained with greater certainty.
Mr. Woodward’s short lists, at pp. 62 and 63 of his Norwich memoir,
show slight but not unnoticeable differences between the upper and
lower part of the section. Tellina balthica, which is stated by
Messrs. Wood and Harmer to be almost the only shell in the Pebbly
Sands that does not occur in the Norwich Crag, is not found in the
lower bed at Wroxham, although it is at Belaugh; but I think (for
reasons to be given hereafter) with Mr. Woodward, that the occur-

* Quart. Journ. Geol. Soe. vol. xxvii. p. 456 (1871).

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 95

rence of this one shell is a very insufficient paleontological dis-
tinction.

Where the Chillesford Clay is absent, evidence of its former pre-
sence o:ten exists at the base of the Pebble-beds in the form of
pebbles of clay, derived probably, in some cases, from that clay.
The instance recorded by Mr. Woodward in the typical Wroxham
_ district, of a gravelly bed with clay pebbles at the base of beds of
buff sands and pebbly gravel (the Bure-Valley Beds*) in a cutting
near the station may be of this character. It is easy, therefore,
to imagine that, owing to this removal of the Chillesford Clay, the
Bure-Valley Crag may often be in contact with beds of the age of
the Norwich Crag, and that in the case of beds so much alike it
would be difficult to detect the line of separation, while the fossils
of the lower beds would be apt to get mixed with those of the
upper one.

Therefore, while I admit the value of the distinction drawn by
Messrs. Wood and Harmer between the Norwich Crag and the Bure-
Valley Pebble-beds, [ do not think that either the palzeontological
or stratigraphical proofs respecting the position of these Pebbly »
Sands are so well defined and certain in the Bure-Valley district as
they are in the Westleton and Southwold districts, or so fitted to be
taken as the type of a wide-spread geological zone. For these
reasons, although the term of Bure- Valley Crag or Beds may be con-
veniently applicable to a local fossiliferous condition of the Pebbly
Sands, I do not think it to be, for a general term, so suitable as the
term of “ The Westleton und Mundesley Beds.”

This is the term that in 1881 ft I proposed to adopt in place of my
original term of ‘‘ Westleton Sands and Shingle,” in 1870, for the
reason that when a particular series of strata presents, in adjacent and
conterminous areas, markedly different paleeontological and structural
characters, it may be convenient, as in the case of the ‘ Woolwich
and Reading Beds,” to give them a double geographical name, indi-
cative of the localities where the two types are respectively best
developed, and their relation to the overlying and underlying strata
best exposed. It will, however, be convenient, when speaking of
the inland continuation of these beds, to use merely the term of
*« Westleton Beds or Shingle,” as then we shall have to deal with that
type of them alone,

§ 4, The Structure and Paleontological Characters of the Westleton
and Mundesley Beds, in Norfolk and Suffolk.

Before proceeding with the inland range of these beds, I will
describe more fully my view of the relation they hold—on the one

* Similar cases, having reference to this and other underlying clay-beds of
the Forest-bed series, are common in the coast sections, and are recorded by
Mr. C. Reid (op. cit. p. 15 &e.) and by myself (Quart. Journ. Geol. Soe. vol.
XxVii. p. 465).

+ This paper is an amplification of the one then read before the British
Association, and which appeared only in Abstract,

96 PROF. J, PRESTWICH ON THE RELATION OF THE

hand to the Fluvio-marine Crag, and on the other to the Glacial
beds in Snffolk and Norfolk. |

The composition of the shingle will engage our particular atten-
tion, as it is an instance in which the evidence afforded by it is of
more stratigraphical value than that of the fossils, as the latter are
confined to the sea-board of the Eastern Counties, while the former
has to be our guide over the wide inland area,

I will now drop the term ‘ Pebbly Beds,” which, although con-
venient as a temporary term, marking, as it does, a very distinctive
character, has the inconvenience of defining a feature common to
many other strata, as, for example, the Pebble-beds of the Bagshot
Sands, or those of the Woolwich and Blackheath Beds. It is like

Fig. 1.— General Section of the Westleton Beds on Westleton Common.

Se eS ee

SSS SSS ee

a. Surface soil—gravelly.

6. Fine shingle, with lenticular beds of white sand.

c. White sands—quartzose—horizontal bedding.

d. Light greenish clay.

e. White sand passing down into ochreous pebbly sands, with a few large
unworn blocks of flint and some ironstone bands and concretions.

No fossils were met with in these pits *.

* In another pit on the common, I found, in digging a few feet lower, a
sandy clay with very friable specimens of TYeldina and Natica.

WESTLEION BEDS TO THOSE OF NORFOLK, ETO. 97

the old designations of ‘ Plastic Clay ” and “ Mottled Clays,” which
would specialize characters common in formations of Tertiary as well
as of Secondary age.

The localities where the Shingle Beds are most extensively de-
veloped, and where the joint lithological and paleontological cha-
racters are best combined, will be found in the Ordnance Map, Sheet
49 W.and50 KE. From this centre I will first take their range
northward.

Between Westleton and Dunwich there is a large tract of common,
formed by low hills of pebbly shingle, which extends with little
interruption to Blythburg and Southwold, and thence to Easton
Bayant and Covehithe, forming a belt some 2-4 miles wide and
10 miles long. The higher ground is everywhere capped by Boulder-
clay, from beneath which the Shingle Beds crop out, whilst on the
coast the Chillesford Clay rises from beneath the latter (except where
it has been denuded before the deposition of the Shingle), thus
defining accurately the stratigraphical position of the Shingle Beds.

The Shingle consists of flint pebbles as well rounded and forming
beds as massive as the Tertiary Beds of Blackheath or Addington,
with subordinate sands and thin clays. From two of the closely
adjacent large pits on the common, the accompanying general
section (fig. 1) is constructed from notes taken some years since.

Unlike the overlying Glacial Beds with their northern drift, we
have evidence in this Shingle of a decided transport from the south-
ward in the presence of subangular worn fragments of Chert and
Ragstone of the Lower Greensand, probably of Kent, a fact to
which I formerly drew attention*. With these are associated a
considerable proportion of small white quartz-pebbles and a few
large flattish ovoid pebbles t of light-coloured Quartzite and Sand-
stone, with small pebbles of Lydian stone and jasper &c. There
is a total absence of the larger darker red and grey rounded
- quartzite-pebbles (cobbles) of the New Red Sandstone, so common
in the Glacial Series. The average composition ¢ of this Westleton
Shingle at Westleton may be roughly taken as under :—

Per cent,
Se eM TER ISO DIOS a ils adaess sic ail sslunae daddies daieeeesesceneesdascen'cesess 60
2. White quartz-pebbles, with a few rose-coloured ............seseeeeee 20
Pee UbAMemiat HATItS, NOG StAINEM: .....: 2... sieaeseveecwsccececatoveerccss seers 10
4. on a a fragments of grey pin-hole ragstone and dark yellow
SCO fete rer ee WU pals vice Nea easets cna pMuances pub ecoaitessssuse 4

5. Large flattish pebbles of light-coloured quartzite, light and dark
sandstones, and small pebbles of veinstone, Lydian stone, and
jasper, with a few subangular fragments of black chert (Carbo-
niferous ?), of a dark slaty rock, and of quartz

* Op. cit. pp.461 and 477 (1871); and British Association Reports for 1881,
. 620.

+ They are very similar in shape and colour to the recent quartzite-pebbles
on the Chesil Bank.

+ The determinations in all cases can only be given approximately. For
reasons given in Part II. of this paper these proportions may not be quite
correct locally ; but as the same error, if any, runs through all the localities,
the general result is not seriously affected.

Ova. G. 8. No. 181. H

98 PROF. J. PRESTWICH ON THE RELATION OF THE

The proportions, as might be supposed, vary in every pit, and
even in different parts of the same pit; but the constant presence of
the first four constituent parts, and the absence of certain others, is
a remarkable feature, and enables us to recognize these beds when
other evidence is wanting, and to distinguish them from beds of
Lower Tertiary, Bagshot, or Glacial age with which they might
otherwise be confounded. |

Near Halesworth, 6 miles N.N.W. from Westleton, where sub-
angular flints are more abundant, the shingle consists of :—

1.Flint-pebbless.cehewak:: Pee ee ee 50
2.. White. quartz—-pebbles\. scerecacvaternasddsont 10
o. Subangular fits. oie ep eees encodes 34
ey ACNERE CGC? Sic ru ece anes eigae ee seet es ae eeenenee 6

100

At Henham, on the other hand, the proportion of flint-pebbles to
the other constituents is larger. In a pit in the Park, where there
were about 20 feet of shingle, the upper 6 feet consisted of horizontal
layers, while the lower beds exhibited an oblique lamination as good
as that figured by Mr. 8. V. Wood in the Red Crag at Bawdsey
Cliff as typical of current-bedding *.

At Blythburgh and Reydon, the Westleton Beds are seen in the
same relation to the Glacial Beds, and it was ina pit near the
latter place (Quart. Journ. Geol. Soc. vol. xxvii. p. 462), that I
found in a seam of pebbly sand concreted by iron-peroxide numerous
casts and impressions of Mytilus edulis, double, and in all stages of
erowth. The beds generally have, however, been extensively decal-
cified, so that shells are extremely scarce.

At Easton Bavant cliff, the superposition of the Westleton Shingle
on the Chillesford Clay and Sands, both of which latter are here
fossiliferous, is very distinct, while the former exhibits very clearly
the special characters which serve to distinguish it from Glacial
beds.

It is composed as under :—

; Per cent
Te Hlinit-pebbles: \52. se eceiia + om Seeten eennien eras ndaciens ceeieehi nic ieee 2
2, White quartzpeb bles x. asc sence sn eaow eyes ee aor conceive tact he eee 18
5. Subaneular fins |... eeagcescnecievane wo geb re ecceeeecoae centage een eee 20
4, Worn fragments of chert, quartzite pebbles, one large pebble of

indurated clay with indistinct vegetable impressions ...............

Here also I found, as at Reydon, a thin seam of ironstone inter-
calated in the upper part of the Pebble-bed with casts and im-
pressions of Cardiwm (C. edule ?), Mytilus (M. edulis?), Lnttorina,
and Natica.

Since I visited this district it has been described by Mr. Whitaker,
and allowing for changes in the coast-sections caused by the en-
croachment of the sea, our observations are in close agreement. He

* Ann. & Mag. Nat. Hist. for March 1864, p. 3.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 99

also describes the various interpretations * to which these beds
have given rise.

As there is little positive evidence of ice-action during this period,
it is interesting to note the discovery, recorded by Mr. Whitaker
(p. 77), of a wedge-shaped block, 13 x 13x 192 inches, of a mica-
ceous quartzite in the pebbly gravel at Kaston. I noticed in 1869
in a farm-yard near Reydon, a rather large boulder of granite,
which may also have come from these beds.

At Kaston Bavant the Chillesford Clay is well marked with its
characteristic shells; but at the extreme north end of the cliff,
near Covehithe, there are indications of a change. Some trenches
opened at the base of the cliff a few years ago exposed the section
annexed (fig. 2).

Fig. 2.—Sestion in Covehithe Cliff, north of Easton Bavant.

Soda?

feet
UTE SAICUV ROU 2) its. 2te. once cddess-canseccvesedecenscesnecs 2
6. White pebbly sands (Westleton) indenting into ¢ ...... 3
e. Irregular white and yellow sands.............cecessesceeves 4
I ATNAALEE OLOWN CLAY... 2cc0cicsenndsccasecdacswareensiencs 4
Geer ctemilan carbonaceous band. ......-versccedeosseccsenseoces +
f. Laminated grey clay (Chillesford ?)..........sesecsseseeree 6
PeMRUMeNE VOU AMG SAMO 2... seccssestesepeccnsscvecctesee 2
Peemell-bed(CHUvIO-MarING) .......2...100ccaecavecacsovseesovee 2+

Here the Chillesford Clay is unfossiliferous, and is overlain by a
thin seam of carbonaceous matter succeeded by two beds of lami-
nated clays and sands, also without fossils, on which rest the sands
and shingle of the Westleton Beds. The beds ¢ to e may represent
a commencement of the Forest Series, and would thus show its
relation to the Fluvio-marine Crag (gq).

Another point of interest in this section is the presence of small
pockets or indents of sand filling hollows on the top of the laminated
bed c, on which rest the horizontal seams of sand and shingle 0.
The sand in the holes is the same as that of bed 6. Mr. Whitaker
(p. 75 of his Southwold Memoir) has described similar small
contortions in these cliffsT, and Mr. ©. Reid speaks of the

* “Geology of the Suffolk Coast,” Mem. Geol. Surv. 1887, pp. 57-59, 68-72.

+ It was possibly these contortions which led Mr, Wood to refer the sands

and loam in the upper part of the Covehithe cliff to the “ Contorted Glacial
Drift.”
H2

100 PROF. J. PRESTWICH ON THE RELATION OF THE

same structure in the Forest Series at Trimlingham and other
places. He remarks that the carbonaceous clay and overlying
sand are apparently contorted together, and that the contortions
are cut off by the overlying evenly bedded freshwater clays, and
he suggests that this contorted structure may be due either to the
treading of some of the large Mammalia in shallow waters, or else
to the lateral thrust caused by alternate freezing and thawing of the
beds in winter (p. 33).

In one of my note-books, I have the following sketch (fig. 3) of a
similar contortion, but it was there, as at Covehithe and Haston
Bayvant, immediately under the Westleton Beds 6.

Fig. 3.—Section at the base of the CUff near Trimlingham.

feet
a... Boulder-clay i(basecoh)i peeerces eee tee ates andsceeeeeees —_
6. White sand in horizontal layers, with indents in c...... 3
ec. Laminated black clay and white sand ..................0+ 8

May not these small contortions be due to floes of river- or
shore-ice impinging on beds of soft clay? just as at St. Acheul
(Amiens), where there is reason to attribute the contortions (which
are, however, on a larger scale) to the action of the river-ice* at
the high-level period.

Another section exhibiting similar intermediate characters as at
North Bavant, but still without anything definite, was formerly to
be seen in a pit one mile W.S.W. of South Cove Church. It was as
follows :—

feet.
a. Westletom Simple y:f24..sisadicethadsas opectaannee 4to5
b.. Light-colouned sand)5. .) spatiactewesotnegahcpWaraseet castes 4
e. Light-coloured laminated clay .....2..soses<s-sseeee- 3
G. Wark orey’ Clavie. wemctnaagecesene nals naseNavenbeeniec coma 3

The clay was underlain by loam and then (it was said) by Crag
(?). At the Frostenden brick-pit the same dark clay, also without
fossils or pebbles, was worked under the Boulder-clay.

The coast-section resumes again, after a break of 13 mile, at the
south end of Kessingland cliff (fig. 4), but it is often obscured, and
owing to encroachment of the sea varies considerably from time to
time. On the occasion of one of my early visits traces of the
Westleton Shingle were to be seen resting on grey clay and sand,
showing similar contortions to those before noticed at Covehithe and

* Phil. Trans. for 1860, p. 299, and 1864, p. 269.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 101
Easton. The Shingle d is, however, soon replaced by the Middle

Glacial sands and gravel c, which then rest directly on the Forest-
Bed series, and maintain that position as far as Pakefield.

Fig. 4.—Section at the south end of Kessingland Cliff.

Of CEsT@.e NTP Gio NI Bee eee ee 3
Re em ese oe Ne ane vie dis vs niesidndetangiidasscccereedsene 1
é. Irregularly bedded sand and gravel...............sessceses 5
d. Yellow pebbly sands (Westleton) indenting into @...... 4
e. Laminated grey and brown clay and sand ...,,.......... 6

mLhe laminated bed ¢ is without fossils, and resembles bed d of
section, fig. 2. Further north the cliff becomes higher, and the
Upper Chalky Boulder-clay sets in; while at the base of the cliff
there appears a compact greenish clay, with small fragments of flint,
traversed to the depth of from 3 to 5 feet by rootlets, generally cut
off on the top by the Glacial Sands. Between the beds 6 (fig. 5)
and the Pebbly Clay, and forming at one place a shallow depression
about 150 yards across, lies the dark carbonaceous clay with plant-
remains, at the base of which is a thin seam of gravel and sand
with Unio, Cyclas, &c., which I referred in 1871 to the Forest
Series of Norfolk. The Pebbly Clay passes in places southward into
a light-coloured sand, and again into clay, while at other places the
flint-fragments disappear. Nearer Pakefield Mammalian remains
occur in some abundance; but I failed to recognize the exact posi-
tion of these remains, and was under the impression that the pebbly
clay (¢) represented the Chillesford Clay. Fig. 5 (p. 102) is a part
of the section I then gave of this cliff*.

In 1872, Mr. 8. V. Wood remarked that all that could be safely
averred of those beds (the Forest Beds) at Kessingland is, “ that
they are anterior to the Middle Glacial and probably posterior to
the Crag,” an opinion endorsed in his subsequent papers of 1877
and 1880, although in the latter he seems to imply that the Mam-
malian remains are of the age of the Norwich Crag *.

In 1876, Mr. J. Gunn ¢ concluded, on the contrary, that both the
so-called Elephant Bed and the Forest Bed in this cliff were not
only beneath the Chillesford Clay, but also beneath the Norwich

* Quart. Journ. Geol. Soc. vol. xxvii. p. 463.

t+ ‘Supplement to the Crag,’ p. xv; and Quart. Journ. Geol, Soc, vol. xxxiii.
p- 74, and vol. xxxvi. p. 462.

+ Quart. Journ. Geol. Soc. vol. xxxii. p. 128.

102 PROF. J. PRESTWICH ON THE RELATION OF THE

Crag Beds. In the following year Mr. Harmer questioned that
view, and contended that the rootlet-bed does not represent the
Chillesford Clay, but that it forms part of a freshwater deposit
occupying a basin excavated in the Chillesford Clay, and is thus
newer than the latter*. In 1880, Mr. J. H. Blake confirmed the
opinion that these beds represent the Forest Bed of Happisburgh,
and determined the exact position of the Mammalian remains as

Fig. 5.—Section at the base of the Cliff north of Pakefield.

a, (@halky: Boulder-clay (base (Of), > @. 2c. ans.: heaniavseascece otek pee eee =
6. White sands with patches of gravel and fragments of shells (one

Tellina balthica entire), irregularly bedded and ochreous at base 15 to 18
e. Laminated black carbonaceous clay, with branches of wood and a

few small angular fragments or flint 2.2.2: so. cererecseeeeeeeee eee 4
d. Band of freshwater shells ( Unio, Cyclas, & 0.) .......ececeseeeeceeeoeees >
e. Compact greenish clay with fragments of flint, traversed by rootlets

PRCT] NRT OPE Renee hs cel SUR SN RIC RNR DONE SS en 5+

‘‘sometimes forming a distinct and separate bed, one stage more
recent than the Chillesford Clay, and sometimes apparently passing
down into the Chillesford Clay and forming as it were the uppermost
portion of the same,” and, ‘‘ with possibly a few trifling exceptions,
all: the Mammalian remains are to be found buried beneath the
more or less denuded surface of the Rootlet Bed and the Chillesford
Clay” T.

Phe only doubt to be felt is whether in this pebbly clay (e) we
have the Chillesford Clay modified by its approach to land and the
Forest estuary, or whether it belongs altogether to the Forest Series.
It appears from the sections of the north end of Easton Bavant
cliff and at Covehithe (fig. 2) that the laminated beds ¢ and d
overlie a carbonaceous seam ¢é, and these may represent the Forest
Beds, while the dark clay (f) appears to pass southwards without

* Quart. Journ. Geol. Soc. vol. xxxili. p. 184.
t Proc. Norwich Geol. Soc. vol. i. pp. 187-160.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 103

break and on the same horizon into the fossiliferous Chillesford Clay.
At Pakefield we have an expansion of the seam e¢ with rootlets
traversing the clay, and occupying the position of f in the Easton
Bavant section. Is it therefore that in the interval between Cove-
hithe and Pakefield that this ‘ Pebbly Clay’ sets in between d and f,
or is it a continuation, modified by altered conditions, of the bed f?

At Alderby, 6 miles inland, the dark clay, which there overlies
the Fluvio-marine Crag, also contains angular flints, and the late
Mr. Rose had in his collection remains of the Elephant, Deer, and
two species of Cetaceans from this same bed. Though it is not
there overlain by the Westleton Beds, it was found to be so in
a deep well sunk at Beccles on the other side of the valley, and is
therefore generally held to be the Chillesford Clay-bed. There are
again traces of the Forest Bed at the cliff at Corton with an under-
lying clay, of the same character as at Kessingland and with rootlets.

If this Suffolk bed isto be considered the equivalent of the Chil-
lesford Clay, then the so-called Forest Bed of Happisburgh, Bacton,
and Mundesley, which occupies the same position and contains the
same remains, must also be referred to that age; but the peculiar
character of its Mammalian remains—its numerous large Deer,
its special Elephants, and other Mammalia, all so different from
those of the Crag—the absence of Mastodon, which occurs both at
Norwich and at Easton Bavant, together with the evident local
and exceptional character of the Forest Series, renders it difficult
to accept that solution of the problem.

Whatever may be the solution, it does not directly affect the par-
ticular question upon which we are engaged, as the Westleton
Shingle is newer than the Forest Bed, and passes indiscriminately
over it and over the Chillesford Beds. At the same time at the
junction of the two former on the Norfolk coast there is to a certain
extent a passage between them, land-conditions there alternating
with marine during the accumulation of the Westleton Shingle. I
shall therefore only refer incidentally to the Forest Bed, which is
the less necessary as it has often been well and fully described, and
will confine myself to following the range of the Westleton Beds.

The Shingle, which is displaced by the Glacial Sands at Kessing-
land, resumes its place in the neighbourhood of Pakefield and
Lowestoft, where it exists in considerable force, consisting of the
usual pebbles of flint and white quartz, with subangular fragments
of flint, ragstone, and chert, and an unusually large proportion of
other rocks, such as fragments of a mica-schist, of a dark green
quartzose rock, and of yellow, green, and brown sandstones. In
this part of the cliffs clay pebbles are common at the base of the
Westleton Beds, arising probably from the partial destruction either
of the Chillesford Clay or of one of the Forest Beds. Glacial sands
again occupy much of the Corton and Gorleston cliffs. As the broad
estuary of the Yare then intervenes, the Westleton Shingle is not
met with again until we reach the Happisburgh Cliffs; and even
there little is seen of it, although the Forest Bed with its multitude

104 PROF. J. PRESTWICH ON THE RELATION OF THE

of old stumps is often well exposed on the shore at low water: At
Bacton, where the Westleton Beds are distinct, the section is as
under (fig. 6).

Fig. 6.—Section at Bacton Cliff.

feet
ae Sandy and sraveliyisoil Pee se eeu ee ae ee 2
b. Brown Boulder-clay, with a few fragments of shells... 10
c. Light yellow and white sands, contorted on top......... 5
d, Pebbly shingle with a few shells (Westleton) ......... 3
é.. A-tangle om woods (localyme. ura ee eee ae eee 2
j- Laminated erey clay and sands. -e..5)-4). 401 4
g: Hine pravelis. 9... ccssetaseton cee ate se aeeeeeecene aera eee » I+

Mr. Gunn informs me that the Forest Bed has been met with
about 8 feet lower. The shingle d contains * :—

Littorina littorea. Astarte borealis.
rudis. | Mytilus edulis.
Purpura lapillus. | Cardium edule.
Scalaria greenlandica. | Trophon antiquus.

Another feature that I had occasion to observe here during one
of my visits was a singular accumulation of twigs and branches of
trees (Pinus, Abies, Taxus, &c.), forming in one place a loose matted
mass from 2 to 3 feet thick, composed entirely of drifted wood
débris, very little altered except in colour (fig. 6, ¢). Between
Bacton and Mundesley the shingle continues with little interruption,
and consists reughly of :—

Per cent.
Paint WED DLER: «nic on ben <ebtancdian te epmaes Paneer Ge sime ae Aye aan 50
White aud rose-coluured quartz-pebbles.................5665 20
puvancular flints, not stated tli sssuk.stee ne eee ecetreet 16
Subangular fragments of chert and ragstone............... 8
Lydian stone, jasper, quartzite, and sandstone pebbles... 6
100

* This shell-bed was discovered by the Rev. C. Green in 1842.
+ I may have under-estimated here and in some of the other places the pro-
portion of subangular flints.

WESTLEION BEDS TO THOSE OF NORFOLK, ETC. 105

Besides the specimens named above, I also here found specimens
of a black chert (Carboniferous ?), of a light-coloured encrinital
quartz (Carboniferous ?), of chlorite schist, of a white fossiliferous
chert, and of a dark-coloured slaty grit.

It is, however, at Mundesley, 23 miles north of Bacton, that we
find these beds with their typical estuarine and freshwater condi-
tions best exhibited. They there form a group of strata differing
from those further south only inasmuch as they were deposited
under local and different conditions, arising from the early emer-
gence of this area, and the consequent introduction of a land fauna
and flora.

In 1870 I made the mistake of supposing that the thin seam
of gravel at the base of the Westleton Beds (m), and overlying
the Forest Bed, represented the Elephant Bed of the Norfolk
geologists. It is true that a few bones have occasionally been
washed out of the Forest Bed, and are found in the gravel and
sand overlying it; but the bone-bed proper is the underlying argil-
laceous sand in which the forest stumps are rooted, and to which
the term of ‘“ Forest Bed” also applies, for it is in this bed that
the remarkable group of mammalian remains with plant-débris are
entombed. It has been questioned whether the stumps found on
its surface are really im sztu on the spot where the trees grew,
or whether they were drifted there from a distance. Such may
have been the case with some, but it is difficult to conceive that
it could have been so with all. Their wide-spreading roots *,
their position on one and the same level, the presence around
them of their cones and branches, and the fact that the same bed at
other places, where seen in section, is traversed by rootlets evidently
in situ, show that the occurrence of such a forest-growth on the
surface was both possible and probable. Some trees may doubt-
less have been overturned and drifted; and some strained by
storms may have had their roots torn and broken. ‘The argu-
ment that the small fibres which end the roots have generally been
wanting at from one to three feet from the stem, has been dis-
posed of by an observer so experienced on this point as Mr. T. M.
Reade T, who states that in the case even of the more recently sub-
merged forests of the Lancashire coast, the fine fibres of the roots
are not preserved, having generally rotted away. The erect stumps
of the Forest Bed, which I have myself from time to time seen,
though not examined critically, seemed to me generally as good cases
of growth in situ as the trees seen in peat-bogs.

I therefore see no reason to question the previous opinion of a
forest-growth in situ, especially as the existence of a land-surface is
confirmed by the presence in many places on the Forest Bed of a
clay with land-, freshwater-, and marsh-shells and plants. This
land-surface I take as the base on which the Westleton Beds were

* In one case mentioned by Mr. C. Reid, the circle formed by the spread of
the roots was 20 feet across.
t Geol. Mag. dec. ii. vol. x. p. 221 (1883).

106 PROF. J. PRESTWICH ON THE RELATION OF THE

spread. It marks a period of slow submergence, succeeded by the
return at intervals of a very depauperized marine fauna.

The Forest Bed itself is a distinct and local deposit, beneath the
Westleton Shingle ; but whether it forms an intermediate deposit
between the Shingle and the Chillesford Beds, or whether it is
synchronous with, and representative of, the Chillesford Clay, I take
to be a still unsettled problem.

Fig. 7.—Section of Cliff about 4 mile north of Mundesley.

Hidden by Talus. Talus.

Baek At

Subancmlar oravels gisz 2) <:)-nessannsn ance cere ease eaeaate ace 1-2
‘Post-slacial fluviatile bed il. ces se stscde tenes sent eek =
Yellow laminated loam (glacial), blue at base............ 20
a cbinuilder-Clay .cii0.« sis Baer ceaveeagnek sade eee Rees Eee te 12
EVEN ONY AAO 8 a5 noutaaias dues cane eect ee a ae \
GTey.Clay, LAMINA LEG | cars: spaeasnah eaten eee cee tds eee
. Fine pebbly gravel and sand, with Succinca, Cyclas, &e.
: ae aen clay and sand, with drift wood ...............
ight-coloured shelly sands and shingle ..................
ee ate nk Ce ann pe
fabime shingle, with Myfiswiee. nc. .cuaytrawnwakontnvts sve eiy
SLIT), 12a a eR eiMie 7 ''3 5:0. 52, ares ameiin eter ca Press 2
m. Gravelly bed, with mammalian remains, resting on
dark sandy clay (Forest Bed) |. cases. .uc-cscassacacrune }

On either side of this section of the Mundesley series (¢ to m) very variable
beds are hidden by talus. The position of the Forest Bed is also shown beneath
the beach on the left hand.

MoS. s- exQ%, 9 AS SS

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 107

It is on this part of the coast that the Forest Bed attains its
greatest development. Mr. Gunn had a bore-hole driven into it at
Happisburgh to a depth of 12 feet without reaching its base; while
Mr. C. Reid, from observations made by dredging beyond low water-
mark, concludes that its thickness is not less than 60 feet *. What
may form the base of the Forest Series is at present a matter of
conjecture. From the presence of drifted peat and plant-remains
at its outcrop near Cromer, Mr. Reid infers the presence of another
freshwater bed, beneath the main bed, and below that he places the
Weybourn Crag.

The flora of the Forest Series has been admirably worked out by
Mr. C. Reid and Mr. Carruthers, and the fauna by the late
Dr. Hugh Falconer +, Professor Boyd Dawkins§, and Mr. E. T,
Newton ||. I need not further allude to them here, except to
mention their extreme interest and importance.

The relation of the Westleton Beds to the Glacial Series above
and to the Forest Beds beneath is extremely well shown on the
coast at Mundesley, although it is only occasionally that the tree-
stumps can be seen. Mr. Dix informed me that on the south side of
Mundesley the greenish sandy clay of the Forest Bed crops out
beneath the beach. Bones and teeth have often been dug out of it,
and shortly before my last visit he had seen at low water the large
erect stump of a tree, with, he said, all its roots branching from it.
On another occasion, at very low water, a number of tree-stumps were
seen with a mass of clotted leaves and branches. The best general
section is that presented by the cliff on the north of the village (fig. 7).

Little of the Forest Bed is seen in this section, but in the gravel-
bed (m) are occasionally found a few bones washed out of it. To
this succeeds in places a grey clay, which to the south of Mundesley
contains numerous freshwater shells, above which is a gravelly clay
with Mytilus and Succinea. The sand and shingle 7 contain marine
shells and fragments of wood. In bed h drifted wood occurs, while
in the sand and fine shingle (g) freshwater shells are common. In
the overlying laminated clay (f) are some wood and plant- remains.
This section differs a little from those of Mr. Reid, owing to the
variability of the beds, there having been an interval probably of
some 20 years between our observations. The following is a list
of the marine shells obtained from bed /: :—

Cardium edule, Z. Littorina littorea, Z.

Mytilus edulis, Z. —— rudis, Mat.

Pholas crispata, L. Purpura lapillus, Z.

Balanus, sp. Scalaria groenlandica, Chemn.,

* Tt would be very desirable to have a deep boring made at Happisburgh or
Mundesley.
+ ‘Geology of the country around Cromer,’ p. 62 (1882). See also a paper by
Mr. Reid in the ‘ Annals of Botany,’ vol. ii. p. 178 (1888).
t ‘ Paleontological Memoirs,’ vol. ii. chapter ii. and pp. 476-480.
Quart. Journ. Geol. Soe. vol. Xxxvi. p. 395, and other papers,
|| Geol. Mag. dee. ii. vols, vii, & viii., and Survey Memoir.

108 PROF. J. PRESTWICH ON THE RELATION OF THE

The freshwater shells in beds 2 to & consist of :—

Anodonta cygnea, L. Bythinia tentaculata, L.
Pisidium amnicum, Mil. Paludina gibba, Sandb. ?
Spherium corneum, L. Valvata piscinalis, Midd.

rivicola, Lea.

Bed g contains fewer species ; the chief are :-—

Planorbis complanatus, L, Succinea putris, L.
Spherium corneum, L. oblonga, Drap.

Beds e and frepresent Mr. Reid’s Arctic freshwater beds, in which
he has found, in places, Saliw polaris, Betula nana, and Hippuris
vulgaris, with remains of Spermophilus; while bed 2 is on the
horizon of his Leda-myalis bed*. The lower beds would, I presume,
be included by Mr. Reid in his Upper Freshwater and Forest-Bed
division. The relation to the lower and the Weybourn beds cannot
be seen in this part of the coast-section.

The divisions of the strata under the Cromer Till (Lower
Boulder-clay) on the Norfolk coast, according to Mr. C. Reid,
are :— |

Older Pleistocene { Cromer Till.
(Glacial) pew Freshwater Beds.

( Leda-myatis Bed.
| Upper Freshwater Bed.

Newer Pliocene < ‘‘ Forest-Bed”’ Series. | “ Horest Bed” (Hstuarine).
| Lower Freshwater Bed.
\ Weybourn Crag.

Chillesford Clay?

The minor subdivisions are subject to considerable variations, and
are of very restricted range, depending upon local conditions. It
seems to me that all the beds e¢ to m (fig. 7) are members of one
series, and | have therefore grouped all down to the Forest Bed under
the one term of “‘ Mundesley Beds”; and as I take these beds to be
on the same horizon and synchronous with the marine Westleton
Beds of Suffolk, the term “‘ Westleton and Mundesley Beds” t+ will
serve to indicate the two types.

Mr. Reid considers that these terms t can scarcely be adopted,
because the shingle “at Westleton is now believed to belong to
the Glacial Beds, and, at Mundesley, beds deposited under quite
different conditions, and showing marked changes of climate, are
included.” It is quite true that the beds show somewhat different
conditions, but that arises solely from the emergence of this area,
and the introduction of a land-and marsh-fauna and flora oscillating
with a marine fauna as the sea from time to time encroached §.

With respect to the climate, I do not see that the fossils indicate
anything more than the continuance of that lowering of temperature
which set in with the Crag beds. As the cold increased, many

* Op. cit. pp. 37, 48, 83.

t Report British Association, 1881. + Op. ttt. p. 9.

§ Dr. Sandberger came independently to the same conclusion from an exami-
nation of the fossils.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 109

old forms gradually disappeared, the more northern and arctic
forms alone surviving, until in the terminal ‘“‘ Arctic Freshwater
Beds” both flora and fauna are such as show a climate fitly in
accordance with the now near approach of the great ice-sheet.

The sea was probably too shallow to admit of the floating of
large bergs with their massive boulders, yet we are not without
evidence of ice-transport and ice-action on a small scale.

Large unworn and unbroken flints and smaller subangular ones
are Dot uncommon. Small blocks of foreign rocks are, as before
mentioned, occasionally met with, and Mr. H. B. Woodward records
the occurrence in Norfolk of a block of basalt, about 18 inches
square, in the Pebbly Sands near Aylsham *, all pointing to trans-
port by ice.

The Forest Bed, with its trees and mammalian remains, may
thence be traced northward as far as Cromer, but it finally dis-
appears about one mile N.W. of that place, where the Upper
Freshwater Bed and the basement beds of the underlying Forest-Bed
series come into contact. Mr. C. Reid states that it is only at this
point and at Trimlingham that his Lower Freshwater Bed at the
base of the Forest Series is exposed. I cannot, however, agree with
him in his interpretation of the Trimlingham section. I take
the upper beds, nos. 2 to 4 of his section (p. 33), to be the base of
the Mundesley series, nos. 5, 6, and 7 the Forest Bed, and no. 8 the
Norwich Crag.

Another point at issue is whether the Weybourn Crag of Mr. Reid,
considered by him to form part of his Forest Series, should be thus
grouped, or whether it represents the Norwich Crag.

At the south end of the Forest-basin no marine bed underlies the
Forest Series+ until at a short distance beyond Kessingland the
Chillesford Sands (Norwich Crag) setin. In the centre of the Basin
at Happisburgh and Mundesley, nothing is known of the lower beds
under the Forest Bed of Mr. Reid. As we proceed northward,
owing to the thinning out of this latter bed, the base of the Mun-
desley Series with its pebble-bed (m) and derived bones comes, as
pefore mentioned, into contact with the lower part of the Forest-
Bed series. |

But the sections are mostly obscure, and it is not until we reach
the West-Runton Gap (fig. 8) that the upper part of the series
is seen clearly as at Mundesley, and the special character of the
Westleton Shingle is again well marked. It here consists approxi-
mately of :—

Per cent.

BUint= Pebbles <iwasvinscssnd voesye ce Weadens 7

White quartz-pebbles ..............606. 20

Subangular flints .........ceseeeseceeeees 15

Chert and ragstome ........sce-seseeeens 10
Lydian stone and quartzite, and light-

coloured sandstone-pebbles ......... 8

100

* Mr. Reid’s Memoir, p. 53.
+ Except a doubtful specimen of Buccinwm undatum at Pakefield.

110 PROF. J. PRESTWICH ON THE RELATION OF THE

Besides these constant constituents, I found in this shingle, which
is sometimes concreted by iron-peroxide, some large subangular’
fragments of a fine-grained granite and mica-slate; and Mr. Reid
mentions the occurrence of “a boulder of greyish granite measuring
2x12 feet among the clay pebbles and bones,” at the base of the
Series, a short distance eastward of Runton Gap (p. 28).

Fig. 8.—Section at West-Runton (or Woman-Hythe) Gap.

G4 SUVAU SUIT STAVE card. dete deco cas <was ds acapeote sion aeeeee 8
b. ‘Chalk-mualbbley cme sereasen-ccee-t seuces otek snes a eee 5
c. Sand and gravel, with patches of broken shells ......... 6
d. Boulder-clay ....... Be ieleaa hsieetsloateia Clee peels eee ete 15
2: Samid, amd ItOnStOmM Sy é xia cm< Secs acs eatetaeepate nists ee tata teem 2
Fe Mbieht-coloumed: sami). 6 ceaacesrmadaneniny «sedaesn torneaae 6
g. Loamy sands, very variable, with a few shellsin position 3
h, Shingle, with shells mostly in fragments............ saconcdieeee
q, Hine sand, ‘variable <:...wke eke SU ee L ee
j. Peaty bed, with freshwater shells .................+ sictclaeteaced whee

The position of the Crag bed described by Mr. Reid is shown in faint outline
below the base line on the left: g is not carried far enough.

The section at the Gap (fig. 8) does not show the beds down to the
Chalk, but this is shown by the sections in faint lines which are
given beneath.

This brings us to the moot point concerning the age and relation
of the so-called Weybourn Crag to the other Crags. According to
Mr. 8. V. Wood it is synchronous with the Bure-Valley Crag or the
Pebbly Beds, and therefore newer than the Forest-Bed Series ; whereas
Mr. Reid places it at the base of, and consequently as older than,
that Series, although still newer than the Norwich Crag. Mr. H. B.

WESTLETON BEDS T0 THOSE OF NORFOLK, ETC. tre

Woodward also places it in the same division as the Bure-Valley
Crag.

Although the Forest-Bed Series thins off to the north, the fresh-
water bed at the base of the Mundesley Series is prolonged, and
forms a definite zone whereby the relative position of the associated
strata can be fixed. These beds are in general thin, and the fossils
few and badly preserved, but at one spot, a short distance east of
Runton Gap, Mr. Reid found beneath them a bed of Crag abounding
in well-preserved shells (fig. 8). The section he gives as under :—

feet.
Laminated clay full of lignite, small twigs
Pe %» and occasional fir-cones, and fragments of
Forest-bed. HULSE OEE a ME Ae oP SUE ee eae Bae ?
Mass of rolled clay-pebbles on uneven surface. ?
(Grey shelly Crag, in the lower part altern-
Patines rrt tie LOANS ..!.....00c.cseressecunares about 4

Weybourn Crag.< Bed of unworn flints mixed with clay, and
containing Mya arenaria and Tellina obliqua
Pe POSMIGM OL WC <2)... ccnesconsenasecncndee about 44
Soft chalk with Paramoudras and rings of flint.

His list of the Mollusca is the most reliable one we have for the
Weybourn Crag, for at this spot it is free from any possible inter-
mixture with the Pebbly Beds * :—

Lamellibranchiata. Gasteropoda.
Astarte borealis, Chemn, Buceinum undatum, Lz.
, oval var. Bulla alba, Brown.
—— compressa, Mont. Cancellaria viridula, Fabr.
incrassata, Brocchi. Chiton, sp,
— crebricostata, Forbes. Hydrobia (Paludestrina) subumbili-
suleata, Da Costa. cata, Mont.
Cardium echinatum, Linn. Littorina littorea, Linn.
edule, Linn. rudis, Maton.
grenlandicum, Chemn. Melampus (Conovolus) pyramidalis,
Corbula contracta ?, Say. J. Shy.
striata, W. & B. Natica catena, Da Costa.
Cyprina islandica, Linn. -—— clausa, Brod. § Shy.
Donax vittatus, Da Costa. helicoides, Johnst.
Leda oblongoides, S. Wood. Pleurotoma (Clavatula) linearis, Mont,
Lucina borealis, Linn. turricula, Mont.
Mactra ovalis, J. Shy. Purpura lapillus, Linn.
stultorum, Linn. Scalaria groenlandica, Chem.

Trevelyana, Leach.

Mya arenaria, Linn.
Turtonis, Zurt.

truncata, Linn.

Mytilus edulis, Linn. Tectura virginea, Mii//.
Nucula Cobboldizx, Sby. Trochus tumidus ?, Mont.
Pecten opercularis ?, Linn. , Sp.
Pholas crispata, Linn. Trophon antiquus, Linn,
Saxicava arctica, Linn. , reversed var.
, gigantic var, Turritella terebra, Mont. (=communis,
Scrobicularia plana, Da Costa. Risso).
Tellina balthica, Linn. Velutina levigata, Linn.

] Gmelin (T. calearia). :
pees eas Ge eat 4 Brachiopoda.

preetenuis, Leathes. Rhynchonella psittacea, Chemn.
EA SSR RNe On eke a ee eee eee NORV e re cove NnnnrEne ee Senn

* Mem. Geol Survey, p. 18.

112 PROF. J. PRESTWICH ON THE RELATION OF THE

As the upper part of this section belongs to the base of the
Mundesley Series or else to the Forest-Bed Series, this Crag (in the
absence of the Chillesford Clay, which may have been denuded, or
may be represented by the mass of clay pebbles) occupies the
position of the Fluvio-marine Crag of Norwich, while there is
nothing to show relation to the Forest-Bed Series. ‘The presence
of the pebbles and the eroded surface show, on the contrary, a
decided break between this Crag and the overlying beds. For
these reasons, and also because all the 51 species in this list,
are, with two exceptions, Crag species, I would assign this bed to
the Norwich Crag. One exception is Tellina balthica, which hag
been found on this north-eastern coast only in the Crag Beds of the
Bure Valley ; the other Astarte crebricostata, which is only recorded
from the Upper Glacial Beds. Besides these, there are found here
two shells—Cardium echinatum and <Astarte incrassata—which are
Red-Crag species. On the other hand, of the 36 species recorded by
Mr. H. B. Woodward from the Bure-Valley Beds, only 23 appear in
the above list.

Mr. Reid, on the assumption that this Crag is the equivalent of
the Bure-Valley Crag *, considers that Messrs. Wood and Harmer
are wrong in placing the latter above the Forest Bed; but if I am
right in referring this patch of Crag to the Norwich Crag, then the
shingle h (fig. 8) above the lower part of the ‘‘ Forest Bed” would
correctly represent, as supposed by Messrs. Wood and Harmer,
the Bure-Valley Beds.

It is evident that the paleontological differences are very
small. The only marine Bure-Valley shell not found in the Crag
at Norwich is Yellina balthica. But this shell is extremely uncer-
tain in its habitat, and a slight difference in the quality of the
water or of the bottom might account for its presence in the one
district and its absence in the other. Dr. Gwyn Jefireys informed
me that at the present day it is abundant in Swansea Bay, although
it is not to be found nine miles distant in Oxwich Bay. It prefers
brackish waters, and ‘“‘ though in the main a northern shell, it is
likewise common in many parts of the south of Kurope.” It is clear
likewise that this Runton Crag presents far closer analogies with
the more distant Crag at Norwich than with the Bure-Valley
Crag in the intermediate area.

Between Runton and Weybourn, where the Forest Series entirely
thins out, or few traces of it remain, the overlying Pebbly Beds
come inte juxtaposition with the Fluvio-marine Crag beneath that
Series. The slight paleontological and lithological differences are
then not sufficient to furnish any apparent distinction, except possibly
in places where the Westleton shingle retains its more pronounced
characters. ‘The true faunal value of these zones can only be cor-
rectly determined by selecting localities, such as the one above, where
they cannot possibly be in contact.

* Mr. Reid, however, suggests the possibility that the Weybourn Crag, as a
whole, is the equivalent of the Chillesford and Aldeby Beds.

WESTLEION BEDS TO THOSE OF NORFOLK, ETC. 11s

§ 5. Conclusion.

The plan I have therefore adopted has been to confine myself
to those localities where, owing to the Chillesford Clay or Forest
Beds intervening, there is no possibility of the Westleton Shingle
having come in contact with the Norwich Crag. For this purpose I
have limited the list of the marine Molluscan fauna of the Westleton
and Mundesley beds (see p.115) to the species found at Reydon, Easton
Bavant, Bacton, Mundesley, and West Runton (the last two being in
the Leda-myalis Bed of Reid). This gives a list of only 19 species,
all living, excepting possibly two, about which the most competent
authorities differ. T'ellina obliqua was considered by Sowerby and
Searles Wood to be an extinct species, whereas by Forbes and Hanley
and Gwyn Jeffreys it was considered to be a variety of 7’. lata, a living
northern species; according to Jeffreys Nucula Cobboldie is now repre-
sented in the seas of Japan by a variety of the same species ; whilst
Searles Wood considered that they are distinct and that the Crag
species is an extinct form. With two exceptions all the others are
existing British species, although on the whole they are of northern
types—10 ranging to Scandinavia and 9 to the Arctic seas: Astarte
borealis is Scandinavian and Arctic only. The elimination of the
more southern types seems to constitute the distinctive feature of
this fauna.

The land- and freshwater Mollusca, of which there are 53 species,
are from the freshwater beds (q to m, fig. 7) of the Mundesley
series—the Upper Freshwater and Leda-myalis Beds of Mr. Reid.
They are, with three questionable exceptions, all living species.
All the others except four are species still living in Britain, but
having a very ubiquitous range from north to south. Of the four
latter, Valvata fluviatilis is now living in Belgium and Germany ;
Hydrobia Steinit in the north of Europe; H. marginata in the
South of France; while Corbicula fluminalis ranges from Thibet to
the Nile. The three extinct species include a slug (Limaa modio-
hformis) ; Paludina gibba, formerly referred to P. contecta, a British
and Finnish species* ; and Hydrobia runtoniana: they are found
fossil also in North Germany.

The freshwater bed (7) at West Runton is rich in Fish-remains.
There are 10 species, all still living in the rivers of this country.

The Reptiles (2) and Amphibia (4), found in the same bed are
also living British species.

Of the 21 species of Mammalia, 6 are extinct; and it is to be
remarked that out of the total number there are 14 which are
not met with in the Forest Bed and make their first appearance in
this stage, and it is the same with all the Reptiles and Amphibians.

The 24 Plants are of special interest from the rarity of plant-
remains in such deposits. ‘They are all living species,—19 still
living in this country, 5 being now relegated to more northern lati-
tudes, and, as in the case of the Mammalia, a large proportion (14)
are confined to the Mundesley freshwater beds, though this may

* P. glacialis and P. media are doubtful, and thought by Mr. Reid to be
derived.

Wee. G. bs No. 181. I

114 PROF. J. PRESTWICH ON THE RELATION OF THE

possibly be due to the circumstance that they consist in large part
of small seeds which may have escaped notice or been destroyed
from haying been lodged in a matrix not so favourable for their
preservation as the other bed.

- In conclusion, if 1 am right in my interpretation of these intricate
sections, the Crag of the Weybourn Cliffs has no standing per se, but
results from the junction of the Bure-Valley and Norwich Beds;
‘while with respect to the Bure-Valley Crag, as at present
held, I cannot but think it open to the same doubt, although I believe
-in the existence of an upper division with marine shells, newer than
the Norwich Crag, but having a much more limited fauna,

The construction I would therefore put upon the Pre-Glacial .
strata underlying the Boulder-clay Series on the coast of Norfolk is
as under :—

(1. Laminated clays, sands, and shingle with plant-
| remains and freshwater shells (The Arctic
Freshwater Bed of Reid).

THe Westieton anp | 2. Sand and quartzose shingle with marine shells
Munpustey Beps. (The (The Leda-myalis Bed of King and Reid),
Mundesley type.) | 3. Carbonaceous clays and sands, with flint-gravel

| and pebbles of clay, driftwood, land- and lacus-
' trine shells and seeds. (Zhe Upper Freshwater
\ Bed of Reid.)
(4. A greenish clay, sandy and laminated in places,
| containing abundant Mammalian remains and
| driftwood, with stumps of trees standing on
its surface. (The Forest- and Elephant-bed of
authors. The Estuarine division of Reid.)
5. Ferruginous clay, peat with land’and freshwater
remains, and gravel. (The Lower . Freshwater
\ Bed of Reid.) |

The marine fauna of the ‘‘ Mundesley and Westleton Beds” is
very limited and often fails us. On the other hand there is a
structural feature singularly persistent, that is, the presence through-
out, from Southwold to Bacton, Mundesley, Runton, and Weybourn,
of a shingle everywhere of the same character. The intercalated clay
and peaty beds, with their land and freshwater remains, are subor-
dinate, and confined to the east coast of Norfolk. .

Although allied to the Norwich Crag by their marine fauna,
and conformable with it in places, the Westleton and Mundesley
beds constitute on the whole a distinct and separate group
formed under changed physiographical conditions,—conditions that
led to their extension far beyond the Crag area ; while, as I shall

|
Tue Forgst-Bep Grour * {

* The fauna and flora of these beds are of peculiar interest, and have for
years past been the object of active research on the part of many geologists.
Large collections of the remarkable Mammalian remains have been made by
Miss Anna Gurney, Mr. J. Gunn, and Mr. R. Fitch, and are now in large part
preserved in the Norwich Museum. ‘The later careful researches of Mr. C. Reid
have made great additions to the smaller life and vegetable forms. (For details
and lists, see Mr. C. Reid’s Cromer Memoir before cited, and Mr. John Gunn’s
‘Sketch of the Geology of Norfolk.’)

+ We have evidence, however, of a similar southern drift in the presence
of chert from the Lower Greensand, and quartz, quartzites, and other such
specimens either from the Ardennes or the: Rhenish Provinces, at the base of
the Red Crag, and somewhat similar indications at the base of the Coralline
Crag.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 115

hope to show in the second part of this paper, they are separated
from the deposits of the Glacial Period by further and equally im-
portant physiographical changes. In one case we have currents
and drifts from the south and east; in the other, northern drifts
solely. The importance of these features will be seen when we
come to questions connected with the relative age of the drifts in
the London Basin, especially as I take this Westleton Shingle as the
base of the Quaternary Series, and as marking the time when the
existing forms of life, both animal and vegetable, began to predomi-
nate in this country.

Lists of the Organic Remains of the Westleton and Mundesley
Beds of Norfolk, compiled in greater part from the lists of
Mr. Clement Reid’s Memoir on Cromer, but grouped in accord-
ance with the stratigraphical order proposed in the foregoing

pages.
PLANTA.
Cryptogams.

. Chara, sp. ;
Hypnum turgescens, Jes. ........-.ceceeees Moss. (Northern regions.)
Equisetum, sp.

Osmunda regalis, Linn. .............ec cence Fern-royal.
Gymnosperms.
Piusisylvestris, [77 we... tees Scotch Fir.
Me wos cane ct nee ec se tse cunnees Spruce Fir.
ame paccata, Lan ce cele Yew.
Monocotyledons.
Carex & Cyperus, sp. (several) ............ Sedges.
WUE Mec iag sc aicp ce vps eve cs usesasinaases Rush.
Potamogeton flabellatus, Bab. ............
heterophyllus, Schreb..............2.66 Pond-weeds.
trichoides, Cham. ....0.0.0.0000.0.0...
Zannichellia palustris, Linn. ............... Horned Pond-weed.
Dicotyledons.
MME PLUMOSA, L712. ...1..ceccccecsssececses Alder.
So bl) Dwarf Birch.
Ceratophyllum demersum, Linn. ......... Hornwort.
Corylus ayellana, Lim. ..........00.2cse0e0s Hazel.
Hippuris vulgaris, Linn. .............08.6 Mare’s-tail.
Menyanthes trifoliata, Linn. ............... Bog-bean.
MPPIGAV INUIT, SDs xn. aasecnenecsacasscscneees Water Milfoil.
Prunus communis, Huds. ...........icees-- Sloe.
Ranunculus aquatilis, Linn. .............+5 Water Crowfoot.
NE eri cdiidin wabicicurs hats cis ays veccee Buttercup ?
Rumex maritimus, Linn...........cc.0.200003 Golden Dock.
RE DOIATIS, VGMID. oo. esecnnrccrevesssusess Polar Willow.
Thalictrum flexuosum?, Bernh. ........- Meadow Rue.
SEPM TIAGANS, LAM, © cocasccccrcencesecserses Water Chesnut. (Central Europe.)
NMI Vex fab ew arc dc User este sexe =s© Clover ?
InsECTA.
Donacia sericea, Linn. Timarcha ?, sp.

Notiophilus aquaticus, Linn.

116 PROF, J. PRESTWICH ON THE RELATION OF THE

CypprispBrowienay? )...ccctsessss.crth os

Candona candida, Miill.

Gasteropoda,

Buccinum undatum, Linn.
Littorina littorea, Linn.
rudis, Maton.

Natica catena, Da Costa.
Purpura lapillus, Linn.
Scalaria groenlandica, Chemn.
Trophon antiquus, Linn.

, var. contrarius.

ENTOMOSTRACA.

( Extinct.)

Mo.uvsca.

Marine.

Lamellibranchiata.

Astarte borealis, Chemn.
Cardium edule, Linn.
Cyprina islandica, Linn.
Leda myalis, Couth.
Mya truncata, Linn.
arenaria, Linn. ?
Nucula Cobboldiz, Sdy. ?
Ostrea edulis, Linn.
Pholas crispata, Linn.
Saxicava arctica, Jinn.
Tellina balthica, Linn.
obliqua, Sby. ?

Land and Freshwater.

Lamellibranchiata.

Anodonta cygnea, Linn.

, var. anatina.
Corbicula fluminalis, Mz//.
Pisidium amnicum *, Mil.
(casertanum), Poli.
— pusillum, Gmel.
nitidum, Jenyns.
roseum, Scholtz.

Ancylus lacustris, Linn.
Bythinia tentaculata, Linn.
Leachii, Sheps.
Carychium minimum, Will.
Clausilia, sp. ?

Helix arbustorum, Linn.
nemoralis, Linn.
hispida, Linn.
concinna, Jeffr.

fulva, Mil.
pulchella, Miil/.
pygmeza, Drap.
Hydrobia marginata, Mich.
Steinii, v. Martens.
runtoniana, Sandb.
Limax Sowerbyi, Fér.
modioliformis, Sandb.

Limnea limosa (peregra), Linn.

stagnalis, Linn.
palustris, M/il/.
truncatula, Mill.

Pisidium Henslowianum, Shep.
pulchellum, Jenyns.
Sphzrium corneum, Linn.
rivicola, Leach.

ovalis, ér.

Unio pictorum, Linn.

Gasteropoda.

Paludina gibba, Sandb.t
Physa fontinalis, Linn,
Planorbis corneus, Linn.
albus, Mill.

crista, Linn.
carinatus, Mill.
complanatus, Linn.
vortex, Linn.
spirorbis, Linn.
contortus, Linn.
nitidus, Mill.
Pupa marginata, Drap.
Succinea putris, Linn.
oblonga, Drap.
Valvata fluviatilis, Codd.
piscinalis, Mil.

, Var. antiqua.
cristata, Mill.
Vertigo antivertigo, Drap.
Vitrina pellucida, Mild.
Zua lubrica, Mii/l.

——_—_

* Pisidium astartoides, being generally considered a variety of P. amnicum, is
omitted, though Mr. C. Reid shows some reason for its being a distinct species.

+ This is Dr. Sandberger’s species, determined from specimens sent by Mr.
Reid.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 117

VERTEBRATA.
Pisces.

PRISRIPPUOVINIATIS 2 1 o.002 on cjceis once venceeere Ruff.
PIERS ac ee sccbs<escceccencenesacess Sturgeon.
ADPaMIS DRAMA, [1270......0cccacccersscoeees Bream.
Barbus vulgaris, lem. ..............-.0000 Barbel.
Leuciscus erythrophthalmus, Linn. ...... Rudd.

BUI PETIT. sinew cm rnerre cern deisione es ow ones Roach.

S700 TT re Chub.
Perca fluviatilis, Linn. ......... ih eae Perch.
PRC VU ATIG, CWO <0. coc. 0csccewcoseeceves Tench.
PGR EME LM nick. scdde sacs he veiees Pike.

Amphibia.
Lo. Q)u.chho hen se tet aae Aino: ae Toad.
30) GEV: 12) ee Edible Frog.
See TP OEAIID Dciaretaa ts «ie sees ewe nats an ete Common Frog.
PIO GPU ACU ye aed vn ence nee sdsd oneso'e Common Water-Newt.
Reptilia.
eT UAIIGU Seo. c Saf 2 i acasc send eapenesisvasdes Viper.
PITTI GMOS ACTIX | oso... coc yeeesce sees Common Snake.
Aves.
EEL telat vie eet vie ans avceeervorine Duck
Mammalia.

Arvicola amphibius, Linn. ? ............... Water-Vole.

BEMIS EL QNUS) cies casseccccieceecedeess Vole. (Central Europe. Extinct in

Britain.)

plareolts, Sched. 0.<...00..iiervecvacnss Bank-Vole.

intermedius, Newton ...........sceeees Extinct.

PRGA, CE GUAS \aneveessucnarsacnasecss Vole. (Central Europe. Extinct in

Britain.)

Danis Vilpes, Li. 2 vice diescsccsnieeves Fox.
Castor europzeus, OW. ..........csceceeeeeeees Beaver.
Cervus Sedgwickii, Walconer ............... ( Extinct.)

WOEUGCORWIS, DQWHUIS. ..ccsrecnreareeres (Extinct.)
Equus caballus-fossilis, Riitim. ............ Horse.
Martes sylvatica, Linn. .....cceccecsceeeeees Marten.
Misi sylvatious, 20700.) 5.0.0... ..cccdedveaderss Long-tailed Field-mouse.
Myogale moschata, Lint...............csc000e Shrew, var. (Russia.)
Rhinoceros etruscus, Falconer .........44 Rhinoceros. (Extinct.)
BOMrUs VUlEATIS, L007. 7 ...cccsserscsenrecens Squirrel.
Sorex vulgaris, Linn. .....ccceccssceceveseees Common Shrew.

PYSMBUS Pallas? coi. ddcscicoesye eden Lesser Shrew.
MSRM N HUNG SP. shih eveiddecerisewsvedseseves Marmot,
Talpa europsea, LINN, .occ.ssscscesenesceceees Mole.
Trogontherium Cuvieri ..........s.s.csesees Gigantic Beaver. (Extinct.)

Misia’ HSleeus) Biwi. oo... cscscecsenvetceees Cave-Bear. (Extinct.)

118 PROF. J. PRESTWICH ON THE RELATION OF THE

Discussion.

The CHarrMAN remarked on the importance of the problem of
the correlation of the East Anglian Drifts with those of the Thames
basin, and of the especial qualifications of the Author of the paper
for dealing with this great question.

Mr, Crement Rerp noticed that the Author went further than he
had previously done in accepting recent results. With regard to
the correlation of the beds on the northern coast of Norfolk with
those of Westleton, he thought it most dangerous to take the unfos-
siliferous beds of the latter place as a type. On the Norfolk coast
the Weybourn Crag was classed by himself with the Forest Bed
as a matter of convenience. Its fauna was sufficiently marked
to show that it was slightly newer than the Norwich Crag. It
always contained Tellina balthica, whilst that shell had never
been found in the Norwich Crag. The fauna was also slightly
more Arctic than that of the Norwich and Chillesford Crags.
The beds which the Author bracketed as the Forest Bed, did not
include the Upper freshwater bed. He gave reasons for his having
himself included it with the Forest-Bed series. As to classing
the Arctic freshwater bed with the Upper freshwater bed, he noted
that the floras showed a difference of climate of 20°, and he con-
sidered the grouping together of the two unadvisable. He thought
it unsafe to use the term Westleton Beds until some definite fauna
was found at Westleton. If any definite name for the whole series
was used, Mr. 8. V. Wood’s old term “ Bure-Valley Beds” should be
adopted. ; |

Mr. H. B. Woopwarp believed that, for purposes of correlation, the
terms Norwich-Crag Series, Forest-Bed, and Glacial Series should be
used, while minor subdivisions, such as Bure- Valley Beds, Chillesford
Beds, and Westleton Beds, might, with advantage, be dropped. He
had himself come to the conclusion that the Westleton Beds were in
the Glacial series. He agreed with the Author that the Weybourn
Crag was Norwich Crag, for he placed it on the same horizon as
the Bure-Valley Beds. Unfortunately beds which belong to a
horizon higher than the Forest Bed had also been included with the
Bure-Valley Beds by Mr. 8. V. Wood. The name Mundesley Beds
was a useful local term for these higher beds; but if the term
Westleton Beds was associated with them, it might turn out in the
end that there were no ‘‘ Westleton Beds” at Westleton.

Mr. J. A. Brown had obtained a stone apparently worked by
human agency from the Weybourn Crag of Runton Gap. He had
also found a black flake at Westrand in peat.

Mr. Tortey remarked on the indebtedness of the Society to Prof.
Prestwich for his many years’ labour on this ground. The Survey
had now agreed not to mark by any definite name these beds under
dispute. Whatever classification might eventually be. adopted, the
lines on the Geological Map marked actual lithological differences.
He would deprecate the re-introduction of the term Bure-Valley
Beds.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 119

The Avrnor, in reply, stated that whilst Mr. Wood was working
from north to south, he himself had worked from south to north.
He had come to the conclusion that the beds, as he understood
them, were distinct, both as regards their association and classi-
fication, from those which Mr. Wood had described as the Bure-
Valley Beds. Tellina balthica is very irregularly distributed at
the present day, and has a wide southern range. When the
Chillesford Clay is absent, confusion arises from intermixture of
Norwich-Crag and Westleton forms, whence the modified fauna
known as the Weybourn Crag. Some of the fossils of the upper-
most beds of his Forest-Bed series may also have been washed into
the Mundesley or Westleton Beds. It is difficult to show that
the Forest series is different from the Chillesford Beds; though his
impression was that itis different and newer. The subordinate Arctic
Freshwater Bed is of small dimensions and shows the setting in of
cold, which we should expect as introductory to glacial conditions.

QiJd. GS. No. 182; K

120 PROF. J. PRESTWICH ON THE RELATION OF THE

9. On the Revarion of the Wustteton Bzps, ov Prssiy Sanps of
SUFFOLK, to those of Norroix, and on their Extension INtAnp ;
with some OBSERVATIONS on the PErtop of the Finan Etnva-
tion and Denupation of the Wratp and of the THames
‘Vatiey, dc. By JosrpH Przestwicu, M.A., D.C.L., F.R.S.,
F.G.8., &e. (Read December 18, 1889.)

PARA ae
[Puate VII. ; see also the Map in Part ITI.]
Page
1. Classificatory Objects and Historical Summary .........s02..sceececeeeees 120

2. Range inland of the Westleton Beds north of the Thames: Suffolk
(p. 124) ; Essex (p. 128); Middlesex (p. 136); Hertfordshire (p. 137);
South Buckinghamshire (p. 159); South Oxfordshire (p. 140); Berk-

shires. WAM): 5 - a2 hag Sie-eeme = St cemeentiescec oe eaeees ia cae eee 124
3. Westleton Beds on the South of the Thames: Kent; Surrey and

MVATTNPSINIEE: 1. Soio.s ose sare bate 3's nie ewpipeop ee taecieui- taste ad ee seep eee eee 145
4. Possible extension of the Westleton Shingle beyond the Thames Basin

unto: Wiiltshivevamd ‘Somerset (0 igis..sc.snae ee baw cnttebes<8. acl eee 143
5. Relation of the Westleton Shingle to the Glacial Drifts of the Thames

IVAN CYS eivci nai siinn vai 'nsiielele ode an ecopehion Beewshmas@alekndy moeeeet Sacer 144
62 Onioin of the Shimele oJ... 01.2. eter tere ecete. . 2 occ asck eee eee 145

7. Conclusion—Elevation of the Westleton sea-floor ; Formation of the
Gorge of the Thames at Goring; Measures of Glacial and Post- .
Glacial Denudation. Age of the Chalk and Oolitic Escarpments... 148

1. Objects of the Paper Sc.

In the first part of this paper * the relation of the Westleton Beds
in the Eastern Counties to the Crag Series on the one hand, and to
the Glacial Series on the other, was discussed. My object in this
part is to trace the extension of the former beyond the area of the
Crag, and to show that a Westleton Shingle-bed passes trans-
gressively over the Red Crag, the Tertiary strata, and the Chalk,
and ranges westward through the length of the London Basin, while
it rises to considerable heights above the Glacial Drifts and exists
independently of them; and although it occupies only isolated
and detached outliers, if the relation of these outliers to the Pre-
Glacial Beds of Suffolk and Norfolk—the position of which has been
proved—can be determined, we shall then have a definite base by
which to correlate them and establish the order of succession and
relative age of the many Drift Beds of the London Basin.

I purpose therefore to proceed step by step and to take each stage
separately, confining myself now to the oldest and highest stage,
where the distinctive characters of composition are best defined.

* Quart. Journ. Geol. Soc. for February 1890, p. 84.

=

Quart. Journ. Geol. Soe. Vol. XLVI. Pl. VIL.

a_ Post glacial Dritt (site of )
6 ssoxescs Bonlder Clay and Gravel.
C mmm Westleton, Beds.

@ === Brentwood Shingle.

| - N 1_ Gag and Chillestord Beds.
| 2_ Tertiary Strata.
Hatfield, Writtle Park. S Chalke.
st = 4 _ Upper Greensand & Gault.
| 5 _ Lower Greensand.

6 _ Wealden.

== Seale. —
Vertical __ ibinch — 100 feet.
Horizontal _1'inch = 52 miles.

A’_ Boulder Clay Gravel.
B_ Westleton Beds.

Marks
Pn (rag Beds.

D :.. Bagshot Sands.
E _ London Clay.

Vertical Seale
/ inch = GO feet

woe

ie oe

Te ve
ay:

»
Fa
‘
|
}

i

+
ie

vy ‘hal rd ;

DIAGRAM- SECTIONS OF THE PRE-GLACIAL HILL-DRIFTS OF THE THAMES BASIN.

Ww
Valley of Fic.l. SECTION FROM OXFORDSHIRE TO THE COAST OF SUFFOLK.
the Thames = =
Wallingford —— ee Pees eee ee, See Totteridge Whetstone Valley Highbeech. Theydon Valley of Ongar. Valley of Braintree Valley of Dares Hadldgh. Barstall, Bramford Woodbridge Valley oF
= x0, m= ew. Were = bs ge 20 So. 20 (4 of the Lea wo the Roding the Chelmer: 240 the Gre oo eel

a_ Post glacial Drift jsite of)
6 xmas Bolder Clay and Gravel.
c meme Westleton, Beds. :
Fic.3. Section FROM Surrey To HERTFORDSHIRE. Fic.4. Section FROM KENT TO Essex. d ==s== Southan Drift.
€ m= Brethvood Shingle.
1_ Guag and. Chillesterd, Beds.
N Ss N ]
2_Tertiary Strata.
3_ Chalk
4_ Upper Greensand. & Gault.
5 _ Lower Greensand.
6 _ Wealden.
— Seale.—
Vertical __ Winch — 100 feet.
Horizontal _Vinch — 52 miles.

Nutfidd. White Hill Norwood. LONDON Highgate. Whetstone Potters Bar. Hotfidd Hadlow Comp Woods. Purush. Cobham. Valley of Lengdon Fill, Billericay Writtle Park
SH 7. a9 az JK, 400 200. A. 6R Wood. the Thames. 78. a. Tw.

A_ Boulder Clay

: A_ Boulder Cay Grave.
Fic.6. Raitway Cuttinc, Black NOTLEY NEAR BRAINTREE. B_ Westleton Beds.

C _ Gag Beds.

D _ Bagshot Sands.

= London Clay.

Fic.5. Rauway Cuttinc, BRENTWoop.

Fic.7. RaitwaAy CuttinG BETWEEN CHAPPLE aNd Marks Tey.

Vertical Seale
/ inch = GO feet

WESTLETON BEDS TO THOSE OF NORFOLK, ETC, Epa

These are lost in later stages, owing to frequent reconstruction, but
we can then follow by levels.

In 1847* I showed that in the neighbourhood of London there
were hill-gravels as distinct from valley-gravels, but I was not then
in possession of any clue whereby to fix their separate age. Subse-
quent observations, especially aided by the cuttings on the Great
Eastern Railway then in course of construction, enabled me to
follow the Pre-Glacial Beds of Suffolk in their inland range, and to
recognize their higher position in relation to the Drifts of the
Thames Valley.

In my paper of 1871 on the Westleton Beds I briefly alluded
to their extension into the Thames Valley area, but reserved the
details for subsequent description. Other occupations and the need
for verification of some of my early observations led to a long delay
in publication, though in 1881 ¢ I gave a short preliminary notice of
some of the hill-drifts in the London Basin—such as those at High-
beech, Barnet, Southgate, Hertford, Hatfield, South Mimms, St.
Albans, Tiler’s Hill, Horsington, and Bowsey Hill $—which are
capped by Drift Beds of Westleton age. I now purpose giving these
in detail, and I only regret that owing to the lapse of time many of
the sections I have to describe are no longer visible. The delay,
however, gives me the advantage of the observations recorded by
other geologists, and especially by Mr. Whitaker and other officers
of the Geological Survey, and also enables me to avail myself
of the heights and contours given in the last published sheets of
the l-inch Ordnance Survey, so indispensable in an inquiry of this
description, and for which I had previously to depend on the obser-
vations I had made with an aneroid barometer ||.

In 1864, Mr. Whitaker, in his account of the Post-Pliocene
Series §[ of parts of Middlesex, Hertfordshire, Buckinghamshire,
Berkshire, and Surrey, alludes to the occurrence of a ‘‘ gravel wholly
or for the greater part made up of flint pebbles ” on the tops of vari-
ous hills in Hertfordshire and Buckinghamshire.

In 1877 he stated that there were two gravels in East Essex**,

* «The Ground Beneath us,’ p. 30. ,

+ Quart. Journ, Geol. Soc. vol. xxvii. p. 477.

+ Reports Brit. Assoc. p. 420. I was not then acquainted with Mr, Whita-
ker’s latest Memoir.

§ Other hills were named, but these relate to the Southern Drift, which I
now take separately.

|| I regret also that I find it impossible to revisit, as I had intended, the
many localities described, in order to check and revise my early observations,
the greater number of which were made before my views were matured. Conse-
quently, there may be inaccuracies which have escaped me, or analogies which
1 may have ovérlooked. I could also have wished to have given greater
certainty to the percentage values of the Westleton and Southern Drifts—a
plan which only occurred to me after much of the work had been done. I fear
JT may have overestimated the relative proportions of some of the essential
constituent materials, but not to such an extent as to vitiate the general argu-
ment, while the facts, I trust, are recorded with suflicent accuracy to justify the
conclusions at which I have arrived.

{ Mem. Geol. Survey, Expl. Sheet 7, p. 69 (1864).

** «On the Geology of the Hastern End of Essex (Walton-on-Naze and Har-
wich),” Expl. of Sheet 48 S8.E, p. 16, "

K 2

T23 PROF. J. PRESTWICH ON THE RELATION OF THE

one of which he considered to be of Glacial age, and the other
Post-Glacial ; and in the following year he noticed a small deposit of
pebble gravel capping the hills near Hertford *, which he thought
might “be of Pre-Glacial age, but all that is known of it with
absolute certainty 1s that it is older than the Boulder Clay (which
occurs over it in other parts), and Mr. 8. V. Wood, Jun., has classed
it with his ‘ Middle Glacial.’”

In 1875, and again in 1880, Mr. Whitaker noticed in more
detail f this ‘ Pre-Glacial (?) Pebble-Gravel,” and assigns to it more
definite limits. He says, ‘‘Onu the tops of the London-Clay hills
there is often a mass of sandy gravel of an exceptional sort, that
is to say, it is almost wholly wanting in the more or less angular
pieces of flint that form the greater part of the other gravels to be
described, and, like the far older gravel-beds of the Blackheath and
Bagshot Series, its component stones have been rounded into the
form of pebbles. Showing at first sight a very great likeness to
these old Tertiary pebble-beds, after a more careful examination
this gravel is seen to be easily distinguished from them ; for whilst
the former are made up of Aint-pebbles, that is not the case with
the latter, which contains also a large proportion of pebbles of
quartz and quartzite, and here and there a sub-angular flint.”
‘¢ The flint-pebbles have probably been derived from the destruction
of the old Tertiary pebble-beds ; but the pebbles of quartz, quart-
zite, and other older rocks that occasionally occur must have been
derived from beds that are not found anywhere in our district.

“Of the age of this gravel we cannot yet speak with certainty.
It is newer than the Lower Bagshot Beds, for it is known to overlie
them; and it is older than the Boulder Clay, which is found above
it, but between these extremes we are left to reason by analogy and
by the evidence given by the manner of its occurrence.”

‘¢ From its occurrence on the tops of the hills, whilst the Middle
Glacial gravel often lies at their base, or on their flanks, it would
seem that the pebble-gravel is the older of the two and was
deposited long before those hills were cut into their present form, a
process which must have been somewhat advanced before the other
gravel was laid down. It.is possible, therefore, that the pebble-
gravel may represent some part of the ‘ Lower Glacial Drift’ (of
Mr. Wood), any known occurrence of which is, however, as far
distant as the Crag.”

“‘The chief localities are Stanmore Heath from Shenley south-
eastward, west and north of Barnet, and at Totteridge, in Middle-
sex; at Highbeech, Jacks Hill, and Gayne’s Park, east of Epping,
in Essex, and at Shooter’s Hill, in Kent.”

In the larger valuable memoir ¢, published since these pages were
written, Mr. Whitaker describes these Beds, which he places with

* «The Geology of the N.W. part of Essex and the N.E. part of Herts,”
Mem. Geol. Survey, Expl. of Sheet 47, 1878, p. 52.

t “Guide to the Geology of London and the Neighbourhood,” Mem. Geol.
Survey (Ist edit. pp. 49-51, and 3rd edit. pp. 54-57).

+ ‘Geology of London,’ vol. i. pp. 290-298 Psi:

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 123

‘“* Doubtful Deposits,” in greater detail and with some slight changes,
and retains the open term of “ Pebbly Gravel.”

In 1867* Mr. Searles V. Wood, Junr., called attention to the
relations between the Post-Glacial, Middle, and Upper Glacial
deposits of the Valley of the Thames, in connexion with the
position of the latter two on the hills and in the valleys of this
area. Prof. Boyd Dawkins showed, however, that his contention —
based on theoretical grounds, that certain valleys “ could have had
no existence at the period of the Glacial Clay ’”—was not in accor-
dance with the Survey observations.

In 1868 + Prof. T. M°K. Hughes described an outlier of peculiar
gravel he had noticed near Hertford, under the term of ‘ Gravel
of the Upper Plain” in contradistinction to the ‘Gravel of the
Lower Plain.” ‘The latter he referred to the Glacial Series.. Of
the other he says, ‘‘ From their great extent, persistent character,
and uniform level, | think these gravels of the Higher Plain must
be a marine deposit ; but without a careful examination of the old
coast-line, and of their behaviour as they approach the Crag country,
J should not like to give any opinion as to their age.” He further
states that they were of great antiquity and older than the Boulder-
clay.

Mr. Wood, commenting on this communication, contended that
this Gravel of the Upper Plain was of an age intermediate between
his “‘ Middle Glacial” and the Boulder-clay ; while the outliers of
other pebbly gravels at Brentwood, Highbeech, South Weald,,
Langdon Hill, and others t, were “ not improbably of Kocene age.”

Another paper of Mr. Wood’s on the Wealden Denudation §, only
bears incidentally on this question, as showing the existence and
extent of Drift Beds in the Thames Valley older than the lower-
level Valley-gravels.

The most important contributions to this subject by Mr. Wood
are, however, those in which he sums up his numereus and exten-
sive observations, and gives his final views on this and collateral
questions ||, accompanied by a map of the area occupied by the
Chalky Boulder-clay, and a Plate of Sections showing the range
and distribution of the Pre-Glacial, Glacial, and Post-Glacial Beds,
with the position and probable relation of the hill-grayels throughout
the south of England. ‘The second part is devoted more especially
to the.consideration of the Post-Glacial Beds, particularly of those
in the Thames and Hampshire Basins, and to the elaboration of his
views respecting his Periods of Depression, Rise, and Glaciation.
These papers, however, are not easy to summarize, but can be con-
sulted with advantage.

The reader will also find in a paper by Mr. F. C. J. Spurrell,

* Quart. Journ. Geol. Soe. vol. xxiii. p. 394 (1867).

t Jbid. vol. xxiv. p. 283 (1868).

+ Ibid. vol. xxiv. p. 464 (1868).

§ Lbid. vol. xxvii. p. 3 (1871).

| “On the Newer Pliocene Period in England, Part I.,” Quart. Journ,
Geol. Soc. vol. xxxvi. pp. 457-528 (1830); Part I1., iid. vol. xxxviii.
pp. 667-745 1882).

124 PROF. J. PRESTWICH ON THE RELATION OF THE

F.G.8. *, a notice of many of the hill-gravels of the London district,
including the outliers on Shooter’s Hill, Warley, Epping, Langdon
Hill, and others, which he refers, with Mr. 8. Wood, to the wreck of
local Bagshot Beds.

The admirable ‘“‘ Drift Edition” maps of the Geological Survey,
show the intricate ramifications of the Glacial and Post-Glacial
Drifts in Suffolk, North Essex, and part of Herts (Maps 48, 47 7,
and part of No. 7); but the Pebbly Gravel (Westleton) in Essex 2,
owing, I presume, to its being almost invariably hidden under
Glacial beds, is not represented. Although, however, in that county
the Westleton Beds are generally covered by Boulder-clay, the
cuttings on the Great Eastern Railway which I had the oppor-
tunity of seeing showed that throughout that district they pass
under the Glacial Series, and so help to connect the Hertfordshire,
Buckinghamshire, and other outliers with the Westleton Shingle
of Suffolk. These sections I will now proceed to describe. |

2. Range inland of the Westleton Beds.

Suffolk.—In the westward range of the Westleton Beds, sands
predominate in some places, shingle in others—often finely stratified
and false-bedded. Besides their distinctive composition, they may
generally be distinguished at sight by their pure white or ochreous
colour, in contrast with the red of the Crag or the light drabs of
the Glacial gravels. They pass, south of Westleton, from off the
Chillesford Clay on to the unproductive sands of the Crag, as shown
in the following section (fig. 1) :—

Fig. 1.—Pit on Rundell’s Farm, Leiston Common (1860).

b
a, Trail.
b. Boulder-clay not seen in pit, bat showing a short distance higher up on
the hill.

c. White sand, with seams of flint and white quartz-pebbles (Westleton).
d. Laminated ferruginous and yellow sands, ochreous and ferruginous sands.

Speaking of this district, Mr. Whitaker notices ‘a deposit of
less certain classification which has been mapped only over the
small tract north of the Minsmere Level. This is a gravel, with
occasional sand, composed for the most part of pebbles (chiefly of
flint, but some of quartz); and whilst it seems to underlie the
lowest beds of the Glacial Drift, rests generally irregularly on the

* «A Sketch of the History of the Rivers and Denudation of West Kent,’ 1886.

+ Excepting the extreme N.W. corner and Hertford Heath.

+ Geology of the N.W. part of Essex and the N.E. part of Herts, with parts
of Cambridgeshire and Suffolk, 1878.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 125

Crag sand”*. Two pits near East Bridge where it is to be seen
are also noticed’. Mr. 8. Wood, on the other hand, was of opinion
that most-of these gravels, as well as those of which we shall have
to speak in Hast Essex, belong to his Middle Glacial.

Eastward of this place the shingly sands pass apparently over the
Crag of Sizewell Gap; while to the westward they form part of the
sandy commons and heaths of the Snape and Tunstall districts, but
definite sections are wanting.

To the west of Wickham Market, a bed of white gravel and sand
is worked in several small pits; and in one near Easton indistinct
traces of shells are observable in some thin intercalated seams of
ironstone. The furthest point inland here at which I have seen
the Westleton Beds is under the Boulder-clay at Brandeston (fig. 2).
There may, however, be a little doubt about this determination.

Fig. 2.—Section at Brandeston Brick-pit (1847 £).

\ S33 = =a PRES =
6. Dark bluish-grey Boulder-clay.

¢. Light-coloured coarse quartzose sand with seams of gravel consisting
largely of flint-pebbles and some of white quartz, with a few fragments of
shells.

At Ufford Bridge, between Wickham Market and Woodbridge, the
Westleton Shingle rests on the Red Crag, with the Boulder-clay
above it. At Kyson or Kingston, near Woodbridge, the railway-
cutting exposed a fine section of the Red Crag and overlying sands,
capped by a bed of Westleton Shingle. The following are the
local particulars; a general section is given in Plate VII. fig. 8 §.

feet.

1. White gravel of flint- and quartz-pebbles (Westleton) ......... 2
See vy mite and light yellow sand. .......c.cccosceescooccscarseceesesecqeaes 2
Daamtent, yellow sand without fossils...........-.c2esvessestacenesseese )
4. Gritty sand, false-bedded and with local and irregular seams |

of shells, and an underlie of a few inches of gravel resting on | _
5. A thick bed of Red Crag, abounding in shells at the west end } 28

of the cutting, but with very few at the east end ............
6. A thin seam of Coprolites with flint- and a few other pebbles |

resting on a floor of London-Clay Septaria ...............eeees
. London Clay.

T

* Mem. Geol. Survey, Quarter-Sheets 49 S. and 50 8.E. p. 27 (1886).

t+ See Quart. Journ. Geol. Soc. vol. xxxiii. pp. 101-111 (1877).

t I give dates, because in all probability many of the sections no longer
exist.

§ See also Quart. Journ. Geol. Soe. vol. xxvii. p. 334.

126 PROF. J. PRESTWICH ON THE RELATION OF THE

The Shingle (No. 1) is approximately composed of :—

per cent. —

1, Flintepébbles i. .diiadeedatnasencb ss «ves qdbawiuedthewitkawessh aa memne 30

2. White quartz- pebbles Jeti dan detent swenendlenisls cmmangemodt obatae ee beneae 30

aby PULA AUIS ae ros oe Me nncnnirsinins oe inuinte minnie alate ai eat eae 20

4. Subangular fragments of chert and ragstone ............seeeeeeee 12
5. Pebbles of light-coloured quartzite, sandstone, greyish arkose,
and dark metamorphosed slate .........c.0tcessseececesneventeunes

100

Its thickness is uncertain, as the Boulder-clay does not show until
the higher part of the hill is reached.

West of Woodbridge the Westleton Beds have undergone consider-
able denudation, and are generally removed and replaced by Glacial
gravels and Boulder-clay. They, however, sweep round to the north
of this area, and were to be seen in some small exposures in pits
north-east of Ipswich.

At Finnford Bridge the section gave :—

Bluish Boulder-clay with chalk pebbles, &e. ......... 6
Seam of laminated iorowanelay 0257 26.00 so sec ctentanee ee
c. White sands and gravel, the lower part false-bedded. 12

In the lane leading from Witnesham Street to Tuddenham I
took the following section :—

feet
b.. Light brown Boulder-clay...... OE ak aaa vet 5
ce. White sands and gravel (Westleton) ... 2 to 4
G2 Meds Cnae.zSyour. iv Ree. ase ee Sia eee Rn ae 8

In the fine section described by Mr. Whitaker * near Bramford, 3
miles north-west of Ipswich, he expresses an opinion that Bed No. 2
may be of Crag age. I would take it to represent the Westleton
Beds. The following is Mr. Whitaker’s description of this pit.
Beds 3 to 6 are given ‘only j in abstract.

feet.

1. Glacial drift. Gravel and sand, resting irregularly on 2... up to 8
2. Fine light-coloured sand with thin clayey layers; at
the bottom a thin layer of gravel with phosphatic

nodules (may belong to the Crag) ...........:eeeeecees up to 15
3 & 4.-London Clay with a Pebble-bed at base ...............4.. 10
e Reading Beds with a few flints and pebbles... ie cacsaces- 18 or more
, Thanet ‘Sands «222. 2.cs1.4.tsv snus ceeeteaeanes eeu ated one oot deaeemetes 5
. Chalk.

Three miles south-west from the last pit is the village of Burstall,
and on the slope of the hill on the banks of the small stream I found
(1856) the following section :—

feet.
6. Boulder-clay,, challkiqerccjpdesnenecteess= 3 to 10
White gravel or shingle (Westleton)... 8 to 10
AW Uitte Sans. avie tan deedoenat Oo anaiea stint ack uiseeemes 2

* Mem. Geol. Survey, ‘Geology of Ipswich,’ &., 1885, p. 14.
t This pit had not been opened out to its full extent when I last visited it
several years ago.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC, 127

Lower down the hill the yellow sands of the Crag crop out.
The gravel has the well-marked characters of the Westleton
Shingle, its approximate composition being as under :—

. per cent.
HSMM ITE-PEODICS . .v.ccniegecosescxtevacessvsessaneatsctepas
BNVIMIEG, QUATIZ—PeDOLes ...... .sesenecedeedsernecseardeeveres mee 25
pees MOAT MI EL VINES) 7, aint kics sya vais Pew Bak Could ddweum’ etleonsle» 23
4, Subangulaar fragments of chert and ragstone ...... oe ee
5. Pebbles of light-coloured sandstone and quartzite, and

AOC Ieee Sein yina)s Sb -Ssaiciniepsae eter enraice ses 10
100

Mr. F. J. Bennett has noticed a very similar section at Elmsett, 3
miles to the north-west of Burstall, where the Boulder-clay overlies
a “rather coarse sandy gravel, with pebbles of quartz and of quartzite,
about 2 to 10 feet,” overlying a “fine buff rather clayey sand ” *.

The railway-sections in this intermediate district afforded little
information respecting the Westleton Beds. The Norwich line,
between Ipswich and the valley of the Ottley stream, passes almost
exclusively through thick Boulder-gravels and clay very much dis-
turbed and deeply eroding the underlying beds ; whilst the Yarmouth
line, between the Orwell and the Deben, passes through Glacial
loams, with but little gravel or Boulder-clay, overlying the Red Crag
and unfossiliferous sands.

My notes, I regret to say, are not sufficiently detailed to give a
definite account of the deep cutting on the northern side of the
tunnel at Ipswich on the London line. This section, unlike that on
the southern side of the tunnel, which was through a mass of
Post-Glacial Drift, exposed :—

feet
Light-coloured sands with seams of gravel in horizontal layers......... 40
Pee eeeeich mich false-Dedding T ..............sscwcseecererenccceoerccoes 20

Dark brown London Clay.

But though I failed to note the exact composition of the gravel,
my belief. is that this bed belongs to the Glacial Series. The
next cutting (fig. 3), where the line passes under the London Road,
shows how extensive the denudation accompanying the advance of
the Boulder-clay has been.

Fig. 3.—Section on the Railway near Ipswich.

a. Ochreous gravel. 0. Boulder-clay. b', Light-coloured gravel.
ce. Red Crag.

* «Geology of Ipswich,’ &e., p. 77.
+t Here, as at the Kyson Cutting, a layer of Septaria divides the Red Orag
from the London Clay.

128 PROF. J. PRESTWICH ON THE RELATION OF THE

Essex.—On the south of the Crag area, the well-known cliffs at
Walton-on-the-Naze exhibit a small patch of the Westleton Beds,
composed of :—

per cent.
i, WlinitpeObies. cca veeed. obsaccce ac caeeeeee ec enee 36
2. White quartz-pebbles. ...i....-os sees dee eer 20
OO UOARGWMAT AUIS! c.0.i a0. nner teeeeen ne seem 20
4. Subangular Cher. ....sc--cecscveesecemedereteesems 14
5. Quartzites, Lydian stone, Kc. ...............00 10
100

This gravel caps the cliffs near their western extremity, over-
lying a bed seemingly of the Chillesford Clay *. At the eastern
end of the cliff, the unproductive sands are replaced by very_fos-
siliferous beds of the Red Crag.

Fig. 4.—Section of Cliff east of Walton-on-the-Naze.

feet. '
g. surtace-soil and) gravel {sccm eocees 1 nnmaterne tests Verena ee eee 1 to2
e. Westletow. Shingle: 0.2. aduk eee Seve sc Thadeths tesa tte tet se 5
d Light-coloured laminated sands and clays ............ ssseseeseerees 4
* | Dark carbonaceous clay with much wood and lignite ............... 2
e. White and yellow sands. These are replaced at the other end
(east) of the cliff by fossiliferous Red Crag.............sssseeeeeee 10

f. London Clay.

From Walton to Clacton the low cliffs consist of London Clay
capped by gravel. There are no Crag Beds. This gravel forms
apparently one thick bed (12 to 20 ft.), but in reality it consists of
two parts. The upper bed is much disturbed and not stratified, and
is derived in considerable part from the débris of the lower bed;
whereas the lower one is regularly stratified, and often shows well-
marked false-bedding. It may be a question whether, although
both the Red Crag and the Boulder-clay are absent in these cliffs, the
lower gravel should not be referred to the Westleton Shingle. That
there is a material difference of age between the two beds of gravel

* Mr. Clement Reid considers it to be something newer.

WESTLEION BEDS TO THOSE OF NORFOLK, ETC. 129

is evident from the circumstance that at the Clacton end of the
cliffs these gravels * divide and admit between them the Post-
Glacial mammaliferous deposit described by the late Mr. J. Brown
and by the Rey. O. Fisher f.

Pa |

Fig. 5.—Section of the Cliff one mile south-east of Clacton.

PEPSe OCHYGOUS GTAVEl......0-.ccc0ccescseccccccecacecanaaomccecess 4 to 6
?¢, Alternating beds of fine and worn gravel, finely bedded or
with oblique lamination. Colours ochreous, white, and
eee Tee UO IIS pes SMU E EME hiarsiis <2ids)s Dplnawevwewanld ace snnsemniian le 8 to 12
Ff. London Clay.
At Clacton the two gravels are divided at —> by the Post-Glacial clays
mentioned above.

The Lower Gravel, which is imbedded in a matrix of loamy
brown quartzose sand, quartz-grit, with innumerable fine fragments

of flint, is composed as under :—
per cent.

NM ra te SSG soak a senaiwls a ciwe snes sons evs sean eacensereoeses 24.
MNP UCMAMARUZ-DEDDICS Liicccecccacnsasecesscesscsodsoreessocvaccccesesccese 16
3. Subangular fragments of flint, mostly white, but a few stained
Rees he. cde vce daqcnviadededdoawontbnchnentesdé sowed 32 ?
4, Subangular fragments of white and yellow cherty ragstone ......... 10
Subangular fragments of brown and red chert ............:0ce0s0es 00 8
5. Pebbles of light-coloured (?) quartzite, dark sandstone, and Lydian
SE NR ere SST ca ke ce nck cue’. chur ectatducancondesceceasssresie
100

I have, however, some doubts about this correlation. The bed
may be of Post-Glacial age.

It is also a question whether some of the thick gravels of Central
east-Essex may not be of Westleton agej. Some well-sections
seem to indicate that such is the case in respect to the base of the
great spread of gravel west of Colchester. This bank is from 30 to
50 feet thick, and the upper part consists of gravel of Glacial age.
It maybe seen from the railway-sections how closely associated

* The surface of the lower gravel should be examined for palseolithie flints.

t Mag. Nat. Hist. ser. 2, vol. iv. p. 197 (1840); Geol. Mag. vol. v. p. 214
(1868). See also the Survey Memoir by Mr. W. H. Dalton.

t{ The Rey. O. Fisher informs me that the pebble-gravel is well developed
at Elmstead, near Colchester, and at Alresford, near St. Osyth.

130 PROF, J. PRESTWICH ON THE RELATION OF THE

the Glacial and Westleton Series are in some parts of Essex,
and how difficult, without the intervention of the Boulder-clay,
it sometimes is to distinguish between them.

There is no group of sections in Essex more interesting ee
those adjacent to Sudbury. The Chalk, the Lower Tertiary Beds,
together with Pre-Glacial, Glacial, and Post-Glacial Drifts, are there
exhibited in the same or in neighbouring pits. Since I visited
them they have been fully described by Mr. Whitaker, to whose
sections I would refer the reader *. The Pre-Glacial beds are ex-
posed at some of the pits on Balingdon Hill, where the Boulder-clay
reposes upon so irregular a surface that in some places it rests on
Pre-Glacial Sands, in others on some of the Tertiary strata, and in
others on the Chalk.

On my first visit to these pits in 1845, I was inclined to believe
that the thick bed of sand and gravel under the Boulder-clay
belonged to the Crag; but later, 1 was led to conclude, on the score
of position and composition, that it should be grouped with the
Westleton Beds. I found no fossils; but Mr. Whitaker has since
then found traces of shells (broken) with unbroken specimens of
Purpura lapillus (var. crispata); and in another pit he discovered a
bed of sandy ironstone, with casts of shells, of which 11 species
(op. cit. p. 31) were determined, though with doubt, by Mr. Etheridge.
With them were a few coprolites. On these grounds Mr. Whitaker
classes this bed with the Red Crag, with a query.

The Red Crag has not, however, been met with within a con-
siderable distance, and the fossils found are of a negative character.
The Purpura lapillus occurs in the Westleton Beds of Norfolk and
Suffolk—as also species of Natica, Cardiwm, Mytilus. Or the fossils
and the coprolites may have been derived from the Red Crag; for
the beds under the Westleton shingle are, as will be shown further
on, often greatly eroded. Or we may have here a remnant of Red
Crag at.the base of sands and gravel belonging to the Westleton Series.

I express this opinion, however, with all reserve, though IL
think it is confirmed, not only by the section at Burstall, but also
by one nine miles to the west of Sudbury, at a place called Burnt
House, near Stoke (fig. 6). In the pit there avery similar, but much
thicker bed of gravelly sands is seen resting on the Chalk, while
the Boulder-clay is worked in another pit just above.

I found no fossils at this place ; but they have been since recorded
by the officers of the Survey, who give the following description of
the pit t:—

feet.
‘Glacial Drift. White, grey, and yellow false-bedded sand, partly
coarse, partly fine, irregularly bedded, A mass of shells (Pur-
pura lapillus) said to have been found at the bottom at one
SOG CU CRAD) oii. ac. -Sansoeuidachen nuke uo cba ibis dude daele wey Spero ean 30
? Drift or Red Crag. Bed of flints &c. (a piece of phosphatized
PONG) Vitesceeaccsoek’ ws ccst duscuvcneagoceuasoaenens chase cat seit ay ei coe 1 to 2
Chalk, ae with flint, (soso ac sNeers ven seeeutwe ne heek sewer meee Memeeeae 30”

* Mem. Gea. Survey. Ganen of ‘the NW. ae of we ae pp. 14, 16,
31, 57 (1878) ; and op, cit. p. 182 (1885).
+ Mem. Geol. Survey. Geology of the N.W. part of Essex &c. p. 49 (1878).

= T

WESTLETON BEDS TO THOSE OF NORFOLK, ETc. 131

I omitted to notice whcther chert and ragstone were present,
nevertheless the composition and character of the sands and
shingle are, I think, of the Westleton type. Both flint- and quartz-
pebbles occur, it is true, in the Red Crag*, but never in such
numbers, or proportion, as to form a compact bed of shingle like
that of Westleton.

Fig. 6.—Section at Burnt House, near Stoke (1848).

feet.
_ 6, Bluish Boulder-clay exposed in another pit a short distance higher
on the hill.

e. Bright yellow and white micaceous sands, fine at top, coarse below,
succeeded by fine gravel or shingle.. The sands show oblique
lamination, and contain concretions or balls of soft limonite,
Meee SIAOINETA CLIMTMCHGI \soy desc ciee eee. acicscwadeuetenessadgedecedanrions 2%

d, Layer of large flints, angular and rounded.

The railway between Sudbury and Mark’s Tey exposed .some in-
teresting sections. The first deep cutting, 2 miles south of Sudbury,
showed 5 or 6 feet of ochreous flint-gravel and sand, overlying from 5
to 10 feet of greyish-blue clay (Glacial), of which the lower part was
finely laminated. Beneath this were 4 or 5 feet (base not reached)
of white and yellow sands with seams of small shingle (Westleton ?).
The Lamarsh and other smaller cuttings were through Post-Glacial
brick-earth and gravel. Between Bures and Chapple, the cutting
passed through 12 feet of a blue Boulder-clay, separated from 10
feet of a brown Boulder-clay by 2 feet of ochreous gravel. Below
the Boulder-clay was a bed, 4 feet thick, of ochreous gravel, under
which were 7 or 8 feet of white sand and gravel (Westleton).

But the most important cutting was that between Chapple and
Mark’s Tey. It extends for nearly a mile, and reaches a depth of

from 20 to 25 feet. At the two ends, the section exposed from 8 to

10 feet of Boulder-clay overlying Westleton Shingle, but in the centre
resting on London Clay. The whole section is given at length in
Pl. VII. fig. 7, A small enlarged portion is given below (fig. 7).

* Reference will be made to these in the third part of this paper.

1S2Z PROF. J. PRESTWICH ON THE RELATION OF THE

Fig. 7.—North end of the Railway Section between
Chapple and Mark’s Tey (1849).

feet

6. Bluish-grey Boulder-clay. 1.2: .-cccisc-p.:--24cereensnon ce cdhtows-ssaeeeeiiae 12

b'. Coarse ferruginous gravel .....-..sass-qse eat eee «0. cca 2
c. Stratified sands and shingle, yellow and bright qorau tua ochreous
CWrestlet@i)i fo.) sge nsec ssa ve che see eeeseen Eee Talents s nsipca'siee Sea eeaees

f. London Clay.

No fossils were found in any of the sections, except in some
Post-Glacial Beds at Sudbury and Lamarsh.

Similar sands and shingle have apparently a considerable develop-
ment in North Essex; but they are generally hidden by Boulder-
clay, or masked by Glacial gravel, which, when fine and stratified,
they resemble in general appearance, and sometimes assimilate to it
in composition, owing to an adniixture of the two beds. On a hill
14 mile north of Coggleshall there was a section showing 4 feet of
Glacial gravel overlying 6 feet of bright yellow and ochreous sand
with flint- and white quartz-pebbles (Westleton).

The Witham and Braintree branch line likewise exhibited some
very illustrative sections of the Glacial and Westleton Beds (figs. 8, 9).

Fig. 8.—Section on the Railway, one male north of Witham.

a. Brick-earth. ,
. Flint-gravel. \ Post-Glacial.

b “Chalky Boulder- clay.

White sand with shingle at base (Westleton),
f London Clay.

The shingle consisted of—

per cent,
IROBAUGL-PODDLGS. 55. ar hac or aqaee anon Sat W segceten dane tau ee eee ame 32
ema ithe quartz—pobbles ir. cis. a osuonca betecsk tant ee ease eae 24.
oo subangular fragments of Hint \\...0:.-....0asgeeneseseieee eae 35
4, Subangular fragments of chert and ragstone .........+2.006 9

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 133

Similar beds were passed through at various cuttings between
this point and Bulford; but it was between Black Notley and
Braintree that the section of greatest interest was exposed.
The cutting, which is 25 feet deep, showed the Chalky Boulder-
clay resting upon a deeply indented surface of coarse Glacial gravel,
much contorted. This latter had likewise pioughed heavily into
the underlying light-coloured Westleton sands and shingle, which
were regularly stratified in horizontal layers, and intersected by a
number of small faults of 7 to 3 feet throw, which did not pass
upwards into the Glacial Beds (Pl. VII. fig. 6).

The shingle consisted mainly of small flint- and white quartz-
pebbles with a few subangular flints. No fossils were found. The
overlying Glacial gravel.consisted of large worn flints and some
Chalk-débris, with pebbles of sandstone, of red quartzite (N.R.S.),
and some small pebbles of flint and white quartz, the latter probably
derived from the underlying beds. (See explanation of Pl. VII.
pe lo2).

The Westleton Beds were again exposed at the ballast-pit near
Braintree Station. They are there much more ferruginous than
usual, and are deeply indented by the overlying Glacial clay and
gravel. In one part of the pit the section was as under (fig. 9) :—

Fig. 9.— Railway ballast-prt, Braintree (south end) (1848).

feet.
a. Brown clay with subangular flints... ‘ a
b. Very chalky Ha Gldee clay ert cancae eo y sheen ae
b'. Ochreous Gravel (Glacial) .......0..+- este
¢. Finely stratified white sands and gravel, yellow
Westleton DE EMLe MO WOR MOG estanis\cvenisiinnasinsneebadssenensecias 15
Beds. ce’, Coarse dark ochreous gravel, with ferruginous
POMCUELLOMS Mag ten Wari <nuavewssscmcsscnsueseasiseeneness

The shingle consisted of the following materials, placed in the
order of their relative abundance :—

. Flint-pebbles.

. Pebbles of white quartz.

. Subangular flint-fragments.

. Subangular fragments of chert and ragstone.

. Large flattish light-coloured quartzite-pebbles.

. Subangular pieces of Tertiary sandstone and puddingstone.
. Small Lydian stones and pieces of white quartz.

Tao CON eR

Beneath ¢’, a hole sunk at the bottom of the pit showed 8 feet of
interstratified white and yellow sands, with a shingle composed

be4 PROF. J. PRESTWICH ON THE RELATION OF THE

largely of white quartz-pebbles. This gives a thickness at this spot
of 25 feet of Westleton Beds ; but these sands and gravels extend
nearly to the top of the hill on which Braintree stands, and as the
well at the waterworks lower down shows that the base of the sands
is there 140 feet above O.D., while the summit of the hill is
above 234 feet, the Westleton Beds, round which the Glacial Beds
wrap, would seem to be here not less than from 70 to 80 feet
thick (see Pl. VII. fig. 1).

It would appear fon this and other spunk to be named that
these Westleton Beds had a large development in Central and Nor-
thern Essex, but that that they have been extensively denuded by
the overlying Glacial drifts. The independence of the Westleton
Beds in respect to those of the Glacial Series here also becomes
more apparent, owing to the rise of the land and its waste before
the deposition of the Glacial Beds, in consequence of which the
latter, in the districts further to the west, where the rise was
greatest, gradually come to occupy a lower level than the former.
The separation of these two Drift-series, first clearly apparent in
this part of Essex, becomes more pronounced as we proceed west-
ward in the London Basin. The presence of Chalk and Jurassic
débris, with Quartzite pebbles derived from the New Red Sand-
stone, readily serves to distinguish the Glacial from the Pre-Glacial
drifts.

The Westleton Beds extend to the north-west, though but rarely
exposed, by Wethersfield to Dunmow and Thaxted. In a pit just
south of the latter place is a section of some interest (fig. 10), as the
pebbly sands, which I take to be of Westleton age, and the overlying
Boulder-clay are both faulted. This, however, is from recollection.
I omitted at the time to note the constituent parts of the gravel.
The Survey officers consider it to belong to the Crag.

Fig. 10.—-Section near Thaxted (1850).

a. Pebbly soil.

b. Whitish Boulder-clay.

c. Coarse white sands with a few patches of gravel.
ce’. Ferruginous sand,

The Westleton Beds again showed in a pit at Braxted, 2 miles
S.W. of Thaxted, the section of which was as under :—

1. Gravelly sand and clay.

2. White chalky Boulder-clay.

3. Ochreous gravel, consisting essentially of flint- and quartz- pebbles,
with very few subangular flints.

4, Ochreous sand.

WESTLETON BEDS TO THOSE OF NORFOLK, EIc. ‘135

To return to the main line of railway. The sections from Witham
to Manningtree are all through Glacial or Post-Glacial Beds, and
are not of importance; while on the branch line to Maldon they
are chiefly through London Clay and Post-Glacial gravels.

Maldon stands on a hill about 120 feet high, capped by gravel
probably of Westleton age. My notes refer to it as a flint-shingle
with quartz-pebbles and fragments of chert.

Danbury Hill, 6 miles 8.8.W. of Witham, and 317 feet high, is
capped by gravel of an anomalous character. It consists chiefly of
subangular flints with a large proportion of flint-pebbles, and a few
pebbles of quartzite, quartz, chert, and some old rock having more
the character of a Glacial Drift. It may have been a Bagshot
outlier invaded by the Glacial gravel. Lower down (about 150
feet) on the southern slope of the hill is another gravel in which
chert- and quartz-pebbles are more prominent.

At the cutting on the main line which begins one mile west of
Witham, and which reaches in places a depth of 25 feet, a very
white chalky Boulder-clay passing down into bluish grey, overlies
5 feet of white sand with a seam of flint- and quartz-pebbles
(Westleton) at base. At the-western end of the cutting the same
eravel, but with ochreous and white seams alternating, lies in
hummocks beneath the Boulder-clay. The Hatfield cutting 18
through 20 feet of gravel at the eastern end, and through chalky
Boulder-clay capped by 8 feet of brick-earth at the west end.

Tne long cutting from Springfield to Chelmsford (30 feet deep in
the centre) is of interest from its showing the great erosion of the
London Clay and the very irregular distribution of the gravel and
Boulder-clay ; but my notes relating to the gravel which underlies
the Boulder-clay are insufficient for me to say whether it is of
Glacial or of Westleton age.

A range of hills, capped by pebble-beds, commences a short
distance westward of Chelmsford. But these, though really older
than the Westleton Beds, I have relegated to Part IIL. of this paper.
They include Writtlepark, Brentwood, Rayleigh, and other hills.

The Westleton Beds, which thus far have not reached a level of
above 160 to 200 feet, now rise more rapidly as they trend westward,
capping the hill-tops, and leaving the Boulder-clay and the Glacial
eravels at lower levels in the intermediate lower ground. There is
thus a considerable break before the next outliers are reached,
though there are, I think, traces of the Westleton Beds to be met
with near Ongar.

The next well-defined outliers are therefore on the western side
of the valley of the Roding, on the range of the Epping hills, which
at Highbeech and Jack’s Hill attain a height of from 340 to 370 feet.
On the top is a well-marked hed of the Westleton Shingle. The
following is its approximate composition in a pit near the “ Wake
Arms,” Jack’s Hill :—

Q.J.G.8. No. 182. L

136 PROF. J. PRESTWICH ON THE RELATION OF THE

per cent.
I. Bilimt-pebblests.-2 da. 0kc sees inaveaeen tees 'cedudenageaeee 50
2: White .cuariz-pobbles... ...5.iis.. seeks vettinnsacaeaeaees 15
3. Subangular, travmonts: of Tint... ..c-nesenacs+ seve waseameetes 20
4. Subangular fragments of chert and ragstone ......... 10
5. Pebbles:of Tbydian stone &e.) 22... tits. de... ocnenenen 4)
100

A bed of white and yellow sand (Bagshot) underlies the gravel.

At Coopersale Common (or Gaynes Park), two miles N.E. of
Epping, is another range of hills, from 340 to 360 feet high, on
which there is also a capping of Westleton Shingle composed of

per cent.
lin tpebbles. sce fs ewes ake tptaere satis elksloeloran ted nee ee eee 56
2. White quartz=pebblesi¢ .< .ccposes-ecunseieseeie soba ceoneeane 20
3; pubangulardragmentsyof fmt ys -..ce-esvlew «ace sence ree 9
4. Subangular fragments of white Ragstone............... 12
©: Pebbles of duydian stome er, Jo p...ctse-noe torment 3
100

imbedded in a matrix of light yellow, loamy, quartzose sand.

To the south of these, and extending from Buckhurst Hill to
Woodford Hill, is a considerable spread of pebbly gravel, 10 feet thick
in places, of a character intermediate between the Brentwood and
the Westleton Beds, but more analogous to the former. It consists
almost entirely of flint-pebbles (Bagshot), with a very few white
quartz- and other rock-pebbles imbedded in a variable matrix of
sand and clay. The lower part is roughly stratified—the upper
passes into an unstratified mass of brown and ferruginous clay
with few flint-pebbles.

Middiesex.—The Drift Beds of the eastern and lower part of
the county consist chiefly of Glacial and Post-Glacial gravels ; while
the higher hills on the north are capped by the Westleton Shingle.
Thus the ridges from Barnet and Barnet Gate (410-460 feet), and
from Totteridge to Highwood (400-410 feet), and again at Mill Hill,
are capped by a poor gravel of this age, from 2 to 5 feet thick, and
composed of

per cent.
1, Wlitt-pebloless oc saynese-n aces ees cepa on teee ena cuaues casas 50
25 W hite iquartz-pebbles e.. 020 b.sque morn cet reas scasackess ade 15
3. Subangular flints, staimed white and brown............ 20
4, Subangular ragstone and chert ............0..sssecsssseee 12
DT Liydian Stone Mit. .0.skmarn saver asnaraens eencadtacehe belt eran 3
100

in a matrix of quartzose sand and greenish clay.

The Boulder-clay. at a level of about 100 feet lower, extends
from Whetstone to Finchley and Muswell Hill. The gravel which
underlies it in a pit near Finchley Church is of Glacial origin, and
is full of northern débris. That at the old section opposite to
the ‘ Bald-faced Stag” has been referred to the Pebbly Gravels ;

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 137

I should have placed it also with the same Glacial Beds; but my
notes are insufficient.

The Westleton Beds are difficult to follow in this direction.
They do not seem to rise so high as further north. Some beds
at Hendon (280 feet) may possibly be referred to them, as also
a small outlier which caps the hill (278 feet) at Horsington, two
miles south of Harrow. This isolated patch, which is a mere
remnant scattered on the surface, consists of

per cent,
MOEN PU AMA Creat nani tetl Gunna dacaienWinwrcavcescrsanceossecexses 42
PIECE IAN Z-PEODICS. 0... carer cence ccessevevecncessantas 10
3. Subangular flints stained brown ...............ececeeees 30
4. Subangular chert and ragstone — .............seseseecees 18
100

With respect to Highgate and Hampstead Hills, which rise
to the height 412 feet, I hesitate how to class them. I have
found some fragments of worn cherty ragstone and a few rare
quartz-pebbles on Hampstead Hill, with abundant flint-pebbles of
local (Bagshot) origin; but the characters are not sufficiently
marked to satisfy me. They may be Westleton or they may be
outliers of the Southern Drift.

In the north of the county, a well-marked Westleton outlier may
be seen in the wood (400 ft.?) 14 mile north of South Mimms,
consisting of :—

per cent.
PUSNIMDE ACIDS eer N tence ore oed die des nde ssescecertocevaces 38
PPM MG NC MAT DA POODICS 22.) si. teecaadercscccscesevescccesceseucersce 28
Peeomodnrilar fints, NOt StAIMEM is... .ccscccc ccs erecccensceseenes 24
ee eMAIOTINAT CMOTD (QOCs Lacie cndtecey edad ences vslaceeeeeee's eee 6
5. Pebbles of white quartzite, Lydian stone, &c. .............4. 4
100

The adjacent ridge, extending from Potter’s Bar to Bell Bar (380
to 400 ft.), is also capped by a thin bed of Westleton Shingle, but
there were no sections open at the time of my visits.

The Pebble-Beds of Stanmore, Elstree, and some adjacent hills
belong to the Brentwood group.

Hertfordshire.—The London-Clay hills of the north of Middlesex,
capped by Westleton Shingle, are continued into Hertfordshire,
where they form, between Hatfield and Hertford Heath, a con-
spicuous range from 320 to 380 ft. high, and overlooking, at a
level of from 180 to 240 ft. lower, the broad valley of the Lea and
Mimram, over which are spread Glacial gravels and sands, covered in
places by the Boulder-clay. The material difference of level and
the marked character of the beds here bring out very clearly the
discordant relation of these Glacial and Pre-Glacial Beds, as shown
in the following section (fig. 11) :—

138 PROF, J. PRESTWICH ON THE RELATION OF THE

Fig. 11.—Section from Hatfield Brick-pit to the G. N. Railway near
Digswell Junction.

a. Post-Glacial beds.

b. Boulder-clay.

b’. Light-coloured sands and ochreous gravel.
c. Westleton Shingle.

T. Lower Tertiary strata.

C. Chalk.

Speaking of the characters of these gravels, Prof. T. M‘K. Hughes *
says: “The gravel of the Upper Plain consists chiefly of pebbles ; of
these, about fifty per cent. are of quartz, about ten per cent. of
quartzite, about five per cent. various (such as jasper and a
conglomerate of quartz pebbles in quartzite), and the rest flint.”
These gravels have also been noticed by Mr. Whitaker and Mr.
S. V. Wood in the papers before referred to.

This Hertfordshire shingle is remarkable for the large proportion
of pebbles of white quartz and of Lower-Greensand débrist. A
specimen from Brickenden Hill yielded broadly :— .

per cent.
ie Bib peb bles... .5. cue ce apaies snes romipmaeiaaeara cance oe naneoesarnncen saan 34
2. WW nite quartta-pebbles v.20 0c ...t sncieem isolesees ar maleeies PORE Ren eee 28
3. Subangular flints—2 stained brown, and 3 not stained ......... i:
4, Subangular fragments of red and brown chert and of white
TAO SEOWS cele ctns ah onc chobinde p tonbianeteinai paneer cans ba ciate meee 18
5, Pebbles of nydian, stome Ge. ytae.d. -mdandoopeenencte<cee- son ceeeeereeee 3
100

Further to the south-west similar beds are met with at Shenley
Hill and again a little northward at Bernard’s Heath near St.
Albans, where they form a bed from 8 to 10 ft. thick, capping Lower
Tertiary Sands and Clays, at an altitude of 406 feet, They there
consist of :—1. Flint-pebbles; 2. White quartz-pedbles; 3. Sub-
angular flints, not stained; 4. Subangular cherty ragstone; 5.
Pebbles of Lydian stone, yellow quartzite, &c.; imbedded in a
loamy red and yellow mottled sandy clay, disturbed at top.

Notwithstanding the extreme denudation which the high Chalk-
plain, extending from Hertfordshire into Bedfordshire, Buckingham-
shire, and Oxfordshire, has undergone, a few small outliers of Lower
Tertiary strata still remain, rising above the general level of the
Chalk-plateau with its scanty Glacial Drifts and its “* Red Clay with
flints ”

These little isolated hills are frequently capped by a gravel- or
shingle-bed, which I believe to be of Westleton age. They are

* Op. cit. p. 285.

+ The chert and ragstone débris does nos seem to have been hitherto
recognized, or is mentioned under some other name.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 139

very few in number, and gradually become rarer as we proceed
northwards, although in a few instances they extend to the edge of
the Chalk Downs.

At Collier’s End (348 feet) and Sacombe Green (362 feet), five
miles north of Ware, are two small Lower Tertiary outliers with a
thin capping of quartzose shingle (Westleton). Others lie on some
of those near Weilwyn,—on Ayot (406 feet) and Burnham Green
(407 feet) hills.

North of St. Albans, and between the valleys of the Lea and the
Gade, traces of Lower Tertiary strata may be found as far north as
Kerkhampstead Common, but they are rarely in sufficient force to
be worked, or high enough to bring in the Westleton Beds. At
Bennett’s End, near Hemel Hempstead, the Tertiary strata are
capped at a height of 456 feet by a bed of sandy clay with a thin
uneven patch of Westleton gravel, consisting in large proportion
of flint- and quartz-pebbles with a few subangular flints (not stained),
fragments of Lydian stone, and afew flat ovate light-coloured quartz-
ite-pebbles. The bed varies from 1 to 6 feet in thickness, and rests
on from 30 to 40 feet of London Clay and Lower 'lertiary strata.

There is another Tertiary outler at Little Heath and Potten,
extending to Berkhampstead Common, or rather it is a mass of
Tertiary strata preserved in a depression in the Chalk, of great
extent. ‘There is some appearance of Westleton Shingle, but too
indistinct for description.

The hills to the west of the Gade present similar features. The
Tertiary Beds are, however, so mixed up with Glacial débris that
they are to be recognized only in a few instances. At Langley
Common (440 feet) there are traces of Westleton Shingle, and closely
adjacent to the borders of Hertfordshire is the more conspicuous
outlier of Tiler’s Hill.

South Buckinghamshire-—In this county, as in Hertfordshire,
the picturesque high ground of the Chilterns is covered by a
sprinkling of Glacial Drifts (but no Boulder-clay), and ‘ Red Clay
with Flints,” with occasional Tertiary remnants.

Tiler’s hill*, 2 miles east of Chesham, rises to a comparatively
considerable height above the surrounding Chalk-plateau, and
consists of Lower Tertiary strata with an o utlier of London ClayT.
On the summit, about 600 feet above the sea-level, is a small
capping of eravel, composed of :—-

per cent.

1. Tertiary flint-pebbles, small and large, many of them

PRETO WULG ve ccitessiconivstph ines son eel heseneee CIRaNRseeeae eh « 55
SP MMGUAIEZ- DEDUCE: Sosuccesesegvocaksssues€aayeseydevarvdsrscvensecces 23
3. Very subangular fragments of flint, stained yellow ; others are

PeCemM CALE AML ULETLE WEN ven. wihdnnekdn ag nembarnaausis itecbecessvces 12
SEES S AAEM Ma ior ck Vier» sjanis’hs da x80) oben ae hd LAGU DY MEW ASRS RAMS vas 08 5
5. Flat ovate pebbles of light-coloured quartzite and veinstone,

with subangular fragments of Tertiary sandstone and pudding-
BEOMC .ecssesscserecccesseseeer® seeceeneserenseseenseeess seeuunseesecses 5

* On the new one-inch map this name is altered to Crow dnote
t+ Described by the author in Quart. Journ. Geol, Soe. vol x. p. 90 (1854),

140 PROF. J. PRESTWICH ON THE RELATION OF THE

The gravel rests on an uneven bed of London Clay. Lower
Greensand débris is comparatively scarce, and the débris of Tertiary
rock more abundant, while pebbles of the older rocks are rare.

There are several Tertiary outliers on the high Chalk-plateau
between the Misbourne and the Wye. One of these, to the west of
the village of Penn, near Beaconsfield, rises to the height of about
600 feet, and is capped by a well-marked bed of Westleton gravel
like that on Tiler’s Hill, while another gravel (Glacial ?), derived in
part from the Westleton Shingle, lies on the Chalk-plain at Penn (547
feet) and Penn Common. At Lane End (600 feet), four miles west
of High Wycombe, there is also an outlier of Lower Tertiary sands
and clays, capped by a similar gravel of flint- and white quartz-
pebbles, subangular flints weathered white, with a few old-rock-
pebbles (see Pl. VII. fig. 1).

South Oxfordshire.—-From the borders of Buckinghamshire to the
Thames between Pangbourne and Wallingford there are but few
Tertiary outliers. ‘The most conspicuous of these is that at
Nettlebed hill*. The Westleton Shingle (?) there attains its highest
level of about 650 feet. It 1s but a small patch, and presents a less
definite composition than the others, as might be expected from its
distance from the main body.

The shingle, which reposes upon a very uneven surface of the
Lower Tertiaries, consists approximately of :—

per cent.
1... Dertiarydlint=pebbles) eure BUR. 2 titles kt eC eee ee 54.
2. Small pebbles of white quartz...............04. te ide otk ok Se 14
3. Subangular flints, mob stained. san. aisdencct <esinestpess nacre sedeeeee 20
A oe CWCET RIC L) temss oricn.as semades tapmiean cans ctpe a kack Geldan oh ate io ee ee 4
5. Pebbles of hornstone (?), veinstone, and Sarsen stone...........+ 8
100

imbedded in a matrix of light quartzose sand.

Five miles S.W. of Nettlebed, and close to the edge of the Chalk
escarpment overlooking the plains of Oxfordshire, a thin outlier of
Lower Tertiaries (the mottled clays of the Reading Beds) overlies
the Chalk at Greenmoor hill (560 to 600 feet) and Woodcote
Common, about 3 miles east of Goring. It is capped by a well-

Fig. 12.—Section on the hill above the Thames, near Goring:

c. Westleton Shingle. | T. Lower Tertiaries.
b'. Glacial Gravel. | ©. Chalk.

defined bed of Westleton Shingle, which is in marked contrast with
the Glacial gravel, with its New-Red-Sandstone quartzites, which sets

* Described in Quart. Journ. Geol. Soc. vol. x. p. 89 (1854).

WESILELON BEDS 10 THOSE OF NORFOLK, ETC. 141

in near Coomb End at a short distance from it westward, and at a
level of about 100 feet lower (fig. 12). This is the most distant
outlier in this direction, and from its position on the edge of the
Chalk Downs overlooking the Great Oolitic plains, possesses more
than usual interest (see Pl. VII. fig. 1).

The shingle forms an ochreous sandy gravel, consisting largely of
subangular flints much worn, flint-pebbles, and with none of the
New-Red-Sandstone quartzites so common ind’, I noted at the
time that it is much like the gravel on Bowsey hill (i/rd).
Approximately it was composed of :— .

per cent
1. Tertiary flint-pebbles, of which some were broken ............+.- 44
NENT er QUST EZ PEDDICS vote. ts oecpiecreswiveguececesevcesessrcuesevscsae 10
3. Subangular and angular pieces of flint ................ce sees ee eee 30

4. Subangular pieces of Sarsen stone, of a hard dark sandstone,
and of ironstone (Tertiary) ..... so gb bdk tong: ae ASSAM aES ee APC
5. Flat ovate pebbles of light-coloured quartzite, with small pebbles
of Lydian stone (?), and of a quartz-grit. ..............ceeceeee oe

I failed to note thee Chert or Ragstone.

A few miles to the south another Tertiary cae extending
from Chazey Heath to Rose Hill (300 to 350 feet) is capped, but not
very distinctly, by a light-coloured gravel very similar to the above,
while the intermediate and lower areas are overspread by the Glacial
gravel, but Boulder-clay is absent.

Further to the south, as we approach the Thames, the valley-
gravels set in and continue to the Berkshire side.

Berkshire and Wiltshire-—Between Reading and Maidenhead *
the broad valley of the Thames, with its Post-Glacial gravels,
becomes greatly contracted between Henley and Marlow by the
high ground of Cookham Dean (350? feet) and Bowsey Hill, which
is 467 feet high, or 350 feet above the Thames at Henley. The
former of these hills is bare to the summit, whereas the latter is
capped by a light ochreous sandy and pebbly gravel, from 5 to 8
feet thick, of a characteristic Westleton type. The following are
its component parts, but I failed to note their relative proportion —

1. Tertiary flint-pebbles, some of them entirely decomposed.

2, Numerous small white quartz-pebbles.

3. Subangular fragments of flint, weathered white.

4, Very few subangular fragments of white ragstone and one of fossil-
iferous chert.

5. Pebbles of light-coloured quartzite, yellow sandstone, and rose- -coloured
quartz-grit, with some small pebbles of veinstone, Lydian or hornstone,
greenstone ?, and red and grey quartz.

The quartzites are not the red and grey quartzites of the northern
Drift.

* It would seem probable that the Thames at an early stage may have
flowed in a direct line from Twyford to Maidenhead, by way of ‘the valley of
White Waltham, which offers a low and straight course, instead of the circuitous
course it took in Post-Glacial times through the Henley and Cookham Hills.

142 PROF. J. PRESTWICH ON THE RELATION OF THE

The Berkshire Downs, which form the prolongation of the Chiltein
Hills of Buckinghamshire and Oxfordshire, rise above Streatly ard
Goring to the height of from 400 10 600 feet. In the line of the
Thames Valley there is a broad high terrace of Glacial Drift,
whilst at a little distance further from the river the Westleton
Shingle appears on a relatively higher level. The Glacial gravel
forms a terrace at Southridge, and between Basildon and Ashamp-
stead, at a level of about 400 to 420 feet, whilst the Tertiary outlier
at Upper Basildon is capped by Westleton Shingle. The Tertiary
outlier (350 to 3880 feet) north of Bradfield is also capped by a
gravel which may be of the same age.

The Chalk Downs of “Berkshire are much barer than those of
Oxfordshire and Buckinghamshire both of Tertiary outliers and of
Drift. The former are extremely scarce until we approach the
borders of the Tertiary basin near Newbury. Nevertheless it is
probable that the Westleton Shingle extended over this area, for I
found on the bare Chalk-hills above East Compton a pocket of
Tertiary Sands and Drift, with flint- and quartz-pebbles, &c.,—a
remnant probably preserved, like the Crag at Lenham, by the chance
circumstance of its being in a pipe or hollow in the Chalk.

To the north and north-west of Newbury there are several
erayel-capped hills, possibly of this date, such as Donnington
Common and the hill east of Basford. One of the most prominent
is that at the end of the spur of Tertiaries which extends north-
westward from Newbury to Wickham. This hill, whichis 560 feet
high and rises 100 feet above the surrounding Chalk-plain, consists
of Lower Tertiary strata (including the base of the London Clay) *,
and is capped by a bed of gravel, from 3 to 5 feet thick, composed of
flint-pebbles, with subangular flints imbedded in a quartzose sand
and grit very much worn. From its position and general cha-
racter | think it may be of Westleton age, but I have no note of
its exact composition.

The bare Chalk-plains of East Berkshire and Wiltshire offer scant
opportunities for determining the prescnce of the Westleton Shingle.
Except in a few rare instances denudation has swept these plains
clean of all but the superficial soil and trail. The higher Chalk-
hills near Baydon, 8 miles E.S.E. of Swindon, are, however, capped
by a gravel consisting of subangular flints and Tertiary flint-pebbles,
with some quartz-pebbles ; and a similar ridge to the east of Ogburn
St. George, on the north-east of Marlborough, is also capped by a
little flint-gravel with quartz-pebbles. .

Quartz-pebbles also occur in places in flint- drift on the hills about
25 miles south of Marlbororght. Patches of a pebbly drift again
occur on the higher points of the Chalk Downs at Bishopstone near
Shrivenham and at Liddington and Basdrop to the south of Swindon,
but they are very indistinct.

* Described in Quart. Journ. Geol. Soe. vol. x. p. 86 (1854).

t+ The Drift-beds of this district have been described by Mr. T. Codrington,
iit the Magazine of the Wiltshire Archxological and Natural History Society,
1865.

WESTLETON BEDS TO THOSE OF NORFOLK, EIc. 143

The last trace of such drift I have met with on these Chalk
Downs was on Monument Hill above Calne, where there are a few
scattered pebbles of white quartz, quartzite, chert, and ironstone,
with subangular flints and fiint-pebbles, but its exact relation is
uncertain.

a

3. Westleton Beds on the South of the Thames.

The Boulder-clay, it is well known, has not been found south of

the Thames, though some Pre-Glacial beds have a considerable
extension in that direction, and evidence of glacial action is not
wanting. Owing, however, to their isolation and want of continuity
the classification of these beds is attended with more uncertainty.
_ Kent.—In the north-eastern corner of Sheppey the cliffs at
Draper’s Point, there about 170 feet high, are capped: by a Drift
distinct from that which is spread over a great part of the higher
ground of that island. It consists of from 15 to 20 feet of yellow
sands with seams of clay and patches of gravel, the bottom bed of
gravel being from 1 to 2 feet thick, and composed essentially of flint-
pebbles of various sizes, of large subangular flints much worn and
stained brown, numerous small flint-fragments, and some very
small pebbles of quartz, and at one spot I found a much worn
fragment of brown chert.. It is not improbable that these beds
are of Westleton age. They are overlain by a flint-gravel in small
pockets.

I know of no other bed of this character in Kent, except one
between Shottenden Hill and Sellings (400 feet), where there is a
sprinkling of Drift consisting of Tertiary pebbles and pebbles of
quartz. But both these cases are obscure.

Ido not refer the shingle on the top of Shooter’s Hill or the
gravel on Swanscombe Hill to this horizon.

Surrey and Hants.—Further westward traces of the Westleton
Beds become very indistinct. There are remnants of a quartz-drift
at Englefield Green (264 feet) and on some adjacent hills ; but it is
another Pre-Glacial high-level gravel-drift (see Part III.) that
prevails almost exclusively in this district.

4. Possible Extension of the Westleton Shingle beyond the
Thames Basin into Somerset.

Passing from the Chalk Downs to the Oolitic Hills further west-
ward, there is at one spot, Kingsdown near Bathford, about 550
feet high and 5 miles from Bath, a Drift of the Westleton
character. It forms only a small patch on the otherwise bare surface
of the Oolites, and consists of a light-brown sandy loam, with
slightly subangular flints, some flint-pebbles, many white quartz-
pebbles, and an occasional pebble of sandstone and of a greenish
quartz *. It is covered by a brown earth with local Oolitic débris,

* The Rey. H. Winwood, F.G.S., has since found a subangular fragment of
Sarsen stone and a pebble of black chert or hornstone.

144 PROF. J. PRESTWICH ON THE RELATION OF THE

The whole is only a few (5 to 8 feet) thick, and is preserved in a
trough or hollow in the Oolite *

Still further westward, on the Carboniferous-Limestone Hills
near Clevedon, Mr. Tetanee + has recorded the existence of a
patch of local débris with, I believe, quartz-pebbles, at a height of
300 feet above sea-level. This may be a continuation of the
Kingsdown Bed, but intermediate connecting-links have yet to be
discovered, and I was not successful in finding the place myself.

On the Chalk-hills to the south of the area we have described
there are a few outliers which may be referable to this geological
horizon, such, for instance, as the pebbly sands with worn fragments
of hard Tertiary sandstones on Windmill Hill, near Alton, and a
pebbly drift on the higher hills west of Andover; but these are too
indistinct to pronounce definitely upon.

_ A better marked case is the one on the Chalk Downs of Copford,
8 miles east of Warminster, where a large Tertiary remnant has
been preserved from denudation by having been let down into a
cavity in the Chalk. This patch of Lower Tertiary (white sands
and mottled clay) is overlain by an irregular spread of Drift con-
sisting of :—

1. Tertiary flint-pebbles—the larger proportion much decomposed, white

and very light.
2. White quartz- pebbles and a few rose- -coloured ones.

3. Worn fragments of a light-coloured sandstone (Upper Greensand ?).
4. Pebbles of a dark chert and Lydian stone.

These were imbedded in a light sandy matrix, and covered by a
sandy clay-drift full of angular flints; this pit at the time of my
visit was much obscured.

5. The Relation of the Westleton Shingle to the Glacial Drifts
of the Thames Valley.

We have thus been able to follow the Westleton Beds from the
coast of the Eastern Counties with some certainty as far as the
Berkshire Downs, and with some probability as far as the Bristol
Channel. On the Eastern coast this deposit lies at the sea-level,
but as it ranges inland it gradually rises to heights of 500 or 600
feet. In the first instance the Westleton Beds underlie all the
Glacial deposits ; in the second they rise considerably above them,
and their first seeming subordination to the Glacial series altogether
disappears (see fig. 1, Pl. VIL.).

The association, which is so close in Norfolk that it had led to the
two series being considered members of the same group, becomes
less so in Essex. At Braintree, where the Westleton Beds are
largely developed, they stand up through the Boulder-clay and
gravel which wrap round their base and partly surmount them.

* Mr.C. H. Weston, who first noticed this high-level drift, states also that
Chalk-flints mixed with Oolitic débris occur on the surface of Farleigh Down
at a height of about 600 feet (Quart. Journ. Geol. Soc. vol. vi. p. 449).

Tt Quart. Journ. Geol. Soe. vol. ix. p, 282 (1853).

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 145

They have there been disturbed and faulted (Pl. VII. fig. 6), before
the intrusion of the Glacial Beds, which have deeply eroded them.
As they rise to higher and more exposed levels, the Westleton
Beds become greatly diminished in importance and are commonly
reduced to a mere shingle-bed. On the hills near Epping, where
they attain a height of 350 or 400 feet, they form athin bed of sand
and shingle, capping the London Clay, and quite apart from the
Boulder-clay, which lies from 80 to 100 feet lower duwn on the slope
of these hills at Theydon Bois and North Weald.

In Hertfordshire the distinction between the two deposits is very
marked, as on the hills between Hoddesdon and Hatfield the
Westleton Shingle forms a plateau-gravel high above the plain of
the Lea, over which is spread the Boulder-clay with its associated
sands and gravel. At Bell Bar and Mimms Wood the hills are
also capped by this Shingle, while in the valley between them
the Boulder-clay in the railway-cutting is ata level of from 100
to 150 feet lower. The Boulder-clay again enters the valley of
the Colne at Bricket Wood and Aldenham, whilst Westleton Shingle
hes on the neighbouring heights of Shenley and Bennett's End.

Here the Boulder-clay ends, and the Westleton Shingle alone is
prolonged westward at intervals on the higher summits of the Buck-
inghamshire, Berkshire, and Oxfordshire Downs, the Chalk-plain on
which these hills rise being in some places denuded, and at others
thinly covered by Glacial Drift-beds. The Shingle-bed may, in
this way, be traced to the northern edge of the Chalk Downs and
to the extreme western end of the London Basin, which shows
how extensive the submergence of these districts must have been
at a time immediately antecedent to the Glacial period.

The height (500 to 600 feet) to which the Shingle-bed attains
is sufficient to carry it over the summit of the Chalk and Oolitic
hills of the Warminster and Bath districts. There may thus have
been a Pre-Glacial sea bounded on the south by the Wealden anti-
clinal, and spreading northward over great part of Hertfordshire,
Buckinghamshire, and Oxfordshire (and possibly beyond), while it
stretched in the other direction from the North Sea to the Severn
Basin or the Bristol Channel (see Part IL]. and Map).

6. Origin of the Shingle.

The distinctive features of the Westleton Shingle are of so marked
a character and so different from those of the overlying Glacial
series, that it is at once evident that their origin must be different.
The characters of the latter are so well known that it is unnecessary
to repeat them here; suffice it to say that they are essentially
Drifts from the north and north-east, whereas that of the Westleton
Beds is from the south and south-east, for the reason that the
sources whence the severe] different component pebbles are de-
rived is to be traced in those directions.

Thus :—1. The flint-pebbles are doubtlessly derived from the
shingle-beds of Diestian, Bagshot, or Lower Tertiary (Woolwich)

146 PROF. J. PRESTWICH ON THE RELATION OF THE

age, whether in Belgium, the North of France, or Kent. 2. The
Pebbles of white and rose-coloured quartz come apparently from
the older rocks of the Ardennes or indirectly from some of the
Bolderberg or Diestian beds of Belgium. 3. The subangular frag-
ments of flint, some retaining their natural colour, others more
worn and stained brown, are derived, the former directly from the
Chalk, the latter from an older Drift, possibly of Pliocene age; or
both may have been derived, in part, from the Southern Drift*.
4, The worn and subangular fragments of chert and ragstone are
derived from the Lower Greensand of Kent and Surrey ; or also,
in part, possibly from the “‘ Meule de Bracquegnies,” or indirectly
from the Southern Drift. 5. The Large Pebbles of a white or light-
coloured quartzite and of a flat ovate shape, unlike the red or dark-
coloured round ovoid quartzites from the Triassic conglomerates,
may be derived indirectly from the shingle-beds of the Woolwich-
and-Reading Series, where I have occasionally found them; or they
may come from quartzites of the Paleozoic rock of the Ardennes,
or possibly from both. 6. The small pebbles of Lydian stone, Jasper,
veinstone, and worn fragments of old rocks may be derived, some
directly from the Ardennes, and some indirectly from the pebbly
beds of the Lower Greensand.

It is obvious, from the fossils found in it in Norfolk and Suffolk,
that the Westleton Shingle is a marine Drift, the absence of
shells in its inland range being no doubt in great measure owing
to decalcification. Even in Suffolk, where the beds are more pro-
tected, it is rarely that anything more than casts are found.

But while marine conditions extended as far as the north of Bel-
gium, on the south the Ardennes formed an elevated area of dry
land, drained by the old Meuse and its tributaries as well as by the
Schelde. The lower range of hills bordering these valleys above Spa
and Liége are often capped by a terrace of gravel derived from the
quartzose and schistose rocks, hard sandstones, and conglomerates
of the Ardennes, Pebbles of quartzite, sandstone, and white quartz
are consequently the common constituents of these gravels; while
occasionally they contain fragments or pebbles of porphyry, slate,
and, very rarely, of granite. Generally the pebbles vary in size from
that of a marble to that of an egg, though they are sometimes the
size of a man’s head. Large blocks, but little rolled, are also occa-
sionally met with.

Such was the old alluvium of the eastern tributaries of the
Meuse, while on the terraces of the main stream at Dinant and Namur,
pebbles of Triassic sandstones, of Cretaceous, Jurassic, Carboniferous,
and Devonian rocks are met with, but a large proportion of them
disappear lower down the course of the river, and only the havder
rock-pebbles remain in its lower reaches. On the hill above Liége
I noted in the flint-gravel paleozoic-rock pebbles very analogous to
those found in the Westleton Shingle, namely :— _

* To be described in Part III.

WESTLETUN BEDS [0 THOSE OF NORFOLK, ETC. 147

(Angular and subangular fragments of flint ;)
White quartz-pebbles (numerous) ;
Flat ovate pebbles of light-coloured quarizites ;
Pebbles of light-coloured sandstones, veinstone, and subangular fragments
of a hard micaceous Sandstone, &c.,—
imbedded in a white and ochreous sandy matrix.

In descending the river the terraces become wider, and in the
neighbourhood of Maestricht they spread out into plateau-sheets of
great breadth, as in an estuary.

Another set of Drift-débris, including flint-pebbles from the Lower
Tertiaries together with débris from the Carboniferous and Cretaceous
strata, would be carried down by the Schelde, which flows through
rocks of that age; while the Khine may have furnished débris from
the rocks of the Rhenish Provinces, including possibly the basalt
of the Rhine borders.

This mass of shingle, transported into the open sea to the north
and aided by ice-action, drifted over to the coast of Norfolk
and Suffolk, and thence, as the land subsided, was carried west-
ward, in a direction towards the Severn Valley or the Bristol
Channel. What, then, turned it aside from the northern sea,
where it would seem it might have extended more northward as
the Crag did* at the period immediately antecedent ? Could it have
heen that the great Scandinavian ice-shect was then ploughing its
way across the sea towards the coast of Norfolk, and so blocked up
the sea in that direction and diverted the waters of the North
Sea through this westward channel ?

On the south, the spread of the Westleton Beds was limited by the
anticlinal of the Ardennes and the Weald, which then constituted
a low mountain-range, for there are no marine beds of that character
south of the line I have described. At the same time paleonto-
logical evidence of contemporaneous land conditions is very scanty.

In recent papers by the Rev. O. Fisher f+ and Mr. J. C. Mansel-
Pleydell, F.G.S. ¢, we have accounts of the discovery of the remains
of Elephas meridionalis on the Chalk-plateau at Dewlish, near
Piddletown, in Dorsetshire, in a bed of sand and gravel 90 feet
above the level of the adjacent stream. The facts of the case led
Mr. Fisher to suppose that the deposit might be Pre-Glacial, while
Mr. Mansel-Pleydell considered it to be of Pliocene age.

It is possible also that the high-level fossiliferous Drift on the
summit of Portland §, which contains débris derived from the Ter-
tiary and Cretaceous strata of the hills to the north of Weymouth,
may be of the same age, and older than I was first led to believe
on the evidence of the sparse remains of Elephas antiquus, FE. primi-
genius?, and Equus fossilis. This view of the greater antiquity of
that deposit would be more in conformity with the enormous amount
of erosion, probably of Glacial date, that led to the formation of

* Mr. T. F. Jamieson, F.G.S., has shown that Crag-beds exist on the east
coast of Scotland (Quart. Journ. Geol. Soe. vol. xvi, p. 371).

+ Quart. Journ. Geol. Soc. vol. xliv. p. 818 (1888).

t Trans. Dorset, vol. x. p. 12 (1889).

§ Quart. Journ. Geol. Soc. vol. xxxi. p. 31 (1875).

148 PROF. J. PRESTWICH ON THE RELATION OF THE

the broad valley between Portland and Upway, above six. miles
wide and from 400 to 500 feet deep, since the deposition of that
high-level Drift.

Dr. Mourlon has also recently recorded * the occurrence, at
Ixelles near Brussels, of a bed of sand and gravel with Mammalian
remains, which he thinks may be of the age of the Forest-bed ; but
the evidence is yet uncertain, owing to the fragmentary condition
of the specimens. Amongst the species on which Dr. Mourlon
relies, but which are determined with doubt, are Hlephas antiquus,
Equus plicidens, Cervus canadensis, and Bison priscus.

ConcLUsION.

It is clear from its uniformity and its marine origin that the
Westleton Shingle must originally have formed a comparatively level
sea-floor (or broad coast-line) throughout the area over which its
outliers extend, and that all the inequalities of the surface below
that level have been formed since it was deposited. If this con-
clusion be correct, then it follows that all the Tertiary strata, which
-spread originally over all the Chalk Downs of Hertfordshire, Buck-
inghamshire, Oxfordshire, Berkshire, Wiltshire, and some adjacent
districts, have been removed subsequently to this early Pleistocene or
so-called Pre-Glacial period; also that the gorge of the Thames at
Pangbourne and Goring has been formed since then ; and that most
of the Pre-Glacial valleys in the district, to which no date, except
that they were Pre-Glacial, had been assigned, are of the same geo-
logical age. It follows further that before this date the Thames
had no existence; to this point we shall revert on another occasion.

During the Westleton period, we have to imagine a sea, with a
coast-line extending from Belgium to the West of England, bounded
on the south by the anticlinal range of the Wealden, and open to a
yet uncertain distance to the north. ‘This area then underwent an
elevation from east to west, and from south to north, whereby it
was raised at the extreme points from 500 to 600 feet or more above
the sea-level, whereas it remained nearly at its original level and
comparatively undisturbed at its other or eastern extremity; so that
while on the east the chronological orders of succession of the strata
continued unbroken, to the west they became discordant, in conse-
quence of the physiographical changes which intenreued between
these successive stages.

These changes fp the action of meteorological agencies on the up-
raised land, determined the plotting-out of its hills and valleys during
the early Glacial epoch. Of the first stage we have now, in some
cases,an exact measure. Thus, to take a few examples, it is obvious
that at the gorge of the Thames at Goring the Westleton Shingle
and Tertiary Strata were continuous from side to side of the valley
until the last elevation of the land. As they emerged, and a
land-surface was formed, these beds, together with the underlying
Chalk, were first denuded in the line of the present Thames valley

* Bull. Acad. Roy. Belgique, 3° sér. vol. xvii. p. 131 (1889).

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 149

to a depth of about 160 feet, and a width of from 2 to 4 miles, when
the newly made channel received its covering of Northern Drift
(2, fig. 13).

The successive increments of depth *, acquired during the different
periods, are exhibited in the following section (see also fig. 12),

Fig. 13.—Diagram-section across the Gorge of the Thames through
the Escarpment of the Chalk at Goring.

3
Se eo sea anda Sone nee eae een en enone —— es
4 Ses i zs...
SSS ii Al Sin a Rh 2 = |
——— =, |
5 —E—————’ B =
SST Oe rr = ——7 i
a — /
1. Post-Glacial Drift. | 4. Lower Tertiary strata.
2. Glacial Drift. | 5. Chalk.
3. Westleton Shingle. |
feet.
A. Denudation during the early Glavial Period ...... about 160
B. Denudation during the later Glacial Period ...... so, 220
C. Denudation during the Post-Glacial Period ...... Baa iw.

Taking the height above the sea-level of the Westleton Beds here
at 600 feet, and that of the river at Goring at 150 feet, the
above figures give, but very approximately, the depth to which the
denudation of the valley at this place was carried during the succes-
sive Glacial and Post-Glacial epochs.

The relative depths of B and C may be subject to considerable
correction. In the absence of sufficient evidence at Goring, I have
been guided by the height of the high-level river-gravels at Oxford
and Reading, where they are better developed.

These measures, of course, vary at different places. Lower down
the Thames Valley, the channel A above Henley-on-Thames
(Bowsey hill giving the Westleton level) is above 200 feet deep,
while B is reduced in proportion.

In the valley of the Lea, at Ware (fig. 14), taking the level
of the Westleton Shingle at Hertford Heath on the south at 316
feet, and at Sacombe Green on the north at 362 feet, and that of
the Lea at 110 feet, A and B together seem to amount, in round
numbers, to about 200 feet, whilst C does not seem to exceed 50 feet.

In the valley of the Roding the level of the Boulder-clay is
about 100 feet below that of the Westleton Shingle, at Jack’s Hill,
near Epping, whilst the extent of C is probably less than 30 feet.

Other instances might be mentioned, but these will suffice to
show some of the stages in the denudation of this area and the
initial step in the formation of its river-valleys. It will appear,
from these facts, that the main denudation of the district has been
effected after Pliocene times, and that the first stage (A) in the
formation of the present gorge at Goring dates back to the time of

* These hold whatever may be the age of the shingle.

150 PROF. J. PRESTWICH ON THE RELATION OF THE

Fig. 14.—Diagram-section of the Valley of the Lea at Ware.

b", Glacial sands and gravel with T. Lower Tertiaries and London
Boulder-clay atx. Clay.
c. Westleton Shingle. Ch. Chalk.

A B. Denudation during the Glacial Period.
C. Denudation during the Post-Glacial Period.

the emergence of the Westleton floor and is due to early Glacial
action. To what extent the subsequent denudation (B) is due to con-
tinued glacial action it is difficult to say; but as the gravel-bed
No. 2 (fig. 13) belongs to one of the earlier stages of the Glacial
period, and Post-Glacial river-action (C) is hmited to narrow bounds,
there is reason to infer that the valley to about the base of B is
due to erosion during the Glacial period.

The position of the Westleton Shingle enables us also to suggest
a solution of another question, namely, that relating to the age of
the great escarpments of the Chalk and Oolites which run through
the centre of England. ‘The fact that the Westleton Shingle caps
various Tertiary hills on the Chalk-plateau, which Tertiary strata
extend to the edge of the Chalk-escarpment, renders it probable
that this Shingle had, before the denudation of the Tertiary strata,
arange to acertain extent coextensive with that of the Tertiary
strata, and extending further northward than at present. This
is manifested by the presence of the Shingle on an outlier so near the
escarpment as Nettlebed Hill, and still more by the outlier on the
very edge of the escarpment at Woodcote. Consequently, if, as
this would show, the Westleton Beds had a range over and beyond
the escarpment, the origin of that escarpment must be of a date
subsequent to that of the Westleton Beds (Pl. VII. fig. 1).

Another argument is, I think, conclusive. The terraces of
Glacial gravel (No. 2, fig. 18) which flank and originally spread
across the gorge of the Thames at Goring at the height of 440 feet
are evidently connected with the outlers capping the Coralline
Oolite at Foxcombe and Wytham Hills near Oxford, at a height of
about 500 feet, and which, again, cap the Forest Marble and Great
Oolite on the higher hills of Wychwood Forest, near Witney. At
the time that this spread of gravel took place, the intervening
valleys must have been bridged over by a flooring of Cretaceous
and Jurassic strata, which have been since removed and denuded
to the depth of from 300 to 350 feet, as shown in the following
diagram (fig. 15).

If, therefore, the channel through which the Glacial Drift
passed from the north into.the Thames Valley was formed, as
we suppose, subsequently to the spread of the Westleton Shingle,
but before the deeper late Glacial erosion, then it is evident that
as the valley at the foot of and giving rise to the escarpment could

WESTLEION BEDS TO THOSE OF NORFOLK, XTC. 151

have had no existence at that time, the base of the escarpment
must have been limited by the level of the line of 440 to 500 feet.
By analogy the further relative heightening of the escarpment was
concurrent with the deepening of the valley itself, which would
correspond with Bin fig. 15. In any case the escarpment could not

Fig. 15.—Diagram-section from the Gorge of the Thames at Goring
to the Oolitic hills (J) near Oxford.

2. Glacial gravel with Triassic, Cretaceous, and other rock-débris. mm. Position
of Tertiary strata and of Westleton Shingle (outside the section).
Cr. Cretaceous strata. J. Jurassic strata. (See also fig. 15, p. 149.)

at that early Glacial period (A) have had a face more than from
100 to 150 feet high, while at the Westleton period it is more
than probable that it formed, with the distant Oolitic hills, a con-
tinuous plain (x).

Of the escarpment of the Oolites one can speak with less certainty,
though if we admit the Kingsdown Drift outlier to be of Westleton
age, it favours the conclusion that the escarpment of the Oolites
dates no further back than the commencement of the Quaternary
or Pleistocene period. The fact likewise that the two escarpments
run in parallel lines seems in favour of a common denuding cause
in the same direction. The time, geologically measured, is, however,
so limited, and the extent of denudation so vast, that it is not
easy to realize that these limits can suffice. Nevertheless, I do not
see how the conclusions we have arrived at on this subject can well
be avoided.

Another point to which I would draw attention is the small
amount of erosion by river-action (C) in the area under review,
compared with that effected by glacial or other agencies. To the
latter are due the broad plains and passes and the isolated hills,
whereas the effects of the former are limited to the valleys of com-
paratively moderate depth and width, which have been subsequently
-cut through the glaciated and deeply abraded land.

EXPLANATION OF PLATE VII. (see also Map, Pl. VIII.).

Diagram-sections of the Hill-Drifts of Pre-Glacial date in the Valley of the
Thames within the Chalk-basin. Owing to the length of these sections and the
limits of space the vertical scale is unavoidably exaggerated. In Fig. 1 it is
not so important, as the gradients of the Westleton Shingle and Boulder-clay
bear a tolerably uniform relation one to another; but in the other figures it
misrepresents the incidence of level between the several Hill-Drifts, for which
allowance must be made. The relative height of the hills and depth of the
valleys are, however, on a true scale, and this is the essential point connected
with the question. These are taken from the new 1-inch Ordnance Maps.

Q.J.G.8. No. 182. M

PROF. J. PRESTWICH ON THE RELATION OF THE

Fig. 1. Section from Oxfordshire to the coast of Suffolk. The length of this

section is about 140 miles. The dotted lines prolong the levels of
the Westleton Bed and Boulder-clay, and serve to indicate the
extent of denudation which has taken place since each of these epoclis
respectively.

. Section, about 50 miles long, passing from Hindhead through the Bag-
shot district and across the Valley of the Thames, near Windsor, to
the borders of Hertfordshire.

. Section from the edge of the Weald across the Norwood Hills, the
Thames at London, and the Tertiary hills north of London, to the
Valley of the Lea near Hatfield: distance about 40 miles.

bo

Se)

_ +. Section from the Valley of the Medway, near Tunbridge, by Cobham,

near Rochester, across South Essex to the Brentwood group of hills:
distance about 36 miles.

Railway-Cuttings.

. 5. Section of the Great Hastern Railway, through Brentwood Common.

This cutting was of greater depth; only the upper 40 feet are represented
in the figure. ‘The surface is 360 feet above O.D.

A. Boulder-clay of a dark grey colour, containing fragments and small
blocks of chalk, sandstone, Jurassic rocks, angular flints, and flint-
pebbles, with a few specimens of Gryphea incurva and a species of
large Oyster. Hastward, it passes into a sandy bluish-green clay with
flint-pebbles, and then into a brownish clay, roughly laminated and
without pebbles. It has a maximum thickness of 30 feet.

A', Sand and gravel, consisting chiefly of flint-pebbles. ‘The sand contains
thin subordinate layers of grey and brown clay.

(1. Fine white sand passing into bed No. 2. ............... 10
2. Ochreous and ferruginous, sandy, with some iron-
SANGStOMC® - Late ssceeee odie anne te ureometines <tc aeee taeeen a
3. The upper part of this bed consists of a tough brown
laminated clay, with grains of green sand and a few
patches of white micaceous sand, passing down into
a massive argillaceous dark green sand, with some
lighter seams. This bed contains numerous small
Lingule, with casts of various bivalves in iron-
pyrites, teeth, and vertebrze of Shark and Carcha-
rodon, and fragments of wood pierced by Teredo... 16 to 20
4, Fine light-yellowish sand, interstratified with thin
irregular seams of laminated dark-grey clay.
Traces of carbonaceous matter. No fossils. This
bed varies in thickness, resting on an uneven surface
\ of the London (Clay |. .J/sis..idbestten. one reteseeenccwes 4 to 12

D. Lower Bagshot Sands.

Ra a I

E. London Clay: dark grey with grains of green sand and concretions
of iron-pyrites. Only traces of fossils.

ge. 6. Section of the Black Notley Cutting on the branch line from Witham

to Braintree. This fine and typical section was about half a mile in
length, and about 25 feet deep in the centre.

A. Boulder-clay containing numerous large angular flints and chalk-pebbles ;
it passes from dark brown to a whitish colour,

A’. Boulder-clay gravel, very coarse and much contorted. It consists
chiefly of subangular flints, pebbles of flint and white quartz, of dark
quartzite and sandstones. The upper part is of a dull brownish-white
colour, whilst the lower part is dashed with ochreous, ferruginous,
and black seams and streaks, passing in places into a dark ferruginous
CUMIOMORALS: «5 csspsancasengtnn pe cnevs guns ee sickanas Mien Ppl Menate 5 to 10 feet.

WESTLETON BEDS TO THOSE OF NORFOLK, ETC. 153

B. Fine sand and shingle, horizontally stratified, and in places obliquely
laminated. It consists essentially of sand, with subordinate seams of
shingle, composed of small flint- and white quartz-pebbles with’ some
subangular flints. The upper half of this bed is ochreous, and coarser
than the lower half, which is of a light yellow colour with faint
ochreous seams. It is traversed by a few small faults of from 3 inches
PemMREEER PINON USAW S) fa chon Wc ckiaiedeky andin om ivneis oad nnewin ce ocielnaenee 15 feet.

Fig. 7. Section between Chapple and Mark’s Tey on the branch line to
Sudbury.

A. Dark grey Boulder-clay, divided into an upper chalky and _light-
coloured bed, and a lower one of a dark bluish-brown colour. 14 feet.
B. Sand and gravel; the upper part coarse and ferruginous, the lower
part white with ochreous seams and regularly stratified ...... 10 feet.
E. London Clay with seams of Septaria. This cutting is from 20 to 25 feet
deep. At the time of my visit the central part was but just com-
menced, and is filled in from inference afforded by the trial-holes only,

Vig. 8. Section on the Railway at Kyson, one mile South of Woodbridge.
The Boulder-clay does not show in the Section, but crops out a little
higher up the slope of the hill, above B.

a. Trail of loam and gravel.

feet.
B Wrest- 1. White sand, full of small flint- and white quartz-pebbles,
dobina subangular flints, chert, &c. (see p. 125) ............ceeee 2
ee ey eotke ana Met yellow SANA. ...cc.0csecescsouisaeedessesceaes-oed ]
(1. Bright yellow sand, with occasional oblique lamination,
MMPS ab aie tnee nen somscacyeanensid sates ecdtedereswsne 10
2. Coarse sand, much oblique lamination, shells in local
C. Orag. 4 SL CTRGLIVESS 08 Oey ee ern er eee eee eee )
‘ 5° } 3. Red Crag; very fossiliferous at the west end of the cutting,

but fossils scarce at the east end. At the base is a thin
bed of Coprolites, on a denuded floor of London-clay
\ Rie RIM PN Pave ct steht Wee shea boceh gach eae u stele sciedstececseoees 12
E. London Olay.

Discussion.

The Prestpenr said that a paper of this kind was the result of
enormous observation and very careful reasoning. ‘There was one
point which had occurred to him: if the Westleton series were
marine, either the whole area had been depressed uniformly, or
there had been a greater depression to the westward. On the first
hypothesis, thicker marine strata would probably have been found
to the eastward and westward, and in the latter case it was remark-
able that no marine beds of this age were found on the Western
coast. He had no doubt that the Author had carefully considered
the possibility of the subaerial origin of these beds before rejecting it.

Mr. Torrey called attention to the section at Hertford Heath, and
asked whether the composition of the beds was not peculiar. The
evidence as to the southern origin of the pebbles he considered
very important. If the older beds and the Westleton Beds are com-
posed of Southern Drift, they are sharply marked off from the
Glacial beds. A section exhibited from Hindhead to Windsor was
of interest as bearing on the relation of these beds to the Chalk
escarpment and the Weald. The escarpments might possibly be

M2

154 RELATION OF THE WESTLETON BEDS TO THOSE OF NORFOLK, ETC.

older, and the Westleton Beds have lapped over them. Even if older
than the escarpments, the beds were evidently newer than the
elevation of the Weald.

Prof. Hueuss pointed out the difficulty of correlating unfossiliferous
and variable beds when they were separated by considerable intervals.
He thought that movements along the Weald-axis and affecting
all East Anglia had occurred many times down to a late age. The
Glacial beds rest quite irregularly on the higher- and lower-level
gravels of Hertfordshire. he Hertford-Heath beds had, he believed,
nothing to do with the Glacial deposits, but that between them there
had been an elevation, denudation, and resubmergence of that area,
and that the ingredients of these beds might have come from the
north and west. The pebbles became smaller, tracing the stones from
Hertford Heath to Hampstead, where he recognized two Pebble-beds,
the upper with quartz being the equivalent of the Hertford-Heath
beds, and the lower being the Bagshot pebble-bed. He had traced
them along the top of Epping Forest also, and would look for them
- on the North Downs. The Sheppey gravel was an angular one,
and different from that of Hertford Heath; whilst there was a
gravel near Chatham on the mainland opposite Sheppey of different
origin, being the deposit of a stream flowing northwards from the
Weald. He shared the general regret that the Author was unable
to be present, especially as he could probably have cleared up some
of these difficulties either by reference to parts of the paper which
had not been read or by supplementary remarks.

Mr. J. Atten Brown had collected rocks from the high-level drifts
of the Thames valley, and there was no doubt as to the occurrence
of southern drift therein, though the northern drift preponderated.

Mr. Monckton agreed with the criticism of Prof. Hughes. There
is a considerable break in the continuity of the proposed Westleton
Beds north-east of High Beech, Essex.

The East-Berkshire plateau-gravels were shown in one of the
diagrams; they were very different from the High-Beech gravels—-
quartz was, for instance, very rare in them, and he had placed on
the table the only large block of quartz he had found in them.

Dr. Irvine was sceptical as to the identification of the Berkshire
gravels with those of Essex and Suffolk. The Author appeared,
since his York paper, to have altered his views as to the date of the
upheaval of the Weald. He was in accord with Prof. Prestwich
as to a certain amount of glacial erosion, by which he meant
the work done by floating ice. He believed that the plateau-gravels
were themselves fluviatile and of much older date.

Mr. Marr stated that if the paper had been read in full many of
the questions raised by the previous speakers would have been
answered.

Southwold.

$
RS 8
=

SS

»

/ py)

SSS:

SS

SS

Geol. Soc. Vol. XLVI.PL VII

ad
SS

Journ

‘S)

vA

Quart

Ct aoe,
.

Ae
bi eA
Oe a ft
Car atG es
OSE
Bees
ee &
© tetek
FES YZ
Ae la

‘
Ls
Wy

Quart. Journ. Geol.. Soc. Vol. XT.VIPL. VII.

Map OF THE PREGLACIAL DRIFT BEDS OF THE & ~
BASIN OF THE THAMES.

@ Westleton Beds.
@ Brentwood Pebble Bed
© Southern Drift.

|. Crig Beds. 4. Upper Greendsand & Gault. BE
2. Tertiary (Eocene). ~ 5. Lower Greensand. NE
3. Chalk. 6.Wealden, or Jurassic. F ‘
=== Southern boundary of the Boulder Clay.
----Tanes of Section (PU.VIL)

-— =
2g :
\S
£

& —
a —

3
Chosham2_|\
~s

Wycombe
AAO

. S VX SS a»
WS

Wy
’

\y

, aD ¥sSY SS SSSA fern
J lariborouwg Sv ternnet BRU)? S SR S Le /
o> Se | oro 8 we x 2g R\ "2a, as = y

Mersthia:

SAN
KIN

cae ry. Se

ON THE DRIFIS OF THE THAMES VALLEY, ETC. 155

10. On the Retation of the WusrLeron SHINGLE to other PRE-GLACIAL
Drirts in the THames Basin, and on a SourHern Drirt, with
OBSERVATIONS on the FinaAL ELevation and Inir1aAn SuBAERIAL
Dernvpation of the WEALD: and on the Genesis of the THAMEs.
By Josrru Prestwicu, D.C.L., F.R.S., &c. (Read February 26,

1890.)
Pan TE,
Tae SourHern Drirt.
[Puate VIII.]
Page
1. Distinctive Characters of the Southern Drift ...................6 155
2. Its Distribution in Kent, Surrey, Hampshire, Berkshire,
re EAD MEME NE ae were het reves atcracasslstete sed dsstenencss 156
3. Other Pre-Glacial Hill-Gravels: the Warley and Brentwood
Reearan ree hehehe et ue Poel ind OK. cdi <4 Pakdudedunsesacees 162
4. Early Physiographical Conditions of the Wealden Area......... 166
ROME OL TAS SOULROIM Drift... .0-cecsccceecereceratsccaeeccossnese 168
6. Relation of the Southern Drift to the Westleton Shingle and
fe Ee evACIAL DRILLS, 5... 22cccccasscrncsecaesrasscbiPerestccserets 174
7. Main Lines of Elevation and Drainage of the South-east of
Bugland -) Genesis of the Thames ..c..c00dserscessscceasececsssee 176
STS MUUNGATG, oe coir «le wcsiow soci arahsisien cs tnasacinaneciacaadsacccwunses 178

1. Distinctive Characters of the Southern Drift.

Taine the strata in their order of succession, this paper ought to
have preceded the last, but for the fact that for the purpose of
classification it was essential to have a base-line of which the posi-
tion had been previously determined, such as that offered by the
Westleton Shingle, before the relation of the other pre-glacial Drift-
deposits in the Thames Valley to one another and their relative age
could be established. It is for this object that I attach importance
to the Westleton Beds last described; but besides these, which are
confined almost entirely to the north side of the Thames, there is
another closely allied hill-drift, which I propose to call the “* Southern
Drift,” of more limited range and confined chiefly to the south side
of the Thames. I at first thought it possible that they might be
synchronous *, but now I have come to the conclusion that the
Southern Drift is the older of the two, in the sense afterwards to be
explained. Both of them are so restricted to outliers, often very
small and far apart, and have been so much encroached upon by
Glacial Drifts of later date, that the relation they bear to one
another is generally much obscured.

The leading points on which we have mainly to depend are the
relative levels and the differences in the character and origin of
the rock-fragments and pebbles composing the two deposits, and in

* Much hinges upon their relative levels. These I had originally taken with
an aneroid barometer, but the new 1-inch Ordnance Maps have now furnished
me with the more accurate data required.

x

156 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

the proportion and condition of those which are common to
both. For example, the Westleton Shingle is, as before men- .
tioned, characterized by the constant presence of numerous peb-
bles of white quartz with a few small pebbles of Lydian Stone,
Jasper, and others of old rock origin, and some pecular larger
quartzite-pebbles ; whereas a similar abundance of quartz-pebbles
is wanting in the Southern Drift, which, on the other hand, is cha-
racterized by a large though variable proportion of worn frag-
ments of chert and ragstone—not that these are wanting in the
Westleton Shingle, but they are in less abundance, more reduced, and
hold a more subordinate position. ‘The materials common to both,
but present in different proportions, are subangular flints and flint-
pebbles; while the absence of quartzite-pebbles derived from the
Triassic rocks of Central England equally stamps both, and is one
of the marks of distinction from the Northern Drift. The Westleton
beds also had a marine origin, whilst the other seems to have been
formed in great part ander subaerial conditions.

The followins are the component materials of the Southern rit,
taken in the order of their relative abundance, and with the sources:
whence derived :—

1. Angular and subangular feipionts of flint, some retaining
their natural colour, others much worn and stained uniformly of a
deep warm brown eolour. The tormer are derived directly from
the Chalk, and the latter from an older Drift, the location of which
is still uncertain (probably Diestian). 2. Pebbles of flint derived
from the Lower Tertiary strata of Kent and Surrey, which formerly
extended over the Chalk-area more generally and also further
southward. 38. Subangular fragments in very variable proportions,
and more or less worn, of chert and ragstone, derived from the
Lower Greensand of Kent and Surrey. 4. Occasional small pebbles
of white quartz (smaller and more opaque usually than those of the
Westleton Shingle), derived, together with a few quartzites and
some old rock-pebbles, from the Lower Greensand or from the
Wealden. 5. A few subangular fragments of ironstone-grit and
ironstone derived either from the Lower Tertiaries, the Diestian,
or the Lower Greensand. No organic remains have been found
in this Drift, of which the negative characters are the absence of
the white and often chalcedonic quartz-pebbles of the Westleton
type, of Triassic quartzite-pebbles, and of Jurassic débris.

2. Distribution of the Southern Drift.

This we will take, as in the former paper, in the order by counties.

Kent.—There is a considerable spread of very ferruginous sandy
gravel on the Tertiary hills of East Kent, consisting of subangular
flints with a small proportion of flint-pebbles. Although fragments
of chert are wanting, or extremely scarce, I think it probable that
the gravel on some of the higher grounds, such as Dunstead, the
hills west of Canterbury (250 to 300 ft.), and a few other of the
higher hills of the district, belongs to this Southern Drift, as it is

8 ——————————— = Cre rr
5 >

VALLEY AND 1TS RELATION TO THE WESTLETON BEDS, ETC. 157

much above the level of the Post-Glacial Drifts, contains no organic
remains, and is distinctly a plateau or hill-gravel.

It is not, however, until we reach the neighbourhood of Rochester
that the Southern Drift is found well characterized. It there caps
the wooded hill extending eastward, at a height of about 400 feet,
from the mausoleum in Cobham Park to within a mile of the Med-
way (see Pl, VII. fig. 4). Itis a coarse gravel, lying bare on the
surface, and consists roughly of *—

1. Subangular flints but little stained, with others more worn and | 3
Sete TAMIR DROW io... eee ceck egete sc dessaceeedeelaecteceses 5
2. Fiint-pebbles, some of them broken and white, with abraded
edges, and green-coated flints from the base of the Thanet +=
MA MN eet Se cri at aah. Woiplahiy a gittwuida bounty osdedincdegesh speene
5. Subangular fragments of chert and ragstone from the Lower } 1
Greensand, and a few pieces of iron-sandstone .................. } 5

—_

There is an absence of white quartz-pebbles.

Traces of similar gravel occur a few miles to the south of the last,
on the hills between Halling and Punish Farm, near the edge of
the Chalk-escarpment.

On the high Chalk-plateau between the Medway and the Darent
there is in several places, namely at Ash, Fairseat, Plastal Green,
Wrotham Hill, Cotman’s Ash, Bower Lane, and others, a thin sprink-
ling of this old flint- and chert-drift. But there is no bed of it, —
except on the isolated Tertiary outlier at Swanscombe Hill t, 33 miles
north of the main Chalk-plateau, where it forms a small patch, 316
feet: above the sea-level, and almost identical in composition with
the gravel on Cobham Hill.

A much more important bed of this character is one which I
met with long ago on the summit of Well Hill, near Chelsfield, a
ridge from 550 to 600 feet high, forming the water-shed between the
Darent and the Cray, and extending about one mile from south to
north, with a width of only a few hundred feet. This bed of gravel
is from 5 to 12 feet thick, very coarse and unstratified, and consists
mainly of ;—

1. Subangular flints, many of them very large and very much worn,
and having the interior texture altered to an opaque white or brown
colour ; with a fewsmaller ones stained brown on the outside, and still
more worn.

2, Numerous flint-pebbles (some of them broken and worn) from the
Woolwich and Reading Beds, and a very few green-coated flints from
the base of the Thanet Sands,

3. A very small number of subangular fragments of chert and ragstone.

4. A few rare flat ovoid white quartzites.

The whole imbedded in ochreous quartzose sand and clay. This
Drift rests on an uneven surface of Lower Tertiaries, which forms an
outlier rising above the surrounding Chalk-plateau, see fig. 7, p. 170.

* The relative proportions vary so much in different localities that it is not
necessary to describe it very closely.
+ I have described this bed in Quart. Journ. Geol. Soe. vol. xlv. p. 291 (1889).

158 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

Though Lower Greensand débris is extremely scarce in this
gravel, there is, lower down (500 feet above O.D.) on the south side, ©
and resting on the Chalk-plateau, at a spot above the railway-tunnel
opposite Colegate Farm, a small patch of gravel composed in large
part of fragments of chert and ragstone. Another small patch caps
the hill with the clump of trees (366 feet) just north of Lullingstone
Park.

More recently, I have discovered a bank of this gravel, very coarse
and with much chert and ragstone, some of large size, on the slopes
of the hill on the left bank of the Darent, between Eynsford and
Farningham. There it does not cap the hill, but extends on its
slope from 250 feet nearly to the summit at 350 feet. It is not
worked, but, being bare, is easily examined.

Thence westward to the borders of Surrey I know of no well-
marked body of this gravel (unless a sprinkling of flint-gravel on
the top of Red Hill near Chislehurst should be grouped with it),
although here and there on the Chalk-plateau there is, as on the
downs east of the Darent, an occasional thin sprinkling of chert-
fragments and much-worn brown-stained flints.

Surrey.—Here it is on the Tertiary hills, and not on the Chalk-
downs, that we find the best exhibition of this Southern Drift. A
thin bed of it resting on London Clay caps West-Ho Hill, Norwood
(see Plate VII. fig. 3).

The following is a detailed section taken some years since :—

Fig. 1.—WSection of Gravel-pit on West-Ho Hill*.

\

1
Aue

ft. in
@. Suelace-sOW, oy csc cence ae eae eens aes ee a enueo sheer 2 “0
G, Ligaim'y Sravel Vion cnn res ater soot one aplons caepiee ies saci ti 0
c. Fine ochreous gravel with veins of grey sandy clay 1 0
d. Grey sandy clay .........scsceceeceacsececsencterscenenees 6
€. Yellow gravelly sands ........:cscecessseceeceeeeerseeces 2 HO
Ff. Guy samy selaiy ie Plescrittrta don bee sae cxvae as nopesp apples 6
G- Ochreous Sand .........seeeecenseereeneeceereeseeererencens Lis
Ah. Grey SANs. 10. vx.teasvers<ehatvienas cease os ovcsnceennere¥s 3
2.. Coarse OChTeous PYAVEl......65020-.-aecsescssveertennace 2 O+

* This pit is now probably built over.

VALLEY AND ITS RELATION 10 THE WESTLETON BEDS, ETC. 159

According to the one specimen I kept, this gravel consists of :—

1. Subangular flints, unstained and stained brown,—in largest proportion.
2. A considerable proportion of Tertiary flint-pebbles—some broken and
worn.

»%. About 10 per cent. of subangular fragments of chert and ragstone.

With one pebble of a hard sandstone or quartzite (Tertiary ?) and
one small pebble of quartz.

This gravel extends southward all along the top of this hill, at a
height of from 360 to 380 feet above O.D.

From the Norwood hills we pass westward over a lower tract of
country with gravels of later age, as far as Wimbledon Common,
which rises to the height of 183 feet above the valley of the
Wandle. It is capped by a Drift-gravel, about which I feel un-
certain. It has all the elements of the Southern Drift, but in
addition it contains quartzite-pebbles, which have the Triassic
characters. It is therefore either of Glacial age, or else a Southern
Drift invaded by a later Glacial Drift. It consists, in the order of
their relative abundance, of :—

. Subangular flints stained yellow.

. Tertiary flint-pebbles.

. Subangular fragments of cherty ragstone and of a yellow chert.

. Pebbles of white quartz, of dark quartzite, sandstone, and ironstone.

l
2

He Co

Imbedded in a ferruginous matrix of coarse worn quartzose sand.

The next hill to break the uniform level of the later Thames-
valley gravels is the isolated and conspicuous hill known as St.
George’s Hill, which rises 14 miles to the south of Weybridge to the
height of 245 feet, and is capped by a Drift-gravel much like that
of Wimbledon, but without the quartzite pebbles. I have less diffi-
culty, therefore, in referring it to the Southern Drift, although it
contains some small white quartz-pebbles, but these may be derived
from the Lower Greensand or Wealden. The gravel is composed
as under :—

per cent.

1. White and yellow-stained subangular flints ...............c cece ee ee 44 .
2. Tertiary flint-pebbles, some broken ................csccccesseeeasoesees 30
3. Subangular fragments of ragstone and brown chert ............... 15
See NY MIDE GZ LE DALE ss woceneae sca enMunnedan skew tncadawlesebseesnda eda’. 5
Br Pebbles Of FANGSHONE, ITOMStONE, GE, sc .s.seoncercecccscavcsevecssver 6
100

in a matrix of quartzose sand.

The greater part of the Surrey Chalk-Downs are bare, with the
exception of a few Tertiary outliers and the red clay with flints.
But on Merrow Down, near Guildford, there is a gravel which
seems to belong to this Drift. It consists in large proportion of
Tertiary flint-pebbles and subangular flints, mostly white, of some
subangular fragments of cherty ragstone, and of a hard sandstone
(Tertiary), with a few small rough quartz-pebbles, imbedded in a

160 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

matrix of bright yellow and red sands. The Downs at this spot are
from 400 to 500 feet high. The Hog’s Back, which rises to the height
of 500 feet between Guildford and Farnham, is bare of any Drift.
To the north of these Downs are the extensive heath-covered hills
of the Bagshot, Chobham, and Frimley ridges, from 350 to 415 feet
high. These are capped by the Southern Drift, with a certain
proportion of ragstone and chert, imbedded in a coarse ochreous and
ferruginous sand. The gravel is from 6 to 12 feet thick, roughly
stratified, and becomes white on exposure. Large blocks of Tertiary
sandstone * occur not unfrequently, and in places there are a few
small quartz-pebbles (Pl. VII. fig. 2). .

Berkshire-—The lower part of the valley of the Thames imme-,
diately adjacent to the river exhibits only Glacial and Post-Glacial
Drifts. The higher hills which range from Windsor Forest to
Sandhurst are covered in great part i the Sonthern Drift. ,

The most striking instance I know of is that exhibited on Cherry
Down (named Burleigh in the new 1-inch Ordnance Maps), near
Ascot. Subangular fragments of chert and ragstone are there so
abundant that they almost equal in number the subangular flints,.
which, with flint-pebbles and a few fragments of iron-sandstone,
constitute the other portion of this eravel. These are imbedded
in a yellow quartzose sand with some black grains and quartz-
grit: in the gravel there are a few intercalated grey and red argil-
laceous seams as at Norwood. This hill is about 300 feet above
sea-level, and 220 to 240 feet above the plain of the Thames at
Windsor and Slough (see Pl. VII. fig. 2).

Further westward the ridges are less persistent, and isolated
hills more frequent. Several of these are capped with this gravel.
On one of them, called “ Gravel Hill” on the map, 400 feet high,
and | mile east of Ceesar’s Camp Hill, near Kasthampstead, the gravel
consists of :—

per cent.
. Subangular fragments of flint, part not stained, and part stained
yellow and ‘brown . Qi siccccuesceee ecco one wavek ote ane eens 40
. Tertiary flint-pebbles, of which about one fifth part are broken. 32
. Much-worn fragments of light-coloured ragstone and yellow
chert, a nd ironstone-grit ndaihactee ihe nmecabiees hbecaheotittale eked 1
“small Spebblesof white quarts teesseesseeeencteer erate yee ed ene aaaee 4
. Pebbles of white sandstone and subangular fragments of Sarsen
stone. (Tertiary) :..csacaseies occ dee eee nteee toate eee Gio Sates Oe aebeta

teal

Ore SUR)

Long exposure has bleached the upper part of the gravel, which
is roughly stratified, as seen in the following section :—

* Some of dies are 20 tons in weight. They mostly occur deep down at
the base of the gravel, and are derived from the Upper Bagshot Sands on
which the gravel rests.

+, a ee eee

VALLEY AND 1TS RELATION TO THE WESTLETON BEDS, ETC. 16]

Fig. 2.—Section of Gravel-pit, Gravel-pit Hill, near Easthampstead.

PE MEMOIR SME red chi gancocss-sstecaunsecardssnaeneserscncenenaseseua |
MM MAP RINPUIEU MEE CEP ch sated aveee.teli cs duct ge sudea.d duvdal. dyetouceds F
cidtrepular black carbonaceous band. ......5..ccac.sdecesecerepereseee

d. Ochreous gravel with sandy beds showing oblique lamination. J

The same gravel caps Ueesar’s Camp Hill, but is not worked
there.

Hampshire.—Among the most conspicuous of the gravel-capped
hills in this county are Hungary and Cesar’s Camp Hills near
Farnham and Aldershot. They are respectively 577 and 600 feet
high, and the gravel on the former consists of :—

per cent,
1. Much-worn subangular fragments of flint weathered white ...... 50
2. Tertiary flint-pebbles, of which about two thirds are broken and
ON cept ei tee fu tesa aiys'sdidas'e'airnidfcieineld'me clara cdursitig wc» aseplelae ries 36
3. Small subangular fragments of light-coloured cherty ragstone
and of ironstone-grit (Lower Greensand)...............:...eceeeees (5
4, Pebbles of Tertiary sandstone and Sarsen stone, some with rude
MSPS MMPRESAIOM OG! cess. celdAveees tet ivee de eel te aes 8
100

Imbedded in a matrix of yellow loam with much-worn quartzose
sand, passing into coarse quartz-grit the size of peas.

A tract of flat country intervenes between these last hills and the
smaller ridges of Hartley Row, Bramshill, and Hazeley. The gravel
at the first-named place is roughly stratified and disturbed at top,
and is composed of :—

1, Subangular worn brown-stained flints.........0.ssesseeeeeeeeereeee ZG

2. Tertiary flint- “pebbles, some of them broken ...........:+ssseeeeee 7h

3. Subangular pieces of ragstone and iron-sandstone with a very
HOF HUME MM CO IAEUILOS: 8 loess. ctcesacslevsveuvns: sueserencceteduers om l

10

Imbedded in an ochreous sand with veins of a greenish-grey clay.
The whole is roughly stratified, and the upper part much disturbed.

The Confines of Hampshire and Berkshive.—Between Hazeley
Heath and Reading the country is flat, with the exception of the
hills at Heckfield and Farley, near Swallowfield (300 feet?). These
are capped by a little flint-gravel, weathering white.

A low tract of bare London Clay then intervenes at Strathfieldsaye
and on to Burghfield, where a bed of flint-gravel commences (on the

162 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

Common), and continues past Silchester, Tadley, and Brimpton
Commons, to Greenham Common near Newbury. This gravel, which —
is sandy, roughly stratified, and weathers white, consists essentially
of subangular flints with Tertiary flint-pebbles, and some much-
worn fragments of a very fine-grained variety of Sarsen stone.
There is also a certain number of small blocks of Sarsen stone, or so-
called Druid Sandstone, scattered over the district; and one well-
known large block (the Nymph Stone) of hard Lower Chalk lies on
Silchester Common. Though there is in this gravel an absence or
extreme rarity of Lower-Greensand débris, I think, from the level
of these plateaux (330 feet on Silchester Common to 402 feet near
Newbury), and from its. relation to the valley-gravels, that it
belongs to the period of the Southern Drift. The Wealden anticlinal
did not bring the Lower Greensand to the surface to the south
of this district ; it only raised the Chalk.

Wiltshire.—Westward of this point there are few traces of this
flint-gravel. I have found it capping Upper Kirby Green hill (573
feet), near Inkpen. A little also occurs on the high ground of Mar-
tinslee Hill, near Marlborough; but I have not recognized it further
westward in this direction, though traces of it extend over some of
the Oolitic hills, 7

. 3. Other Pre-Glacial Hill-Gravels: the Warley and Brentwood
Groups.

Besides the two distinctive Pre-Glacial Drifts here described,
there are two others not so easily assigned to a definite horizon,
although there can be no doubt of their Pre-Glacial age. One has
many of the characters of the Southern Drift; and the other, which
is better known, has the essential characters of a Bagshot pebble-
bedi*.

The first of these groups caps Langdon and Rayleigh Hills in South
Essex, and Hampstead and Highgate Hills in Middlesex. They
are so few in number and are so nearly on the same plane as the
other two groups, with which they possess many characters in com-
mon, that I can scarcely doubt that they belong to one or the other
of them.

Rayleigh.—This range of hills, which is a little to the north-west
of Southend, and rises to the height of 250 or 260 feet, is capped by
a thin gravel consisting of :—1. Numerous flint-pebbles. 2. Some
white subangular fragments. of flint. 3. A very few small white
quartz-pebbles. 4. Fragments of Tertiary Sandstone (one piece
measured 18 x9 inches). 5. Subangular fragments of brown chert

* See Mr. S. V. Wood, junr., ‘‘On the Pebble-beds of Middlesex, Essex, and
Herts,” Quart. Journ. Geol. Soe. vol. xxiv. (1868), p. 464; Mr. W. Whitaker’s
‘‘ Geology of the London Basin,” Mem. Geol. Survey, vol. iv. (1872), pp. 820-328 ;
and ‘ Guide to the Geology of London,’ 5th edit. 1884, p. 55; and Messrs. H.
W. Monckton and R. S. Herries, ‘‘On some Bagshot Pebble-beds and Pebble
Gravel,” Proc. Geol. Assoc. vol. ix. (1889), p. 1.

VALLEY AND IfS RELATION TO THE WESTLETON BEDS, ETC. 163

(one small block measured 4 inches each way) and ragstone
imbedded in a bright ochreous clayey sand. I found no pebbles of
the older rocks.

Bagshot Sands, 30 feet thick, and overlain by from 2 to 3 feet of
a ferruginous pebble-conglomerate, cap Boyce Hill (200 feet), near
South Benfleet*. Two to three feet of a Drift-gravel overlie the
conglomerate.

Langdon Hill.—Kight miles westward of these hills, and
separated by a low tract of nearly bare London Clay, is Langdon
Hill the highest (373 feet) in South Essex. It is capped by some
40 or 50 teet of Bagshot Sands, over which is a thin sprinkling of
gravel, composed almost entirely of flint-pebbles, with which are
mixed a few subangular flints, and some very much weathered
fragments of chert and ragstone (Pl. VII. fig. 4).

The Glacial Beds to the north do not approach within some miles
of Langdon Hill, and then they are on a much lower level (150 to
200 feet), as they are also at Rayleigh.

Hampstead and Highgate.-—On the Bagshot Sands at Hampstead
there is in places a thin sprinkling of flint-pebbles (Bagshot), mixed
with which I have found a few subangular fragments of flint and
of a cherty ragstone, whilst at Highgate we can only surmise that
similar traces occur; but the ground is too much built over for any
sufficient observations to be made. ‘The relation of this Drift to the
Glacial Beds is here much the same as that of the Westleton Beds
at Totteridge to the Glacial Beds at Whetstone—that is to say, that
in both places the Glacial Beds are about 100 feet lower than the top
of these hills. At Highgate the Boulder-clay comes in at the foot
of the south slope of the hill (Pl. VII. fig. 3), and is not met with
higher.

The summits of Hampstead Hill, and of Mill Hill near Tot-
teridge, are nearly on the same plane, whilst the summits of
Langdon Hill and Rayleigh Hill differ little from the height of
Brentwood and Writtlepark hills. In the latter instances, the
Westleton Shingle seems to be on a level somewhat lower,
although it is at a sufficient distance for a slight alteration in the
dip to lessen or annul the difference. The dip, however, of the
Westleton Beds is in general southward, and not northward.

On the whole, these Drift-beds show more analogy with the
Southern Drift than with the Westleton Beds. It is possible, how-
ever, that in the case of Hampstead Hill the two may have had
the same floor and got intermixed. In the case of the Essex Hills,
there may be a connexion with the Brentwood group, but further
research is required to decide the exact relation of these drifts.

The Brentwood Group.—The other hill-drift of this section may
be termed the Brentwood or Warley Group, from its being best
developed in that part of Essex, where it forms a number of
detached outliers. The most eastward of these hills are those
which range from a little west of Chelmsford to near Brentwood,

* This would seem to indicate a fault between this spot and Rayleigh.

164 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

with a height of from 300 to 350 feet. These hills consist of London
Clay, with remnants of Bagshot Sands on the summits of some of ~
them. The Boulder-clay wraps round the east end of this range at
a level of about 150 feet below its summit, but on the northern
slope it rises much higher. The Pebble-beds which cap the hills
at Writtlepark, Beggarhill, Mill Green, Fryerning, and Norton
Heath seem to be little else than Bagshot Shingle more or less
disturbed and mixed with a few subangular flints, quartzite-pebbles,
and pieces of quartz.

A more conspicuous range of hills is that which extends a few
miles further to the south-west, from Brentwood to Warley and
Billericay (see Pl. VII. fig: 4). On Brentwood Common (352 feet)
the Pebble-bed is thin and very much disturbed, as shown in the
_ annexed section :—

Fig. 3.—Section of disturbed Pebble-bed, top of Railway-cutting,
(west end) Brentwood Common.

a. Grey clay, with flints and pebbles .................. |
bi Pebble-bed! disttirbed:. 2s. t. Verdacasotencer coh anewes bee 3 to 4 ft.
e Dight-coloured sands)....b-). s-c--nrapster seaea semen see J

The railway-cutting exposed other features in connexion with the
Bagshot Beds, which require some notice. TheWarley Pebble-bed does
not extend so far as the cutting, or rather it is there hidden by a
bed of clay, which displaces the Bagshot strata, and soon acquires
a thickness of 30 feet. As it increases in thickness its true
Boulder-clay character is apparent ; it becomes darker, and contains
imbedded large subangular flints, flint- and chalk-pebbles, pebbles of
sandstone, and fragments of Jurassic rocks, with specimens of
Gryphea incurva and a large Oyster. As this Clay trends further
eastward, it passes into a sandy brown and bluish clay with only a
few pebbles, and finally thins out as a greenish clay or marl (see
A, 'Pl. VII. fig. 5,.and p, 152).

At the base of this Clay is an irregular bed of sand and gravel,
thickening as the overlying clay thins out, and consisting chiefly
of flint-pebbles, while the way in which the Boulder-clay has
mounted the hill and displaced the strata of the Bagshot Beds de-
serves notice.

The Bagshot Beds themselves, which are here 40 feet thick, will
be found described in the explanation of the section (PI. VII. fig. 5,
p- 152). There are no Pebble-beds here in situ. They were

¥

VALLEY AND 118 RELATION TO THE WESTLETON BEDS, .ETC. 165

apparently disturbed and displaced on the north side of the hill and
pushed southward.

At Warley Heath (378 feet) the pebble-gravel is thick and little
disturbed. The flint-pebbles have a distinctive character of their
own. They are unlike those of Blackheath or of the Westleton
Beds. Dr. Mitchell speaks of them in his papers (MSS.) as the
Warley pebbles. They are larger and less shapely than those of
Blackheath, and are often weathered white. Of their derivation
from the Bagshot Beds, with which these shingle-beds are in close
association, there can be little doubt, for at Billericay there is a thin
bed of flint-pebbles intercalated in the yellow sands of the Bagshot
which cap the hill, and Mr. H. B. Woodward gives a section at South
Weald Park, near Brentwood *, showing a bed of pebbles 15 feet
thick in situ, and overlain by 6 feet of Drift-gravel. We have, in
some cases, therefore, this Kocene Shingle zn situ, whilst in others
it seems to have been affected by the Southern Drift and by subse-
quent Glacial action.

This range of hills formed here, as did the Hampstead and
Highgate on the north of London, and the Bushey and Stanmore
Hills to the south of Watford, the boundary to the advance of the
Boulder-clay ; for though Glacial gravels and evidences of Glacial
action are to be found further south, there is no Boulder-clay.

Stanmore.—An important mass of shingle-gravel spreads over
Stanmore Heath (400 to 450 feet), from little Bushey to Bentley
Priory. It is composed in large part of :—

1. Flint pebbles, a good many being white-coated.

2. Very few subangular flints, stained brown.

3. Some small white quartz pebbles.

4, A few worn green-coated flints, from the base of the Lower Tertiary
sands.

Imbedded in a matrix of coarse yellow and ochreous sand, and
resting upon an indented surface of London Clay, as though due to
pressure (glacial) from above. Many of the pebbles also have their
longer axes upright.

I did not notice any chert or ragstone in this shingle, and in
other respects it resembles the Brentwood and Warley, more than
the Westleton Shingle. The few quartz-pebbles may have been
derived from the Lower Tertiaries, which in the Pinner district
contain a few such pebbles.

The hill (380 to 400 feet) between Pinner and Watford, as well
as Brockley (416 feet) and Elstree Hills (450 feet), on the other
side of Stanmore, are capped by a small spread of similar shingle,
but it is not worked.

There is no Boulder-clay to the west or south of these hills; and

- =:* “The Geology of the London Basin,” Mem. Geol. Survey, 1872, p. 324 ;
and ‘ Geology of London,’ 1889, p. 273.

166 PROF, J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

that at Bricket Wood and Aldenham on the north is on a level of
from 150 to 200 feet lower. |
The only outlier belonging to this group on the south of the Thames
is that on the summit of Shooter’s Hill, 424 feet high.. The shingle
is there composed essentially of flint-pebbles, with only a few sub-
angular flints anda very few rare quartz-pebbles. The flint-pebbles
closely resemble those of Warley Heath. The bed is only 2 or 3
feet thick, and is disturbed at the top lke that on Brentwood
Heath Common and Stanmore.

Fig. 4.—Section in the Brick-field to the West of Bentley Priory,

Stanmore, Middlesex.

a; Unstratified bedsiof shingly araivel 0°): -ccicnece eee oteeeee 6 to 7 ft.
b. Upper loamy bed of the London Clay disturbed by the pressing down
of bed a.

It will be observed that on these hills there are either remnants
of the Bagshot Sands, or else the London Clay is of such a thickness
that little is wanted to bring them in; or, as the London Clay
varies somewhat in thickness, it 1s quite possible that at Shooter’s
Hill, Havering Atte Bower, and Buckhurst, there were depressed
areas in which the Bagshot Sands and pebbles gained at the
expense of the London Clay, and that in these cases, as at Brentwood
and Billericay, the Pebble-beds are nearly an situ.

That the Pebble-beds have been disturbed and partly reformed is,
however, evident from the introduction of materials foreign to the
Bagshots. This may have been effected at the time of the Westleton
or Southern Drifts, though further changes in their condition seem
to be due to ice-action in the Glacial period,

4. Early Physiographical Conditions of the Wealden Area.

To understand the relation which the Southern Drift bears to the
other Pre-Glacial and Glacial Beds, it is necessary to go back to
earlier times to see what were the physiographical conditions pre-
viously prevailing in the south of England and the adjacent con-
tinental area. 3

The denudation* of the great dome of the Wealden anticlinal
commenced in the early Tertiary period tT; but though the Chalk,

* On the general subject of the Denudation of the Weald see chapter 16 in
Mr. Topley’s ‘ Geology of the Weald,’ pp. 270-301 (1875).
+ The author in Quart. Journ, Geol. Soc. vol. xiii. p. 256 (1852).

SS ee

VALLEY AND ITS RELATION TO THE WESTLETON BEDS, ETC. 167

which then extended possibly over the anticlinal, must have been
largely denuded, in order to have furnished the mass of flint-pebbles
in the Woolwich Beds, there is no evidence that the denudation
reached down to the Lower Greensand and Wealden, as no débris
from these sources has been found in the Tertiary strata. For
our present object we need, however, only commence with the state
of the area in Pliocene times.

It is obvious, as I have shown on a previous occasion *, that in
an early Pliocene epoch, before the later denudation of the Weald,
the North Downs from Folkestone to Dorking and possibly beyond,
together with the adjacent area to the south, were submerged under
a sea which extended probably from the North Sea to Brittany and
so southward in one direction, and in the other, eastward, over parts
of France and Belgium to the foot of the Ardennes. The Pebbly-
sands, occasionally fossiliferous (Lenham), that occur at intervals
on the edge of the North Downs are proofs of this submergence.
On the continent beds of the same early Pliocene age and cha-
racter are found capping, amongst others, the hills of Mont-de-la-
Trinité, near Tournay, and the hills near Boeschepe in Belgium,
and of Mont Noir near Bailleul, Mont Cassel near Dunkirk, and the
Chalk-hills between Calais and Boulogne, in France, showing the
same sea to have extended over that area also.

In these Beds, the Diestian of the Belgian geologists, the fossils
have generally been removed by infiltration, and it is only occa-
sionally that a few casts are met with. Where, however, they pass
under the newer Crags of the Antwerp district they are very
fossiliferous. This deposit, which does not exceed 50 or 60 feet:
in thickness, consists of pebbly sands, sometimes very ferruginous
and passing into iron-sandstone, while the flint-pebbles are often
so decomposed that they break under the pressure of the fingers into
a white powder.

From the position of the Beds at Lenham, we may assume that
they originally extended, together with the Chalk, further over the
Lower Cretaceous and Wealden strata to the south, as remnants of
the Beds are preserved in the sand-pipes, the ends of which occur in
decreasing lengths on the bare slope of the Chalk-escarpment,
showing that the deposit itself at one time spread over the now
denuded area at the foot of the escarpment, as exhibited in the
subjoined diagram (fig. 5).

It is clear from that section, that the valley v between the Chalk
and Lower Greensand hills is of later Plocene or Post-Pliocene
date, and the same reasoning applies to the whole length of this great
valley, and in all probability to the Wealden valleys in general.

There can be little doubt, also, that in the early Pliocene times
of which we have been speaking, Belgium and the south-east
of England and Western France (Normandy and Brittany) were
separated, not by the present narrow strait, which was not exis-
tent at that time, but by a broad sea-channel extending across

* Quart. Journ. Geol. Soc. vol. xiv. p. 322 (1858).

Q.J.G.5. No. 182. N

168 PROF. J. PRESIWICH ON A SOUTHERN DRIFT IN THE THAMES

Fig. 5.—Section of the Chalk-escarpments above Lenham, showing
the former extension of the Lenham Sands.

1. Lenham Beds (early Pliocene).
2. Chalk. 3. Gault.
4, Lower Greensand.
a. Sandpipes in the Chalk.
a'. The dotted lines represent the former extension southward of the Lenham
Beds over the Chalk and Wealden.

the Wealden area and over a part of North-western France and of
South-western Belgium, before the elevation and denudation of
those areas and the excavation of the Straits of Dover.

As neither the White nor the Red Crag of Suffolk extend over
the Lenham Sands, while the sand-pipes could only have been
formed after the emergence of the latter and a lengthened exposure
to atmospheric agencies, it is evident that the east and west elevation
of the Wealden area must have taken place at or soon after the
White-Crag epoch, possibly at the insetting of the Red-Crag epoch.
The effect of this emergence was to bar the Crag sea of the EHastern
Counties on the south, and to establish a land-connexion with the
continental area along the line of the Wealden and Boulonnais
anticlinal, which then, with that of the Ardennes, probably formed
a continuous range.

The final elevation of the broad anticlinal dome of the Weald was
therefore subsequent to the deposition of the Lenham Sands, and
it must have been after that time that the excavation of the valleys
v, fig. 5, commenced. Hence we may conclude that the denudation
of the Weald, as generally understood, is of a date subsequent to the
early Pliocene period, that is to say, after the emergence of the
Lenham or Diestian Beds, just as we have shown that the exca-
vation of the valleys of the Thames district took place after the
elevation of the Westleton Shingle, or subsequent to the early
Pleistocene period.

5. Origin of the Southern Drift.

The foregoing conclusion respecting a Wealden barrier in Pre-
Glacial and Glacial times is confirmed by the circumstance that the
component materials of the Southern Drift consist exclusively of
débris derived from rocks in the Wealden area, or from those which
formerly extended over it. The deep valley (v, fig. 5) now separating
the range of the Chalk-Downs from the range of the Lower Greensand
could, for a long time, have had no existence, for otherwise the
débris of chert and ragstone of the Lower Greensand could not

VALLEY AND 1TS RELATION TO THE WESTLELON BEDS, ETC. 169

have been carried from the Greensand-range on to the Chalk-plateau
on the north. The valley, v, must then have been bridged over by
the Gault and Chalk to have allowed the transport across it of
this débris by streams from the central Wealden area; for there is
no reason to suppose it was effected by floating ice.

Let us now try to conceive the condition of the Wealden area at
the period of this, its last, emergence. At present, the height of the
anticlinal ridge at Crowborough does not exceed 803 feet. To
realize the condition of the dome before denudation, we have to add
the thickness of the strata removed, which may probably be esti-

mated as under :—
feet.
1. Chalk. J¢ is doubtful whether this extended to the centre of
the Weald, for, as I have already shown*, it had before this time
‘been planed down at its edge to a thickness of 300 feet by
Tertiary marine denudation. If that rate of wear were main-
tained, it is probable that the Chalk either did not extend to

the central area, or else was greatly reduced in thickness ...... LOO
Pempemorecencand and Gault .......0.....2cctescersccccncscaseassaceee 150
PME MCRMSA NC Gc vives cece cenit cueseaaeisoescdesesvecsssiectonseeces 450
SEM MN MEE, Foner Bye aG.cctves cae toont focus Sok ons aggaeses bone tenes 700
aelimpridge’ Beds and Wadhurst Clay ..... 0.0.6. ..ccccccsseeseeres 400
1800

Add present height of Central ridge (Ashdown Sands &e.)... 800

26001

There would thus have been, even supposing that there has been
no subsequent subsidence, a low mountain-range extending into the
Boulonnais, on the site of the present Wealden area. It is pro-
bable also that at this time the Ardennes were considerably higher
than they are now (2800 feet), for MM. Cornet and Briart have
shown that during their diverse upheavals some 12,000 to 15,000 feet
of strata have been removed}. This, however, was at a date very
long anterior to the Pliocene.

The Wealden range having been uplifted in late Pliocene times,
it soon became exposed for a vast length of time to the heavy
rainfall, snow, and ice of the Pre-Glacial and Glacial periods, when
torrents scored the flanks of the hills, and carried down the harder
débris to the lower grounds at their base.

Amongst the earlier results of these denuding agencies is, I con-
ceive, the coarse and much-worn gravel of Well Hill. The large
heavy flints with their angles greatly worn, and the unstratified
character of this gravel, give it the appearance of having been
brought down by a torrent, and of not having been spread out under
water. This would account for its very local occurrence; for this
stream of stones is confined to Well Hill, and the hill itself seems
to result from the protection afforded by the mass of flints, while

* Quart. Journ. Geol. Soe. vol. viii. p. 256.

t+ The estimate formed by Mr. Topley, supposing the whole amount of strata
removed by denudation to be restored, varies at different parts of the axis from
1000 to 8000 feet (‘Geology of the Weald, p. 217).

¢ Mém. Soc. Géol. de Belgique, vol. iv. p. 71 (1877).

n 2

170 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

the soft unprotected Tertiary strata on either side have been removed
by denudation. That the gravel is of great age is indicated by the
extreme weathering of the flints, and by the alteration and dis-
coloration of their substance; while although flint-pebbles from
the Tertiary are abundant, débris from the Lower Greensand is
extremely scarce, as though the denuding agencies had at that time
scarcely reached down to the Lower Greensand, a state of things
that may be represented by the following diagrams (figs. 6, 7) :—

Fig. 6.—Theoretical longitudinal Section along the summit of Well
Hill (ante p. 157) to the flanks of the Wealden Range.

S. The Chalk N.
Slope of the Wealden The range of the escarpment. Well Hill.
anticlinal. Lower Greensand. 700 ft. 600 ft.
~ (pee

—
—
_—>—

‘
‘
/

|
\*
|
|
|
|
!
\

1. Well-Hill gravel. 3. Chalk and Gault. 5. Wealden strata.
2. Lower Tertiary strata. 4. Lower Greensand.

The dotted lines show the prolongation of the beds before denudation.

The transverse section shows the position of the gravel in rela-
tion to the Tertiary strata formerly on either side.

Fig. 7.—Theoretical Section across Well Hill and the old
Gravel-stream.

W. Well Valley of i.
Hill. the Darent.

The upper dotted line shows the position of the removed Tertiary strata.

The conjecture that at this time much of the Wealden and Lower
Greensand were still hidden under a mass of Chalk and Tertiary
strata, finds corroboration in the analogous condition of the gravel
on some of the other higher and earlier drift-covered hills, where
flints from the Chalk, or flint-pebbles from the Tertiary strata, con-
stitute the whole or nearly the whole of the mass of gravel, and
Lower-Greensand débris is either absent or very scarce. Thus, for
example, on Hungary Hill there are but few traces of Lower-Green-
sand débris, and in the flint-gravel of the hills near Canterbury it
is absent or nearly so.

VALLEY AND 1TS RELATION TO THE WESTLETON BEDS, ETC. VA

Later on, as the covering of Tertiary strata and of Chalk was
removed, the Lower Greensand became more exposed, and its hard
and indestructible siliceous débris was scattered more widely along
the base of the old Wealden range of hills. ‘Thus it is that on the
Bagshot hills of Hampshire and Berkshire we find the chert and rag-
stone of the Lower Greensand occurring in quantity, and in Kent
also scattered freely, though thinly, in places over the Chalk-plateau,
having lodged there after the denudation of the Tertiaries and
their removal around Well Hill.

Another and somewhat later phase occurred when the drainage of
the Wealden Highlands became restricted to narrower bounds and
more defined channels. It was then that some of the main trans-
verse valleys received their first rudimentary channelling, as, for
example, in the case of the Medway, where the flint- and chert-
gravel above Halling and on some hills above Stroud point to old
channels in the line of the present Medway valley, but at heights
of from 200 to 300 feet above the existing river; or, in the case of
the Darent, the bank of flints and chert on the slope above Eynsford,
at a height of from 250 to 350 feet above that stream. Another
instance is that of the Wey through the gorge of the Chalk at
Guildford. On the east side of this passage, Lower-Greensand
and flint-débris cover Merrow Down at a height of 400 feet, or of
300 feet above the Wey. Im all these cases this old gravel is
considerably above the Post-Glacial gravel more intimately con-
nected with the existing valleys, though at the same time the Chalk
around rises to still greater heights than this Drift.

In the foregoing instances, the valleys flanked by this old chert-
drift pass through the Chalk-escarpment into the Wealden area,
showing that there has been continuity of action along the same
lines from the initial stages of the formation of these valleys to the
present time, and therefore that it was not, as has been suggested,
the present streams which have cut their way back through the
escarpment.

There are other instances where the continuity has been inter-
rupted, and the original drainage diverted into other channels, leaving
the valleys, as it were, half formed, and the old channels were
left dry, but retaining a drift carried in from beyond their present
precincts. A good instance of this is to be seen in the narrow
valley of Smitham Bottom (fig. 8), which, commencing at Croydon,
runs up to the Chalk-escarpment above Merstham, where it is cut
off by the transverse valley draining into the Mole, and no longer
passes into the Wealden area. At present it is a dry valley,
excepting that during certain seasons there is an outbreak for
about half its length of a bourne, which continues to run for a few
months, but is in no way connected with the old drainage-area.
Along the upper part of this valley, and extending to its end above
Merstham, is a thin bed of gravel composed of subangular flints,
and flint-pebbles, with subangular fragments of chert, ragstone, and
ironstone derived from the Lower Greensand. It is clear, therefore,
that this Drift was deposited before the strata beyond the escarpment

8

phy.) PROF, J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

had been removed, and when the valley was prolonged in a southern
direction into the Wealden area, and the drainage brought down thé
usual complement of Lower-Greensand débris from the hills beyond
the Chalk-escarpment.

At this stage, some disturbance connected with the Central
Wealden area diverted the drainage in another direction, cutting off
the upper part of the vailey, denuding the face of the Chalk-escarp-
ment, and leaving the truncated end of the valley at a height of 174
feet above the stream at the foot of the escarpment (0, fig. 9) which
now drains into the Mole. The bed of the valley at the point where
it is cut off is 438 feet above O.D., while the hills on either side
rise nearly 200 feet higher, showing the valley to have been in an
advanced stage, but still 200 to 300 feet short of the depth subse-

‘quently acquired by that of the Medway or of the Darent.

The date of this old transverse valley is, however, far removed
from that which has left its traces on the summit of Well Hill, inas-
much as at the latter date the Tertiary strata had not been denuded
from the surface of the Chalk floor, whereas at this time not only
had the Tertiary strata. been denuded from the Chalk-plateau, but
the Chalk itself had become channelled to a considerable depth. The
position of the valley in its longitudinal course at the time of its
arrested growth, when it had its origin in the Wealden area, is
shown in the following diagram :—

Fig. 8.—Course of the Valley of Smitham Bottom, restored.

: Nis
The Wealden Range of the
anticlinal. Lower Greensand. The North Downs.
a
3
Sea-
level.

a. Level of the valley of Smitham Bottom through the Chalk-hills.
a’. The same prolonged beyond the chalk-hills southward before the
denudation of the area.

3. Chalk. 4. Lower Greensand. 5. Wealden.

The section transverse to the above showing the intersection of the
valley in the face of the chalk escarpment is as under (fig. 9).

The gravel at Croydon, which belongs to the earlier stages of the
valley, is not that on the lower levels, which is of Post-Glacial age,
but that which forms the higher banks on Duppa’s Hill on the west,
and Park Hill on the east of the town.

We will now revert to the earlier streams of Lower-Greensand
Drift, described in pages 156-162, and connected with the pri-
mary streams or torrents flowing from off the slopes of the Wealden
nighlands and over the Chalk-plateau. At this period the Wealden

VALLEY AND ITS RELATION TO THE WESTLETON BEDS, ETC. 173

Fig. 9.—Seetion in front of the Chalk-escarpment above Merstham.

Ww. Ee

Sea-level.

v. Valley of Smitham Bottom.

a. Valley Drift.

b. Level of valley at foot of escarpment.
2. Lower Tertiary strata. 3. Chalk.

anticlinal may have formed a range from 2000 to 3000 feet high,
with a drainage north and south.

As the channels of the early streams became deeper and larger,
and the Lower Greensand more exposed, the mass of débris carried
down increased, and the proportion of chert and ragstone became
greater. It was then that were formed the extensive plateaux of
gravel of the Chobham and Frimley Downs, and of the other hills we
have named in Berkshire, Hampshire, and Surrey.

In the absence of organic remains of any sort in these plateau
eravels, we are miiant a clue as to whether fluviatile or marine
action kad to do with their origin. It is not improbable that they
are, in part, of subaerial origin; and to compare small things with
great, they may have been formed in a manner analogous to the
fan-shaped masses of débris carried down by torrents from the
mountains bordering the plain of the Indus as described by
Mr. Drew*. ‘This would account for the localized form of these
sheets of gravel, and for their absence on the intermediate Chalk-
hills. It is also possible that the cone may have discharged under
water, and so spread out to a greater extent and more uniformly,
and with the rough sort of bedding this gravel sometimes shows.

In any case, whatever may have been “the manner in which these
hill-gravels were formed, there can be no doubt of the source
whence the materials have been derived. They clearly come solely
from the Lower Tertiary, Chalk, and Lower Greensand, lying south
of the area over which they are spread. Flints and flint-pebbles
might have been brought from other directions, but the chert and
ragstone are characteristic of the Lower Greensand of Kent and
Surrey, and the peculiar character of some of the chert of the

* Quart. Journ. Geol. Soc. vol. xxix. p. 441 (1873).

t+ Prof. Rupert Jones arrived independently at the same general conclusions as
inyself with respect to the age and origin of the Bagshot plateau-gravels, though
he ascribes more to marine action. I should have liked to give an ‘abstract
of his paper, but must refer the reader to the original work (Proc. Geologist’s
Association, vol. vi. pp. 457-443, 1880). The Rev. A. Irving has also written on
the subject, and concluded that these beds were of estuarine origin and pre- or
interglacial age (Proc. Geol. Assoc. vol. viii. pp. 161-171, 1883),

174 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

Folkestone Beds between Sevenoaks and Maidstone, spread over the -
Chalk-plateau to the south, renders a mistake impossible.

The time of the first appearance of the Lower-Greensand débris is
significant. We have seen that the Wealden anticlinal was uplifted
after the deposition of the Lenham Beds, while the first beds in which

. we find chert and ragstone of the Wealden area are those of the Red
Crag—at least I found none in the single small exposure of the
Pebble-bed at the base of the White Crag. Hence we may presume
that the Wealden range was raised and became exposed to atmo-
spheric waste at some time either towards the end of the White-
Crag epoch, or very early in the Red-Crag epoch. But during the
time of the Red Crag the waste was still small, and it was not
until the time of the Westleton Shingle and Southern Drift, that it
acquired larger dimensions—dimensions which had their climax in
the plateau-gravels of the Thames Valley. These successive stages
are, I imagine, coincident with the increasing cold of the period,
and the increased disintegration and denuding action. If, on these
limited premises—and we have none others to judge by—we might
suggest time-equivalents for these several stages in the early
denudation of the Weald, I would take the Well-Hill Drift to
belong to the Red-Crag epoch, and the Plateau-Drifts to corre-
spond broadly in time with the Chillesford, Forest Bed, and Westle-
ton Shingle. A more definite concordance is hardly at present
practicable; for nowhere are the hill-Drifts found in juxtaposition,
and the extensive denudation of the subsequent Glacial period has
swept away any connecting-links that may originally have existed,
and left only the fragmentary remainders we have described.

While this glaciation was going on in the Thames Basin, it is
probable that the Wealden Highlands were the centre of another
snow- and ice-field, to which the denudation of that area is to be
more particularly ascribed. It was this range of high land which
obstructed the advance of the northern ice and the Boulder-clay, for
the Tertiary hills of the Thames Valley were then only the out-
posts of that more important Wealden range. ‘This ice-tield may
ultimately have been confluent in the Thames Valley with the
great northern ice-sheet, though it may have yielded finally to it
as the destruction of the Wealden range proceeded, and the obstacles
to the further southward progress of the latter were removed.

6. Relation of the Southern Drift to the Westleton Shingle and
other Pre-Glacial Drifts.

Let us now endeavour to follow the successive changes that took
place from the time of the early Crag deposits down to that of the
Westleton and Southern Drifts in South-eastern England and the
adjacent continental area, and note the relation of these drifts one
to another.

There can be but little doubt that a marine deposit of early
Pliocene or Diestian age extended generally over a portion of the
south-east of England and adjacent parts of France and Belgium, and

VALLEY AND ITS RELATION TO THE WESTLETON BEDS, EC. 175

that the formation of this deposit was followed by an upheaval which
brought it to the surface, and gave rise to a low mountain-range on
the site of the present Wealden area. We are able to fix the time wita
tolerable accuracy, by the absence of the later Crags in the upraised
district, and by the presence of débris derived from that district
in some of the deposits in the area which remained submerged.

Thus at the base of the White Crag, subangular flints, flint--
pebbles, a few white quartz-pebbles, some light-coloured quartzite- *
and a few sandstone-pebbles, of which one contained the cast of an
Astarte (Oolitic ?), have been found, and with these one consider-
able-sized boulder of red felspar-porphyry. These afford but little
guide for the direction whence they drifted. There is an absence
of chert and ragstone, such as might be expected to be present if
the denudation of the Weaiden anticlinal had commenced or been far
advanced.

With the Red Crag, we have certain proof of denudation of the
Lower Greensand and of the earlier Pliocene bed, for in the Copro-
lite-bed at the base of the Red Crag at Sutton there are found :—

. Large angular flints from the adjacent Chalk.

. Flint-pebbles from Tertiary or Diestian Beds.

. Light-coloured quartzite-pebbles.

. Pebbles of White or Coralline Crag.

. Pebbles of white quartz.

. Pebbles of iron-sandstone (Diestian ?).

. Pebbles of a light-coloured sandstone with impressions of Pecten and
Astarte (Oolitic ?).

8. Subangular fragments of chert and ragstone (Lower Greensand).

And at the base of the Red Crag at Frimley, in addition to the
above :— |

STO Ot GO DD

1. Pebbles of fossiliferous ironstone and box-stones (Diestian ?).

2. Subangular fragment of a white felspathic sandstone.

3. A small boulder of red granite with green and black hornblende.
4, Subangular fragments of brown chert with sponge-spicules.

It is evident, therefore, that the denudation of the Weald had
then commenced 7, and that the Lower Greensand had been reached,
although the quantity of chert- and ragstone-débris had not yet
attained the proportions it acquired at a later period, when the
Greensand-strata had become more worn down and exposed.

If, then, this Wealden range already existed at the time of the
Red Crag, it follows that its denudation which then commenced must
have been going on during the later times of the Chillesford Clay and
of the Forest Bed. It was at that time probably that the winter snow
and spring floods swept down the Lower-Greensand débris over the
Chalk-plateau and Tertiary hills to the north. It was a period in
all probability of great humidity and heavy rainfall, for there is some
evidence that at no great distance to the south of the aforesaid range
there were Pliocene seas with warm currents to furnish an abundant
evaporation. —

* In my earlier papers I used the term siliceous sandstone instead of yuartzite.
t Quart. Journ. Geol. Soc. vol. xxvii. p. 353 (1872).

176 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

Following on this period, a tract extending from the east coast
and reaching either as far as the district near Bath, or possibly as far ©
as the Bristol Channel, was submerged and covered by the waters of
the Westleton sea—a sea bounded by the highlands of the Weald on
the south, but of which the northern barrier has yet to be defined.
I am led, therefore, to conclude that the early stages of the Southern
Drift preceded the Westleton Shingle (in its later stages they may
have been synchronous), and either that the Westleton sea beating
against a land over which the Southern Drift had spread, took up a
portion of that Drift with its chert- and ragstone-fragments, or that
the streams which still continued to run from off the southern hills
carried down thence the Lower-Greensand débris into the Westle-
ton sea. Superposition is wanting, and we have only the relative
position and the peculiar composition of the two Drifts to guide us; _
for although the Southern Drift occasionally contains white quartz-
pebbles, they are so few that they may have been derived from
Lower Tertiary strata, or from the Lower Greensand and Wealden.

The Westleton Drift, as already explained, is, in the main, con-
fined to the district north, and the Southern Drift to the south, of
the Thames. But it is probable that on the southern slopes of
the Wealden highlands and their prolongation westward, similar
causes were in operation to those we have pictured on the northern
slopes, that a similar Drift was there in course of formation at
the same time, and that it was there subject to conditions analogous
to those experienced by its equivalent in the London Basin.

As instances of such outliers, I may brietly mention Alderbury
Hill, near Salisbury, the higher hills between Southampton and
Winchester, and those in the New Forest between Lyndhurst and
Wimborne; I have, however, now to confine myself to the Thames
Basin. I would merely state further that in these districts this
drift, like that on the opposite side of the dividing-range, con-
tains a considerable proportion of chert- and ragstone-débris mixed
with the angular and subangular flints of the Chalk.

7. Main Lines of Elevation and Drainage of the South-
east of England: Genesis of the Thames.

Another point remains for consideration, and that is, the effect
produced, not only on the configuration of the country, but also on
the lines of drainage, by the elevation on the one hand, at an early
Pliocene date, of the Wealden anticlinal, and, on the other hand, of
the Westleton sea-floor in early Pleistocene times.

The east and west direction of the anticlinal of the Wealden axis
necessarily gave rise to a drainage northwards into the area of the
Thames Basin, and plotted broadly the direction of those valleys,
which subsequently, with certain modifications, caused by minor
disturbances, and by the action of glacial erosion, became the main
lines of the transverse valley-system and rivers of the Weald.

The emergence of the floor of the Westleton sea was, on the con-
trary, effected not by any sharply-defined axis, but by flexures

VALLEY AND ITS RELATION TO THE WESTLETON BEDS, EITC. 77

ranging S.W. and N.E. through parts of central England, and of
which the direction is coincident with the parallel ranges of the
Chalk and Oolitic escarpments in that area. ‘he Westleton beds,
when raised, consequently dipped east and south-east on an incline
at right angles to these elevation folds.

The result of this has been, that whereas on the Norfolk coast
the Westleton Beds are close on the sea-level, they rise westward in
Berkshire to the height of from 400 to 500 feet, and northward in
Hertfordshire and Buckinghamshire to 500 and 600 feet. Thus a
drainage from the raised area was established to the south-east, but
diverted eastward as it approached ba already raised Wealden area
with its northward drainage.

The Thames necessarily tot from these tributary lines of
drainage; but the river must have been restricted at first to the
Tertiary and Chalk Basin, with the Kennet (passing round the
Tilehurst Hills) as the main stream and source of the river. The
Chalk-escarpment was not breached by the Isis until later. This
river before that time probably flowed to the north-east, parallel
with and between the Chalk and Oolitic escarpments, and emptied
itself into the Wash on the east coast *.

The old landmarks are, however, so obliterated by subsequent
Glacial action and earth-movements that this requir es confirmation.
Of the fact, however, that for some time after the rise of the Chalk-
escarpment, the pass of the Thames at Goring did not exist, and
that the first breach through the belt of Tertiary strata and Westleton
Shingle capping the Chalk-Downs was effected by a Glacial current
coming from the direction of Warwickshire and Staffordshire, there
can, | think, be little doubt. It was not until the gorge was enlarged
by later glaciation, possibly aided by disturbances of the strata,
that the Isis was diverted into this new channel, and so formed a
junction with the Lower Thames and Kennet.

This may be illustrated by a diagram showing the two lines of
elevation with the resultant conditions of drainage (fig. 10).

This is a branch of geology which opens some very large and
interesting problems. I have treated it briefly. Owing to the vast
erosion of the surface, the evidence respecting the older Drifts
is generally very fragmentary, and has often been entirely swept
away. Some speculation is therefore unavoidable, though it is
essential that the consequences that may result from hypothetical
assumptions should be in harmony with the results of observation.
In putting together my notes, many new views have suggested
themselves to me, and | should much lke, as | have before
said, to have gone over the ground again, with the object. of
confirming or, if necessary, correcting my early work; but that is
no longer possible, and I must leave the task to my younger
colleagues.

* The width of the Wash between Lynn and Boston, and the extent of the
Bedford level and adjacent marsh-lands, convey the idea precisely of the
estuary and alluvium of a large river, such as the Isis with its tributaries
would, in the case here suggested, have been.

178 PROF. J. PRESTWICH ON A SOUTHERN DRIFT IN THE THAMES

Fig. 10.—Diagram of the lines of Elevation bounding the Tertiary
Basin of the Thames, showing their relative Age and Direction.

7
Ww / Cini E

VA, =
7 Vv Ss
v4 7 ™ a:

1. Anticlinal axis of the Weald (Late Pliocene).

2. Escarpment of the Chalk. 3 .
3. Escarpment of the Oolites. } (Hamlyn tetstorens),

V. Valley of the Thames.
— Dip of the strata. sa-->Lines of drainage,

8. General Summary.

The results of the foregoing inquiry may be summed up under
the following heads :—

1. That the Westleton Shingle ranges from the Crag in Suffolk
inland to the Chalk-escarpment in Oxfordshire and Berkshire,
rising gradually from the sea-level, until it attains a height of
from 500 to 600 feet.

2. That the Tertiary strata were co-extensive with this Shingle
at the time of its deposition, and that both extended to the
edge of the Chalk-escarpment, where they have been cut off
by subsequent denudation.

3. That the upraising of the floor of the Westleton sea, or of the
Westleton Shingle, immediately preceded the advance of the
Glacial deposits, so that while they are concordant or in con-
formable superposition in the eastern counties, they become
discordant as they range westward, and the Boulder-clay
occupies valleys formed, after the rise of the Westleton Shingle,
by early glaciation.

4, That the belt of Tertiary strata and of Westleton Shingle on the
northern borders of the Chalk-Basin, formed originally a con-
tinuous and unbroken zone, and that this was not broken
through until after the elevation of the Westleton floor and
the inset of the Glacial period.

er)

Tey,

PAL.

1

13.

14.

15.

VALLEY AND ITS RELATION [0 THE WESTLETON BEDS, ETC, 179

. That none of the valleys on the north side of the Thames Tertiary

Basin date back beyond the Pre-Glacial epoch, and that the
whole of the valley-system of that area is of later date.

. That the escarpment: of the Chalk, and probably that of the

Oolites, in the Midland Counties, is of a more recent date than
the Westleton Shingle, and therefore not older than late Pre-
Glacial or early Glacial.

That there is a Southern Drift as well as a Northern Drift in
the Thames Basin: and that this Southern Drift has been
derived from the Lower Greensand of the Wealden area and
from the Chalk and Tertiary strata formerly extending over
portions of that area and the adjacent downs.

. That during the early Pliocene (Diestian) epoch the Wealden

area was partly or wholly submerged, and that a continuous
sea extended thence over certain portions of France and Bel-
gium, while the present Strait of Dover was non-existent.

. That subsequently to this period, but before the in-setting of

the Glacial period, the Wealden area and the Boulonnais
underwent an upheaval, resulting in the formation of an anti-
clinal range 2000 or 3000 feet high.

That it was from the slopes of this anticlinal that the materials
composing the Southern Drift were derived, and spread over
the area now forming the southern side of the Thames Basin.
That this denuding action commenced at the time of the Red
Crag, and was continued uninterruptedly through several
successive geological stages.

That consequently, though the Southern Drift preceded the
Westleton Shingle, the two must at one time have proceeded
synchronously, though possibly at times on different levels.
That the valley-system of the Wealden area had its origin after
the Diestian or early Pliocene epoch,—the initial direction of
the transverse valleys dating from Pre-Glacial times, and of the
longitudinal valleys from Glacial times.

That the formation of the Thames Basin is the result, on the
one hand, of the elevation of the Wealden anticlinal, and, on
the other, of the flexures of the Chalk and Oolitic strata in the
midland counties, and dates therefore from a period subsequent
to that of the Westleton Beds.

That the genesis of the Thames dates in like manner from
late Pre-Glacial or early Pleistocene times, whilst its con-
nexion with its upper tributaries and the Isis took place during
the subsequent Glacial period.

EXPLANATION OF PLATE VIII.

This Map shows the position of the outliers of Westleton Shingle and of the
Plateau-gravels in the Thames Basin, with the lines of section given in Pl. VII,
A line marks the southern limits of the Boulder-clay, but the other Glacial and
Post-Glacial drifts are not given.

180 PROF. J. PRES! WICH ON A SOULHERN DRIFT IN THE THAMES

Discussion.

The Cuarrmawn remarked on the difficulties connected with the
identification of gravels over large areas, and with the problems of
Tertiary physiography.

Mr. Wuiraxer noticed the wide range of the paper, and believed
that there was no problem more difficult in the geology of the South of
England than the classification of various deposits of gravel. Prof.
Prestwich, he understood, put in the same class the gravels of Nor-
wood, Hampstead, Rayleigh, and of the hills between Faversham
and Canterbury. The geological surveyors had not felt that they
could successfully correlate these various gravels. At Norwood,
Mr. Spurrell considered the gravel was an old Wandle gravel, while
he himself rather inclined to suppose it an old Thames gravel. The
geological surveyors lad coloured certain gravels as plateau-gravels,
without any attempt to assign them to any definite age. He (the
speaker) had noticed pebbles on end in many gravels. When Prof.
Prestwich supposed that some gravel was synchronous with Crag-
deposits, he could not follow his line of reasoning. As regards the
supposed Wealden ice-field, he felt that the beds were not strong
enough to carry much wear, and that the hills would soon be denuded.
The pebbles in the Red Crag showed that the sea of that age extended
to the Lower Greensand, pebbles of Ammonites biplea which had
been phosphatized in Lower-Greensand times occurring in the
phosphate-deposits of Red-Crag age. Between Southampton and
Winchester he had seen hardly any high gravel which he was inclined
to classify as Drift. He agreed with the Author as to the import-
ance of insisting on the occurrence of a southern drift; but he
pointed out the difficulties in identifying gravels by their included
fragments. Whether the breaching of the escarpment of the Chalk
was so late as the Author had considered it seemed to him doubtful.

Dr. Irvine said that he was in accord with the Author as to the age
of the plateau-gravels of Berkshire. He had published his views as
to the fluviatile character of these gravels, and now brought for-
ward evidence of glaciation at lower levels, proving their pre-
glacial age.

Mr. Tortey was interested in the distinction between Southern
Drift and Westleton Shingle. He had not altogether appreciated the
distinction which Prof. Prestwich had endeavoured to draw, and
thought that some of the materials of a river would be eliminated as it
flowed further from its source. As regards thedenudation of the Weald,
the Author had shown that the denudation of the Chalk had ex-
tended so far that Tertiary deposits rested directly upon the Lower
Greensand. He did not follow the Author’s mode of estimating the
height of the Wealden hill-range, for much denudation must have
‘succeeded the deposition of the Tertiary beds previous to the forma-
tion of the Southern Drift. He thought changes of drainage in the
Weald were frequently due to the cutting back of escarpments, and
he gave an illustration of the method in which this might be done.
He called attention to the important earth-movements which had

VALLEY AND ITS RELATION TO THE WESTLETON BEDS, ELC. 181

affected the Weald and surrounding districts, and referred to Mr.
Poulett Scrope’s views that during the elevation of the Weald the
beds glided over others, which would account for the varying thick-
ness of such deposits as the Gault.

Dr. Evans congratulated the Society and Prof. Prestwich on his
having been able to sum the results of the observations of so many
_ years in the series of papers which he had lately read. In taking
samples of gravel, and attempting to correlate beds of gravel over a
large area, mistakes might arise from local variations; but he
thought that the facts brought forward by the Author went to a
large extent to confirm his views. Possibly some further confirma-
tion might be found in the country to the west of the axis of eleva-
tion that bounded the Westleton Beds. He hoped that Prof. Prest-
wich would allow a longer period of time to have elapsed for the
production of the physical changes he had described than he
had previously allowed for Postglacial changes. As one of the
older Fellows of the Society, it would have been impossible for
him to refrain from saying a few words in congratulation of one
with whom he himself had laboured so long.

The AvrHor, in reply, was not surprised at the difficulty speakers
had experienced in following all the details of so intricate a subject.
He acknowledged the assistance derived from the admirable Drift-
maps of the Geological Survey. He had differed from them in ven-
turing upon a chronological classification of the pre-glacial ‘Drifts.
He had attempted to describe three kinds of hill-drifts—the Westle-
ton, Brentwood, and Southern Drifts. The Brentwood Drifts certainly
originated with the Bagshot Beds, but showed differences which allied
them to the other Drifts. He often found a sufficient number of
vagstone- and chert-pebbles to show that the Bagshot Beds had
been intruded upon and disturbed. In some cases, where infiltration
had been suggested to account for the upright position of the
pebbles, the pebbles rested upon clay-beds, where infiltration was
impossible. He had felt the same difficulty as Mr. Whitaker as to
the gravels of Well Hill, and could only suppose they had been
derived from a destroyed hill-range. Amongst others Alderbury
Hill, three miles from Salisbury, was capped by gravel full of chert
and ragstone like the southern drift of the Thames Basin. No doubt,
as Mr. Topley had said, the denudation of the Weaid commenced
in early Tertiary times; but he believed that the great upheaval
to which he, the Author, referred took place after the spread of the
Lenham Beds.

182 MR. R. LYDEKKER ON REMAINS OF SMALL

11. On Rematys of Smart Savropopous Drvosaurs from the
Weatpen. By R. Lypexxerr, Esq., B.A., F.G.S8., &e. « (Read
December 4, 1889.) |

[Pratz IX.]

Amone the Dinosaurian remains from the Upper Jurassic of the
United States, recently described by Prof. Marsh, none are perhaps
more interesting than the vertebree and teeth upon which the genus
Pleurocelus* has been based, since they indicate a comparatively
small form closely allied to the gigantic Morosaurus, and less nearly
so to the still more huge Brontosaurus. In the type species of
Pleuroceelus the teeth are said to be of the same general type as those
of Morosaurus, but are not distinctly spoon-shaped, and are thus
more like a compressed cone. The centra of the dorsal vertebrae,
which are less than four inches in length, are elongated and very
markedly opisthoccelous, with a long and deep lateral cavity, of
which the upper portion gradually shelves towards the arch.

Outer and profile views of a tooth of Plewrocelus valdensis ;
from the Wealden.

Recognizing the Sauropodous nature of the teeth from the Wealden
of Sussex and the Isle of Wight, provisionally referred by Mantell
and subsequently by Sir R. Owen to Hylwosaurus (one of which is
shown in the woodcut), I proposed some time ago to regard them
provisionally as indicating a European representative of the American
genus, with the name of Pleurocelus valdensis. These teeth indicate
a very small member of the Sauropoda, and, although their crowns
are subject to considerable variation in form, many of them show
the absence of a decided spoon-shape, characteristic of those of the
type species.

In the same notice I referred to the imperfect centrum of a dorsal
vertebra from the Wealden of Cuckfield, preserved in the British

* Amer. Journ. ser. 3, vol. xxv. pp. 90-92 (1888).
t Geol. Mag. decade 3, vol. vi. p. 325 (1889).

Quart.Journ.Geol. Soe. Vol. XLVI. Pl. IX.

Mintern Bros.

BR. Mintern del. et lith.

VALDENSIS,

>

c
‘

LEUROCHLU

A

ie]

SAUROPODOUS DINOSAURS FROM THE WEALDEN. 185

Museum (no. R. 1616), which it was suggested might belong to the
same species as the teeth. Of this vertebra two views are given in
Pl. IX. figs. 1, 1a; and it will be seen from these figures that
this specimen comprises the greater part of the centrum, with the
exception of the anterior ball. The base of the neural canal still
remains, but the surfaces for the articulation of the neural arch are
destroyed. From the circumstance that the neural arch is lost, it
is highly probable that the specimen is not fully adult; but the
smooth outer surface of the bone indicates that it did not belong to
a very young individual, being, in this respect, very widely different
from the vertebre from the Kimeridge Clay, described by Sir Owen
as Bothriospondylus suffossus, which Prof. Marsh suggests may have
belonged to a foetal Dinosaur. I take it, then, that this vertebra
indicates a comparatively small Dinosaur, and since it evidently be-
longs to the suborder Sauropoda, there is a strong presumption that
it belongs to the same form as the above-mentioned teeth. When I
say the same form I would, however, guard myself by adding that
it is quite likely the teeth may indicate more than a single species.
Compared with the figure of the dorsal vertebra of the typical
P. nanus, it will be seen that this specimen agrees in the great depth
of the posterior cup, and also (allowing for the loss of the anterior
ball) in the comparative length of the centrum, aud in the large size
and shelving upper portion of the lateral cavity. Compared with
the large dorsal of Hoplosaurus (Ornithopsis), figured by Mr. Hulke
in vol, xxxvi. pl. iv. of the Society’s Journal, the greater propor-
tionate length of the centrum and the larger size and more sloping
boundaries of the lateral cavity are very noticeable in the present
specimen. ‘The approximate length of the entire centrum was pro-
bably some three inches, against 3°8 inches in the typical dorsal of
P. nanus. So far therefore as I can see, the provisional reference
of the Wealden teeth to Plewrocalus is confirmed by this specimen,
which appears to differ from the dorsal vertebra of the type form
by features of merely specific value.

The second specimen I have to notice is a somewhat larger im-
perfect vertebra, obtained from the Wealden of Brook in the Isle of
Wight, and till recently preserved in the Dorsetshire County
Museum at Dorchester. This specimen is represented from the left
lateral and anterior aspects in Pl. IX. figs. 2,2a. It is a dorsal
vertebra, evidently referable to the Sauropoda, and, from the com-
plete union of the arch with the centrum, clearly belonging to a
fully adult individual. The neural arch is preserved in fair con-
dition, as high up as the platform from which the transverse pro-
cesses took their origin; and the union between the arch and
centrum is so intimate that even the neuro-central suture cannot be
detected, although its approximate position is indicated in the figure.
The centrum has lost its lower half, the horizontal fracture extending
through the plane of the central pit of the lateral cavity. The im-
perfect upper portion of the anterior articular ball remains, but the
contour of the posterior cup has been entirely destroyed. The outer
lamina of bone on the upper part of the sides of the centrum has

Q.J.G.8. No. 182. 0

184 ON REMAINS OF SMALL SAUROPODOUS DINOSAURS.

also been more or less completely destroyed, so that the contour of
the shelving superior half of the lateral cavity has been lost. In the
figure an approximate restoration of the lower half of the centrum
has been made from comparison with the preceding specimen.

So far as its imperfect condition admits of comparison, the contour
of the portion of the centrum now remaining appears to be very
similar to that of the preceding specimen, the upper half of the
lateral cavity having the same shelving form, while its central fora-
men was small and clearly defined. Moreover, when entire, the
centrum must evidently have been of an elongated type, its approxi-
mate length being about four inches. There is accordingly no
apparent reason why this specimen should not have belonged to an
adult individual of the same species as the one to which the preceding
vertebra pertained ; although I would not deny that we may have
to do with two distinct but allied species.

In the absence, however, of any evidence in favour of a contrary
view, I propose to refer both these specimens provisionally to
Pleurocelus valdensis. Their especial interest lies in the circum-
stance that, in conjunction with the above-mentioned teeth, they
afford absolutely conclusive evidence of the occurrence in the English
Wealden of a diminutive Sauropodous Dinosaur, which was the con-
temporary of the huge Hoplosaurus, and the still more gigantic
Pelorosaurus ; and they also serve to increase the evidence as to the
similarity of the Dinosaurian fauna of the Upper Jurassic of North
America to that of the Upper Jurassic and Lower Cretaceous of
Kurope.

EXPLANATION OF PLATE IX.
Vertebree from the Wealden; referred to Pleurocelus valdensis.

a, lateral cavity of centrum; 0, anterior ball of centrum; c, posterior
cup of centrum; d, neural canal.

Fig. 1, la. Left lateral and posterior aspects of the imperfect centrum of an
immature dorsal vertebra, with a restoration of the anterior ball ;
from Cuckfield, Sussex. 2 nat. size. (Brit. Mus. no. R. 1616.)
2, 2a. Left lateral and anterior aspects of an imperfect dorsal vertebra,
with a restoration of the lower half of the centrum ; from the Isle
of Wight. 43 nat. size. (Brit. Mus. no. R. 17380.)

PECULIAR HORN-LIKE DINOSAURIAN BONE FROM THE WEALDEN. 185

12. On a pecutiaR Horn-iixe Drnosavrtan Bonz from the WEALDEN.
By R. Lypexxer, Esq., B.A., F.G.S. (Read December 4,
1889.)

Amone a small series of vertebrate remains lately sent from the
Dorsetshire County Museum to the British Museum there is an im-
perfect bone from the Wealden of Brook, Isle of Wight, so unlike
any specimen from those beds which has hitherto come under my
observation that I deem it worthy of a brief notice. This specimen,
which is represented on a reduced scale in the accompanying wood-
cut, is a stout and short cone-like bone, of some 53 inches in
length, with the larger basal diameter measuring 4 inches. The
cone is somewhat compressed, with a distinct backward curvature,
the summit being imperfect. The outer surface is rugged, with
irregular longitudinal ridges ; while the base is extensively hollowed,
and has a smooth and mamillated surface, recalling that of the
cancellous cavities found in the base of the horn-cores of the Bovide.
In all these respects this specimen appears to present a close resem-
blance to the horn-cores of the Dinosaurian skull from the Jurassic

Horn-core(?) of a Dinosaur; from the Wealden of the Isle of Wight.
3 nat. size.

of North America, described and figured by Prof. Marsh in the
‘Amer. Journ.’ ser. 3, vol. xxxvi. pl. xi., under the name of Ceratops.
A less marked resemblance is also presented to the longer horn-like
bone from the Greensand of Austria, figured by Prof. Seeley in vol.
Xxxvil. pl. xxvii. fig. 4, of the Society’s ‘ Quarterly Journal,’ under
the name of Cratwomus, which Prof. Marsh (Geol. Mag. dec. 3, vol.
vi. p. 207) regards as a veritable horn-core. The dermal spines of
Hyleosaurus and Polacanthus do not show .a basal structure at all
like that of the present specimen; and it certainly does not belong
to Lguanodon.
02

186 PECULIAR HORN-LIKE DINOSAURIAN BONE FROM THE WEALDEN.

IT do not at present regard this curious specimen as affording
conclusive evidence of the existence in the Wealden of a large Dino-
saur furnished with horn-like projections on the skull like the
American form to which the name Ceratops has been applied; but
I do suggest that this may really prove to be its true nature, and I
have accordingly brought it to the notice of the Society in the hope
that additional evidence may some day prove whether this suggestion
is right or wrong.

Discussion.

The Pres1ipENT commented upon the interest of finding a large
number of Dinosaurs common to Britain and America.

Mr. Hvrxr thought the Author had done wisely in speaking
cautiously concerning the supposed horn-core. He suggested that
two different sorts of soft tissue had been implanted upon this
bone.

The Aurnor said that he had spoken very cautiously about the
horn-core.

PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS, ETC. 187

13. On the CrystaLtine Scuists and their Revation to the Mxsozoic
Rocxs in the Lepontine Atps. By T. G. Bonney, D.Sc.,
LL.D., F.R.S., F.G.8., Professor of Geology in University
College, London, and Fellow of St. John’s College, Cambridge.
(Read January 22, 1890.)

TABLE OF ConTENTs.

Introductory.
1. Jurassic and crystalline rocks near Andermatt.
2. The schists of the Val Piora.
3. The Rauchwacké and its relation to the schists.
(a) Val Piora sections.
(6) Val Canaria section.
. The Jurassic rocks with included minerals and fossils.
(a) Preliminary.
(6) Sections on the Lukmanier Pass (Scopi and Alp Vitgira).
(¢) The Nufenen Pass.
. Conclusions.
. Appendix, with microscopic details.
(a) The “ Val Piora” schists.
(6) The Rauchwacké.
(c) The Jurassic rocks.

a

So Or

Art the close of the year 1888 I read before this Society a paper
** On two Traverses of the Crystalline Rocks of the Alps,” in which
I maintained that these rocks could be arranged in certain fairly
definite groups, which exhibited a stratigraphical succession. On
this communication only two criticisms of importance were offered.
Of these one expressed a doubt of the value of the method which I
had adopted in my work; the other affirmed that certain schists,
regarded by me as members of a very ancient series, probably
Archean, had been demonstrated by the presence of Mesozoic fossils
to be of the latter age; or, in other words, that, in the Alps, ordinary
sediments deposited in the Jurassic epoch had been subsequently
converted into true crystalline schists, a result of metamorphic
action which I had implicitly affirmed to be incredible. The former
criticism, which amounted to an assertion that the general suc-
cession of the Alpine rocks could only be ascertained by very
detailed mapping, in my opinion, indicated an imperfecti knowledge
of the subject, while it was scientifically unsound and historically
incorrect. It indicated an imperfect knowledge, because, as a
matter of fact, a considerable part of the Alps has already been
mapped, not by irresponsible amateurs but by official surveyors, and
it was with the interpretation of these maps that I was largely con-
cerned ; and because it assumed that an impossibility could be
performed. As I have had the honour to fill the same position in
the Alpine Club that I have done in this Society, I may to affirm with-

188 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

out fear of contradiction that a very elaborate petrographical map-
ping of the Alps is impossible ; for the most painstaking and con-
scientious of surveyors must assume much that is incapable of
demonstration. A very large part of the whole area is concealed by
snow, glaciers, débris, pasture, forest ; and some one of these ob-
‘ stacles very frequently interferes, in the most provoking way, just
at the most critical point. Further, no small amount of the rock
which is visible can only be regarded from a distance. Many a
cliff, many a ridge, is inaccessible, and the examination, even of
every point which it would be possible to reach, would require the
expenditure of such an amount of time, that I am certain it
never has been, and believe that it never will be done.

But further, the criticism, inmy opinion, was scientifically unsound
and historically unjustifiable. Scientifically unsound, because very
commonly the most important problems which are presented by the
crystalline rocks receive a decisive answer from one or two sections
only*. I have not the slightest desire to undervalue elaborate map-
ping, but we must be careful not to treat it as a fetish, as though it
were the only means appointed for the discovery of geological truth.
Its results more commonly are the removal of minor difficulties in a
conclusion already attained, and the disclosure of the precise mode
in which certain effects have been produced. The criticism was
historically unjustifiable, because, so far as my knowledge goes, it is
a fact that in regard to difficult petrological questions, infallibility
has not been found to reside with the makers of geological maps.

My work, both in the Alps and in other regions, which has been
carried on with a definite object and a fairly clear idea as to the
needful evidence, has led me to the following conclusions, which,
though they have been already expressed, I will venture to repeat
for the information of the reader.

(i.) That a group of truly crystalline schists is always more
ancient than any rock to which, on the evidence of fossils, a date
can be assigned.

(ii.) That many such groups can be proved to be older than any
Paleozoic rock.

(i1.) That though crystalline schists have often been claimed as
metamorphosed sedimentary strata of Paleozoic or Mesozoic, if not
of Tertiary age, the evidence in support of this claim has hitherto
always broken down on careful examination, and in not a few
instances has proved hardly worthy of the name.

(iv.) That in certain cases structures exist in the crystalline
schists which must be indicative of sedimentation, and that in not
2, few instances a sequence can be detected which must be due to

* For instance, whether an igneous rock be interbedded or intrusive may be
an open question in every section but one. Whether a group of slates forms
part of a continuous series with a group of schists may be uncertain in most of
the sections, but may be settled in the negative by the discovery, in a single
section, of a conglomerate or breccia of the latter in some member of the former.
I do not suppose that this statement will be questioned by any one familiar with
this department of geology; but if it were, I could fill a page readily with
examples of the proof or disproof of a theory by a single section.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 189

successive deposition. Great as the modifications resulting from
subsequent pressure very frequently are, these may often be separ-
ated, and the earlier record, as in the case of a palimpsest, be
decyphered.

In the Alps there exists, as has frequently been pointed out by
those who have preceded me™*, a great group of crystalline schists,
the bulk of which must be metamorphosed sedimentary deposits.
This group can be traced, practically without a break, from one
end of the chain to the other. These schists certainly overlie,
sometimes it would seem unconformably, another great series of
gneisses and schists t, generally coarser in texture. These seem to be
divisible into two groups differing in lithological characters, of
which the upper, though sometimes well developed, is not seldom
wanting ; so that instead of the gradual transition from it to the
first-named group, which can sometimes be observed, we find the
latter resting with marked discordance upon some part of the lower
series. The present paper deals mainly with this highest group.

The oldest unaltered rocks in the Alps generally belong to the
lowest part of the Mesozoic system, Jurassic or Triassic (possibly
sometimes Permian), but in certain districts not inconsiderable
deposits of Carboniferous age (quite disconnected from the last
named) occur, and in the North-eastern Alps Paleozoic rocks of yet
earlier date have been identified. All these are practically unaltered.
An exceptionally wide experienee enables me to affirm without fear
of contradiction that, in the case of any large mass which would
be referred without hesitation to the Jurassic, Triassic, or Carbon-
lierous group, there will not be found, however great may have been
the mechanical disturbances which it has undergone, any transition
exhibited by it into one of the normal gneisses or schists; at most
a microfoliation has been developed or a superficial resemblance set
up. The crystalline schists also do not exhibit, as a rule, any ten-
dency to pass into ordinary sedimentary rocks. Appearances sug-
gestive of this transition are found on closer examination to be due

* T have made no attempt to compile, in accordance with a growing prac-
tice, a list of books on Alpine geology, because the greater part of them would
have little real bearing on the subject: of this paper. A list of those treating on
the geology of the Lepontine Alps will be found in Von Fritsch’s volume, to
which and to such as I have used in writing this paper references are given in
the text. Others there may be, for I do not pretend to have spent much time
in searching ; but if any one has come to conclusions identical with my own, I
can assure the author that there is no plagiarism. At the present stage of the
questions treated of in this paper, I find work in the field or with the micro-
scope of far more value than “ hours in a library.”

+ In the remainder of this paper I follow my invariable practice of using
the term schist to express a foliated rock, and so as the equivalent of the “ crystal-
line schist” of some authors. This is the restriction long ago insisted upon by
Jukes. As I have frequently pointed out, the lax use of schzste and schiefer by
continental writers, and of schist by some English geologists, has been a fruitful
parent of confusion of thought and inaccuracy of expression. By a foliated rock
I mean one which is crystalline and exhibits a certain parallelism in its consti-
tient minerals, especially those ike mica and hornblende. If in addition to this
certain minerals predominate in certain layers, the rock is also called banded.
Thus the terms schist and gneiss imply foliation, but not necessarily banding.

190 PROF. T. G. BUNNEY ON CRYSTALLINE SCHISTS AND THEIR

either to pulverization of the rock by pressure, or to the inclusion of
a later series by folding or faulting.

But while there can be no doubt of the general truth of this
statement, it has recently been asserted that in certain districts of
the Alps there is a passage from Jurassic rocks into truly crystalline
limestones, while in others fossils of that age occur together with
garnet, mica, and a mineral resembling staurolite, in schists which
cannot be distinguished from certain members of the above-named
group *. If this assertion be correct, it must follow (1) that the
Alps exhibit true schists which are metamorphosed sediments of
Mesozoic age, and (2) that, inasmuch as these are undistinguishable
from schists which by stratigraphical evidence can be proved to be
very much older than any Mesozoic rock, a schist, like a granite or
a dolerite, might belong to almost any geological epoch.

This last opinion can claim the sanction of antiquity and the
authority of weighty names, but the progress of investigation had
largely diminished the number of its supporters, when it seemed to
recelve a new life from a recognition of the amazing effects of me-
chanical forces in modifying rock-structures and from the above-
named discoveries in the Alps. Specimens illustrative of the latter
were exhibited at the International Geological Congress in Sep-
tember 1888. Those supposed to indicate the passage of an ordinary
Jurassic limestone into a crystalline marble (from a district which I
had already visited) did not appear to me convincing. But those ex-
hibiting fossils in a rock resembling a true schist were certainly very
remarkable, and seemed to afford considerable support to the opinion
mentioned above. I was not, however, convinced by them, because
though I had not examined the two localities in which the supposed
‘‘ fossiliferous schists” occurred, I was fairly acquainted with the
geology of the district, and had been very near, in one case within
less than a mile, to each locality. I had also examined rocks iden-
tical, as I believed, with those in which the fossils occurred. The
knowledge thus obtained, notwithstanding the apparent evidence
of the specimens exhibited, suggested to my mind the possibility of a
mistake, and a doubt whether the identity of the fossiliferous rock
with the true schists of the district was not more apparent than
real, Still so remarkable were the specimens, so great was the
weight of authority, that when these cases were quoted against me
in the discussion on my paper, I departed from that which has
become almost a rule to me—viz., to pay no regerd to criticisms
founded on second-hand information—and stated that I accepted the
challenge. A‘part of my last summer vacation was devoted to the
study of the district. I had hoped to have been aided by my old friend
and fellow-worker Mr. Hill, but his entry upon a new field of duty
prevented him from leaving England. I had, however, the good
fortune to obtain the company of Mr. J. Eccles, F.G.S., who joins to

* Asthe volume of papers presented at the Geological Congress has not yet
been published, it will be better to refer, not to the copies then distributed,
but to the translations by Dr. Hatch, printed in ‘ Nature,’ Sept. 27 and Oct. 4,
1888: see especially p. 524.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 191

an exceptional knowledge of the Alps much experience in field-work
in England. For his constant, unwearied, and friendly help I can
hardly adequately express my thanks. He was accompanied by his
guide, Michel Payot of Chamouni, a shrewd observant man, who took
great interest in our investigations and was often very useful.

We began our work, at Andermatt, by examining the crystalline
limestone at the back of Altkirch and the rocks in that neighhour-
hood. ‘Thence we crossed the Oberalp Pass to Dissentis, and walked
therefrom to the summit of the Lukmanier Pass, where we halted
to study the sections on either side (Alp Vitgira and Scop1), localities
where fossils were said to occur in schists. Thence we crossed the
Passo del Uomo to the Upper part of the Val Piora, where we ex-
amined (for the third time in my case) the sections around the Lago
di Ritom. Descending thence to Airolo we investigated the section
in the Val Canaria, described by Dr. Grubenmann; and then, in
crossing the Nufenen Pass, examined another case of the occurrence
of fossils in ‘‘ schists,” reaching the valley of the Rhone by the Egi-
nenthal. This concluded the work specially described in this paper,
but I may add that we afterwards visited the Binnenthal, in order
to verify some points in my former work, and then proceeded to
Zermatt. From both these localities some valuable information was
obtained which bore indirectly on the genoral] questions involved in
the investigation.

The results of our work will, I believe, be made more generally
intelligible by grouping them (irrespective of chronological or topo-
graphical order) under the following heads :—

1. The Andermatt Section.

2. The Schists of the Val Piora.

3. The Rauchwacké and its relation to the schists.

4, The Jurassic rocks containing minerals and fossils.

1. Tar ANDERMAT? SECTION.

At the base of the slopes leading from the upper valley of the
Reuss to the Oberalp Pass, and not far from the southern opening
of the Urnerloch, is acraglet of white marble, which is quarried near
a chapel, Altkirch, and can be seen cropping out for some distance
up the hill side. This rock is now considered by certain eminent
Swiss geologists to be a limestone of Jurassic age, and is so repre-
sented on the Andermatt sheet of the Survey map. Specimens
were exhibited at Burlington House, during the Geological Congress
of 1888, to illustrate the supposed transition of this marble into the
indubitably Jurassic limestone which occurs in the upper valley of
the Reuss, not very far off the line of strike, at a minimum distancc
of about 3 furlongs, and can be followed for a long distance west-
ward. ‘The evidence of these specimens did not, however, appear
to me satisfactory ; for a very wide gap seemed to exist in the chain
of demonstration which, from my knowledge of the locality, IL believed
would be difficult to fill. But as this identification had evidently
been made a basis of correlations of crystalline with sedimentary

192 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

strata in the Alps,—correlations which were of the highest theoretic

importance, and had affected the more recent geological maps pub-~

lished in Switzerland,—we began our work by carefully examining
these slopes. Before giving the results it is necessary to preface
them, for the sake of those unacquainted with the district, with a
brief description of its physiography.

The upper waters of the Rhone, Reuss, and Rhine occupy an oro-
graphical trough between the range of the Lepontine Alps and that
which prolongs the line of the Central Oberland. Through a nar-
row gap in the latter the Reuss escapes northwards; and the passes
of the Furka on the west, and the Oberalp on the east, limit its
basin, and form watersheds in the trough. This is bounded north and
south by schists, gneisses, and gneissoid granites; but there is a
rather marked lithologieal difference, as has often been pointed out,
between the rocks of the two massifs. Enfolded between them
and not reaching to so great an elevation above the sea, are various
schists, sometimes more or less calcareous, which have a more
modern aspect than the above-named rocks, though they are often so
much crushed that any assertion as to their original condition
demands great caution. Furthermore, a long strip of dark Jurassic
rock, often calcareous,—sometimes a blackish limestone (not unlike
one of those in the English Lower Carboniferous series),— extends
from the valley of the Rhone over the top of the Furka Pass, is
restricted after a time to the left bank of the Reuss, and finally dies
out on the hiilside about due north, so far as I can see, of the vil-
lage of Andermatt, its disappearance being of course due to denu-
dation. If then, as a glance at Von Fritsch’s map will show, this
Jurassic limestone is identical with the white marble of Altkirch,
there must have been a displacement of the latter southwards of
two or three hundred yards. This, however, would not be a diffi-
culty of any real importance ; I only mention it to show that the
masses at present are not really in the same line of strike. Judging
from the outcrops, the slopes up which the road winds to the Ober-
alp Pass are mainly composed of gneissoid rock, which obviously
has been greatly modified by pressure *; between this (the “ sericite
gneiss” of the Swiss map) and the Urnerloch is the marble in
question, with certain apparently associated rocks; while on the
other side of the “sericite gneiss,” between it and the Lepon-
tine massif, is phyllite and black slate, referred by the Swiss geolo-
gists to the Carboniferous series f. According to Von Fritsch, the
former group of rocks consists of a lenticular strip of marble, on the
south of which is a band of Jurassic rock, which in one place is
fringed by rauchwacké. Where the marble narrows to a point at
its eastern extremity, a mark indicates the occurrence of fossils.

* More than one variety of rock is present, but I have thought it needless
to enter upon details. The most conspicuous feature in the part nearest to the
marble is a cleavage-foliation ; but on examining a fractured surface at right
angles to this, we see that the rock has been a granite or granitoid gneiss.

t Perhaps also some of the newer group of schists occur here, but I did

not carefully re-examine this section last summer, no controversy existing in
regard to it.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS, 193

On the present occasion we chiefly devoted ourselves to the exami-
nation of the rocks lying betweeu the “ Urseren gneiss” and the
‘“‘sericite gneiss.” They are not very well displayed, for so much
of the hillside is covered by turf. Briefly related, this is what we
found. Beginning on the northern side, and keeping near the base
of the slope, we passed over a crushed-looking gneiss. This, which
(to quote from my note-book) ‘‘ was examined again and again dur-
ing the day, may be the ‘ Devil’s-bridge’ gneiss in a very crushed
condition, still it has a more friable, saccharoidal aspect, and thus
bears some resemblance to the gneiss of the St. Gothard Pass.”
After a brief interval of turf, we came to a very fissile, black, slaty
or schistose rock, shortly followed by cale-mica schist *, which indu-
bitably graduates into the marble quarried at the back of the chapel.
This rock on its southern side passes back again into a calc-mica
schist. Yet further to the south we came to the “ sericite gneiss.”
Two other traverses made higher up the slope gave us the same suc-
cession, though certain changes presently to be described take place
in the marble, which does not long retain the whiteness and com-
parative purity exhibited in the quarry. We failed to discover
any fossils at the locality indicated on the map; and we could
only find a very small patch of a friable cream-coloured limestone
in the bed of a glen to represent the rauchwacké. At a rather
higher level, however, we came upon asmall outcrop of dark unaltered
rock which bore a considerable resemblance to the ordinary Jurassic
rock of the district. It is therefore possible that a small outcrop of
this age containing fossils may occur on the right bank of the Reuss
valley ; but we failed to find it, though we searched carefully, and
visited, as we believe, every outcrop between the “ Urseren” and
the “ sericite ” gneisses.

This section then exhibits rocks, which appear not highly altered
close to a distinctly crystalline calc-mica group. Let us now subject
them toa more minute investigation, taking first the crystalline
eroup. ‘The marble has a flaggy structure. The surface of the slabs
exhibits frequently filmy flakes of white mica, and not seldom the
superficial “ flutings ” which indicate earth-movements. In one part
of the quarry the marble is banded with layers of mica, often about
1 inch thick, and it passes, as has been said, into a calc-mica schist.
On microscopic examination wesee that the rock givessome indications
of pressure, but that in many parts it exactly resembles one of the
ordinary white marbles which, in many other districts of the Alps,
are associated with true crystalline schists. It is never quite free
from flakes of whitemica, and grains of quartz, obviously authigenous,
are not rare. There is nothing to suggest that the crystalline
structure of the rock is in any way the result of pressure; but we
may confidently affirm that such modifications as can be attributed
to this agent of change were produced after the rock had assumed a
erystalline condition, and when it differed in no material respect

* In the field the cale-mica schist might be thought to exhibit a tendency to
graduate into this phyllite. This, however, proves on further examination to
be illusory.

194 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

from its present condition. There are, however, certain rocks out-
cropping higher up the hill, obviously in close relation with the
above-mentioned marble, which demand careful study ; for at first
sight these might be supposed to retain traces of organisms. Some
300 feet above the level of the valley, we found that the marble
(here rather more fissile and flaggy) shows on the southern side elon-
gated markings of a lead-colour, bearing a rough resemblance to
flattened tubes. These vary in size ; the larger are a couple of inches
or even more in length, a quarter of an inch wide, and perhaps one
twentieth of the same in general thickness. They weather more
rapidly than the rest of the rock, so as to be indicated on an old sur-
face by irregular hollows. Higher up, about on the same horizon,
the rock is obviously not quite so pure a limestone (having, at first
sight, as is common with such rocks, a slightly gneissoid aspect), and
is more distinctly “slabby” in habit. In this variety also the rudely
tubular markings are very distinct ; they are lighter in colour than
the body of the rock (which here is greyish), and are occupied by a
substance resembling a yellowish-white or greyish elay.

Specimens of these rocks have been studied microscopically, more
especially with a view of determining the nature of these peculiar
structures. The first one, with the lead-coloured streaks, is a fairly
coarsely crystalline limestone (grains commonly about :03” in dia-
meter) with a few flakes of white mica, grains (variable in size, but
generally smaller than those of calcite) of quartz *, and a few black
grains, prabably graphite. The matrix does not appear to be gene-
rally crushed, but some grains exhibit the usual indications of pres-
sure. The “ tubes” (cut transversely in this specimen) are occupied
by minutely granular calcite with occasionally a small flake of mica,
which mineral seems slightly more abundant here. The sections
are irregular in outline. They. are streak-like masses, which have
a tendency to die away in a string of granules; now and then a
larger grain of calcite occurs in the dust-like mass, and the grains
of the matrix on either side of the streak seem as if broken away.
These streaks obviously lie, whatever be their significance, in sur-
faces roughly at right angles to the general direction of the pressure
by which the rock has been affected. A specimen of the rock with
light-coloured tubuli, in close relation with the last deseribed, though
a little further away from the more typical marble, does not exhibit
any important difference under the microscope, but the grains of
calcite are more dirty-looking. Sections of the tubuli are numerous,
often very irregular and “‘ inorganic ” in outline, sometimes darkened
as if by graphitic matter, either crushed up im situ or subsequently
infiltered. Another specimen, taken from higher up the section,
obviously less calcareous, consists of calcite as before, quartz, in
amount perhaps one third of the whole, with a little white mica
and granules of graphite (?). Sections of the tubuli are numerous ;
they are very irregular in outline, “streaking” away into the ma-
trix, and small ones occur which are hardly more than strings of

* T think it possible that a colourless silicate may also be present. Not sel-
dom crystallites are enclosed.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 195

granules. Indications of mechanical disturbances also are rather
conspicuous.

What explanation are we to give of these markings? Are they
organic or inorganic? At the first glance they look very like the
former. But atubular mollusc seems to be out of the question, since
the forms under the microscope are so very irregular ; further, so
far as my experience goes, a calcareous organism generally crystal-
lizes more readily and is thus coarser in structure than the matrix.
Still this difficulty might perhaps be explained away ; but the former,
even allowing for subsequent distortion, seems to me insuperable.
But they might be Annelid burrows. Here, however, is the diffi-
culty that the matrix is often an almost pure limestone, and the
contents of the tube also are calcareous, while the fact that they often
“ streak away ” into the matrix and sometimes are mere “ strings”
in sections, seems fatal to the hypothesis. After a long and, I hope,
unprejudiced examination, I can come to no other conclusion than that
these markings are inorganic, and their appearance accords best
with the hypothesis that they are the result of local crushing. This
may sometimes be due to the accident of the rock being slightly less
homogeneous at these places, but I venture to suggest the following
as a general explanation. Suppose a pressure acting upon a rock,
which if it were mainly composed of parallel folia of a mineral like
mica, would produce in them a series of parallel undulations: parallel
with the crests of these would be lines of maximum strain or stress
which might produce local fracture in the calcite, and when a line of
grains once yielded, these would give rise to a linear band of crushed
material, which would obviously take a form roughly resembling
a flattened-out tube.

The black schistose rock which occurs north of the marble is
macroscopically very difficult to determine ; its dominant structure
at the present time is obviously due to pressure. Is it a dark mica-
ceous schist which has been greatly crushed, or an ordinary shale simi-
larly treated ? In other words, is the development of mica, to which
its schistose aspect is due, mainly anterior or posterior to the action
of the pressure which has caused the present cleavage? I have
seen, as, for instance, in the ‘lyrol*, in association with white crys-
talline limestone a dark mica-schist which has so yielded to pressure
as to bear locally a very close resemblance to a phyllite, while the
associated marble has been but little affected. Partly owing to the
difficulty of obtaining good sections in so fissile a rock, and partly to
the destruction of the original mica-flakes in the production of the
cleavage, which is followed by a further development of minute
filmy mica, a rock in this condition is sometimes locally not easy to
distinguish, even under the microscope, from an ordinary phyllite
or schistose slate.

My first impression in the field inclined me to think that this was
probably a repetition of the 'T'yrol case, but a more careful study of
the question leads me to the other conclusion. The difficulty of

* Q.J.G.8. vol. xlv. p. 91.

196 PROF. T. G. BONNEY ON CRYSTALLINE SCHISIS AWD THEIR

examination is increased by the abundance of a brownish to black-.
ish material, ferruginous or carbonaceous, which, so to say, stains
the rock ; but the matrix itself appears to consist mainly of small
flakes of white mica and granules, often elongated in form, of quartz
or of some silicate. There are no signs of strain-slip cleavage. The
present microfoliation seems due either to original sedimentation or
to pressure acting on a material which has not possessed a very
definite structure. Oblong crystals of a silicate, often about :01"
by °003”, are not uncommon, usually lying with their longer
axes at a high angle with the structure of the matrix; these are
posterior in date to the latter, because the dark lines indicative ef it
can be traced through them ; sometimes they are rendered partially
or wholly opaque by reason of the dark matter. When clear they give
low polarization-tints, and are often twinned on the Carlsbad type;
one section gives extinctions of 14°-25 and 17°25 respectively on
either side of the twin line, so they are probably monoclinic. I
have seen similar crystals in other Alpine phyllites, and occasionally
in much crushed schists, but am not able to identify the mineral
with any species known to me by name. After comparison of the
slide with specimens of typical phyllites from other parts of the
Alps, the Ardennes, &c., I think we must refer the rock to the same
group. .

This identification is confirmed by an examination of specimens
from the rocks pierced by the St. Gothard tunnel, which runs nearly
under the marble-quarry. The section disclosed in this reveals a
still more extraordinary state of things than has been just described.
It is well illustrated by the collection of specimens procured for the
British Museum from the late Dr. Stapf, which has been carefully
described by him*. In the tunnel the space between the two
gneisses mentioned above seems to measure about 270 yards. In
this interval we find that the following rocks are present :—
(1) phyllite, (2) marble and calc-mica schists, (3) phyllite, (4) cale-
mica schists, in which occurs a curious brecciated rock, (5) phyllite,
followed by soft rotten-looking calcareous rock (? representing
rauchwacké). From the distances at which the specimens are col-
lected, I conclude that the phyllites, &c., are not so thick as the
crystalline calcareous rocks. The specimens of the former come
from distances of 2562, 2637, and 2766-2790 metres from the north
entrance. They seem to owe their schistose condition to pressure:
the latter group are clearly ordinary cale-schists or calc-mica schists
more or less affected by subsequent pressure.

Strange, therefore, as the association above described may be, 1
can come to no other conclusion than that we have in this section
a newer argillaccous sediment and an older mass of crystalline
(calcareous) schists faulted together (in process, doubtless, of folding),
so that the apparent sequence is misleading, and that pressure, as is
commonly the case, has affected the softer argillaceous sediment
more than the more solid crystalline masses. I am, however,

* Tam indebted to Mr. Fletcher for great facilities afforded me in the study
of these, and to Mr. Miers for much kind help.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. gs We

doubtful whether the phyllite which occurs at Altkirch, and pre-
sumably those pierced by the St. Gothard tunnel, of which the
northernmost at any rate may be safely identified with the former
rock, are of Jurassic age. The Swiss geologists consider (rightly, as
I believe) the phyllites south of the ‘“sericite gneiss” (above the
village of Andermatt) to be members of the Carboniferous group,
as also an infolded strip which crosses the Lukmanier road at
Curaglia. Other like infolds occur (according to the older authori-
ties, who, I believe, are correct) in the valley of the Rhone, as, for
instance, at the north base of the Simplon Pass and elsewhere in the
neighbourhood of Brieg; and a narrow strip of the same rock, in my
opinion, is cut through by the Binnenthal, to the north of the great
mass of dark orystalline schists, from which it is macroscopically
not easily distinguished *. I am, of course, aware that in a case of
this kind it is hazardous to rely on lithological resemblances, but it
is at any rate remarkable that there is not only a strong family like-
ness, in such Alpine rocks as I have examined, among the phyllites
of Carboniferous age on the one hand and those of Jurassic age on
the other, but also a distinction between the two groups, due, as I
believe, to an original difference in the materials, the former having
been more directly derived from the older crystalline rocks. If this
identification of the Altkirch phyllite be correct, the relation of the
crystalline series, the Carboniferous phyllites, and the Jurassic rocks
of the upper Reuss valley would very closely resemble that which
I have already described, and which is universally admitted, in the
valley of the Romanche 7.

Be this as it may, whether the Altkirch phyllite be Carboniferous
or Jurassic in age, if we place it in the same group with this marble
and cale-mica schist, the section presents us with the following
difficulties. ‘The argillaceous members of a consecutive sequence
are comparatively unaltered, while the calcareous are intensely
metamorphosed ; for in them not only have the calcareous consti-
tuents become completely crystalline, but also the argillaceous have
been converted into flakes of mica of considerable size—a result of
environment which is hardly im accordance with the general teaching
of nature. Again, both rocks have been affected, though, as is
usually the case in associated strata of unlike composition, to a
different extent, by pressure. This has produced the usual effect
upon the clay by converting it into a phyllite; but it has first of all
(according to the hypothesis) converted the calcareous rock into
erystalline limestone and banded calc-mica schist, and has then im-
printed upon it the usual mark of dynamic change. Further, the
section appears to prove too much for the advocates of theories of
‘pressure metamorphism,” for the transition between the phyllites

* [twice walked over this strip without observing the distinction, but detected
it on a third occasion, as the occurrence of fragments of a dark schistose rock
in the adjacent rauchwacké led to a more careful examination of the underlying
rock. The similarity is probably due to the “ anthracit-schiefer”’ having been
largely composed of fragmental mica, and having derived locally much of its
material from the adjacent dark schist.

t Quart. Journ. Geol. Soc. vol. xlv. p. 73.

198 PROF, T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

and the cale-mica schists seems to be too abrupt to be explicable by
the difference in their chemical composition. In addition to these
difficulties there is a further one, which to myself seems also of
great weight. In the Alps crystalline limestones and calc-mica
schists are anything but rare. These rocks differ in no respect of
the slightest importance from those at Altkirch, and they are asso-
ciated again and again, under circumstrnces which preclude the
possibility of error, with other true crystalline schists (micaceous,
chloritic, &c.). Such rocks, wide as is my experience, I have never
seen in undoubted sequence or intercalation with true phyilites, nor
have I found, even in the most highly disturbed regions occupied by
Mesozoic strata, crystalline limestones and cale-mica schists (not
even in the most restricted areas) which presented any real resem-
blance to those which abound in the other (and, as I believe, much
older) series. Yet probably few geologists have had better oppor-
tunities of meeting with such rocks if they really did occur in the
Alps. Surely, then, if the “ upper schists ’’ (as I have termed them)
are merely Jurassic sediments, to which a crystalline structure has
been given in the process of mountain-making, these cases of transi-
tion, these instances of resemblance, should be of common occur-
rence. ‘There should be a frequent tendency among the sediment-
aries to assume the crystalline character, among the crystallines to
revert to the sedimentary. This argument will perhaps not appeal
very strongly to those who have devoted themselves to a minute and
elaborate mapping of a single district; but I am confident of its
effects with those who have compared rock with rock, and section
with section, from one end of the Alps to the other.

Thus the Altkirch section, a difficult and perplexing one in any
case, presents us with such anomalies, if interpreted as a case of
selective metamorphism in a group of Jurassic rocks, that it must
not be made the basis of a theory which is to be applied with un-
questioning confidence to every part of the Alps. As it seems to
me, the evidence tendered on the spot demands a verdict of * not
proven;” that obtainable in other parts of the Alps, as I now hope
to show, will compel us to add “ not provable” *.

* T ought to mention that Stapf, in his description of the rocks from the St.
Gothard Tunnel, states that he finds in one rock (No. 43), about 2600 metres
from the north entrance, organic remains like sponges, corals, or Polyzoa. One
of these he figures and describes (Zeitschr. d. deutsch. geol. Gesellsch. xxx.
p. 130, pl. vi.). He admits that in the same rock a network structure occurs
which is due to the infiltration of graphite into the cleavage-planes of calcite.
I have examined microscopically specimen No. 43 in the collection belonging to
the British Museum, and cannot satisfy myself that there are any true remains
of organisms, but think that the imitation structures (often very curious) are of
mineral origin. A remarkable pseudo-organic structure is described by Prof.
Heddle (Min. Mag. vol. v. p. 275), and the same epithet, as is well known,
would be applied by many to Hozoon. The rock itself macroscopically and
microscopically appears to me to be closely related to the crystalline limestone
described above, and to differ much from any Mesozoic limestone known to me.
After arriving at this conclusion, I found that Dr. Otto Meyer and Prof.
Zirkel were of the saine opinion (Untersuchungen iiber die Gesteine des Gothard-
tunnels’ (Inaug. Diss.), Leipzig, 1870). For the above references I am indebted
to Mr. Miers. The rock which has furnished No. 48 lies just south of the schis-
tose slate described above, and appears to pass into the white fissile marble.

. RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 199

2. Tue Scuists oF THE VAL Prora.

The Val Piora is a well-marked and fairly wide upland glen run-
ning roughly from east to west; at its lower end is the Iago di
Ritom, a sheet of water about 2000 metres long by 500 wide.
Formerly it must have extended about 880 metres further east, the
upper end of the rock-basin in which it lies being now a level and
rather marshy meadow. ‘The water from the western end escapes
through a narrow gap in the mountains and leaps down (at first in
fine cascades) to the Val Bedretto. The lake is 1829 metres above
the sea, and the range rises rapidly on either side of the gap, on the
west to about 2200 metres, on the east to a long ridge, which varies
from about 2000 to 2800 metres. On the northern side of the Val
Piora the mountains rise steeply to the watershed parting the drain-
age systems of the Rhine and Rhone from that of the Ticino. As is
shown on Dr. von Fritsch’s map, the southern range consists of
eneiss, the northern of a group of gneisses or schists. Of these the
members which crop out nearest to the Val Piora are commonly
characterized by the conspicuous presence of red garnets and green
actinolite; they are lithologically identical and practically continu-
ous with the well-known rocks displayed on the lower part of the
southern slope of the St. Gothard Pass, for which (merely to avoid
circumlocution) I have proposed the name of the Tremola schists.
The Val Piora itseif is occupied by the rauchwacké and its associated
rocks *, and by the group of schists with which we have now to
deal; this apparent trough, sometimes narrowing, sometimes widen-
ing, extends eastwards along the upper part of the southern slope of
the Lukmanier Pass, and westward across the Val Canaria to
Airolo in the Val Bedretto, and in both directions far beyond these
limits.

At the first glance the map suggests that the last-named schists
overlie the rauchwacké and occupy a trough between the two
masses of gneiss. But a further study of it, and still more an exa-
mination of the terrain, indicates the existence of the gravest difti-
culties in this hypothesis. For the moment, I will place the rauch-
wack¢é on one side and confine myself to the mineral characters and
relations of the schists: that these form one group of rocks of con-
siderable thickness, but very closely related, cannot be doubted.
They vary much in mineral character, but for the present minor
details may be passed oyer in order to concentrate our attention on the
more salient features. We will refer to them again, for the sake of
brevity, as the Piora schists. They exhibit two fairly well-defined
subgroups or types—one, the thickest and most persistent, being
strong schists consisting of alternating bands (of variable thickness)
of a brownish or yellowish quartzose rock and a dark, sometimes
almost black, micaceous schist. Some members of the latter are
characterized by the presence of numerous garnets, about the size
of a pea, but sometimes rather larger, generally black. So far as

* For brevity and distinctness I will refer to this group, which consists of a
peculiar limestone with dolomite, anhydrite, or gypsum, as the ‘ Rauchwacké.”

ov. G. S. No, 162: P

200 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

I have been able to ascertain, these, though occasionally very abun-
dant, are rather impersistent in their occurrence. Apparently under-
lying these is a zone which, were it not still less persistent and
much thinner, one would be disposed to regard as another subgroup ;
this is characterized by the presence comments of large staurolites,
sometimes of kyanite (disthene).

The second subgroup consists of a number of calcareous and mica-
ceous schists, occasionally quartzose, generally light in colour, fre-
quently varying from cale-mica schists to a slightly micaceous
marble, the latter usually of no great thickness. I will refer to the
first as the Dark-mica schists (‘‘Graue oder Biindner-schiefer in
Glimmerschiefer tibergehend,” von Fritsch), the garnet-bearing
variety as Black-garnet schists* (“‘Granatfuhrende schwarze Schiefer,
id.), the next as Disthene schists (‘‘ Disthen und Staurolith fuhrende
Schiefer,” id.), and the last as the Cale-mica schists (“ Kalkglimmer
Schiefer,” 2d.).

After examination of these rocks both in the field and with the
microscope the following conclusions appear to be beyond any
doubt :—(1) That the series originally consisted, mainly if not
entirely, of sedimentary deposits; (2) that its members are now
truly crystalline and generally rather coarsely crystalline; (3) that

Fig. 1.—Section (diagrammatic), with interpretation, across
Lake Ritom and the Val Prora.

F?
@) EF
i}
B ah
) LE
Vy yf,
iu Le rr a
hf Wp pe
"Vt, Yuye Mig
; it dy
ay, fs
t ae
G. Gneiss &e. A. Dark-mica schist &e. B. Staurolite schist.
C. Cale-mica schist. F. Fauits. (1). Lake Ritom.

after they had become foliated rocks they were subjected to pres-
sure, often great, which very commonly, but by no means always,
has acted at right angles to the original foliation—that is, these
rocks exhibit a cleavage-foliation as well as a stratification-foliation,
though very often the two are coincident in direction.

What, then, is the geoJogical position of these rocks ? The annexed
section (fig. 1) exhibits their mode of occurrence in the neighbour-

* T formerly spoke of it as melanite-schist, but from a partial analysis made
by Dr. Grubenmann (Mitth. der Thurg. naturf. Gesellsch.. Heft viii. 1888)
the mineral appears to be an alumina-lime garnet, its blackness being due to
inpurities which prevented any precise determination.

" Oe a,

RELATIUN TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 201

hood of the Lago di Ritom. To a considerable extent it is diagram-
matic, as it is designed only to indicate the relation of the principal
types. The questions, then, for which we must seek an answer are
these :—(1) Are we dealing with a simple fold? (2) What is the
order of succession in the series? Omitting for the moment the
rauchwacké from our consideration (as we shall presently see we
are justified in doing) it is evident that these schists in the Val Piora
do not form a simple fold. ‘he Dark-mica schists with the Black-
earnet schists are exposed on the Alpine pastures between the Lago
di Cadogra and the Lago di Ritom. ‘They form the cliffs overlook-
ing the Ritom Boden, whence they sweep upwards in a westerly
direction, and may be traced up the flanks of the Pian Alto and on
the summit of Fongio, two mountains on either side of a pass west.
of the Lago di Ritom, leading into the Val Canaria. Beneath these
(apparently) we find above the S.E. end of the Lago di Ritom some
kyanite schists, and at the N.K. end the well-known schist with
fine staurolites *, which overlies a white quartzite. The latter rocks
J did not succeed in tracing very far, and could not find at the top of
the above-named pass. The Calc-mica schists appear to rise from
beneath this quartzite, and are found in great force on the hill-side
leading to the pass. Commonly they are concealed beneath turf
or débris, but a fair section is obtained in a gully near the N.W.
corner of the jake. The neighbourhood of the col affords important
evidence (fig. 4, p. 208). North of it rises the Pian Alto, a craggy
mass of the Dark-mica schist. Just west of it, and a few dozen
feet lower down, some rauchwacké crops out from the turf. The
former rock occurs on the rounded summit of Fongio, on the S. and
S.W. sides of which is the Black-garnet schist f. At the base of
the actual summit and near the edge of the crags descending to
the Val Piora we find schists of the Calc-mica group with some
white marble, much crushed, and a little further to the south
eneiss, also much crushed, crops out. It is therefore clear that
the greater part of the Calc-mica-schist group is cut out by a
fault.

If we follow the “ Piora schists” eastwards to Olivone and
westwards to Binn (and over all this distance they can be traced
practically without a break), we find that the characteristic Black-
garnet schist is repeatedly picked up and that this rock generally
oecurs very near to the gneiss or to the Tremola schists—that is, to
some member of what I have termed the Lepontine series, which is
unquestionably the more ancient. I think therefore that the appa-
rent order of succession in the Val Piora is the reverse of the true
one, and that it exhibits only a part of an overfold the remainder of
which is cut out by thrust-faults (fig. 1). It is possible that the
Dark-mica schist also may be divided from the Tremola schists by a

* Dr. von Fritsch gives 20 metres as its maximum thickness. I have never
seen so much as this exposed.

+ The whole of Fongio south of the rauchwacké is coloured in Von Fritsch’s
map as gneiss. This is one of the few errors which I have noticed in this ex-
cellent map.

p2

202 PROF, Tf, G@. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

fault ; but on this matter I have not been able to come to a conclu-
sion, and I regard it as subordinate in importance.

This Piora series, aS already said, is very variable in mineral
character. As I have previously noticed some of its members*, and
as 1t has been described in this or that locality by Dr. von Fritsch,
Dr. Grubenmann, and others, I shall pass very briefly over the macro-
scopic characters of all but the Dark-mica and Black-garnet schists,
which alone have a direct relation to the main subject of this paper.
Suffice it, then, to say that all the members of the Calc-mica-schist
group are distinctly (and, if uncrushed, moderately coarsely) erystal-
line; and that they almost invariably exhibit a cleavage-foliation
which often is very marked. Sometimes it seems to have obliterated
the original ‘ stratification-foliation,” sometimes it coincides with it,
sometimes it crosses it at high angles. The evidence for all this
has been so often stated in detail by myself that I need not weary
the reader by repeatingit 7. White mica is common, and generally
glazes the “sheen surface;” but some specimens have a fair amount of
greenish or brown mica. Light-coloured quartz-mica schists and a
rather soft schist with two micas are found; but, as said above, in this
district the rock is more commonly calcareous, varying from calc-
mica schist to white shghtly micaceous marble. Rocks with iden-
tical lithological characters occur at intervals from one end of the
Alps to the other, and are connected by other schists which exhibit
only varietal differences.

On the staurolite- and disthene-schists it is needless to dwell, for.

these also have been often described. It may suffice to say that I
have examined microscopically specimens of both, and that they are
true crystalline schists. Once, no doubt, they were sediments; but
all trace of their original clastic structure has been obliterated.
The crystals of staurolite and disthene are sometimes as much as a
couple of inches in length, though this, so far as I have seen, is an
exceptional size.

The Dark-mica schist, however, with the Black-garnet variety,’

demands a longer notice, because it is through these that a link is
sought with the fossiliferous Jurassic rocks. It will suffice, however,
to describe the latter schist minutely, because the description, when
the garnets are omitted, will apply, in general terms, to the former.
The Dark-mica schist with black garnets is rather fine-grained, of a
very dark colour and graphitic aspect. The matrix, especially on
slightly weathered surfaces, exhibits a fairly, sometimes very, distinct
foliation, though the mineral constituents do not appear to be large.
Though the rock in cross-fracture has a strong tough aspect, resem-
bling that of one of the harder schists, it has a more or less fissile
structure, doubtless the result of pressure subsequent to foliation,
and the ‘“‘*sheen surfaces” exhibit a distinct lustre, which varies
from one not very unlike that of “ black lead” to that of a silvery

* Anniversary Address to the Geol. Soc. (Proc. Geol. Soe. vol. xlii. (1886),
p. 45-47).
: t Quart. Journ. Geol. Soc. vol. xlii., Proc. pp. 386, 37, 69; see also vol. xlyv.
pp. 82 &e.

ee ee

———

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS, 903

mica. On examining a cross-fracture with a lens many glittering
minute black particles are seen to be thickly interspersed with the
more micaceous constituents. Garnets are numerous; they are
seldom more than one third of an inch in diameter, and commonly
about the size of peas. Though somewhat distorted, evidently
by pressure, they exhibit fairly definite crystal faces (dodecahedral)
and the usual aspect of a dark garnet when fractured; but not un-
frequently they are traversed by a rude cleavage coincident with the
divisional planes of the rock, and obviously due to the same cause.
Their crystalline form is often better exposed on weathered surfaces,
and in this way sometimes fairly regular crystals may be obtained.
It is rather difficult to detach them from the matrix. The faces
are then lustrous, though corroded by the more rapid weathering
of the enclosed impurities, which are abundant. The ordinary colour
is black, but not seldom a slightly brown or reddish tinge may
be noticed, and occasionally they are of a deep claret-red.

The folia in the matrix bend round them, and there is every indi-
cation that the rock has been subjected to severe pressure since they
were formed and it was foliated. This dark schist is associated with
layers of a light brown to greyish rather fine-grained quartzose
rock, of somewhat felspathic aspect, apparently resulting from the
alteration of a rather earthy sandstone. The one rock passes
rapidly into the other; sometimes the two are closely interbanded,
lamine of black schist alternating repeatedly with those of quart-
_ aite, the thickness of either varying from that of a stout card up to
about half an inch, now one now the other predominating; but
sometimes the rocks occur in much thicker masses. Garnets are
common in the dark Jayers, sometimes bulging out a little beyond
the surface of a thin one, but are very rare and small in the
quartzose layers. The pressure to which the cleavage-foliation is
due has acted commonly (in the Val Piora) at right angles to this
lamination, but there are occasional exceptions to the rule, and
the rock then exhibits contortions.

Some details of the microscopic structures of these Piora schists
are given in the Appendix (p. 224). It may suffice to say here
that, after careful study of the rocks of this group in the field and
with the microscope, the following conclusions appear to me fully
established :—

1. This group was once a series of more or less banded sediments,
not unlike some of our Coal-measure shales and sandstones.

2. By some agency these were completely metamorphosed, all
traces of the clastic structure of the sandstones being obliterated,
and a number of new minerals formed, among them (in the black
bands) garnets of considerable size.

3. The whole mass was subsequently exposed to severe pressure,
doubtless during one or more of the processes of mountain-making,
which has produced the usual effects.

4, There is no evidence whatever to show that a pressure definite
in direction had anything to do with the production of the garnets.
So far as we can tell, they, as is usual with the garnets in the Alpine

204 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

schists, appear to have developed themselves with equal ease in all
directions in the enveloping matrix, and any deformations which they
may present have been subsequently impressed upon them.

3. Tur RAvcHWACKE AND Its RELATION TO THE SCHISTS.

(a) Val Piora Sections.

Rauchwacké is a name employed by the Swiss geologists to desig-
nate a peculiar rock which occurs, as a glance at their map shows,
in a curiously irregular way, generally in elongated patches, over a
large part of the Lepontine and Pennine Alps. Commonly it is
a rather cavernous or carious-looking limestone of a yellowish,
ochreous, or darkish cream-colour,—not unlike some rather soft
varieties of tufa—which bruises under the hammer, is rather tough
than brittle, and has a dusty surface. Itis frequently associated with
rather thick beds of anhydrite or gypsum or passes into a dolomite,
in which condition it is usually, so far as I have seen, harder and
more solid. But, as a rule, the rauchwacké is a rather soft, non-
crystalline rock, and, even when dolomitic, is not so ‘‘ metamorphic ”
in aspect as many of the “dolomites” of the Southern Tyrol. It
frequently contains mica, usually more or less silvery. The irre-
gular form, the variable size, the unequal distribution, and the occa-
sional association in flakes of this mineral suggest that it is in great
part if not wholly derivative, an idea which is confirmed by the fact
that occasionally fragments of mica- and other schists are very
abundant*. The Swiss geologists regard the rauchwacké + as a Tri-
assic rock, and I see no reason for doubting the general correctness
of the reference. There can be no doubt that in some cases it is
overlain by Jurassic rocks +. Though once or twice the rauchwacké,
from the abundance of mica and the effects of pressure, superficially
resembles one of the calc-mica schists, no one, after a study of the
rock in the field or even of a fair series of hand specimens, would
think of calling it a ‘“‘ metamorphic” rock in the ordinary sense of
the word, or of suggesting a close relationship between it and one of
the above-described schists. In the one a detrital or fragmental
character, when it occurs, is perfectly retained; in the other, though
doubtless the rock had a clastic origin, not a grain of the original con-
stituents can be identified. If, then, we are required to regard this
soft unaltered rock as the basis of the great series of crystalline
schists described above, we should be involved in such serious theo-

* Dr. Grubenmann states that in the gypsum he found quartz, pyrite, mica,
tale, tourmaline, disthene, and zircon, most of which are also mentioned by Von
Fritsch (doc. cit. pp. 119, 120). He does not, however, appear to have thought
it necessary to consider the possibility of their being derivative, but assumes
them to be authigenous. I should have thought that the appearance of the rock
would have suggested the need of rigorous demonstration,

+ For brevity I use the term inclusively, the presence of dolomite, anhydrite,
or gypsum being, for my present purpose, of subordinate importance.

+ Von Fritsch (doc. cit. p. 3) says the Lower-Lias Belemnites Oppeli has been
found on the Nufenen Pass.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 205

retical difficulties that we are entitled to demand a very clear
demonstration of its stratigraphical position. What instance, which
has stood the test of careful examination, can be produced where a
bed, practically unmetamorphosed, is intercalated in a thick series
every member of which is highly crystalline? Making every allow-
ance for differences of composition (though it might be observed
that highly crystalline calc-schists, limestones, and dolomites are
common enough among the supposed overlying series), we are
still compelled to ask, What process of selective metamorphism can
have produced such a result? I put this question in the interests
of ‘“‘a rational uniformitarianism.” Accurate observation and
scientific induction lead us to believe that Nature acts in accordance
with laws, and that these are related to their results. This would
be an anomaly without precedent, and thus cannot be accepted
without very clear evidence.

But when we come to study the rauchwacké more closely (con-
fining ourselves for the present to the Lepontine Alps) we find that
to regard it as the base of the Piora series (as is done by some of
the Swiss geologists) would lead to results which would be often
perplexing and sometimes self-contradictory.

For instance, in the Lukmanier-Piora district a brief study of the
map shows that the distribution of the deposit is very puzzling, and
our difficulties grow the more minutely we examine the terrain.
Below the mineral-bearing Jurassic beds of Scopi and Alp Vitgira the
rauchwacké is thin and sometimes wanting, but it occupies a consi-
derable area a little below the summit of the Lukmanier Pass, and
the group * soon attains a thickness which can hardly be less than
a hundred yards, and may probably be much more. This mass
(which seems as if embayed between Scopi and the hill of gneiss
facing it on the 8.W. across the open basin traversed by the upper
part of the road) is an offshoot from a broad strip which runs east-
ward to beyond the Val Greina tT, and westward towards the Val
Piora. ‘The former part, I may remark in passing, is bordered on
the northern side by beds indubitably Jurassic, on the southern by
true schists t. The western strip of rauchwacké crosses a water-
shed, where, in the Pizzo Columbe, unless appearances are very
deceptive, it can hardly be less than 700 feet thick. Thence it
passes into the Val Piora. Here its distribution is very perplexing,
on the hypothesis of its superposition to the Piora schists. On the
northern side of the valley it appears to occur between these and
the Tremola schists. West, and perhaps south of the lake it appears
to divide the former series in one part from mica-gneiss, in another
from ordinary gneiss; but the mass which extends westwards from

* There is a thick bed of anhydrite or gypsum.

| This joins the Val Levantina at Olivone.

{ This is the testimony of Dr. von Fritsch’s map. Personally I can only
answer for the Lukmanier road, which in descending crosses black-garnet
schist, quartz-schist, and mica-schist with reddish garnet, staurolite, and kya-
nite—rocks which bear a general resemblance to those of the Val Piora. Lower

down, at the opening of the Val Greina, in the strike of the same mass, cale-
mica schists are abundantly developed.

206 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

the Pizzo Columbe narrows and disappears in the middle of the
Piora schists. This, with the occurrence of one or two lenticular
patches in like position, can only be explained, if the above hypo-
thesis be correct, by very peculiar rolling and faulting.

Not less perplexing is the occurrence of another irreguiar isolated
and probably interrupted strip on either side of the Pian Alto, west
of the lower end of the Lake Ritom.

Our difficulties increase as we examine the sections in detail.
Assuming the rauchwacké to be at the base of the Piora schists, let
us direct our attention to two sections in ravines on the south side
of the Ritom Boden. If we climb up the ravine traversed by the
second stream (counting from the west) we find the rauchwacké
resting upon gneiss. The upper part of the latter rock is tremend-
ously crushed ; its quartz-veins are rolled out and smaslied ; it is
converted into a fissile silvery schist ; above it comes a foot or two
of rock, which is practically past identification. It may be crushed
gneiss, friction- or basement-breccia, for it has been smashed beyond
recognition. Then comes the rauchwacké, slabby and rather schis-
tose. Here and there it contains a few fragments; but these, so
far as I saw, were gneiss, so they prove no more than that the rock
is much later than the Lepontine gneiss (which all admit) and is
not highly metamorphosed. Here, then, the rauchwacké either rests
directly upon the gneiss or is brought against it by a thrust-fault.
Let us now pass on to the next ravine, which for a considerable
distance runs almost along the other edge of the patch of rauch-
wacké. In the lower part we find the following section, not, indeed,
continuously exposed, but indicated by crags and ridges outcropping
from turf or débris (fig. 2) :—(1) Dark-mica schist (well displayed) ;

Fig. 2.—Section in lower part of Ravine, south-east of
Lake Ritom.

A. Dark-mica schist. C. Cale-mica schist. R. Rauchwacké.
The part left blank is covered ground.

(2) Calc-mica schist, parted by the stream from (3) rauchwacké.
But about 400 feet above the lake we find (fig. 3):—(1) Dark-mica

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS, 207

schist (as before); (2) Disthene schist; (3) Gneiss rather crushed ;
(4) Rauchwackeé.

Fig. 3.—Section in upper part of Ravine, south-east of
Lake Litom.

.
eh aA

A. Dark-mica schist. B. Disthene schist. G. Gneiss. R. Rauchwacké.
The part left blank is covered ground.

In these sections (A) is a thick mass, well exposed in a line of
crags; (B) in the latter is a thin band, the absence of which from
the former section is of little importance, for it may be concealed by
débris or have died out; but after this we find in the one case calc-
mica schist in its ordinary position, and apparently overlying the
rauchwacké, while in the other it is wanting, and its place is taken
by a rather thin mass of gneiss (which ought to underlie the rauch-
wacke). If, then, we adopt the idea of a regular sequence and
simple fold, we are involved in hopeless confusion; while an exami-
nation of the rocks in the field itself suggests that the rauchwacké
is caught between two sets of thrust-faults, one of these being, very
probably, the southern main fault already mentioned.

We pass on to the section already incidentally mentioned near
and about the summit of Fongio (fig. 4). Here we find, apparently
in descending order :—(1) Dark-mica schist; (2) Rauchwacké ; (3)
Dark-mica schist, with Black-garnet schist; (4) Calc-mica schist ;
(5) Gneiss (crushed). Here, then, the rauchwacké appears to be
intercalated in the Dark-mica schist. These sections also, if read
from the south side, would indicate that the Cale-mica schist was
the lower rock, while if we read from the north side it would be
the Dark-mica schist. Obviously, then, the idea of a simple trough
is inadmissible. Furthermore, this strip of rauchwacké, where it
is exposed in the ravine leading down from the alp between Fongio
and the Pian Alto, contains numerous fragments of schists which, to
our eyes, were undistinguishable from members of the calc-mica
schist group, which crop out in the same ravine, as already stated.

208

Fig. 4.—Diagrammatic Section across Pass between Prun Alto and Fongio.

Pian Alto

PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

F, Faults.

R, Rauchwacké.

G. Gneiss.

C. Cale-mica schist.

A. Dark-mica schist &e.

(b) Val Canaria Section.

A little west of the district
just described is the Val
Canaria with the noted sec-
tion described by Dr. Gru-
benmann. His memoir is a
careful and elaborate study
in petrography, so that I may
pass over the minor details

- and confine myself to the

petrology — that is, to the
inductive treatment of these
details—where I cannot say
that the author appears to
me to have been equally suc-
cessful. This section, as Dr.
Grubenmann states, is_ best
seen by climbing up a ravine
which runs roughly from
north to south*, and has
been excavated by a small
stream descending from the
Alpe Pontina to the lower
part of the Val Canaria.
Here, on either side of the
ravine, is a considerable mass
of rauchwacké, with gypsum
or anhydrite and some dolo-
mite (fig.5). Above this a
thick mass of various schists
is ascended, and then comes
another thick mass of rauch-
wacké &c. followed by a small
zone of schists similar to some
of those below ; above which
we find representatives of
the Tremola schist and the
eneilss 7. According to Dr.

* It is not a very easy climb in
all parts. More than once, if we
had not had our ice-axes to chip
an occasional step in the débris, we
should have had to make a détour.

t+ Thus far the section drawn by
Mr. Eccles and myself agrees with
that given in general terms by Dr.
von Fritsch, and in greater detail
by Dr. Grubenmann. Between our
own section and that of the latter
are some slight differences of detail,
but they are insignificant ; and as
we went only once up the ravine
(and the work is not easy) he may
be more correct than ourselves,

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 209

Grubenmann and others we have here the two ends of a fold of
rauchwacké enclosing the overlying schists, the axial plane of the
trough dipping (as is so commonly the case) to the north. But
when we come to study the annexed section (fig. 5) minutely we
find that, though at first sight the Calc-mica schist seems to rest
upon the rauchwacké and to be succeeded by the Black-garnet schist,
we cannot make out any definite order in the upper portion of the
fold (where, of course, the lower should be repeated). Again, as we
pass over the outcropping beds in the ravine, we notice constant
evidence of squeezing, sometimes of crushing, with gliding planes
and other indications of thrust-faulting. But when we have passed
through the upper mass of rauchwacké, we are confronted by a
further difficulty: we find ourselves, after crossing a very few feet
of a mica-schist or gneiss, separated from the mass of the Tremola
schists by a comparatively thin zone of black-garnet schist and
silvery mica- (? disthene) schist *, which are undistinguishable from
those included in the fold below.

The identity of the latter, as a group, with the Piora schists cannot
for a moment be doubted. If, then, the hypothesis that in some
way or other we have the thick mass of the Piora schists compressed
into a fold measuring only a few hundred feet across, be correct,
what explanation is to be given of the occurrence of certain of its
components below the rauchwacké, which is the basal member of
the trough ?

But this is not all. Let us now examine the rauchwacké on
either side of the supposed fold. In the lower member mica, mostly
silvery, is fairly common. This, in its form and distribution, sug-
gests a detrital origin, and there are sundry small flaky bits which
are curiously like fragments of schist. Similar mica occurs in the
upper member, but here, near the top, we find that the rock becomes
a true breccia full of angular fragments, sometimes more than two
square inches in area, similar to schists which occur in the ravine
belowy. That these fragments were broken from members of the
Piora series we had not theslightest doubt. It is therefore evident
that in this Val Canaria section we are dealing not with a simple
trough, but with an overfold broken up by a series of thrust-faults,
as. shown diagrammatically in the annexed figure (fig. 6),—that the
apparent infolding of the Piora schists by the rauchwacké is wholly

* Dr. von Fritsch maps these two beds as identical with the disthene-schist
and garnet-schist below and in the Val Piora. Dr. Grubenmann, though he
says he did not see any disthene under the microscope, admits the identity of
the former with the “two-mica” (disthene) schist below. To myself they are
macroscopically undistinguishable. I was not fortunate enough to find a very
characteristic exposure of the black-garnet schist, but scattered blocks are nume-
rous, and I have no doubt of the accuracy of Dr. von Fritsch’s mapping. I
find, on examination, that the ‘“disthene” schist contains grains of a mineral
like staurolite, and I think I can detect disthene (see p. 227).

t+ We did not, indeed, discover the black-garnet schist, but found the so-called
disthene schist and other silvery and greenish micaceous schists which occur in
the Piora series; these fragments, however, appear to be less modified by subse-
quent pressure than the rocks 77 s¢¢wu below.

210 PROF. T. G. BONNEY ON ORYSLALLINE SCHISTS AND THEIR

Fig. 5.—Section in Ravine, Val Canaria.
(Relative thicknesses of the beds uncertain.)

A. Black-garnet schist.

B. “ Disthene ” schist (‘‘ Two-mica schist ” of Dr. Grubenmann). (2). Thin
band of same.

C. Cale-mica schists, marbles left white. (1) forms a small cascade.

R. Rauchwacké. (3). The breccia of schist-fragments. (4). Thin zone of
variable schists. )

G. Gneiss or Tremola schist.

Fig. 6.—Diagrammatic interpretation of Section in Ravine,
Val Canaria (fig. 5).

The letters indicate the general position of the beds mentioned in the explana-
tion of fig. 5. F. Probable position of more important faults.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. pt a

illusory,—and that the latter really overlies andis much later in date
than the former.

The evidence in this locality appears to me decisive, and it is of
a kind which would render it needless to pursue the investigation
further ; for the schists of the Piora group are so different from those
of the Tremola group that there is little danger of confusion between
a member of the former and one of the latter. Still it may be well
to add that the above case is by no means an isolated one. For
instance, near the top of the Nufenen Pass, as will presently be de-
scribed, some rauchwacké occurs. This also contains fragments of a
satiny mica-schist, resembling the so-called disthene-schist mentioned
above. Again, in the lower part of the Binnenthal, the path to the
village of Binn crosses some rauchwacké at the mouth of a ravine
cut deeply into a mass of dark schists which can be traced up the
valley above Binn, and ultimately passes eastward by the flank of the
Ofenhorn to the Gries Pass, the neighbourhood of the Nufenen Pass,
and the Val Bredretto. These schists are dark-coloured mica-schists,
sometimes rather calcareous. In their lower part they include a
mass of crystalline dolomite*, and the peculiar black-garnet schist
occurs in the bed of the river a short distance above Binny. The
connexion of these schists with the Piora group cannot be doubted ;
both form part of the same great series which, as I have already
said, can be traced from one end of the Alps to the other. Hence
they ought, if the hypothesis which we are discussing be correct, to
be more modern than the rauchwackeé. But this contains fragments
of a rock which has a remarkable resemblance to these schists.

One objection might, however, be made. These fragments are
neither numerous nor large, and it is uncertain whether they repre-
sent the true Binn schists. While there can be no doubt as to the
nature of the rock through which the greater part of the ravine is
cut, there is some difficulty at the opening. A short distance higher
up there are some indications of another bed ot rauchwacké, and the
rock, which south of this is an undoubted schist, suddenly assumes
a more slaty character, and it is difficult to determine whether we
have found the schist in a very crushed condition or a true slate.
Such a rock in this part of the Rhone valley (as, tor instance, near
the foot of the Simplon Pass) is often found in contiguity with the
schist and bears some resemblance to it (being probably largely
derived from it), and might very well occur just in this position.
After careful study of slides cut from two rather typical specimens
collected in the neighbourhood of the rauchwacké, I incline to
regard this rock as only a phyllite, not a true schist. Be this as
it may, the same rock indubitably occurs as a fragment in the
adjacent rauchwacke, This, however, contains other smaller frag-
ments more closely resembling schists, besides mica corresponding

* A white saccharoidal rock resembling the marbles which elsewhere occur
interbedded with schists and totally unlike any rock I have seen in the rauch-
wacké group.

+ It was detected by Mr. Eccles as we were returning from an ascent of the
Ofenhorn.

ALI PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

with that of the crystalline schists, quartz, rutile, &e. Soif we pay no_
attention to the latter constituents, and claim the underlying rock
and the included fragments as representatives of the Carboniferous
series, then, if the dark-mica schists of the Binnenthal are to be
regarded as Jurassic, how is it that these have been so completely
altered, while a neighbouring rock, very similar in composition,
which before Triassic times had attained to practically its present
state of metamorphism, has been so much less changed * ?

Again, some 25 miles away to the south-west near the side of
the Gorner glacier and on the south flank of the Hochthiligrat,
in a region consisting partly of cale-schist, marble, quartz-, chlorite-,
and other schists‘ which lithologically resemble the most highly
crystalline members of the Upper group of Alpine schists, partly of
gneisses of the ordinary character, which appear to underlie the
latter, we find a small mass of rauchwackeé. It is the usual yellow,
friable, non-metamorphic rock. At the first sight it appears to be
interbedded on the mountain-side with the above-named schists and
gneiss, but a closer examination indicates that it occurs in a very
“patchy” way, and that its outcrop hardly coincides with that of
the other masses. This rauchwacké contains not only scales of
white mica, very detrital in aspect, but also indubitable fragments
of the silvery gneiss with which it is apparently interstratified. Even
if it be contended that these fragments only represeut the gneissic
series, the greater age of which is admitted, we have still to explain
the anomaly of a rock which retains the characters of an ordinary
sedimentary deposit, directly underlying a great mass (containing
rocks of very different composition, but some of which are also lime-
stones) which has become highly crystalline.

In short, this rauchwacké, wherever I have seen it +, is not a rock
to which I should apply the term metamorphic. I have little doubt
that it will be found, in many places, to contain fragments of the
great group of schists to which the Piora schists unquestionably
belong. But I always felt so convinced that it was a rock of com-
paratively late date, and that its apparent interstratification with
the schists or gneisses was illusory, that until my last visit to the
Alps I never took the trouble of searching for fragments.

It might, however,’ be suggested that in the above cases I have
mistaken a consolidated talus of schist and rauchwacké—a formation
of recent date—for an integral part of the latter rock. It may

* On referring to the ‘Beitrage zur geol. Karte der Schweiz,’ Lief. xxiii.
pl. i, I find this objection is not likely to be advanced. The rauchwacké is
represented as underlying all these dark rocks of the Binnenthal, which are
marked as forming one mass, and thus are implicitly claimed as Jurassic.

+ These, in the new edition of the Zermatt sheet of the Survey map, are
coloured “ Lias-Jura,” while the older map simply indicated the lithological
character of the deposits. This is one of the unfortunate changes which has
converted the map from an accurate petrographical record into an expression
of the hypothetical opinions of certain geologists, and thus has greatly dimin-
ished its value.

+ I have often come across it, and have also examined typical specimens in
the Berne Museum.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 213

therefore save future trouble to say that the possibility of such an
error was always present to our minds, and that we convinced
ourselves, at any rate when the rock was in situ, that we were not
making any mistake. On this point we were especially careful in
the Val Canaria section, which alone would be sufficient for our case.
But since my return to England I have obtained evidence which
seems to me to place the accuracy of our observations beyond
question. ‘The upper band of rauchwacké in this section—that in
which we found the fragments of schist—is continuous with the
mass which at a little more than a mile distance along the outcrop
is pierced by the St. Gothard tunnel at Airolo. In the British
Museum is a collection of rocks illustrating the masses traversed by
this great work, which by the courtesy of the authorities of the Mineral
Department, I have examined. At the south end of the tunnel a
considerable thickness of rauchwacké was pierced, and the collection
contains several specimens of the rock. In at least three, taken
from between 60 to 72 metres from the entrance, fragments of
schist, like those in the Val Canaria, distinctly occur. Another,
fonnd at 78°5 metres, has similar fragments of considerable size.
Another, at 83 metres, exhibits two parallel slabs of the ‘* two-mica ”
(so-called disthene) schist, which I have described above, cemented
by rauchwacké. ‘This has been taken either from a mass of coarse
breccia or from a very unequal junction-surface of the schist and
rauchwacké. At 85 metres is the schist itself en situ. Thus this
section and that in the Canaria ravine are as nearly as possible
identical, and it is impossible to deny that the breccia occurs at the
base of the rauchwacke.

4, Tur Jurassic Rocks contaINInG Fossrts AND MINERALS.
(a) Preliminary.

The occurrence of fossils in the dark, slaty, sometimes schistose,
but non-crystalline rocks of the Alps has long been well known.
Most of these instances have no more bearing on questions of
metamorphism than the occurrence of fessils in certain districts of
Devonshire or North Wales. ‘The rocks are slates, at most phyllites,
not true schists, and probably no reference would ever have been
made to them in the literature of such questions, had not so much
confusion been produced by the vague use of the term schist.
Studer, however, many years since spoke of finding Jurassic fossils
in the same rock as garnets, and, as I have already said, specimens
illustrative of this were exhibited by Dr. Heim at the meeting of the
Geological Congress in 1888, which, through his courtesy, I was
enabled to examine, so far as could be done with a lens. They
were of much interest, and in one or two cases certainly bore a
strong resemblance to the Black-garnet schist described above.
Still I was not quite satisfied of the identity of the rocks, and some
scepticism seemed more than justifiable, for it was very difficult to
understand how such a fossil as a Belemnite could have retained

214 PROF, T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

its characteristic form while molecular changes of such importance
were taking place in the matrix of the rock. Such inferences as
one could draw from the analogy of other cases in Nature seemed to
render this one extremely improbable, though of course one could
not say impossible *. The more I considered the question, the more
I regarded it in the light of the evidence which I had obtained from
my previous studies both in the Alps and in other regions, the
greater appeared the difficulties involved in the hypothesis, the
stronger the probability of some mistake.

I have already, I trust, shown that the Black-garnet schist of the
Piora group underlies the rauchwacké, and therefore cannot be
identical with these supposed granatiferous rocks of Jurassic age,
which it is universally admitted overlie the rauchwacké and, like it,
belong to the Mesozoic system. Still we have to consider the
possibility that the fossiliferous rock has been converted into a
schist undistinguishable from the former. My previous experience
made this hypothesis appear very improbable to me, but I thought it
ought to be fairly tested. After examining the sections near the
Lukmanier and Nufenen passes I deemed it needless to carry my
investigations further.

In describing the results of these I will not begin by giving a
detailed description of the supposed garnet-bearing schist in which
fossils occur, but will merely state that the mineral constituents
appear either as flattened spheroidal or ovoid graius, about the same
size as the garnets, or as somewhat rounded and occasionally rather
elongated prisms. Before leaving the subject I shall endeavour to
summarize the principal characteristios of these minerals in order to
compare them with those of the Black-garnet schist and its
associates. Meantime, in order to avoid prejudging the question, I
will refer to the rock in question as “the spotted rock,” a. trivial
name which I think expresses fairly accurately its most marked
characteristic.

(b) The Lukmanier Pass.

The upper part of this pass, north of the mass of rauchwacké
already mentioned and east of the highroad, is bounded by a
mountain-mass of which the southern peak bears the name of Scopi
and rises to an elevation of 10,500 feet. On the opposite side of
the road is a lower mass called the Alp Vitgira, which, however, is a
kind of spur from a group of peaks but little inferior to Scopi in

* We know that large and well-formed chiastolites are produced by contact-
metamorphism in a rock (of somewhat similar mineral character) of which the
matrix is but little affected. In the Bastogne also garnets of fair size and
singularly regular crystalline form have been formed in a matrix but slightly
changed. As reference is often made to the latter, I may say that though I
have not visited the district, I am familiar (thanks to Messrs. Renard, Rudler,
and Topley) with specimens of the rocks, and am convinced that they do net
give us much help towards a theory of the formation of crystalline schists, as the
garnets are of a very exceptional character. The metamorphism, such as it is,
appears to me due to some unusual agency (certainly not pressure). Can it be
the passage of hot water?

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS.

altitude. These, together with
the peaks north of Scopi, are
gneiss ; it, with the Alp Vit-
gira, mainly consists of the
“spotted rock,” with slates
and impure quartzites, in
which occasionally Belem-
nites and other Jurassic fos-
sils occur.

We began our examination
of Scopi at the northern part
of the steep slopes overlooking
the Lukmanier road *, and
worked southward over the
area on Which the map indi-
cated the occurrence of fossils.
The annexed section (fig. 7)
represents diagrammatically
the structure of the moun-
taint. At its northern end
is gneiss of normal aspect.
This, in the first little ravine,
is followed by a rather fissile
schist, which appeared to us
to be probably only the gneiss
in a very crushed condition.
Be this as it may, there can
be no doubt that this rock is
a member of the crystalline
series, greatly crushed. Ap-
parently below it, a short
distance up the northern
bank of the ravine, is the
first outcrop of a rock ob-
viously of sedimentary origin,

* The upper part of the pass is
comparatively level, rising from
about 6000 to 6243 feet, the highest
point.

+ We can guarantee its general
correctness; but to arrive at
minute accuracy and give detailed
measurements would be a long
and, in my opinion, needless
labour. We were moving along a
curved line from the western to
the south-western slopes of the
mountain, and were constantly
scrambling up and down over a
band perhaps a hundred yards in
vertical height, and from 500 to
800 feet above the grassy plain
which forms the upper part of the
pass, according as promising out-
crops of rock were exposed on the
steep turf slopes.

Q.J.G. 8. No. 182.

‘syne “WA
‘yood OIssvAnp *f

‘sopUTO Pg x

‘yoor ,, peyjodg ,, “¢

‘SoPIULLOVIUIT |.

‘spuvq OTOJSpURS YIM ‘ours oT, °F

"SSIOUK) “VW

‘oreys “'f

"MOLRITOJ-OSVAVITO YIM ssteus A}quqoad Ysiypog “'¢

‘peysnao Yonut ‘sstous 40 4styog “EF

‘souojspues pavyyT *''P

2
weer ‘~o

. r . < be |
ere a

mn :

iit

Ret ‘a

ou

=

. 2 v2)

Q

215

(‘poajteivns jou s}sodep jo ssouyoryy oAayeyoyy)

216 PROF, T. G BONNEY ON CRYSTALLINE SCHISIS AND THEIR

It is a dark-coloured, somewhat schistose rock, having a rude

cleavage variably developed, and occasionally is quite an ordinary

‘“‘ bastard slate.” The ground-mass has commonly a non-crystalline
aspect, though the rock contains much mica, which appears on a
weathered surface like tiny spangles, and frequently the minerals
already mentioned are abundant. These at first occur rather
sparsely, but soon become more numerous. After crossing a second
ravine, at a height of some 800 feet above the pass, fossils are found
in the “spotted rock.” sBelemnites, though not in very good condi-
tion, are readily recognized, and a little further on the joints of
Pentacrinites can be identified. With both are found the round
minerals—about as big as hemp-seeds—and the prisms up to full
one third of an inch long. Fossils then for a time become rare or
are absent, but the ‘‘ spotted rock” continues, occasionally inter-
banded with a hard sandstone or impure quartzite. Sometimes,
however, the “spots” disappear, and the rock becomes quite an
ordinary black “satiny” slate. We next cross a rather flaggy,
fine-grained sandstone, which forms a crag more than 20 feet high ;
then comes another mass of ‘“‘ spotted rock ” followed by sandstone
banded with slate (‘‘spots” rare); then a dark, rough, slaty
‘spotted rock” followed by sandstone; to this succeeds a great
mass of an extremely fissile rock of variable mineral character.
Evidently it has been intensely crushed, and is thus in a very
unfavourable condition for examination ; but this may be affirmed
with confidence, that it is a member of the crystalline series. The
upper part exhibits roundish spots like fragments of decomposing
felspars, so that it may once have been a gneiss, or even a fine-
erained rather micaceous granite. Parts, however, of the mass
have possessed a stratification-foliation ; for this occasionally can be
seen to “wriggle” across the newer structural planes of the
“cleavage foliation,” which cut the former like a “ strain-slip”
cleavage.

To this mass, which I have no doubt is an upthrust portion of the
old crystalline floor, succeeds another mass of ‘“‘ spotted rock” (the
“spots” perhaps attaining a rather larger size than before) with
sandstone bands, much twisted, crushed, and altogether in great
confusion. This is succeeded by another mass of shivered schists,
and that, again, by more “ spotted rock,” which appears to continue
along the southern face of the mountain*. We had thus examined
a large tract of the “‘ spotted rocks,” and to my eye, in the field, even
the specimens richest in minerals were readily distinguishable from
an average specimen of the Black-garnet schist of the Val Piora.

* Von Fritsch marks on his map a band of rauchwacké running up the flank
of Scopi, apparently about in the position of the line of sandstone crags
mentioned above. We, however, did not find any rock that we could identify
with the rauchwacké group, except that a small crag at the base of the slopes
overhanging the main stream consists of a pale fawn-coloured rock, which,
though rather harder than usual, may be one of the dolomitesin this group. If
so, it would be an outlier of the great mass of rauchwacké which, as already
mentioned, occurs near the top of the pass. We find that in this respect we are
in accord with the more recent map published by the Swiss Geological Survey.

a

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS, Pig

The Alp Vitgira affords the following evidence. Its southern
slopes overlook a glen called the Val Rondadura: the floor of this is
the gneiss of the district, over which, according to the map,
rauchwacké occurs some distance up the glen ; but there is no trace
of this rock at the south-eastern angle of the Alp Vitgira. Here,
at the base of the slope, we have Black-garnet or Dark-mica schist
interbanded with quartzose rock (fig. 8). Except that these dark

Fig. 8.—Diagranmmatic Section, Alp Vitgira.

A. Gneiss. A,. Gneiss with cleavage-foliation.
B. Black-garnet schist, banded with quartzite.
C. Jurassic rock. * Breccia. D. Covered ground.

schists are more squeezed and slaty in aspect than is usual near the
Lago di Ritom, this group is very like the banded Black-garnet schist
of the Val Piora; and microscopic examination fully confirms the
impression, gained in the field, as to the identity of the two groups
of rock. These banded schists form a craggy buttress, and the part
exposed may be some 200 feet in thickness. Crossing this in a
northerly direction, we find that everything for a short interval is
concealed by turf. Then come outcrops of interbanded calcareous
and slaty (rather fissile) rocks. These contain here and there (but,
so far as we saw, less abundantly than on Scopi) the usual mineral
spots and prisms. The more fissile layers exhibit sheen surfaces,
but the matrix in which these minerals are imbedded looks, even to
the unaided eye, very different from that of one of the true schists.
Here also we found ill-preserved Belemnites, with indications of
other organisms. One outcrop consisted of a dark grey sandy
mudstone interbanded with layers, which suggested the presence of
detritus from gneiss; below this was a phyllite, which might have
obtained its materials from the Dark-mica schist ; these contained
Belemnites, &c. Shortly beyond this the usual gneiss crops out and
continues away to the north.

(c) The Nufenen Pass.

The sections here are less accessible than those on the Lukmanier,
but accommodation—though very rough—forthe night can be found
at All’acqua (5266 feet), on the eastern side of the pass, about
23 hours below the summit (8006 feet). Between All’acqua and

Q2

218 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

4

Airolo the Val Bedretto follows very nearly the line of division

between the Calc-mica schist group and the Lepontine group
(including the Tremola schists), The path leading to the Nufenen
Pass for a considerable distance runs near the right bank of the
infant Ticino, over schists which belong to—and in many cases are
very typical examples of—the calc-mica group, now one, now the
other constituent dominating. They are particularly well developed
near the entrance of the little hamlet called Fontana. Just after
leaving Airolo the path crosses a considerable mass of rauchwacké.
It exhibits the usual character, being part of the bed which occurs
in the upper part of the Canaria ravine *. After an interval of
about 13 mile the rauchwacké again appears in force near Villa, on
the left bank of the stream, associated (unless our eyes deceived us)
with gypsum. Beyond All’acqua, at the Cantine de Cruina, is
another strip of rauchwacké t, and then blocks of the “ spotted rock ”
become common.

In the upper part of the pass the section from north to south,
according to Von Fritsch, is as follows :—(1) gneiss, (2) rauchwacké,
(3) granatiferous rock, (4) Jurassic rock with fossils, (5) granati-
ferous rock, (6) cale-mica schist ; the summit of the Nufenenstock
(9400 feet) occurring at the junction of (5) and (6): the crags
which fall steeply to the pass consisting of (4), while the actual
“col,” with the greater part of the final ascent on the eastern side, is
on(3). The track, from near the Cantine de Cruinato the summit,
winds among scattered blocks, chiefly of the “spotted rock.” These
commonly are of all sizes up to about 8000 cubic feet, but occa-
sionally are still larger. The map is coloured as if the rock were i
situ, but most of the blocks which we saw formed part of a sort of
“trail” or scattered moraine. Some might be in sztu, but it was
only in a ravine coming from a tributary glen—the Val Corno,—
and near the summit of the pass itself, that we were sure of the
occurrence of “live rock ;” the distinction, however, is immaterial :
I have no doubt that for all practical purposes the map is accurate
enough. But the great mass of the so-called granatiferous rock on
the north side of the pass (3), and at the entrance of the ValCorno,
the only place where we examined the other band (5), corresponds,
not with the Black-garnet schist of the Val Piora, but, in all its
essential characters, with the ‘‘ spotted rock” of Scopi. Perhaps it
is slightly more “crystalline” in aspect than the latter, but the
difference from the former is marked, as will presently be seen.
Fossils are by no means unfrequent, mainly Belemnites, even in
the most ecrystalline-looking matrix, but good specimens are hard to
obtain. The Belemnites are rather shattered ; the rock also is rather
harder and tougher than one would anticipate from its mode of

* Tt is continuous with that pierced by the St. Gothard tunnel.

+ Von Fritsch maps part of this as dolomite. Doubtless he is correct, but
we did not attempt to distinguish the dolomitic varieties (which are, I think,
usually harder and somewhat more crystalline in aspect) from the ordinary
rauchwacké, into which I believe they graduate, because for our purpose the
difference was not material.

———— — — eee

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 219

weathering : moreover the best specimens have a trick of occurring
towards the middle of the flattish surface of a block, which may be
about 16 square feet in area anda yard or so thick! These blocks
are frequently very distinctly banded, layers of a grey calcareous
mudstone alternating with dark layers full of rounded and prismatic
spots: these minerals are rare and small in the former, but fossils
occur in both. The“ spotted’ bands pass rapidly into the compact
rock, and are sometimes split up by it, as when a grit is associated
witha shale. The mineral “ spots” are rather indistinct on a fresh-
broken surface, but are very clearly displayed on a weathered one by
projecting from the matrix. One block exhibited an interbanding
of a fine-grained, hard mudstone and coarse micaceous layers,
commonly two or three inches thick, curiously twisted, evidently by
subsequent pressure. ‘he rock, as a whole, has been subjected to
considerable pressure and generally exhibits a rough imperfect
cleavage, which is usually parallel with the bedding, but can occa-
sionally be seen to cross the latter at a fairly high angle. Another
peculiarity should be noticed. This rock in weathering breaks up
—sometimes with considerable facility—into rude flakes—as it were
“scaling” off—as is common with rather coarse mudstones in
which a cleavage or bedding may be traced. ‘This characteristic is
very conspicuous just at the top of the pass * (where the rock is in
situ). Here it reminded me of certain hard, gritty, Carboniferous
shales, and it gives to the scenery a curiously dull, dirty, and
generally untidy aspect. In this respect it differs markedly from
the habit of the black-garnet schist. The unpropitious state of the
weather prevented us from ascending the Nufenenstock to examine
the section at its summit, or from devoting much time to a search
for any true Black-garnet schist, and an examination of the rauch-
wacké to the north of the pass. ‘There is not, however, space for
much of either, for the gneiss crops out abundantly at a very short
distance to the north. Rauchwacke, however, is there, but most of
it occurs as detached blocks. One of these contained pieces of a
satiny schist like the ‘‘ Disthene ” schist of the Val Canaria. There
must also be a remnant (as at the Alp Vitgira) of the Black-garnet
schist, for we found a few loose blocks, in one of which the garnets
were of a dark red colour.

lf the rock on the top of the Nufenenstock is identical with that
on the pass itself, as, from what I saw at the entrance of the Val
Corno, | presume it is, the Jurassic rock may form a true trough,
though it must rest upon rather than be intercalated in the Piora
series as a whole. For on the north side of the pass there is
certainly gneiss with at most a mere scrap of the Black-garnet

* A hard sandstone is interbanded in the series close to the top of the pass,
the bands dipping roughly south at an angle of at least 70°

t+ Perhaps I should state that this did not interfere with our examination of
the eastern side. We were able to satisfy ourselves thoroughly as to the great
mass of the fossiliferous and spotted rock, but just when we had completed the
examination of this, a dull morning changed to heavy rain, and obliged us to

hurry down into the Eginenthal without minutely examining the short space
between the “spotted rock” and the gneiss, or climbing the Nufenenstock,

220 PROF, T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

schists, and at some little distance to the south a great mass of the
Calc-mica schist. This accords with what I saw in crossing the
Gries Pass*. This differs from the Nufenen Pass in running
completely across the different rocks mentioned in the above
description ; for at the Tosa Falls we are again on gneiss. The
summit of the Gries Pass is about a mile and a half, as the crow
flies, from the “ col” of the Nufenen. On the last part of the ascent
to it, from the north side, we traverse “‘ spotted rock ”’ close to the
top, and at the commencement of the descent is Black-garnet schist,
followed by other schists of the Piora group 7.

From the description given above it is obvious that even in the
field the resemblance between the “spotted rock” and the Black-
garnet schist, as a rule, is rather superficial. But on a closer study
of the former the differences become yet more marked, as will be seen
by comparing the following description with that given above of the
schist. The description is chiefly founded on specimens from the
Nufenen, which, as it appeared to me, are better imitations of
erystalline schists than those from the Lukmanier, but mutatis
mutandis it will apply generally. The “spotted rock,” even in the
most crystalline specimens that I could find, presents marked
differences from the Black-garnet schist. For instance, on examin-
ing the fresh cross fracture of a slab we find it exhibits a much less
definite foliation ; sometimes, indeed, its structure hardly differs. from
that of an ordinary dark argillaceous limestone which has undergone
considerable pressure, showing a rude cleavage with a dull
glimmering surface. On these fresh fractures the eye less readily
detects the included minerals, and instead of the fairly well-defined
faces or the resinous lustre cf the black garnet, we only detect not
very clearly defined and but rarely lustrous spots. Instead of the
rather bright ‘‘sheen-surfaces” of the schist, we find a dull glim-
mering surface, like imperfectly polished ‘ black lead,” which, on
applying a lens, is seen to be a dead blackish mass powdered with
glittering specks. When we study the included minerals (for
which purpose we must select a well-weathered surface), we - find
that instead of garnets, presenting their usual crystalline form
(though it be occasionally somewhat distorted or flattened), we have
rounded bodies, seldom exceeding about a quarter of an inch in
diameter, which in form are commonly rather flat oblate spheroids,
and sometimes rudely ellipsoidal. The surface of a garnet projecting
from the schist, except where corroded by the weathering-out of the
included impurities, is fairly lustrous ; the spheroidal bodies are dull
and minutely granular in aspect. In the case of the associated
prisms the external angles are generally ill defined, and they too are

* J examined it in 1885.

+ My knowledgé of this pass was one of the chief grounds of my scepticism
as to the occurrence of ‘fossils in crystalline schists.’ Fortunately I had
written careful notes (though then much perplexed by this ‘‘ spotted” rock) and
had brought away specimens. I think it probable that the whole of the “ bulge”
to the north shown on the Swiss Survey Map is the outline of the Kalkhaltig
Glimmer-schiefer, roughly cut off by a line drawn from the Val Corno to the
Mittaghorn, and will be found to consist of Jurassic rock.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS, 221

oceasienally somewhat rounded, as if waterworn. ‘This, indeed, is
so marked in many cases that at the conclusion of my field-work I
was quite prepared to find that these minerals were derivative, and
represented the garnets and staurolites of the schist in a rolled
condition. But, as will be seen from the detailed account of the
microscopic structure in the Appendix, the spheroidal minerals are
totally different from the garnets, the prismatic minerals from the
staurolites or kyanites of the Piora schists, and all have been formed
in situ®™. It was, indeed, already evident from the analyses quoted
by Dr. yon Fritsch t, that the spheroidal mineral could not be a garnet
unless it included a large number of grains of quartz; for it contains
over 53 per cent. of SiO,, while the usual proportion for a garnet is
from 38 to 42 per cent.t ‘The mineral also contains 6°06 of water,
and there is more than 3 per cent. “loss.” Thus it is very different
in all respects from garnets in the Piora schists. Its analysis does
not correspond with that of any mineral known to me. ‘This is not
surprising, because evidently so much impurity is present. One
statement only may be confidently made, that whatever the
cementing material may be to which the form is due, it is not
gvarnet. The prisms, on microscopic examination, are seen to be less
crowded with the detrital material, and the analysis, as Dr. von
Fritsch points out, suggests that of couseranite §; and, as will be
seen from the description in the Appendix, its microscopic characters
fairly correspond with those of a mineral allied to dipyre. I have
examined the specimens of couseranite (all from either Poujac or
some other locality in the Department of the Ariége) in the British
Museum collection and at University College, and find that though
less perfect in external form and less pure, these Alpine specimens
present a general resemblance to them. I think it possible that in
the Lukmanier district a third hydrous silicate is also present.

Thus the resemblances of these fossiliferous ‘‘ spotted” rocks to
the Black-garnet schists are only superficial, while the differences
both of the larger included minerals and of the matrix, as will be
seen from the description in the Appendix, are marked and
essential,

* Tt may be instructive to record my exact impressions. ‘The evidence at the
Tukmanier seemed to me on the whole to suggest a formation of the minerals
in situ; that at the Nufenen seemed to accord better with a derivative origin.
But in regard to the latter I was from the first conscious of a grave difficulty.
If the minerals were detrital—rolled garnets and staurolites—if the bands in
which they occurred were a kind of grit, how was it that I failed to find any
other fragments, such as vein-quartz or the harder parts of some of the schists ?
As, however, one or two bands (without the minerals) do contain detritus of
some crystalline “rock,” I still thought it possible that something might be
revealed on microscopic examination. This, however, as may be seen, places it
beyond all doubt that the minerals have been formed i” situ.

| Loc. cit. p. 127. Ihave quoted these on p, 283.

+t Dana (Mineralogy, s.v. Garnet) quotes 84 analyses, in 82 of which the
SiO, is less than 48 per cent., and it is more often below than above 40. One
rises to 44, the other very exceptional analysis contains 52 per cent.

§ There is, however, too little both of silica and of alkalies.

222 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

5, ConcLustIons.

If, then, we accept the identification of the Andermatt marble
with the Jurassic rock of the Urserenthal and of the Black- garnet
schists with the Jurassic ‘‘ spotted rock” of the Lukmanier and
Nufenen Pass, and (as a necessary consequence of these admissions)
of the upper group of schists with the Mesozoic rocks of other parts
of the Alps, we find ourselves inextricably involved in the following
dilemmas :—

(1) That this upper group of schists, which, in all sections free
from suspicion, consists of highly crystalline rocks, overlies the
rauchwacké, which, in the same region, is quite an ordinary lme-
stone,

(2) That the rauchwacké, though underlying this group of schists,
coutains fragments of more than one characteristic member of it,
identical in all essential respects.

(5) That, if the admissions be correct, metamorphism takes place
in accordance with no principle and in obedience to no law. Rocks,
in regions of intense pressure, are sometimes highly metamorphosed,
sometimes, though with no appreciable mineral differences, are
practically unaltered.

From these dilemmas I can see no way = escape, except by
denying the facts stated in this paper. On their substantial
accuracy I will stake my credit as a worker in science. Moreover
I must confess myself at a loss to understand how some of them
have been overlooked or ignored by previous observers, and feel
justified in expressing my surprise that such slight and superficial
evidence has been held sufficient to warrant the adoption and publi-
cation of hypotheses which, as a little reflection and some general
knowledge of the geology of the Alps would have quickly shown,
could not fail to land us in the gravest difficulties. It would be
imprudent, in the present state of our knowledge, to prescribe
arbitrarily limits to the powers of Nature; but it is justifiable to
generalize from one’s own observations, when these not only have
been made with all possible care, but also are very considerable in
number. So I will venture to end this communication, already
perhaps too long, by stating that though I have been for years
familiar with Paleozoic and still more with Mesozoic rocks of
diverse mineral characters in many parts of the Alps, including
districts where there have been great foldings, strange contortions,
and severe crushings, I have never seen a limestone which presented
any real resemblance to the marbles which are usually associated
with schists and gneisses, or a slate which was much more than a
phyllite, or which, if studied carefully, could not be distinguished
from an ordinary mica-schist*. But I have always found that
limestones, schists, &c., in the crystalline districts possessed cha-
racters, macroscopic and microscopic, in common, by which they
could be distinguished from members of the Palaeozoic and Mesozoic
series. Cases of difficulty do, no doubt, occasionally occur, but, so

* T have seen numerous instances similar to those so well figured in Prof.

Heim’s classic work ‘ Mechanismus der Gebirgsbildung, and have examined the
specimens exhibited in the Berne Museum and elsewhere.

ites. ,

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS, 223
far as my experience goes, they are rare and very local; and these
arise from one of two causes, viz.: sometimes the base of a sedi-
mentary group is a kind of “ arkose”—7. ¢., is composed of frag-
ments, rather uniform in size, of the underlying crystalline rocks.
‘Such material, after pressure and the consequent development of
minute filmy mica, is difficult to distinguish, especially when im-
perfectly exposed, from certain members of the crystalline series
‘when they have been much crushed. Sometimes also a dark
micaceous schist, when crushed, is locally difficult to distinguish
from a dark argillaceous sediment in which severe pressure has
developed a secondary mica. In short, so far as my observations
go, the direct effect of pressure in promoting crystallization is not
very great *, and the minerals which may be connected with it are
usually minute. It appears to be most efficacious when acting
upon a rock already crystalline, and especially in producing changes
more or less of a paramorphic nature. But its result, even in the
case of such a rock, is usually to diminish the size of the crystalline
constituents, to convert coarse- into fine-grained rocks, and thus it
causes a rock to recede from rather than advance towards what may
be called a maximum stage of alteration.

In short, the result of my investigations differs widely from the
conclusions announced to the Geological Congress and embodied in
the following quotation + :—‘“ That by the plication of the Alps the
constitution ot the rocks has been completely changed is most dis-
tinctly proved by an examination of the sedimentary rocks ; because
the latter can be studied in an unaltered condition in adjacent
localities. ‘The commonest changes met with in connection with
folding are .... marmarosis of the limestones . . . . Develop-
ment of new minerals (garnet, staurolite, mica) in places that have
undergone crushing .... Even Liassic slates with fossils have
been converted into garnetiferous mica-schists, &c. The boundary
between the old crystalline schists and real sediments in the Alps
has by such processes of dynamic metamorphism been obliterated,
and the proper character of the rock is altered so as to render
recognition impossible. When we see in true sediments new
minerals developed by the progress of the mechanical metamorphism
(magnetite in the crushed oolitic ironstone of the Windgiille, garnet
in the Belemnite-slates of Scopi), the question arises for the crys-
talline schists of this and the neighbouring regions: Which
minerals are original, and which have been produced subsequently
by orogenetic processes?” It is, then, obvious that I dispute the
accuracy of most of the statements on which this question is
founded, and in so doing have endeavoured to show that it can be
answered without the aid of a geological (idipus.

* See, for a fuller discussion on this point, my note in the Geol. Mag. 1889,
dec. iii. vol. vi. p. 483. It must be remembered also (a point which seems to be
often overlooked) that the formation of new minerals takes place during the
diminution, not during the increase of pressure. This matter cannot be
discussed here, but I am preparing some notes on it for publication.

+ ‘Nature,’ Sept. 27, 1888, p. 524. Passages are omitted to which I take
no exception.

224 PROF. T. G@. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

6. APPENDIX.

(a) Microscopic Structure of the “ Val Piora” Schists.

The macroscopic aspect of this group has been described above ;
the microscopic structure of such members of it as appear in the
Val Canaria Section (where most of the characteristic varieties can
be recognized) has been studied by Dr. Grubenmann. As I have
nothing important to add to his excellent descriptions of the mineral
constituents, I shall content myself with quoting his results, in-
corporating with them some of my notes on specimens from the
Val Piora and on the significance of the rock structures, a point to
which Dr. Grubenmann appears to have devoted less attention than
to their mineral composition *.

The Dark-mica schists, including those containing blackish garnets,
are associated, as has been said, with bands of brownish quartzite of
variable thickness and persistency. The dark schists consist of
quartz, calcite, and two micas, with various other minerals, of which,
in certain cases, garnet is the most conspicuous. Regarding those
first named as the more essential components of the rock, we find
that the ratio of the first two varies much, the calcite sometimes
predominating over the quartz, wbile sometimes it 1s almost absent ;
dolomite also is probably present in some cases. The quartz is
clear, occurring in subpolygonal or rounded grains, and does not
retain any record of clastic origin. These grains, to some extent,
and still more those of calcite, are interspersed, and sometimes even .
crowded, with a minutely granular blackish to greyish mineral
(probably in part graphite). Of the two micas, which occur in
flakes usually -01 to -02 inch long, one is colourless. This is identified
by Dr. Grubenmann with margarite. The other is brown, dichroic,
giving a rich brown for vibrations parallel with the basal cleavage,
and a pale straw- or greyish green for those perpendicular, and is
considered to be probably biotite. The garnets in thin slices
appear of a very faint reddish colour, but the included “ opacite ”
often renders them almost opaque. Pressure, subsequent to crys-
tallization, has set its mark upon them. They are cracked or
rudely cleaved; they are slightly distorted in form, or even some-
what irregular in outline; occasionally their edges are quite
irregular, and the mineral passes into a fine-grained granular
mixture of quartz and garnet t. The adjacent matrix is bent and
disturbed by the resistance which they have offered; frequently it
has gaped open a little “ under the lee” of the garnet as the pres-
sure again diminished, and the space has been filled up subsequently
by secondary quartz, with perhaps some calcite or a flake or two of

* We have, in fact, approached the subject by different paths. I do not
pretend to have investigated the mineral composition of these rocks so elaborately
as he has done; for the history of a rock is to me of more interest than the
exhaustive study of its mineral details; so that I am often content to leave
questions relating to these unsettled. I find also that the use of high-power
lenses and any delicate optical work proves very trying te my eyes, which
are far from strong.

+ See page 235.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 225

mica. We find also, in some cases rather abundantly, a colourless
mineral in moderately elongated prisms (ranging in length from
about :02 inch to :06 inch). These, with crossed nicols, give
apparently a straight extinction and low bluish tints in intermediate
positions. They occur both when garnet is present and when it is
absent. Dr. Grubenmann identifies this mineral with zoisite, and
suggests the possibility of its having replaced garnet; but, so far as
I have seen, it appears to me to have been formed independently, and
to belong to the same period in the history of the rock. In certain
cases, I note among these prisms a slight difference in aspect and
some obliquity in extinction, so that kyanite may also occur.
Tourmaline is present, being sometimes fairly abundant. Some of
it, however, is rather peculiar in aspect, for it occurs not only in
more or less definite prisms, but also in films. In the latter case it
may have replaced brown mica, as it often appears to do in granite.
The colour is a dull indigo or slightly greenish blue. Small prisms,
and occasionally geniculate twins, of a honey-brown mineral, are not
unfrequent ; these are probably rutile. Sometimes they are locally
very abundant. 1 have counted more than 30 in a field, measuring
‘O04 inch in diameter*, Granules of magnetite, haematite, and
pyrite are present. very slide that I have examined of this rock
indicates a crushing more or less severe, with probably a slight
shearing movement. To this also | am disposed to attribute the
brownish dust present in the slide, instead of regarding it as an
original constituent. No one, I think, accustomed to the study of
erystalline schists and of the effects of pressure can have the
slightest doubt that the rock was a crystalline schist, containing
sometimes good-sized garnets, anterior to its being exposed to the
only pressure of which it has retained a definite record 7.

* The following analysis of the Granatfiihrende Thonglimmer-Schiefer has
been made by Dr. Grubenmann. As rock analyses always have great value, and
his paper appears in a publication not very accessible to English readers, I
shall not hesitate to reprint them here. He states that the garnets were too
impure to give a satisfactory result, but that a partial] analysis showed them to
be an alumina-lime garnet (thus corresponding with those in the Tremola
schists). The large amount of TiO, shows that much rutile may be expected
in the rock -—

Re RT MERON Hy ehh foes Lt 72-24
em i RIE GS Aas a 3-01
BN 9. aA oui eN att Ae 11-79
ase. s iann av shinelemennstssinetaeyaseucbels 2:99
G20. £06 Sper =30667.
0 IRI RR Bn ee Ss rose St! 0°80
EE Cass i 00.3. dis eldaati be cbeaemaeteny moet 0°85
DREN gus nso: « ok: sinsmidn ph ahiekrnh coy upweuld asp tp 0:97
Combustion-loss (H,O, CO,) ............ 2°30

100°75

+ See also President’s Address, 1885, Quart. Journ. Geol. Soe, vol. xli., Proce.
pp. 46, 47. No specimen in my collection gives clearer evidence in proof of the
above statement than that which I obtained from the ravine (Val Canaria)
which was examined by Dr. Grubenmann.

226 PROF, T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

The “ quartzite ” interbanded with the dark schist consists, in the
specimen which I have examined *, chiefly of two minerals in
variable proportions. The one is quartz, in grains (often about ‘01
inch in diameter) of roundish but slightly irregular outline, like
those common in many quartzose schists, except that they are rather
full of microlithic enclosures and fluid-cavities. The other is a
mineral, which at times is rather earthy-looking, like a decomposed
felspar, at times is clear with a rather strong double refraction.
The former seems to pass into, as if replaced by, the latter. This
occasionally occurs in rude prisms, and presents some resemblance
to an impure andalusite, having in one or two instances the brownish
tint of staurolite. Their form is hardly regular enough to determine
satisfactorily the extinction-angle, but ii venture to suggest that
they are a mineral allied to andalusite, and have been produced
from a decomposed felspar. Zircon (?) and rutile occur occasionally.
One of my slides exhibits a close interlamination of this rock and of
the dark schists. Here the former contains a few grains which
may be small reddish garnets, and the latter exhibits the tourma-
line-like mineral in a form that suggests a replacement of the
brown mica.

The Staurolite-schist from near the N.E. end of Lake Ritom has
as its matrix a closely felted mass of white mica and quartz (both
minerals being rather minute) i in which are scattered grains of iron-

oxide, flakes af brown mica, reddish garnets of fame size, and the ,

large staurolites. The last mineral is a honey-brown colour in
thin slices. It contains numerous microliths which I will not
venture to identify, but flakes of an iron-oxide (? hematite) are not
rare, and prisms of rutile are fairly abundant. The garnet here is
“cleaner” than in the black schist, still enclosures are plentiful.
The outline of the staurolites is sometimes fairly rectilinear, but
sometimes rather irregular and broken-looking. On the whole the
evidence seems favourable to the existence of this mineral anterior
to the date of the mechanical disturbance which has affected the
group.

A schist, with staurolites of smaller size, in a rather more
micaceous matrix, occurs on the south side of the Lukmanier Pass,
above Somascona. It appears to have been subjected to presaaee
after it had attained to its present mineral conditions T.

To the S.E. of the Lago de Ritom, apparently on nearly the
same horizon as the Staurolite-schist described above, are outcrops
of rock containing kyanites, which sometimes are full 3 inches in
length, in a rather gneissose ground-mass. ‘This, however, does
not call for any special notice, because smaller kyanites are far from
rare in the more micaceous bands of the Calc-mica-schist group.
Kyanite oceurs also plentifully on the south side of the Lukmanier

* From the ravine at the east end of the Ritom Boden. It seemed needless

to have other specimens sliced.
+ For a brief description of the group of rocks with which this schist is
connected, and which evidently is a prolongation eastward of the Piora group,
see ny President's Address, 1886, Quart. Tourn. Geol. Soe. vol. xlii. Proc. p. 47.

—

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 227
Pass, but here of only about ‘02 inch or -03 inch in length, together
with a pale green hornblende, brown mica, and some quartz. This
schist is much crumpled, evidently by the action of pressure
subsequent to mineralization.

In this connexion it may be well to notice the rock in the Val
Canaria mapped by Von Fritsch as “ Disthen-schiefer,’ and fully
described by Grubenmann, although the distinctive mineral is far
less conspicuous than in the cases already mentioned, and in one
instance he failed to find it. He describes this schist as “‘ zwesglim-
merigen (sog. Disthen fiihrenden) Schicfer ;” and undoubtedly micas
are the more conspicuous minerals, Its position in the supposed
fold of the Val Canaria has already been described, and just above
the upper mass of rauchwacké is a schist which, macroscopically, is
identical, and only differs under the microscope by the absence of
the disthene*. Dr. Grubenmann states that the rock also occurs
in the ravine leading up from the Lake Ritom to the pass between
_ Pian Alto and Fongio, and in this view I entirely concur. For a
full description of the microscopic structure, I must refer to his
paper; but it will suffice to say that the rock in the lower zone
(where it is altogether about 6 feet thick) is of a grey-green to dark —
green colour, with a pearly lustre on the cleavage-surfaces, and
occasional marked folia of a dark mica. Among these occur in-
folding layers of mica with a wavy cleavage, and with these are asso-
ciated small blades of disthene, with quartz and calcite. Two micas
are present, one colourless the other dichroic; they are associated
with needles of rutile. ‘Tourmaline occurs pretty frequently, with
some zoisite, black grains of iron-oxide (doubtless magnetite),
pyrite, and zircon. From a discussion of the optical properties of
the micas, and their analyses (given below ft), Dr. Grubenmann
considers the colourless ene to be a kind of margarite, and the
dark one a meroxene. ‘They occur roughly in the proportion of
Us

* AsI follow Dr. Grubenmann in the description of the rock, I will retain
in this-part of my paper the name disthene instead of kyanite, which I am in
the habit of using for this mineral. In my specimen, however, there are some
small-bladed lamellze which, I think, may be identified with disthene, and
several rather irregularly formed granules of a honey-yellow mineral, which
much resembles staurolite. These are about ‘01 inch long.

The Dark Mica.

t The White Mica.
if; ta £ iT.

SOR Racica. sons un ees 3490 34°82 oO ENR a af. Rees. 40°56 40°96
1 a 48°92 48°85 TTR cuttin wsitacaeay 0°38 0°43
TEI iaaaiiesencceeses trace trace De seaenskncss 21°84 22:10
5000, 10°88 10°83 OM ai ents nic a 6°02 7°25
NO Nai dns «vou caa. 2°33 2°69 HN stestin nena 591 5°27
PREM e rie ies sens on 0°49 0-59 AEE TS west amnveden 14:08 14:13
sae 3°05 3°30 1 RO ee 6-41 5:87
—_——- 1 —— INGHO) eusLcntrues 3:07 319
* 10057 101-08 PRUE AA shen 2°31 2°25
Sp. gr. =3'1095. oS) See
10058 = 101-45

Sp. gr. 2°9001.

228 PROF. T. G. BONNEY ON CRYSTALLINE SCHISIS AND THEIR

Associated with the above rock, at its lower occurrence, is a
quartzose cale-schist, of which Dr. Grubenmann gives a description
and analysis *; these show, as will presently be seen, that in
reality it differs little from some members of the Calc-mica schist
division. Indeed, I feel some doubt whether this “ Disthen fuh-
vender Schiefer ought not to be regarded rather as a member of
that division than as an equivalent of the staurolite and kyanite
rock near the eastern end of Lake Ritom.

The second zone of this Disthen fiithrender Schiefer (about 5 feet
thick) does not seem to differ materially in microscopic structure
from the first one; and, like this, it is associated with quartzose and
calcareous schists. The third zone (above the upper mass of the
rauchwacké), according to Dr. Grubenmann, very closely agrees (sehr
weitgehend ibereinstimmen) with the last named, although he has
not detected any disthene. For myself, I may say that the rocks
appear macroscopically identical. I could only distinguish speci-
mens by their labels, and agree with Dr. Grubenmann in not
attaching much weight to the absence of the disthene, a mineral
generally rather uncertain in its mode of occurrence. But, if iden-
‘ tical, how is its presence owtside the fold to be reconciled with his
theories ?

Cale-nuca Schist Division.

The rocks included here vary from a fairly pure white or grey
marble to quartzose or micaceous cale-schists. If attention be paid

Bulk analysis of the Schist containing two Micas, Disthene, &e.

lie II.
SHO Mere stcae seen acee 40-20 39-98
MO Paes. SIeo asec 2:00 2°30
NN Deeg, sete os hnsh ote 26°72 26°20
OO) cece jecnphetceaitoe = 312 oot The ‘‘ Disthene.”
1 SY 2 PES eae eae aa 4:08 3°80 . aie
Gig nobene sik 412 4-01 pss ignated: Pe
NEON) et ens secon epee: 11:39 11°68 SAM a
Eerie ures 6°12 6°02 a
ye Mes LN OD), /0r eee Nal as ti
Combustion-loss ... 2°22 2°18 ate a :
100°54 = 100°18
Sp. gr. =3°0092.
* “ White aluminous Quartz-schist.”
SO 547 sb awalelageGhetrctieeia nae aisemeteae 2.09
ANOS asc odes cu-dtese Sazetenanmee snare 8°95
BesO8 Aye. cscdscascsopd Seda eaesteeet 3°89
SAO Rionnes ees ov ee 29°70
MgO s .. Svacies soe eeeenerer meee te 3°59 Sp. gr. =2°5792:
KO) cei igs conte Ree herrea estes 2°84.
Na gO orn bap en oie «eee 0°84
0] O PRG MAGN MR Sra ney Sh Veiga eyesoaleld)
99°66

This schist must accordingly contain about 57 per cent. (or, at any rate, more
than half) of carbonates (7. G. B.).

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 229

to minute details, it would be possible to indicate many varieties
both in the Val Canaria and in the Val Piora sections, but I agree
with Dr. Grubenmann in regarding these as comparatively unim-
portant, except so far as they indicate (as we both agree in holding)
that the rocks are of sedimentary origin. ‘The principal con-
stituents are calcite, quartz, mica, commonly white, but sometimes
brownish or greenish (from alteration) with black grains—iron-
oxides, and perhaps graphite—and more or less of dusty-looking
material, which Dr. Grubenmann considers to be of organic origin.
He also finds some zoisite, and rutile is occasionally present. The
quartz-grains, often about °012 inch to -025 inch in diameter, are
commonly very clear and give high polarization-tints. In no case
do they retain any trace of a clastic origin, though they often
appear to have been dislocated and again cemented. The mica
flakes are commonly about ‘03 inch long, and the calcite grains
about the same in diameter. Every specimen gives more or less an
indication of mechanical disturbance; sometimes the pressure
appears to have acted at right angles to the mineral layers, some-
times there is evident shearing, sometimes it has acted more nearly
parallel with the layers, producing various flexures and foldings as
I described on a former occasion. Dr. Grubenmann himself states
that the mica flakes are often thrown into strong undulations
(sind oft stark welliqg verbogen) and that the calcite shows con-
stantly twin structure parallel with —3R, and the twin lamelle
are frequently rather conspicuously bent. He remarks that this is
evidence of severe pressure, but does not seem to perceive the
necessary inference that the rock was already thoroughly crystal-
line when the pressure acted.

So far as microscopic evidence goes, these rocks of the Val Piora
group present in many cases close resemblances to members of the
“Upper schist group” (as defined by me) from other parts of the
Western, Central, and Hastern Alps, though, of course, varietal
differences are almost endless. Here dolomite may predominate
over calcite, here mica may be much more abundant, here there
may be a greater amount of this or that accidental constituent, but,
as it seems to me, “a family likeness,” both macroscopical and
microscopical, is strongly marked, and the latter method of study
does but accentuate the difference between these and the so-called
“‘ fossiliferous schists ” of the Lukmanier and Nufenen Passes *.

* Dr, Grubenmann gives the following as a bulk-analysis of atypical example
of the Cale-mica schist series of the Val Canaria, remarking that the rock must
consist of about three fourths of calcite, and the remainder quartz, clay, and
some mica :-—

Je 21-96
AL Oh. - xt RMI eaa may aias = 0x0 1-43
Be, ©, ANGER pat iaxsxcckvieds ss 0°78
GRO 5d TR ri Rxdcnuunccke 46°11 Sp. gr. =2°7674.
MpO<d, :ncvaemiaibetee dk adakesws ess O61
OO, casesmeseeeevensd dds csveseaerse 30°04

100-93

230 PROF. T. G. BONNEY ON CRYSLIALLINE SCHISTS AND THEIR

(b) The Rauchwacké.

So far as concerns the mineral constituents, | have nothing to
add to Dr. Grubenmann’s petrographical studies. Indeed, I have
had only a few slides prepared, because the question which I sought
to determine was petrological, viz. whether the composition and
structure of the rock permitted of its being placed at the base of a
certain group of crystalline schists, a question which, to my mind, was
decisively answered. Dr. Grubenmann describes the lower zone of
rauchwacké in the Val Canaria section more minutely than the
upper, but gives analyses of the latter*. I have only looked at
this through the microscope, and have thought it needless to examine
the anhydrite or gypsum, or one of the more dolomitic bands. But
that the two zones belong to the same mass of rock there can be
no doubt. Quartz, pyrite, mica, talc, tourmaline, disthene, rutile,
and zircon are the chief minerals enumerated’ by Dr. Grubenmann
aud by earlier observers as accidental constituents of this series. In
a specimen from the upper zone he obtained an insoluble residue of
about 2 per cent., consisting of colourless flakes of a biaxial mica,
with a small axial angle (margarite), and greenish flakes of a uni-
axial mica (biotite), quartz-grains, and little crystals of tourmaline,
rutile, and zircon. I selected.for examination two specimens: one,
a clear, fairly hard, cream-coloured rock, in which only a tew tiny
flakes of white mica and specks of some dark mineral could be seen

According to Dr. von Fritsch (/. c. p. 113), Escher von der Linth found in
the calc-mica schists of the Lepontine Alps ‘‘wnbestimmte aber unzweifelhaft
organische reste.’ Of these I have never seen the slightest indication, and
venture to think this evidence insufficient. Studer also states that he found
belemnites in the Knoren-schiefer, at Fontana, in the Val Bedretto. I did not
myself come across either this rock or the black-garnet schist at that locality,
but it is not mapped there by Von Fritsch, and so, being anxious to spend my
time on the important Nufenen mass, I made no search for it. Mr. W. Watts,
however, informs me that he failed to find it, though he spent some time
hunting about. I would venture to suggest that the mass examined by Studer
was not iz situ. The number of the erratics in the upper part of the Val
Bedretto is enormous.

* Analysis of a saccharoidal white dolomite, from a quarry north of Villa
’ (Val Bedretto):

bi IE.
COL Hee ms 46-01 45°97
CaOalhises uss f- we... 89°04 39:14 Sp. gr. =2:8469,
MoO ta. 15-04 15°16
100-09 100-27

Also of a fine-grained, rather yellow-coloured dolomite from the ravine (Val
Canaria) :

O67 2. Be eee 44°96 45°15
Cho ele eee 40°12 40-16
MeO iis exsisvencetecoiad 11°96 11°98 Sp. gr. =2°8303.
1 2) = OR aR 0:42 0°36
Insoluble residue ...... 1:96 2-05

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 231

with the unaided eye—a sample of the purest and most crystalline
condition of the rauchwacké; the other from the matrix of the
basal breccia.

I recognize the above-named minerals, for a careful description of
which I refer to Dr. Grubenmann’s memoir. The structure,
however, of the rock, which does not appear to have impressed him,
appears to me of great importance. -Taking first the specimen
which is more crystalline in aspect, we find a minutely granular
matrix *, which, owing to the interstitial presence of a greyish dust,
is less clear and transparent than one would anticipate from the
macroscopic appearance of the rock. In this matrix are scattered
flakes of mica, mostly white, grains of calcite, of a colourless
mineral, often stained earthy brown, of quartz (here not common),
and of brownish or blackish iron-oxide. There is’also one tiny flake
of a quartz-mica schist. But without the evidence of this last, which
is so small a fragment that I would not wish to rely upon its
testimony, no one, I think, accustomed to the study of clastic and
metamorphic rocks could have any doubt that this rock cannot be
ranked with the latter group, that its matrix is not that of a true
marble, that the above-named minerals have been derived from older
rocks, and that these very probably were crystalline schists such as
have been described above.

In the specimen taken from the breccia-bed (p. 209), the matrix
resembles that of the last one, but is slightly coarser and dirtier. It
is fuller of fragmental minerals; both micas abound; quartz is
common, indubitably in fragments, which are clear and give bright
polarization-colours like the grains in the schists; calcite, iron-oxides,
&e. are present, with a few flakelets of mica-schist. These all are
beyond doubt derived from an older series, as in the other case.

A specimen of the rauchwacké, containing fragments, from the
ravine at the north-west end of Lake Ritom affords a matrix
generally similar to the above, with like mineral fragments. Rutile
is rather abundant in parts of the slide, and frequently occurs in
* nests,” which, with the associated material, suggest the presence
of fragments. Be this as it may, chips of schist are undoubtedly
present, and I can hardly doubt that some represent the adjacent
Cale-mica series.

A specimen also has been examined from the base of the rauch-
wacké in the second ravine, south-east of Lake Ritom (p. 206). It
was selected because it illustrated the rock in a crushed condition.
Even here, though the effects of pressure are very marked and the
rolling and crushing together of the matrix and included fragments,
sometimes of not very different mineral composition, makes it more
difficult to follow the precise outline of the latter, still the calcite of
the matrix is but slightly more coarsely crystalline than in the
cases described above, the clastic character of the rock is not.
destroyed, and it is very different from any specimen which I pos-
sess of the crystalline schists. Among the fragments, cale-mica schists,

* The granules rarely exceed ‘001 inch, and are often less.

Q.J.G.8. No. 182. R

232 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

including a quartzose variety, can be recognized; brown mica is
abundant. Crystallites of rutile (maximum length about -01 inch).
are numerous, often occurring in elongated nests in the flaky
masses of brown mica or in a finely granular, rather dusty-looking
mineral (? crushed calcite) and sometimes also with granular quartz.
With these are a few grains of tourmaline and not unfrequently
small blade-like prisms, about the same length as the rutile, which I
would suggest may be kyanite. These rock-fragments appear to be
exceptionally rich in microlithic constituents, just as I have noticed
is the case with parts of the slides cut from the Piora schists.

(c) Lhe Jurassic Rocks.

Under the microscope the specimens from both the Lukmanier
and the Nufenen Passes present a strong family likeness. The
matrix consists of calcite * in rather elongated and somewhat irregu-
larly outlined grains (generally less than -01 inch long, not uncom-
monly about -005 inch), with a variable quantity of a clear mineral,
part of which is quartz, but part is perhaps a silicate, with flakes of
a colourless mica, which gives rather brilliant polarization-tints,
and with granules, probably of the second mineral described below.
Scattered through the matrix is a minutely granular, greyish to
blackish, sometimes brownish, powder, the colouring-matter of the
rock. ‘There are also occasional grains of pyrite or an iron-oxide,
more or less perfect prisms of rutile t, and (rarely) of (?) tourmaline,
all of small size. It is very difficult to decide how far the con-
stituents are derivative. The calcite, in its present condition, is
probably authigenous, so also may be the quartz; but not seldom
the form of a grain suggests the presence of a fragment as nucleus,
which has only received a slight enlargement in situ. In the case
also of the mica the evidence is inconclusive. Here, again, it is

* Mr. J. Chorley, of University College, has kindly determined the amount
of CaCO, in a specimen in which the “knots” and “prisms” were not
abundant ; the first which I collected on the north side of Scopi. One
estimate gave 82°72, the other 83°53. | Of course, where the included minerals
are numerous, the percentage of carbonate in the whole rock would be lower;
but I should say that this was a fair sample of the matrix throughout, and
that every specimen which I have examined probably contains over 50 per
cent. of carbonate of lime. I have examined the residue of this rock under the
microscope ; it consists largely of generally minute granular graphitic matter,
with small flakes of a colourless mineral of no definite outline and weak
depolarizing power (? mica), sometimes ‘“‘ peppered” with the black dust, and
rather numerous acicular microliths, not generally exceeding ‘002 inch long. Of
these there appear to be two varieties—the stouter brownish yellow in colour,
probably rutile; the other lath-like, colourless, extinguishing either parallel
or at a very small angle with the sides (? kyanite). Also there are granules of
quartz, felspar (?), and possibly zircon. I have not been able, from this study
alone, to form any positive conclusion as to the history of the rock.

t The rutile-crystals occur sporadically, but two or three are in close
proximity. Once or twice I found a large number of rutiles in what appeared to
be a small fragment of another rock. This very closely resembles a portion of
one of the layers rich in rutile in the Dark-mica series. [ may add that one
or two bits in the matrix resemble garnet, but these are almost certainly of
fragmentai origin, not authigenous.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS, woe

possible that derivative flakes may subsequently have been slightly
enlarged. Now and then a slide contuins a little brownish mica
which certainly has a derivative aspect. The larger minerals,
present, as it were, porphyritically, and giving the spotted character to
the rock, are certainly authigenous, and appear to have been formed
after the rock had assumed a slightly schistose structure under pres-
sure. At least three types can be recognized :—(a) The rounded
grains (Knoten). These are found on microscopic examination to con-
sist of the darker granular matter of the matrix with some quartz-
or salcite-grains (smaller than in it) cemented together by a clear,
rather wax-like material, which has occasionally separated itself.
from the other constituents in thin streaks. It has weak double-
refraction, for with the two nicols its tints are low in the scale;
certainly, as the analysis leads us to expect *, it is not garnet; but
it is in a condition so unfavourable for examination that I will not
venture to suggest an identification. Probably it is a hydrous
silicate of alumina and lime, possibly orthorhombic, but it does not
remind me of any mineral with which I am familiar. (6) The
prism-shaped minerals (Prismen), of which there may possibly be
two forms. The commoner are subangular to almost rounded
prisms, with surfaces rarely lustrous, but often spangled with
minute mica-flakes. These, in thin slices, exhibit a faky-granular
mineral affording moderately bright polarization-tints, cementing
together a dusty-looking matrix (in this crystalline calcite cannot
be discerned). The outline of the prisms is rather irregular, but,
so far as one can judge, extinction takes place either parallel or at a
small angle with their sides. With this mineral I provisionally
include a somewhat shorter but decidedly more slender one (com-
moner, I think, on Seopi) which has a slightly fibrous aspect, with
indications of cleavages parallel with and oblique to the axis:

fractured surfaces having a rather resinous lustre. In thin slices,

though the outline is rather irregular, the crystals are more free
from foreign matter. The polarization-tints are rather low, whitish
or yellowish. Though extinction not seldom takes place parallel
with the sides (so far as they can be determined), it is, I think,
more often oblique than would occur with an orthorhombic mineral.
In thin sections some of the former prisms are very hard to dis-
tinguish from the first group, which seem sometimes to take an

* Analysis of the minerals in the ‘“‘Nufenen Schiefer” (Fritsch, Beitrige zur
Geol. Karte der Schweiz, xv. Lieferung, p. 127) :—

(I.) Inden (II.) In den

Knoten. Prismen,

RAL) to eee RRR EDL ork 2 cig wais« 53:09 40:07
PAR URS: eal Se veceess 19°45 22-05
BO, eMac Vchrcrd coms cates 5-93 5°66
aI) eaiabaaaibs tka ohteedan cd 10°95 22:29
GO! ihrer iss nivkvedpins wes ves 1:03 1-20
TARO ie eee Ae Beira Bis nh vine nd 6:06 8°89
TLOHD cn ipetee antes ocne sds be sodaene 3°49 —

100-00 100°16

R2

234 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

ellipsoidal form. I must leave these prisms also unnamed. The
mineral sometimes presents a slight resemblance to andalusite,
but the analysis seems to make this identification impossible,
Naumann * appears to have regarded it as couseranite, for he names
the Nufenen Pass as a locality for this mineral. But the iden-
tification appears to be doubted by Studer, who is quoted by
Dr. von Fritsch in the passage from which the preceding analysis
is taken. This, however, does not correspond well with those
given by Dana, but comes nearer to some of those quoted under
the head ‘“‘ Agalmatolite;” neither does the mineral exactly re-
‘semble any one known to me, though it is not very unlike cou-
seranite, and has a slight general resemblance to dipyre. I
suspect its relations are with this group of minerals. The analysis
corresponds more nearly with some forms of scapolite. (¢) A
mica-like mineral which occurs in rather tabular small masses,
usually not exceeding °05 inch in diameter, and perhaps *03 inch in
thickness, presenting more or less rounded outlines and a very
distinct basal cleavage, a silvery lustre and a slight tinge of green
in colour. Under the microscope it is evidently authigenous, having
developed after the formation of a schistose structure in the matrix,
which can be traced through the crystal. Sometimes, however, it
is fairly clean. It is colourless, very like a mica, but perhaps
slightly more ‘‘ waxy ” in aspect. The polarization-tints are rather
bright; it almost invariably exhibits polysynthethic twinning
parallel with the planes (basal) of cleavage, and extinction which,
if not simultaneous, is very nearly so (and parallel with the same).
Both macroscopically and microscopically it seems to differ slightly
from a mica. Mr. Teall, after looking at my specimens, suggested
that the mineral might belong to the chloritoid group, and the more
I examine them the more probable this suggestion appears to be.

Larger grains of pyrite are also common. ‘These evidently have
been crushed out, for they form rather elongated clusters or streaks,
At each end, ‘“‘ under their lee,” the quartz, calcite, and mica of the
matrix occur in slightly larger grains.

Specimens cut from the finer bands, intercalated, as already
described, with those of the ‘spotted” rock, consist of a matrix
generally resembling that of the latter rock; but the grains are
rather smaller, there is less quartz and mica, and the specimens
more nearly resemble those of an ordinary impure fine-grained
limestone. . The characteristic minerals of the coarse bands are
wanting, but there are grains of pyrite, and vein-like seams occupied
by calcite, with a very little quartz, (?) dolomite, white mica, and
perhaps a colourless silicate.

One of the specimens from Scopi contains numerous joints of a
Pentacrinite. The matrix of this differs slightly from that of the
other examples in being a little. more calcareous, decidedly more
carbonaceous and more irregular in its structure. Fragments of
organisms are frequent, such as I can identify as being Crinoidal.
In these the tubuli, infiltrated with carbonaceous matter, are often

* Hlemente der Mineralogie, s. v. Couseranite.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 235

preserved, but in proportion as the fine granular lool of the cal-
careous organism is lost and a regular mineral cleavage set up, these
structures tend markedly to disappear *. The slide contains one of
the rounded mineral spots, but these and the prisms are not
abundant in the hand-specimens.

Near the base (apparently) of the similar group of rocks on the
Alp Vitgira is a curious-looking nodular rock, which, in the field,
appeared to me as if it were mainly composed of fracments, were, 10
short, a conglomerate or breccia at the base of the Jurassic series,
much crushed. It exhibits, under the microscope, a very peculiar
structure. The chief constituents are calcite, quartz, white mica,
brown mica, sometimes altered into a greenish mineral, and garnet.
This is speckled with ‘“ opacite,” which also is variably dissemi-
nated in the slide. A bit of the slide here and there resembles the
ordinary matrix of these Jurassic rocks, and one small fragment
resembles an organism (Pentacrinites?). The structure of crushed
breccias in the Alpine Paleeozoic and Mesozoic rocks is often peculiar,
the ultimate result of the pressure being to render the fragmental
structure less definite, probably by the direct effects on the frag-
ments themselves and the ‘‘ mashing up” of chips from their
surfaces with the very variable constituents of the matrix. Thus
it becomes difficult to discern the precise boundaries of the fragments
and of the matrix, or to be sure in many cases whether we have
(more especially in the case of quartz and calcite) minerals of
primary or derivative origin. But in regard to this slide, | may
say that the garnet, at any rate, appears to be distinctly derivative.
It occurs in two ways. One piece resembles a garnet which has
been partly broken up and recrystallized. There is a piece, like the
remnant of a crystal, about ‘1 inch long and one third of this wide,
which passes on both sides into a granular mass of garnet, quartz,
and a little brown mica. The others exhibit a mass composed of
garnet, calcite, and quartz, with a very little brown mica, the first
mineral appearing to act as a kind of setting to the others, the
interspaces composed of it being elongated in one direction, so that
the garnet seems to form a kind of root- like growth among the
other minerals. ‘This structure I consider to be a record of pres-
sure; it is a species of foliation; but I observe that, while usually
it is parallel with the structure of the rock-mass which is due to the
Post-Jurassic movements, at least in two specimens, which have a
very fragmental aspect, it lies athwart thelatter. This “ foliation ”
accordingly appears to be of earlier date than the Jurassic epoch.

* T have observed the same thing in regard to the so-called canal-system in
the supposed organism Hozoon canadense. [In the discussion it was stated that
‘‘marmorosis” had taken place in the organisms in these Jurassic rocks. In
those described here there is just as much or just as little ‘‘marmorosis” as
may be seen in any later Palwozoie limestone in Great Britain. The Belem-
nites, being larger and rather brittle, are a little more changed in appearance,
but even these not seldom, on careful examination with a lens, are found to
retain their characteristic structure. If these slides exhibit ‘ marmorosis,’’ so
do hundreds of limestones to which no one would apply the term “ meta-
morphic,” using this in its ordinary sense. |

236 PROF. T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

I admit that the evidence of this specimen is not such as would
convince an ordinary observer, but after long familiarity with
schists and derivative rocks, I am unable to come to any other con-
clusion than that the garnet, to say nothing of other minerals, has
not been developed in situ, but occurs in derivative fragments *
If this be so, no stronger proof could be given of the independence
and antiquity of the Piora-schist group—and this, coupled with
that already obtained from the rauchwacké, if admitted, places the
matter beyond dispute. This instance is only one out of many
which indicate (as I have already more than once observed) that
there had been ‘‘ mountain-making ” in the region of the present
Alpine chain before any Mesozoic “rock was deposited, and even in
Pre-Carboniferous times.

Discussion.

Dr. Grrxie stated that he had sent an abstract of the paper by
Prof. Bonneyy, read to the British Association at Newcastle, to Prof.
Heim, and the latter had favoured him with a réswmé of his views
on the subject of the present discussion, of which the following is a
translation :—

“Tt appears to me that Professor Bonney starts from a misunderstanding. It
has often been maintained that Mesozoic rocks can become crystalline ; but xo
Swiss geologist has, so far as I know, ever asserted that the crystalline schists of
the Central massif of the Alps are metamorphic Mesozoic rocks. In the printed
abstract of his British-Association paper, however, which you have sent to me,
Professor Bonney attacks this supposed assertion—one that has never been
made.

“Tam in perfect accordance with those who know the Central massif best
(Baltzer, Fellenberg, &c.) in fixing the following points :—

‘1. Crystalline schistose rocks of Mesozoic age exist at Scopi, in the Valserthal
(Graubunden), in the Urserenthal, on Piora, at the Nufenen Pass, in the Val
Canaria, in the Ganterthal, and numerons other places. Such rocks are :—

‘“‘(a) Clay-slates, with mica, garnets, zoisite, staurolite, rutile, and Belemnites,

the latter being crystalline and granular,

“(b) Clay-slates, with mica, staurolite, &c., and garnet, alternating with the

Belemnite-schists.

“(¢c) Green plagioclase-amphibole schists, alternating with the Belemnite-

schists.

““(d) Micaceous phyllites and calcareous mica-schists.

“(e) Marble with mica, which has undergone linear stretching, going over

into ‘ Malm-kalk’ with crinoids.

2. We have never given the name ‘ crystalline-schists’ to these rocks, nor
have we ever regarded them as such, but always as sedimentary metamorphosed
zones (synclinal basins) between the central massifs, _ Professor Bonney is right
in saying that they have not the aspect of true crystalline schists. It is true
there are some varieties which it would be difficult to distinguish in the hand-
specimen, and without stratigraphical evidence, from true crystalline schists.
Stratigraphically, they always present themselves as ‘ Mulden-zones’ accom-
panied by other sedimentary rocks.

* My specimen of the Black-garnet schists collected between the top of the
Lukmanier Pass and Somascona (President’s Address, 1886, Q. J. G.S. vol. xlii.,
Proc. p. 47) in parts very closely resembles the fragment here described. The
rock has evidently been much affected by pressure.

+ Prof. Bonney states that the printed document sent to Prof. Heim con-
tained the whole of the note communicated by him to the British Association.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 237

“3. In the Central massifs occur rocks which exactly resemble true crystal-
line schists in mode of occurrence. Petrographically, they are related to them
by passage-rocks ; at least, the line of separation is not easily distinguished.
Such rocks are phyllites, chlorite-schists, felsite-schists, mica-schists, and espe-
cially sericite-qneisses, all of which we regard with certainty as paleozoic. ‘The
proofs are the following :—

(a) In some places in these zones are found intercalated beds of graphitic
and sometimes even anthracitic schists (Bristenstock, &c.).

‘(b) 'Traces of fossils have been often found (trunks of Calamites from Gut-
tannen in the Haslithal, Carboniferous plants in strips wedged in on
the Todi, &c.).

““(e) At the end of the Central-massif distinct zones of Carboniferous slates
are often developed out of the zones of these sericitic gneisses; and
the synclinal (‘ Mulden’) nature of these zones, in comparison with
the old granitic gneisses, is shown there by the wedging in of still
younger unaltered sedimentary rocks.

‘““(d) I have already shown in my Tédi-Windgillen group that even the
Verrocano (Permian), when nipped in between crystalline schists,
assumes a close resemblance to them, and appears as a part of the
erystalline Central-massif.

‘‘ Fragments of these rocks are found in the Triassic Rauchwacké, but this is
not the case with the garnetiferous schists of Scopi, which are younger than the
Rauchwacké, and belong to the true sedimentary synclinal zones (‘ Mulden’).

. “A great unconformity exists in the Central. Alps between Palseozoic and
Mesozoic formations, but not between Palaeozoic and Azoic.

“TY. The Paleozoic formations mostly show an intimate tectonic relation to
the crystalline schists, and have been converted petrographically into crystal-
line schists. The central-massifs consist, perhaps to the extent of two thirds,
of true old crystalline schists, older than the Cambrian, in part, perhaps, the
primitive crust (Hrstarrungskruste, granite-gneisses, protogine); and to the
extent of about one third of Paleozoic mica-schists, sericite-schists, amphibolites
and other similar rocks which have been derived by dynamic metamorphism
from Palzeozoic slates, sandstones, and conglomerates ; and Baltzer distinguishes
between the old nucleus and the younger shell (slates) of the Central-massif.
They are kneaded and pressed into one another.

“II. The genuine Mesozoic deposits follow, sometimes conformably, some-
times unconformably. In places they have become crystalline and schistose
(schiefrig-krystallinisch) ; but they never occur as a constituent of the Central-
massif, but always accompany the Mesozoic deposits, or are intercalated as
‘Mulden’ in, and especially between, the Central-massifs. They are never termed
‘ Orystalline-schists’ in the geological sense of the word—at the most, only in its
petrographical sense.

“The latest literature on these things is, above all :—

“ Baltzer, ‘The Aar-massif and a part of St. Gothard massif,’ ‘ Beitriage

zur geol. Karte der Schweiz, 24th Lieferung, 1888.

“ Grubenmann (Prof. Dr.), ‘The Sedimentary “ Mulde” of Piora.’

** Baltzer furnishes, in the volume above cited, some excellent work on the
rocks indicated under I., and gives a drawing of the Calamite-like trunk from
Guttanen. Grubenmann does the microscopic work in connexion with the
Mesozoic formations belonging to IT., which have never been referred, by us, to
the crystalline schists or to the Central massif.

“* RESULT,

‘‘Much of what have been regarded as genuine crystalline schists in the Alps
is Paleozoic.

“The crystalline metamorphosed Mesozoic rocks always occur as sedimentary
deposits, and have never been termed ‘ crystalline schists’ in the stratigraphical
sense” *, i

* After reading once more Dr. Heiin’s essay, communicated to the International
Geological Congress in 1888, I cannot hold myself to blame for misunder-
standing it, and must contend’that the sentences quoted above on page 223

238 PROF, T. G. BONNEY ON CRYSTALLINE SCHISTS AND THEIR

In continuation of his remarks Dr. Grrx1r complimented the
_ Author on his courage in returning to this difficult ground, but
notwithstanding the arguments so skilfully brought forward that
evening he was not convinced of an error on the part of the Swiss
geologists. Even the Author’s own sections gave some countenance
to their views, since the dark garnetiferous schists might quite well
be part of the same series as the Belemnite-schists. In metamorphic
regions there must be some line, on one side of which fossils are
recognizable, on the other not so. In the Alps, as Heim and
his associates contend, the Belemnite-schists, which have become
markedly crystalline, may be less altered portions of masses from
which all trace of fossils has been generally obliterated.

Mr. Eccrzs declined to say anything with respect to the Andermatt
section. As to the Val-Piora schists, and their relations to the
rauchwacké, he fully concurred with the Author’s views thereon, and
especially in respect of the frequently changing position of the
rauchwacké in relation to these schists. He criticized the sug-
gestions of Von Fritsch with reference to this series of beds, and
pointed out the curious position of the calc-mica schists on this

(and the translation appears to me to represent accurately the sense of the
original German) justify the position which I have taken up in this paper.
Indeed, I find it very difficult to reconcile perfectly the present letter with
that essvy or the published statements of Swiss geologists; and if I might
venture to put my view of the case rather bluntly, I should be obliged to say,
“Tt is not so much that I have misunderstood you as that you have mis-
understood Nature.” Hence, to contend further on the point, whether Dr. Heim
did or did not include rocks of Jurassic age among crystalline schists, is needless,
for if I am right as to the following matters, the dispute is one “‘de land
caprind.” I beg leave, then, to observe that :—

(1) Carboniferous rocks are only incidentally mentioned in my paper, so
that I fail to see the full force of Dr. Heim’s reference to such rocks in another
part of the Alps. Some of these, however, I have examined, and think I know
them well enough to demur to Dr. Heim’s statements concerning them. I have
seen, in the Berne Museum, the specimen with “the Calamite-like stem.’’
When this rock is proved to be a gneiss I shall be prepared to consider the
propriety of extending this name to the Grés Felspathique of Normandy, or
that of mica-schist to some rocks of Carboniferous age at Vernayaz, in Canton
Valais, or of calling the Torridon Sandstone of Scotland a granite.

(2) One of the main purposes of the present paper is to prove that a great
group of true crystalline schists (some of which contain garnets, staurolites,
&c.) does exist in the Lepontine Alps, and that in these Belemnites or other
fossils never occur.

(8) Also to prove that the supposed infra-position of the Rauchwacké
(Triassic) to this group is the result of misinterpretations of the stratigraphical
evidence, and that this Rauchwacké (a comparatively unaltered rock) contains
fragments of more than one member of the above-named group of schists.

(4) Also to prove that the schistose (Jurassic) rocks, in which Belemnites
and other fossils occur, only resemble superficially the above crystalline
schists, and do not contain (not to mention other minerals) authigenous
garnets or staurolites, the minerals which have been taken for these being
certain hydrous silicates, the presence of which does not indicate any extreme
metamorphism.

Hence, in my opinion, Dr. Heim in his letter does not adduce any fresh
evidence, but only reiterates the mistakes, as they appear to me, in correction
of which my paper was written.—T. G. Bonnny.

RELATION TO MESOZOIC ROCKS IN THE LEPONTINE ALPS. 239

supposition. If Jurassic here, they are also Jurassic in the Pennine
Alps, and would carry with them the “ griiner-schiefer” of Studer.
He commented on the brecciated character of the Rauchwacké. He
scarcely agreed with the Author as to the Jurassic schists resembling
poor forgeries of genuine garnet-schists, since it might be easy to
mistake some bands for parts of the calc-mica schists.

Mr, Tratt referred to remarks of his own on a previous occasion
as possibly having had something to do with the production of the
paper. We now had a further illustration that Prof. Bonney’s views
were at variance with those of the modern school of Swiss geologists.
He had dealt with the age of the Val-Piora schists on stratigraphical
evidence; but we must wait to hear what the Swiss geologists had
to say to the criticisms of the Author.

Speaking of the petrographical relations of the two rocks, he
agreed with Prof. Bonney that his specimens of the garnet-schists
were quite different from those of the Belemnite-rock. With refer-
ence to the character of the Belemnite-bearing rock, the Belemnites
themselves are marmorized; the rock itself is schistose, the planes
glistening with secondary (developed) mica; the knots represented
some silicate. The prisms gave distinct outlines. There had been
much molecular change. In fact, he would term the rock a crystal-
line schist.

Dr. Irvine, from personal experiences of traverses in the Eastern
Alps, could bear out the Author’s views as to the succession of the
calc-mica schists &c. in the Glockner region and the small degree of
alteration of the rauchwacké in comparison with some of the dolo-
mitic series of the Eastern Alps. He had studied Grubenmann’s
section of the Val Canaria, and criticized some of his deductions.
He regarded his assumptions as untenable—such as that the schists
are of Mesozoic age, chemically and morphologically altered by
pressure, or that the “‘ calc-glimmer-schiefer ” are altered limestones.
There was a third fallacy, viz. that of the two mica-schist series
recurring three times in the Val-Canaria section, yet only once in
such a position that their suggested origin would seem possible.
Lastly, Dr. Grubenmann had overlooked the important evidence of
the breccias in the dolomites.

Prof. Hugues had been over the ground where the fossil-bearing
altered rocks occur, in company with Prof. Heim. He thought the
case one of evolution as far as the rocks are concerned. There was
a tendency to approach extinction-point, and when at last the fossils
disappeared alteration had gone so far that something altogether
different was produced. But there were degrees of alteration, and
many changes of known series, before we got to the Archean.

Rev. E. Hitz referred to the unlikeness of the Rauchwacké to the
older schists.

The Avrnor said that many of the objections proceeded from mis-
understanding. Heim’s work dealt chiefly with the Central Alps,
of which he had not spoken, but he gave a complete contradiction to
any statements that these fossil-bearing rocks in the Lepontine Alps
are in any proper sense crystalline schists. ‘There are, however,

240 _ PROF, T. G. BONNEY ON CRYSTALLINE SCHISTS, ETC.

crystalline schists in this region; but to reply to the letter which
Dr. Geikie had read would be merely to give a repetition of his.
paper. Im this he had disproved (as he hoped, satisfactorily) the
statements repeated in that letter. He admitted the similarity spoken
of by Mr. Eccles, but it was only superficial ; under the microscope
the differences were at once visible. He complained that, in
Mr. Teall’s argument, words had been substituted for things. By
this process of reasoning the Devonian and Carboniferous Lime-
stones of Britain might be proved to be metamorphic, whereas truly
crystalline marbles are quite different. In the Belemnite-series the
minerals are not (where authigenous) garnets, staurolites, &c., but
dirty hydrous minerals; it is possible to conjecture what these
rocks were, and the organisms are scarcely altered. He could not
quite understand Prof. Hughes’s points ; but in answer to the notion
that we must have connecting-links, he asserted in the present case
the totally distinct facies of the two series of rocks.

Quar? Journ. Geo Soc.Vol. XLVI. PL.X.

$
4
wit Carn Howell
we Seal
, ke)
% 5 e SL &
mo ee

\
€
w -
>. Oo
$
4 (f
$ qv
oO,
ae
Oe

Dimetian. with
haste cykes.

Careg Fran

Fred" Dangerfield Lith. London (9575

mr,

fhe ‘dak

i

?

Quar* Journ. Geo! Soc.Vol. XLVI. PL.X

SKETCH MaP(N? I.)

OF 2
S? DAVIDS DISTRICT, N.W. SB
aE Carn Grwewdig

Scale 6 inches to] mile.

Intrusive ingeour “iil ill

}
2,

Point S¢ Johr:

N.boW.

Pen -carment

Carn Poeth
Diabase fall of Eyidote

Penrhyn Dalar' | ]

Diclstse

a
ef QO Carn Howell

ar

ny Y
puobas®
o& raft
SKETCH MAP (NE 2.) Ye piabore
OF a ) oO

S*Davips DisTRICT, S.W. Sees tn renters
/ in

CO Guel Gelé
ee 4 Zs

Scale G inches to] mile.

Oyofau

More baste Tif fs intern
weathering ritaty with

quarts-andastte inclusions

write gritty auf

Zi si

POE,

Yarialte
altered Ved

Can brian
sanity lols
Ogot’
Mesugn
Conglom &
Pebahorn 17
Dinetian with
haste dykes.

Careg Fran

Fred* Dangerfield Lith. London 19575

Ww. pe: rei octane
ch ee ' oe | nay bop
Caer be sank fu 7 hie

aw i ij a eee *

¥

THE PEBIDIAN VOLCANIC SERIES OF SY. DAVIDS. 941

14. The Pesrpran Votcanic Series of Sr. Davivs. By Prof.
C. Luoyp Morean, F.G.8., Assoc.R.S.M. (Read January 8,

1890.)
[Puate X.]

CoNTENTs.
1. Inrropuction,

2. Tur Revation or PesrpiIan TO CAMBRIAN,

a. General Considerations,

b. In Caerbwdy Valley.

ec. In St. Non’s Bay.

d. At Ogof Golchfa (Whitesand Bay).
e. In Ramsey Sound.

Jf. The Materials of the Conglomerate.
g- Summary of the Evidence.

3. THE PEpip1An SUCCESSION.

a. The Results of previous Investigations.
b. General Results of the Author’s Survey.
e. Further Details:

d, Faults and their Effects.

é. The Cambrian Overlap.

f. The “ Felsitic ’ Dykes.

g. The Porcellanites.

4. Tue RELATION or PEBIDIAN TO DIMETIAN.

a. Dr. Hicks’s Arvonian.
6. The Dimetian Question.
. In Porthlisky Bay.

¢
d
é. At Ogof Llesugn.

Ff. General Considerations.
g

5. ConcLusion.
1. IntrRopvucrion.

Two strongly contrasted interpretations of the structure and geolo-
gical genesis of the St. David’s promontory are before geologists.
The first of these is that advocated for many years by Dr. Hicks
and finally summed up by him in 1884 (Quart. Journ. Geol. Soc.
vol. xl. p. 507). On this view there are at St. Davids, besides the
strata of Cambrian age, three distinct Pre-Cambrian systems—the
Dimetian, Arvonian, and Pebidian. Each is unconformable to the
others. The Dimetian was very much in its present state before the
Arvonian was laid down. ‘The Arvonian hilleflintas, again, were
brought to their present mineral condition before the Pebidian series
was deposited. ‘The Pebidian volcanic beds, once more, were nearly
as highly metamorphosed as they are at present before the Cam-
brian Conglomerate was formed. ach is therefore separated from
the succeeding group by a systematic unconformity, and we have,
on this view, to quote the words of Mr. Tawney, ‘a vista opened

242 PROF. C. LLOYD MORGAN ON THE PEBIDIAN

up to us in the rocks of St. Davids of age behind age most pleasing
to the imagination of the geologist. "

The second interpretation is that advocated by Dr. A. Geikie
(Quart. Journ. Geol. Soc. vol. xxxix. p. 261). According to this
view the Pebidian constitutes a volcanic series at the base of and
forming an integral part of the Cambrian system; the Dimetian
consists of granite intrusive into the Cambrian and of much more
recent age; while the Arvonian group comprises portions of the
Pebidian volcanic breccias and tuffs, where these are invaded by
quartz-porphyries associated with the intrusive Dimetian granite.

To these two divergent interpretations Mr. J. F. Blake (Quart.
Journ. Geol. Soc. vol. xl. p. 294) has added a third, first suggested
by Mr. Hudleston. He contends that the Dimetian (granite),
Arvonian, and Pebidian belong to one volcanic series, the age of
which is anterior to and independent of the Cambrian epoch.

Not only is there this marked divergence of opinion as to the age
of the Pebidian volcanic series and its relations to the other rock-
masses of the district, but equally marked is the divergence of
opinion as to the succession of the Pebidian strata and the mode of
their stratigraphical arrangement. Dr. Hicks maps the Dimetian-
Arvonian ridge as the ancient land-axis against which the Pebidians
were unconformably deposited and from which they now dip away
to the north and to the south. ‘The series to the north of the axis
is thus a continuous ascending series, the older beds, except where
they are ‘‘ dropped” by faults, flanking the ridge, the newest being
those furthest from the axis found near Whitesand Bay to the north
of St. Davids. Dr. Geikie, on the other hand, denies that the series
to the north is a continuous series. He contends that they are
repeated by an isoclinal fold ‘‘ the axis of which must cut the coast-
line somewhere between Pen-maen-melyn and Pen-y-foel.” The
beds to the south of the axis of this isocline are thus, on his view,
repetitions of those to the north, and their northerly dips are
reversed dips. Mr. Blake, however, examined the coast between
Pen-maen-melyn and Pen-y-foei, and though he was ‘“ enchanted
with the glorious confusion of the volcanic masses there exhibited,”
could find no sign of a regular fold, ‘“‘ which,” he says, “‘ among such
rocks would be almost impossible to conceive.”

It can hardly be said that our knowledge of the Pebidian volcanic
series of St. Davids has yet reached a satisfactory position of stable
equilibrium.

I have recently spent some seven weeks in the St. David’s
district, nearly the whole of which time I devoted to field-work *.
J have examined every accessible portion of the cliffs and all the
inland exposures, having the advantage of the 6-inch Survey map
on which to record my observations. The discovery of some new
facts and the formation of an independent opinion on some of the
debated questions impels me, though not without diffidence, to enter
the field of the St. David’s controversy.

* During the greater part of the time I had the advantage of the assistance
and companionship of Mr. J. G. Grenfell, M.A., F.G.S.

VOLCANIC SERIES OF ST. DAVIDS. 943

2. Tus Revation oF PEBIDIAN TO CAMBRIAN.

a. General Considerations.—The Cambrian conglomerate is a
deposit of variable thickness, reaching in some places 100 feet. It
is composed of rolled fragments, consisting in‘the main of quartz and
quartzite. These are well rounded and sometimes of large size, as
big as a man’s head or larger.

The underlying beds, where direct contact is observable, belong
to the Pebidian series. According to Dr. Hicks they formed shore-
lines and were very much in their present mineral condition before
any of the Cambrian sediments were deposited. The conglomerate
itself is, he says, very largely indeed made up of fragments and finer
materials derived from them by denudation, and constantly overlaps
different members of the volcanic series, from which it is separated
by a systematic unconformity.

Dr. Geikie denies the systematic unconformity, admitting only
contemporaneous erosion ; he denies that the included pebbles are
‘“‘ almost invariably for the most part ” derived from Pebidian rocks,
and he denies that they constantly overlap different members of
the volcanic series.

Let us, before examining the evidence in detail, consider what we
are entitled to expect on the one view and on the other.

On Dr. Hicks’s view we should expect to find a more or less well-
marked line of demarcation between the Cambrian conglomerate and
the upturned and eroded edges of the more ancient strata. We
should expect a varying discordance of strike between the uncon-
formable systems. We should expect the included fragments, or at
any rate a large proportion of them, to consist of well-rounded
pebbles of the volcanic breccias similar to those which are abundant
on the present shore-line where Pebidian strata are undergoing
denudation.

On Dr. Geikie’s view we should expect the conglomerate to lie
on a current-swept surface of the volcanic tuffs and breccias which
were then still soft. We might even expect a considerable thick-
ness of the volcanic beds to have been in some places swept away
by currents capable of rolling onwards such large masses of
quartzite. Together with this local contemporaneous erosion we
should expect systematic conformity and accordance in the main
lines of strike. We should expect some shading of the conglomerate
into the underlying volcanic beds at the point of junction and some
inwashing of the volcanic beds into the conglomerate. We should
expect to find occasionally, among the materials of the conglomerate,
subangular fragments of the larger inclusions of the breccias and
tuffs over which the current passed.

Such would seem to be legitimate expectations, What are the
facts ?

There are four localities where the Pebidian-Cambrian junction
may be observed. Two (Caerbwdy Valley and St. Non’s Bay) are
to the south of St. Davids, two (Ogof Golchfa and Ramsey Sound)
to the north. We will consider the stratigraphical evidence in each

244: ‘PROF..C. LLOYD MORGAN ON THE PEBIDIAN

of these localities severally and then the evidence afforded by the
materials of which the Cambrian conglomerate is composed.

b. In Caerbwdy Valley.—This locality is situate about a mile to the
south-east of St. David’s city. The conglomerate is here seen crossing
the valley, striking N. 65° E., and dipping seawards somewhat
steeply. It is underlain by a close-grained red felspathic tuff.
There is no sharp line of demarcation -between the two, and a good
deal of evidence that the felspathic tuff is inwashed into the con-
glomerate. Some three or four feet above the base of the conglo-
merate, for example, a very similar material occurs *. On the east
side of the valley this tuff crosses the road, and associated with it
there seems to be a more argillaceous fine-grained tuff of a pink
colour. The strike here appears to be the same. Higher up the
valley bedded porcellanites are well exposed in a quarry. Their
strike can be accurately read; it is the same as that of the con-
glomerate, N. 65° E.

From Caerbwdy Valley westwards the conglomerate does not
afford facilities for observation until we reach St. Non’s Bay.

Fig. 1.—Sketch-map of St. Non’s Bay. (Seale 1 foot to 1 mile.)

Conglomerate.

——
Cambrian (Caerfai beds).

a-e. Faults.

e. In St. Non’s Bay.—This locality is situate south of St. David’s
city, about a mile west of Caerbwdy Valley. If we approach the
bay from Bryn-y-garn, skirting the field in which St. Non’s Chapel
stands in ruins, we find ourselves at the head of the most westerly
of the series of little creeks shown in the sketch-map, fig. 1. Skirting
this and standing at the point marked w we obtain the view shown
in fig. 2, Along the central line of vision runs the conglomerate,
striking N. 75° E., and forming the northern side of an arch (St.

* Although the microscopic character of the rock is obscure, still the micro-
scope only reinforces the macroscopic similarity.

VOLCANIC SERIES OF ST. DAVIDS. 245

Non’s Arch we may call it), figured by both Dr. Hicks and Dr. Geikie.
To the left, where four birds are placed, we have Pebidian por-
cellanites and breccias nearly vertical. To the right, where there
are two birds, we have Cambrian greenish flaggy beds, also nearly

Fig. 2.—Sketch from Cliff, St. Non’s Bay, looking east.

t

———

ao Caerfai beds of Cambrian Ano

Z Cambrian conglomerate.
with seaward dip.

~~~ Ditto, nearly vertical. prige, Pebidian.

vertical, but disturbed by faulting. Still further seawards purple
Cambrian strata of Dr. Hicks’s Caerfai group dip at an angle of
about 45°. ‘The strike of the Pebidian porcellanites and that of the
green Cambrian sandstones both agree with that of the conglo-
merate.

Reference to fig. 1 will show that there are several little faults in
this bay. To the east over St. Non’s arch there are two faults.
Both are omitted in Dr. Geikie’s figure (/. c. p. 287), the more in-
land of the two by Dr. Hicks (1. ¢. p. 525). These omissions make
the figures in each case incorrect. J have theréfore redrawn the
arch (fig. 3). The two faults are indicated by the single line a on
the plan, fig. 1. Another fault, >, has slightly dislocated the strata
in the middle of the bay. Further westward a fault, c, running
S. 30° E., has shifted the line of the conglomerate about 70 feet
inland and to the north ; while in the next creek, the most westerly
of the series which form St. Non’s Bay, another fault, d, running
inland S. 70° E., has again shifted the conglomerate inland and
northwards about 90 feet. An east and west fault, e, has bevelled
off the edges of the vertical conglomerate and caused red felspathic
Pebidian to lie upon it; while in the western creek a similar fault,

246 [PROF. C. LLOYD MORGAN ON THE PEBIDIAN

f, probably originally continuous with this and with one of those
over the arch, has shifted the conglomerate so as to cause it to rest
on the bevelled edges of greenish-brown Cambrian sandstones,
These faults are not of any magnitude; but they must be taken
into consideration for the understanding of the stratigraphical rela-
tions in this bay.

Fig. 3.—St. Non’s Arch.

aa. Pebidian. ec. Cambrian, Caerfai beds.
6b. Cambrian conglomerate. dd. Disturbed Caerfai beds.
Sf. Lines of fault.

Matters are also complicated by the intrusion of massive quartz
porphyry (++) and diabase dykes (firm dark lines), Concerning
them, however, I have nothing here to say except that the intrusive
nature of the quartz-porphyries is unquestionable.

Both at the east end and at the west end of the bay the Pebidian-
Cambrian junction can be studied.

The little bay to the north-west of St. Non’s Arch is not difficult
of access; a steep grass slope, overshadowed by the face of the
porphyry-dyke, bringing one to the foot of the cliffs. Here the
porcellanites can be studied in detail and are seen to be fine-grained
sedimentary strata altered in situ. Fine lines of bedding are
beautifully shown on their weathered edges. Between the porcel-
lanite-beds are coarser, greenish, softer beds, which show diagonal
cleavage, the cleavage-planes here, as elsewhere, in the district
dipping to the N. at about 60°. Bands of brecciated tuff are here
and there interstratified.

At low-water spring-tides it is possible to climb round under

VOLCANIC SERIES OF SI. DAVIDS. 247

the cliff into and through the arch, and the junction of the con-
glomerate with the underlying Pebidian may without difficulty or
danger be followed up the cliff to within about 6 feet of the grass .
slopes.

The beds immediately beneath the conglomerate very clearly
indicate the oncoming of sedimentary conditions, which is also indi-
cated by the porcellanites. There are fine-grained pink and white
beds, a red felspathic tuff with numerons rounded grains of quartz,
greenish shaly bands, white quartzose beds, and a very close-grained,
white, porcellanitic material. Upon the somewhat hollowed surface

-of these beds lies the conglomerate. ‘There is about 8 or 10 feet

transgression of the conglomerate across the Pebidian strata. Near
the foot of the cliff, for example, the soft pink and white beds are
about 6 feet below the conglomerate. Higher up the cliff the con-
glomerate rests upon this bed and it is washed in among the pebbles,
large stones being well imbedded in this material. I examined this
locality very critically and carefully. In my judgment the facts
favour Dr. Geikie’s view (contemporaneous erosion) rather than that
of Dr. Hicks (systematic unconformity).

In the westerly creek at the foot of the cliff, below w, the junc-
tion of the conglomerate with the underlying Pebidian, here grey
with small water-worn pebbles from 7 to 3 an inch long, may be
seen. The line of junction is an uneven one, the conglomerate
Y-ing into the subjacent material. I could see no satisfactory
evidence here of a systematic unconformity.

Nor is such evidence afforded by the detached conglomerate
masses between this creek and the arch. The underlying beds are
similar to the red sandy beds with rolled quartz pebbles found
beneath the conglomerate at St. Non’s arch, and well seen on the
top of the little promontory which the archway pierces.

In St. Non’s Bay, then, together with clear and unmistakable
signs of local or contemporaneous erosion, I find the general paral-
lelism of the strike most marked. There is no evidence of the
bending round of the conglomerate against the strike of the Pebidians
drawn by Dr. Hicks in his ‘“ Plan of Coast south of Nun’s Chapel ”
(l. c. fig. 3, p. 536), while the unconformity shown in his fig. 2
(p. 525) is much exaggerated. The incoming of sedimentary con-
ditions is also noteworthy.

The contact of the conglomerate with Pebidian is again seen
further west at Ogof Llesugn ; but a description of this locality may
be advantageously deferred.

We come now to the junctions seen on the northern side of the
axis.

d. At Ogof Golchfa.—This locality is a mile and a balf north-west
of St. David’s city, situate at the south end of Whitesand Bay,

Between Porth Sele and Whitesand Bay the conglomerate is well
exposed and is here of considerable thickness. ‘Tracing the cliff
from Porth Sele northwards we have the flaggy sandstones of the
Caerfai series striking N. 15° E. and dipping seawards at about 60°.
These extend for two or three hundred yards, when the succession

Q.J.G.8. No. 182. s

248 PROF. C. LLOYD MORGAN ON THE PEBIDIAN

is broken by a considerable fault, which brings the conglomerate to
the shore-line. This fault is entered in Dr. Hicks’s map; but I
~ have not seen any evidence for the second fault he draws, making
a V with this one. Inland of the fault and on its southern side the
conglomerate is well exposed in the field, so that the amount of
displacement, 175 yards, can be readily measured. North of the
fault the well-developed mass of conglomerate then runs roughly
parallel with the shore-line (though it is thrown seawards by one
or two minor step-faults), striking N. 35° E., with a dip of from
50° to 45°. At the southern end of Whitesand Bay, at Ogof
Golchfa, the underlying Pebidians are exposed for a short distance,
when another strongly-marked fault brings in higher beds of the
Cambrian series.

Dr. Hicks figures the junction at Ogof Golchfa as if it showed a
marked unconformity (J. ¢. p. 543, fig. 15). The figure is, how-
ever, misleading. The conglomerate ends off against the Pebidian
with a faulted junction, as noted by Mr. Blake. The edges of the
conglomerate are truncated wedge-fashion, as shown in the accom-
panying sketch (fig. 4), taken from the cliff so as to look down en

Fig. 4.—Faulted junction of Conglomerate and Pebidian
at Ogof Golchfa.

Sketched at high-water from the cliff, looking down in the direction
of dip of the conglomerate.

the line of dip of the strata. Near the base of the cliff, however,
the slip has taken place in such a manner as to leave some of the
red Pebidian adherent to the conglomerate, and here they end off
against the conglomerate, making with it an angle of perhaps 5°.
A little further north, where the big fault brings in higher beds of
the Cambrian succession, some of the conglomerate is in contact
with the underlying Pebidian, and appears to be quite conformable
with them.

VOLCANIC SERIES OF ST. DAVIDS. 249

The Pebidian strata at Ogof Golchfa, which are troubled by a
basic igneous intrusion, show as clearly as, if not more clearly than,
at St. Non’s Bay the incoming of sedimentary conditions. They are,
indeed, marked on Mr. Blake’s plan (Quart. Journ. Geol. Soc. vol. xl.
p- 298) as “Cambrian sandstone.” They consist of red and purple
and green sandy and very close-grained tuffs. In hand-specimens
the finer red beds are scarcely if at all distinguishable from the red
Lingula-primeva beds of the Cambrian of this district. They are,
however, remarkably schistose, but not more so than the finer beds of
the conglomerate itself. I cannot make 5° difference between the
strike ofthe Pebidian strata and that of the overlying conglomerate..
Both are N. 35° EK. The dip of the conglomerate at the seaward
low-tide face is 45°, near the faulted junction it is 55°; that of the
Pebidians is from 60° to 70°, or even somewhat higher.

Here, then, we have, together with some slight signs of local
unconformity, a marked parallelism of strike, a continuous change
of dip, and a common schistosity. I could find absolutely no
evidence of the divergence of no less than 45° between the strike
of the conglomerate and that of the Pebidian drawn by Dr. Hicks
on his map. The strike of both can be readily observed at Ogof
Golchfa, and they are practically identical.

e. In Ramsey Sound.— Near Rhoson the conglomerate may be
seen in the first field going down to Porth Stinian, to the left of the
path. ‘The strike here is N.45° E. No junction with the Pebidian
can be seen, but these strata near the farm and on the flagstaff-hill
appear to have the same strike. The Pebidian on Rhoson, more-
over, and the conglomerate in the field both have a low dip of from
2a too.

There are several field-exposures of the conglomerate between
Rhoson and Maen Bachau, where it emerges on the coast-line. It
is in close proximity to the outcrop of basic lava-flows, some of
which may have been at or near the surface at the time when it
was deposited around them. There is, however, much evidence of
faulting, and as no direct junction can be seen, these exposures need
not be further described.

The conglomerate is next seen on the coast at Maen Bachau,
south of Castell, a spot readily recognizable, since this rock here
forms the bridge of a conspicuous natural arch. The under surface
of the bridge is a line of slip, the fault-line being indicated by
quartz-spar. But the slip has taken place in such a way as to
leave some red sandy Pebidian adherent on the northern side to the
under surface of the conglomerate. These beds show at this spot
some signs of ending off against and being washed in with the
conglomerate. Beneath the fault, which makes an angle of about
45° with the vertical, and is probably of no great magnitude, the
red Pebidians are seen ending off against the fault-face and resting
on an uneven surface of basic igneous rock. Associated with the
red beds are dark green tuffs with abundant small, black or, rather,
very deep red specks.

To the north of the arch red Cambrian Caerfai beds form the

ts Bhar

250 PROF. C. LLOYD MORGAN ON THE PEBIDIAN

coast-line, and beneath them are green sandy shales. These are
separated from Pebidian by a quartzose fault-line, broken fault-rock
lying on the lower rock-surface. The conglomerate is here cut out.
The Pebidians show the incoming of sedimentary conditions which
is so noteworthy at Ogof Golchfa. The red and green Cambrian
beds are invaded by a dyke of basic igneous rock.

In the little creek immediately to the south of the arch the con-
glomerate, here thick, has been thrown back by a little east and
west fault, and rests upon the surface of green Pebidian tuff with
the dark specks before mentioned. The beds in this creek are a
good deal troubled, and the junction is somewhat obscure. I could,
however, find no satisfactory evidence of anything like a systematic
unconformity. ~

The included fragments in the conglomerate are here remarkable,
as will be presently noticed.

In the next creek southward there must be more faulting; for
the green sandy Cambrians are seen striking at the conglomerate.

The following creek shows the green sandstones (striking N. 25° E.
and dipping about 40° seawards) overlying the conglomerate.

In the next creek there occurs a considerable fault. The northern
cliff-face is conglomerate, against which the silky schistose Pebidians
with associated porcellanites strike about N. 45° E. It is not difficult
to clamber down here. At the base of the conglomerate is a cave
(Ogof Goch) following the line of the fault, which runs 8. 70° W.
The Pebidian in contact with the conglomerate is at first sight a
dirty dark-green basic-looking rock. When polished, however, it
is seen to be a rich green with lighter veins. I prepared a speci-
men for microscopic examination. The following is Mr. Grenville
Cole’s description of the slide :—‘‘A rock probably composed of
ferruginous clayey particles, with lava chips and tuff-fragments,
washed into it. The sedimentary part—the clays—seem reduced
chemically, and the iron separated, probably as magnetite dust.
The whole has undergone squeezing.” Although it is probable that
the rock has undergone alteration, it is obviously very different
from the silky beds and porcellanites on the other side of the dis-
placement. But in the cave and so close to the fault the relations
of Pebidian to Cambrian at the junction cannot be readily observed.

So far as I can ascertain, it is to this spot that Dr. Hicks’s fig. 14
(l.c. p. 542) purports to have reference. I could find nothing here
or elsewhere on this coast-line in any way resembling it. The
Ogof Goch fault, the effects of which are well marked here and
inland, is not noticed by either Dr. Hicks or Dr. Geikie.

Pebidian strata form the coast-line for about half a mile beyond
Ogof Géch until we reach Carn-ar-wig, where another well-marked
fault oceurs. On the south-western point beyond this bay the
last exposures of the conglomerate occur*. Speaking of this locality
Professor Blake says:—‘‘ Though there is no fault here, all the
rocks being laid quite bare, no better proof could be desired, derived

* These exposures are not mentioned by Dr. Hicks or marked on his map.

VOLCANIC SERIES OF ST. DAVIDS. AT AN

from one spot, of the perfect independence of the conglomerate and
the volcanic series, and in particular the silvery schists.” I
approached this locality, therefore, in the full hope of finding satis-
factory evidence in favour of one theory or the other.

The first (north-easterly) exposure of the conglomerate shows
this bed resting upon the surface of a lava. Mr. Grenville Cole
kindly examined my sections * of rocks from this locality, and the
words placed within inverted commas in the following descriptions
are from the notes he kindly sent me. Of this rock he says that
it is an ‘* Andesite lava, with veins of chloritic decomposition. The
flow may result from squeeze, but was probably original when the
rock was brown and glassy.” ‘There are certainly no marked signs
of independence here. The appearance is as if the conglomerate
were deposited in the somewhat concave surface of the lava.

This is, however, not the only exposure of the conglomerate.
Further to the south-west there is the clearest and most unmistakable
evidence of the interstratification of the conglomerate with Pebidian
voleanic beds. In the most westerly exposure there is fair, but not
perhaps convincing evidence that the conglomerate is succeeded by
voleanic beds four or five feet thick, and these, again, by conglom-
erate overlain by fine tuff. The details here are, however, difficult
of mastery and of description. But a little to the east of this
the relations are more readily decipherable. Beneath the conglom-
erate is tuff or broken-up lava. In the midst of the con-
glomerate is a thin band of ashy tuff which, under the influence of
squeeze, has a somewhat fluidal appearance. Above the conglom-
erate are ashy tuffs and perhaps lavas. Pebbles of quartzite are
found in the ashy tuffs adjoining the conglomerate. The two so
shade into one another that it is ofttimes difficult to tell where one
begins and the other ends. The tonguing-in of one series with the
other is complete. One seems to be in presence of an island or
shoal in the sea in which the Pebidian volcanic series were accumu-
lating. In the hollows on the surface of the lavas and tuffs tongues
of conglomerate were formed by the currents that bore onwards
the quartzose materials. Then followed other volcanic outpourings
by which the conglomerate tongues were buried.

Above and inland of these exposures is a highly vesicular amyg-
daloidal rock (in which a quarry has been opened). This Mr. Cole
describes as a “soda-trachyte or highly silicated andesite, with
tendency to spherulitic and granophyric structure.” It may be a
lava, but is more probably a dyke—perhaps a volcanic dyke of con-
temporaneous origin.

I carefully considered on the spot two possibilities—(1) that the
lavas and supposed ashy beds were dyke-material of long subsequent
date which had enveloped the conglomerate. (2) That the ashy
beds and supposed lavas were remade materials consequent on the
denudation of neighbouring Pebidian beds on Dr. Hicks’s hypothesis.
The field-evidence and the microscopic evidence negative both

* Prepared by Mr. Thomas Ryley.

PH? PROF. C. LLOYD MORGAN ON THE PEBIDIAN

suppositions. J am therefore forced to conclude that Pebidian and
Cambrian here interdigitate.

f. The Materials of the Conglomerate-—‘ The pebbles” [of the
conglomerate | says Dr. Hicks, “ almost invariably for the most part
consist of the rocks upon which they lie, and when examined they
tell distinctly that the underlying Pebidian rocks, after they were
elevated, when these fragments were broken off, and before they
were again depressed, were not only consolidated but nearly as
highly metamorphosed as they are found to be at present.”
(Q. J. G.S. xxxiv. p. 162.) On the other hand, Dr. Geikie says (1. ¢.
p. 288), ‘* Of the component pebbles not less than about 95 per cent.
are of quartzite or quartz.” And, as the results of the examination
of microscopic slides, Mr. T. Davies says (Q. J. G. 8. xl. p. 556),
‘‘ The contents of the Cambrian conglomerates of St. David’s, found
in the sections examined are:—quartz, both dirty and clear, small
pebbles consisting of dirty quartz with two felspars, individual felspars
both orthoclase and plagioclase, felsite, quartz-felsite, quartz-schists,
quartzite, basic rocks, porcellanite, and mica much altered.”

Now there can be no question that a preponderating number, I
may say a very largely preponderating number, of the pebbles are
composed of materials from a foreign source, and for the most part
of quartz and quartzite. But there are, especially in some localities,
other included fragments. ‘These are particularly conspicuous at the
Arch, near Maen Bachau, south of Castell. A goodly number of these
may be fairly matched with undoubted Pebidian. This at first im-
pressed me strongly in favour of Dr. Hicks’s contention. But
when I came to study the Pebidian beds more carefully and in
greater detail, I found the fragments imbedded in the tuffs and
agelomerates so numerous, in some cases so large, and so closely
resembling the fragments included in the conglomerate that it
seemed to me that the evidence afforded by them was by no means
so clear as I had at first supposed.

These Pebidian fragments, if such they be, enclosed in the con-
glomerate on Ramsey Sound, are remarkable in that they are for
the most part much softer than the more numerous quartzite- and
quartz-pebbles, and that they are less well rounded. In some cases
they form long flat subangular slabs, in others somewhat lenticular
masses ending in fine points; occasionally they seem to be indented
by the harder and rounder pebbles. Clearly they have not been
brought from a great distance. Clearly they have not been rounded
by long-continued wave-action. —

During a second visit to St. David’s for purposes of verification,
I paid especial attention to the question of included fragments,
both in the Pebidian and ‘in the Cambrian conglomerate. In the
former there are a considerable number of fragments, from, what-
ever source they may have been derived, of a horny porcellanitic
rock. Most of these are small, though fragments from half an inch
to an inchin length are not unfrequent. Fragments of porcellanitic
rock in the conglomerate may therefore be from this source. I
was again struck with the number and variety of the fragments of

eee ee

VOLCANIC SERIES OF ST. DAVIDS. 253

older tuff and more sedimentary-looking material in the upper beds
of the Pebidian series.

Turning to the conglomerate, it appears that the fragments of
Pebidian aspect differ from those contained as inclusions in the
Pebidian tuffs chiefly in their larger size. I paid a good deal of
attention to the Pebidian pebbles on the modern beach in the
neighbourhood of cliffs of this age, and was forcibly impressed by
the fact that no pebbles of similar form, structure, and aspect
occurred, so far as 1 was able to observe, in the conglomerate.

I have no desire to underestimate the value of the evidence of
these abnormal inclusions in the conglomerate. I hold no brief for
either party in this controversy. My sole desire was to reach, if I
might, the truth concerning the relation of Pebidian to Cambrian.
The evidence of these fragments seemed at first to contradict the
stratigraphical evidence. But further study tended to show that
this contradiction might be apparent only, and that the Pebidian
fragments might well be derived from inclusions in the tuffs washed
out of these deposits by the current which bore onward the more
numerous foreign materials of the conglomerate.

ge. Summary of the Hvidence.——The evidence as to the relation of
Pebidian te Cambrian at St. Davids is, in my opinion, not such as
to enable one to lay down the law with ease and precision. It is
such that two geologists who were at one concerning the facts
observed might nevertheless differ as to the exact position and value
in the stratigraphical scheme to be assigned to the Pebidian series.
On the one hand we have in the Cambrian conglomerate an
apparently satisfactory base to a natural system of stratified de-
posits; we have in that deposit fragments derived from the under-
lying strata; we have evidence of some transgression of the con-
glomerate across the edges of the subjacent beds. On the other
hand we have. a marked parallelism of strike and a general uniformity
of dip in the beds of both Pebidian and Cambrian; the included
Pebidian fragments are such as might have been washed out of
Pebidian tuffs ; and the transgression across the subjacent beds is
nowhere more than one has a right to expect where a current-
borne material, such as a coarse conglomerate, follows upon soft
beds of recent formation. It is remarkable that both to the south
of the St. David’s axis and to the north, where in each case the
parallelism of strike is so marked that I could nowhere make 5° of
difference, we have evidence of the incoming of sedimentary con-
ditions in the Pebidian similar to those which are indicated by the
Cambrian beds that succeed the conglomerate. And it is note-
worthy that in those overlying Cambrians we have evidence of the
continuance of volcanic conditions which characterize the Pebidian.
Moreover, at Carn-ar-wig we seem to have satisfactory evidence of
the interdigitation of Cambrian conglomerate and Pebidian ashes.
Taking all the facts into consideration, [ am led to the conclusion
that the break between the two systems was not of any great
magnitude, and that the change of conditions emphasized by the
conglomerate was one which followed. after no great lapse of time,

954 PROF. C. LLOYD MORGAN ON THE PEBIDIAN

on the volcanic condition of the Pebidian, the uppermost Pebidian
beds already foreshadowing the sedimentary conditions of the
Caerfai beds.

And here I think it well to draw attention to the amount of
break for which Dr. Hicks contends. According to Dr. Hicks the
Pebidians were (1) deposited as a volcanic series, (2) upheaved into
dry land, and also (5) metamorphosed to very much their present
condition before (+} they were denuded to form coast-lines of an
Archeean land, which (5) once more sank beneath the sea and (6)
were overlain unconformably by the beach-deposit of the Cambrian
conglomerate. Such is Dr. Hicks’s contention. But it is right to
add that at times he writes as if he held a very different view.
For example, in his answer to Dr. Geikie (Q. J.G.S. xl. p. 536), he
says :—‘‘ Whether the volcanic fires had completely expended them-
selves or not before the conglomerates were deposited may be an
interesting point; but it is virtually of no importance in regard to
the questions at issue.” On reading this I thought I must have
misunderstood Dr. Hicks’s previous statements. But no! They
are quite clear. So also is the testimony of his map. And I
therefore am in some doubt as to which statement represents Dr.
Hicks’s present view. ‘Taking, however, the former, so distinctly
formulated and reiterated, I must distinctly state that [ could find
no evidence to justify it. Coming to St. Davids fresh from a
study of the beach-conditions of the Basement Beds of the Trias in
the Bristol district, | was impressed with the very different nature
of the break between Pebidian and Cambrian in Pembrokeshire. |

The relation of Pebidian to Cambrian is therefore, in my opinion,
that of a volcanic series, for the most part submarine, to the suc-
ceeding sedimentary strata which are introduced by a conglomerate
formed in the main of foreign pebbles borne onward by a current
which swept the surface of, and eroded hollows and channels in,
the voleanic tuffs and other deposits.

The last question which arises on this head is whether we should,
as Dr. Geikie proposes, abandon altogether the term Pebidian; and,
further, if we retain it, what value we should assign to it. I think
that to abandon it would be a distinct injustice to Dr. Hicks, who,
notwithstanding manuscript evidence of Sir Andrew Ramsay’s
views, was the first to draw the attention of geologists to this
interesting volcanic series, and to place on record a great number of
valuable facts concerning it. The name Pebidian should therefore,
in my judgment, be retained for the volcanic series of St. Davids.

What value shall we assign to it? On this there will doubtless
be difference of opinion. For my own part I am clear that it should
not be removed from the Palaeozoic, that it cannot be regarded as
Archean. There remains the question:—lIs it to be regarded as
coordinate with Cambrian, Ordovician, Silurian, or coordinate with
Harlech and Menevian within the limits of the Cambrian? LT incline
to the latter view. Iam disposed to regard it as a volcanic series
at the base of, but not beneath, the Cambrian system. But I should
have no great quarrel with those who hold the other view.

—

VOLCANIC SERIES OF ST. DAVIDS. 255

3. Tar Peprpian SUCCESSION.

a. he Results of previous Investigations.—In his earlier paper
(Q. J. G. 8. xxiv. p. 15) Dr. Hicks divides the Pebidians into eleven
groups. Subsequently (Q. J.G.S. xl. plate xxiv.) he maps five
groups :—

¢. Purple and green schistose breccias.
: Diabase breccias and sheets.
nen felsite breccias and sheets.

. Felsite tutfs &c.
ile aor ates, breccias, and porcellanites.

These are mapped in parallel bands, little disturbed by faults
except where they adjoin the Dimetian and Arvonian axis. In
describing the area to the north of the axis, Dr. Hicks says:—
“Here, again, the evidence of a regularly ascending succession in the
Pebidian, but broken by a few faults, is perfectly clear, and there
is no indication of an isocline. The beds dip regularly in one
direction at a high angle, and the alternations are well marked and
easily traced.” (Q. J. G.S. xl. p. 544.)

Dr. Geikie divides the series provisionally into four groups :—

4. Fine tuffs and silky schists.
3. Diabase sheets with intruded quartz-porphyry and hardened tuffs.
2. Compact green granular tuff.

. Thick purplish-red, green-flecked tuff, with abundant small lapilli of
felsite.

These beds, according to Dr. Geikie, are isoclinally folded, the
axis of the isocline cutting the coast-line between Pen-maen-melyn
and Pen-y-foel.

Professor Blake found only a glorious confusion, which enchanted
him.

b. General Results of the Author's Survey.—Although the time at
my disposal did not permit of anything like an exhaustive resurvey
of the district, yet I was able to lay down on the six-inch survey
map the evidence afforded by all the important inland exposures
and that presented by the long coast-section. The main facts are
indicated in the accompanying sketch maps on the six-inch scale
(Plate X.), in which direct observations alone, and such inferences
as are inevitable therefrom, are included. A short description of
certain special features is also given in the pages which follow. Here
I will describe the main results which I have obtained.

There can be no question that with the exception of some cinder-
beds to the west which appear to be subaerial, the whole series was
accumulated under water, many of the beds containing quartzose
and other sedimentary material. The tuffs vary in colour from
dark green, or dark green and red, through lighter shades to light
ereen, light pink, and white. The former are decidedly basic, the
latter acidic in appearance. Sometimes, as may be well seen in the
Allan Valley, east of the cathedral, differing bands alternate some-
what rapidly. The lighter more acidic beds contain great numbers
of often large felsitic and felspathic fragments. In the more basic

256 PROF. C, LLOYD MORGAN ON THE PEBIDIAN

red and green tuffs there are many fragments ofa red fluidal
quartz-andesite. These fragments are sometimes of large size. One.
which I measured was four and a half feet in length. They also
contain bombs of basic lava, some of which also are of large size, a
yard or more in diameter.

In addition to these fragmental rocks there are contemporaneous
sheets and intrusive masses of basic igneous rock, the olivine-dia-
base of Dr. Geikie, dykes and sheets of felsite or quartz-porphyry,
andesite or trachyte, and perhaps sheets of quartz-andesite.

Concerning the subdivision of the series I do not think that the
facts to be presently brought forward justify us in making any
definite subdivisions or in going further than stating generally that
the series consists of alternating beds of tuff of varying colour and
basicity, but with prevailing tints of dark green, red and green, and
light sea-green. In the upper beds the tuffs of different character
alternate more rapidly, there are more rounded pebbles, and a
larger and increasing amount of sedimentary material, together
with porcellanite bands. Basic lava-flows occur for the most part
in the upper beds of the series. I was quite unable to verify Dr.
Hicks’s five groups. Indeed their existence is negatived by the
folding of the district to be now described.

Great care, much detailed work, and not a little climbing are
required to obtain anything like satisfactory evidence of dip and
strike in these Pebidian rocks. Moreover a persistent shearage of
the rocks along planes dipping at about 60° to the N.W., giving
sometimes the appearance of a true dip, is often very troublesome.
Careful observation of the rock-exposures foot by foot will, however,
disclose the occasional interstratification of finer and coarser
material or the alternation of tufts of different colour, and will thus
enable one to obtain reliable data for determining the nature of the
folding which the beds have undergone.

Detailed work between the headlands of Pen-dal-aderyn and
Pen-y-foel thus brings to light the fact that there is, in place of
the continuous sequence advocated by Dr. Hicks, or the isoclinal
fold suggested by Dr. Geikie, a well-marked syncline, the beds on
the southern. side of which are, however, repeated by small faults.
The syncline is perhaps tilted inland, so as to form the lip or spou
of an elongated basin.

Further inland there is again good evidence for the existence of
this syncline, satisfactory southerly dips of the northern limb being
observed on the prominent craggy exposure south-west of Treginnis
Isaf farm. And I think it not improbable that the low-lying swampy
ground between Trefeithan and Clegyr Foia marks the continuation
of the same synclinal fold*.

North-west of this central syncline runs an anticlinal fold. The

* All along the south-east side of Trefeithan, near its base, the red and green
‘‘diabase” tuffs which underlie the igneous sheets are well exposed, aud are
found to be lying nearly horizontally, the dip being N.W. (about 10°) in one
exposure and 8.K. (about 5°) in another exposure at the south-eastern end of

the hill. This looks as if we were near the somewhat flattened summit of the
northern anticline, and that between Trefeithan and Clegyr Foia there runs a

VOLCANIC SERIES OF ST. DAVIDS. PAS

evidence for this on the western coast is not satisfactory, but its
existence is unquestionable. It would seem to flatten in the neigh-
bourhood of Rhoson and Trefeithan.

South-east of the central syncline runs another anticlinal fold.
Below Treginnis Mill the evidence of the normal anticline is satis-
factory, the seaward dip of about 50° being readily observable even
froma distance. Tracing the beds eastwards

along the coast, the dip becomes higher, up Wee:
to 85°, seawards, and then passes over to a \ =
landward (reversed) dip of 75°-65°. The ;
normal anticline passes into an isocline. The : \\
northerly dips in Porthlisky Bay are reversed
dips. \\
The diagrammatic section (fig. 5) shows N
the structure of the western portion of the
‘St. David’s promontory as I read it. »
The thickness of the Pebidian volcanic
series exposed in the district, I estimate at y
about from 1200 to 1500 feet—a modest // J
figure compared with the 8000 feet claimed Y,
by Dr. Hicks. i
c. Further Details —There are one or two (
points on which further details may be desi- t uy
rable. NN x
(a) The Fault at Ogof Géch—A well- — |\\ aS
marked fault here brings basic beds against \\ Ss.
the more acidic schistose strata of Ogofau- N =
Dduon (the Ogfeydd-duon of previous writers. N 3
I have adopted the spelling of the 6-inch : =

survey map). Dr. Hicks is perfectly right
in contending that these Ogofau-Dduon beds
do not, as suggested by Dr. Geikie, imme-
diately overlie the more basic beds; but by
failing to take note of the Ogof-Goch fault
he erroneously made the conglomerate rest
immediately and unconformably upon these
beds. The fault is not only, as previously
noted, perfectly obvious on the coast-line, —~
but further inland it divides the more acidic
erags of Carn Gwil and Carn Geli Fach
from a triplet of basic crags of which Carn
Coch is the most prominent.

(B) The Porphyry Crags of Treginnis.
—The strongly marked rock-exposures of
which Carn Gwil Geli is the most easterly

UY

LLL / /

OT Bs

Jf
yset

aF

uonpa-npfoh mors hLopuoworg sprang 7 sso.to uoyors-upahoyug—G “Sty

perhaps faulted syncline. It may be, however, that the syncline has flattened
out; that,as Dr. Geikie suggests, the Clegyr Foia sheets lie on the southern side of
an isocline; and that the northerly dips there observable are reversed. I could
not determine this point with certainty. But I lean to the view that the folding
here is synclinal.

258 PROF, C. LLOYD MORGAN ON THE PEBIDIAN

are described by Dr. Geikie as the “ prominent and massive porphyry
crags of Treginnis.” That there is porphyry * I am not prepared.
to deny; but the main bulk of the crags is fragmental—a sea-
green highly acidic andesite-tuff with quartz-porphyry inclusions of
fair size and in great numbers. Some “adinole ” concretions occur
here; and, commenting on one of my slides, Mr. Cole asks “* Has
this rock been saturated (? with silica) so as to become so ‘ felsitic’
and uniform in texture?” The beds apparently dip northwards at
60°. But I was led to look with much suspicion at a northerly dip
of about this angle, since I frequently found it to be illusory and
the result of shearage.

(y) The Red Quartz-Andesite.—At Rhoson and Trefeithan, on the
north side of Porthlisky Bay, at Pen Pedol and elsewhere, there are
in the ‘“ diabase ”-tuffs large fragments of a red fluidal quartz-
andesite. They are for the most part angular. Near the landing-
stage at Carn-ar-wig there is a band or bed of similar lavaform
rock; and at Ogof Geifr a bed closely resembling it may be found.
Mr. Grenville Cole, to whom I submitted it, calls it “a beautiful
fluidal quartz-andesite (being ancient, a ‘porphyrite’ of German
authors). It reminds me of one at Elfdalen, Sweden, and many in
the Permian ‘ Bozen porphyries.’”’

(0) Volcanic Bombs.—The occurrence of large volcanic bombs in
rocks of such high antiquity is worthy of notice. Such a “ diabase ”
bomb, 33 feet in diameter, may be seen in the tuff at the seaward
foot of the craggy boss just inland of Ogof Cadno. Others may be
found along this coast-line. They are rounded, vesicular, and often
radially fissured. '

(e) Pen-dal-aderyn and Pen-y-foel.—t am inclined to regard the
“< diabase ” masses at these two points as intrusive, but unquestion-
ably of Pebidian age. They may almost be looked upon as volcanic
necks. It may be that the extrusion of lava through them has pro-
duced the remarkable confusion in the neighbouring tuffs. Near both
these points, too, the relations of the more basic and more acidic
tuffs indicate local contemporaneous erosion.

North of Pen-y-foel, towards Porthlisky Bay, there is another
great mass of ‘“‘diabase” with well-marked trappean steps leading
down to the sea-level. This may be a massive lava-flow; but I am
more inclined to regard it also as an intrusive contemporaneous
neck. The same may be said of the exposure to the south of Porth-
henllys Cottage.

d. Faults and their Effects —The long stretch of coast-line between
Ogof Golchfa on the north and Porthlisky bay on the south affords
every facility for studying the faulting of the district. In the
maps appended to this paper (Plate X.) I have entered all the faults
of which there seems to me to.be satisfactory evidence. The only
displacement of any considerable magnitude is that which takes

* Dr. Geikie, with great courtesy and kindness, allowed me to examine about
20 of his St. Davids slides, and among others one of the quartz-porphyry from
these crags.

VOLCANIC SERIES OF ST. DAVIDS. 259

place north of Ogof Golchfa, by which Menevian beds, as determined
by Dr. Hicks, are brought down so as nearly or quite to abut
on Pebidian. The other faults, though their effects are sometimes
well marked, as at the Ogof Goch, Carn-ar-wig, and north of Porth
Sele, are of no great magnitude or importance. A glance at the
map will show that the Caerfai beds (e.g. to the west of Porth Sele,
and in the neighbourhood of Castell) are affected by faulting to
as great an extent as the Pebidians which underlie them. In fact I
failed to find any evidence of faulting special to the Pebidian, as
opposed to the other Cambrian strata.

e. The Cambrian Overlap.—tI have before stated that neither in
Caerbwdy valley, in St. Non’s Bay, nor at Ogof Golchfa, did I find
satisfactory evidence for the overlap marked on Dr. Hicks’s maps
and plans. ‘There is such erosion as is inevitable from the nature
of the conditions under which the conglomerate was formed. More
than this I failed to see.

Dr. Hicks, however, contends that between Rhoson and the
exposure of the conglomerate on the coast-line beyond Porth Sele,
“the facts prove that in this mile of country a quarter of a mile in
thickness of nearly vertical Pedidian strata has been overlapped by
the conglomerates.”

The facts are these. Near Maen Bachan, south of Castell, the
conglomerate is seen on the coast-line. Then it is occasionally seen
in the faulted ground between this locality and Rhoson, where it is
seen striking N.E. with a low dip. The underlying Pebidians at
Rhoson are not “nearly vertical,” but have also a low dip and a
strike similar to that of the conglomerate. ‘here is, then, no
exposure of the conglomerate till it is seen in the field inland and
to the east of Porth Sele, where its strike is N.15° E. Here it has
been displaced 175 yards by the fault before alluded to, on the north
side of which it occupies the coast-line, with a strike N. 35° E,

- The faults between Maen Bachau and Rhoson and this fault are

step-faults constantly throwing the beds to the N.K. The proba-
bilities are that it is by step-faults between Rhoson and Porth Sele,
and not by overlap, that the displacement of the conglomerate has
been effected, and this view is borne out by the evidence of faulting
west of Porth Sele and near Porth Stinian (see map). In any case
it is incorrect (1) to speak of nearly vertical Pebidian, and (2) to
neglect the probable effects of faulting. .
But it may be said that the evidence of overlap is not merely a
matter of the strike of the beds, it is the fact that the conglomerate
is found resting upon different beds of the Pebidian series. Here
again Dr. Hicks’s map is misleading. Through missing the fault at
Ogot Goch he makes the conglomerate rest upon his C group of
quartz-felsite breccia and sheets. It does not doso. It is faulted
against them. Even if this piece of evidence be eliminated, however,
we have the unquestionable fact that at Ogof Golchfa the conglom-
erate is resting upon schistose sedimentary-looking beds, at Maen
Bachau it is in close proximity to ‘“ diabase” lava-flows, and at

260 PROF, C. LLOYD MORGAN ON THE PEBIDIAN

Carn-ar-wig point it interdigitates with more acidic lavas and
ashes. .

I have no wish to undervalue these facts. They are, indeed, just
such as I should expect upon the hypothesis that I adopt. I have
already mentioned the great cinder-beds in the western part of the
district which seemed to point to subaerial accumulation ; I have
also drawn attention to the tonguing-in of the conglomerate with
the voleanic beds at Carn-ar-wig. These facts seem to point to
subaerial conditions and shoals to the west. I think the facts point
to deeper water and more sedimentary conditions to the east and
south-east. But I believe that both near Pen-dal-aderyn and near
Pen-y-foel there is evidence of local erosion, within the volcanic
series, due to the fact that the tuffs were brought to or near the
surface, and thus suffered some abrasion from waves and currents.
And then, at the close of Pebidian times and the ushering in of the
Harlechs, the powerful current which bore onwards the materials
of the conglomerate could not fail to sweep away much of the
superficial soft tuff in the shallows and shoals of the Pebidian sea.
Its effect would be less marked in the deeper water to the east and
south-east. .

Let us try to realize the conditions. Volcanic tuffs are being
_ formed around several, perhaps many, small volcanic centres, for it

is probable that Cambrian volcanic efforts did not concentrate
themselves on one focus. The volcanic centres are submarine, or
perhaps form islands. As in the case of Graham’s Island, they may
have given rise to islands which were soon washed away by the
waves, the materials being scattered around as tuffs, commingled
perhaps with some sedimentary materials. Then as the volcanic
fires are dying out (Carn-ar-wig tells us they are not quite dead),
there comes a powerful current sweeping over the tuffs and bearing
onwards rolled quartz- and quartzite-pebbles of altogether foreign
origin. Whence came the pebbles, how was produced the current,
who can say? ‘There is the evidence of it in the conglomerate,
which is no beach-deposit or anything like it. Now if this be
anything like a true story of the sequence of events, and it seems to
me the only view which fits the facts, is it to be expected that the
conglomerate everywhere should lie upon the same voleanic beds ?
Would it not be in the highest degree surprising should it be found
to do so? Is it not more probable that here in deeper water it
should rest upon more sedimentary tuffs (Ogof Golchfa); there, in
shallower water, it should be in close proximity to lava reefs (Maen
Bachau) ; and elsewhere (Carn-ar-wig) it should tongue in with the
later splutterings of the volcanic period? So it seems to me; and
thus I would account for the apparent overlap of the conglomerate
on the Pebidian beds.

f. The “ Felsitic” Dykes.—Cutting through the Pebidian strata
and well exposed at many points along the coast-line are igneous
dykes. These are of two types, the one basic the other acidic.

Some of the basic dykes are seen in close proximity to or actually
connected with the basic intrusions of Pen-y-foel and the neighbour-

VOLCANIC SERIES OF ST. DAVIDS. 261

ing coast-line to the east. They may be regarded as definitely
connected with the volcanic series. Others, however, are of far more
recent origin and are found cutting alike through Dimetian, Pebidian,
and the overlying Cambrian sedimentary beds. Fine examples may
be seen in the Dimetian in the Porthlisky promontory, in the Pebidian
at St. Non’s Bay, and in the Cambrian sedimentaries at Porth-
y-rhaw.

: The acidic dykes are the quartz-porphyries of Dr. Geikie and the
felsites of other authors. Some of these in the Church-school and
Board-school quarries, for example, and in St, Non’s Bay, are
familiar to all who know the literature of St. David’s geology. But
there are other examples in many places along the Pebidian coast-
section. One of these is mentioned by Dr. Geikie as occurring near
Pen-y-foel. It is readily seen as one stands on this headland and
looks westwards across the Ogof Mrs. Morgan inlet. Near the sea-
line there are two converging limbs which appear to meet above to
form a common mass. Between the limbs a triangular mass of tuff
(basic) is enclosed, and similar tuff is seen on either side. I bave had
half a dozen slices cut from various parts of this dyke for micro-
scopic determination. Mr. Grenville Cole has kindly afforded me
much valuable assistance in this examination.

The rock is granophyric in structure, with abundant spherulitic
ageregates in which the radial structure is well seen. Good
porphyritic felspars occur, which Mr. Cole is inclined to regard as
oligoclase. The banded structure along the edge of the dyke is
beautifully seen some 20 or 30 feet above the water’s edge, and in
one part waving flow-lines are very noticeable on the weathered
surface. Vesicular and amygdaloidal structure is well marked in
parts. ‘The vesicles are large, elongated, and oval, with their long
axes parallel. This led me to suspect that the dyke was rather
voleanic than plutonic in origin. For in plutonic dykes the vesicles
are generally rounded and small. In one of my slides the rock
shows much brecciation, which may, as Mr. Cole suggests, contain
fragments from the adjacent tuffs or may have resulted from dragging
and flow along the contact plane.

In the notes with which Mr. Cole was good enough to furnish me
he describes the dyke in general as ‘a good granophyric rock like
the wall of Cader Idris and many other British examples. The
analysis ought to give some 70 °/, of silica, and soda as the dominant
alkali,—a quartz-andesite, or perhaps more nearly an oligoclase-
trachyte had it erupted asa lava. It might well be an offshoot of
a soda-granite or quartz-diorite.”

I subjoin an analysis of this rock (1.), together with an analysis
of the acidic tuffs (II.) of Pen-y-foel hard by for comparison, They
are kindly furnished me by Mr. Cecil Gibbins, who carried out the
analyses in the chemical laboratory of the University College,
Bristol. I have added in the third column (III.) an analysis of
Dimetian, quoted from Dr. Persifor Frazer by Dr. Hicks.

262 PROF, C. LLOYD MORGAN ON THE PEBIDIAN
i Te aT be Ee

Tenition. ... 1:69 ee 1°38
i eat (es 72°30 74:09 75°48
LUE ORS ee 12-09 14°98 9-60
Fe,0, oe : 1:73
may } 216 1-80 { ie
Cal. ceeukat trace. trace. 98
Oe @ eee DAO 1°50 1:32
Le Oe Pee 4°80 27 56
Nig O% ahis) a oil 6°07 5:09
HES He tent es “90

99°37 101-02 100-40

Allusion has already been made to the very vesicular rock at Carn-
ar-wig. It is remarkably lavaform, but is more probably part of
a dyke. Two strong beds of soda-trachyte or highly silicated
andesite interstratified with the Pebidian may be lava, but perhaps
it is best to regard them as sills. Still I should not be surprised if
true lavas of similar character * to the dyke-material were to be
proved at this spot. In any case I wish to suggest the possibility
that the acidic dykes, such as those at Pen-y-foel, Carn-ar-wig, and
others at Ogofau-Dduon, Pen-maen-melyn, Porth Taflod, Ogof
Cadno, to the north-west of Porthlisky, and at Trefeithan, may be
volcanic dykes intruded during the last phase of Pebidian volcanic
activity. How far this view (merely advanced as a suggestion)
would apply to the much larger dykes near the St. David’s schools
and in St. Non’s Bay I am not at present prepared to say. There
is no doubt, however, that all these dykes have the granophyric or
spherulitic structure in common.

g. The Porcellanztes.—That these beds have undergone alteration
since their original deposition there can be no doubt. But whether
this is due to the influence of the quartz-porphyry dykes, as
suggested by Dr. Geikie, is, I think, open to question. They are
seen in Caerbwdy valley, in St. Non’s Bay, and to a less extent
at Ogofau-Dduon ; while a porcellanitic bed is found in the Alian
valley near the boundary-wall beyond the vicarage. In Non’s Bay
the weathered surface gives indication of the originally very fine
sedimentary nature of at any rate some of the bands. Sometimes
the beds are porcellanized in fine bands interleaved with softer
scarcely altered material. In the Allan valley it is a tuff-like bed
with largish included fragments which has been porcellanized.

Dr. Geikie has drawn attention to the concretionary masses (the
so-called adinole) in St. Non’s Bay; but Dr. Hicks regards them as
included fragments. ‘‘ That they are true fragments,’ he says
(p. 548), “of some pre-existing rocks, and not concretions, is clear
beyond dispute from microscopical and chemical evidence.” I am
surprised, however, that any one studying them on the spot in
St. Non’s Bay could doubt their concretionary character. Both the

* The undoubted lavas seem to be somewhat more basic in composition.

VOLCANIC SERIES OF ST. DAVIDS. 263

porcellanite bands and these adinole masses remind one of the
occurrence of flint, or still more of chert in some of the older lime-
stones. That they are all products of some mode of the segregation
of silica is suggested by their appearance and mode of occurrence.
But the microcrystalline structure of the matrix is no doubt
puzzling on this view. It is probable that a fuller microscopical
study of these rocks in different stages of porcellanization would
yield results of considerable, and not merely local interest.

4. Tun Retation oF Pesip1an to Diwertay.

a. Dr. Hicks’s Arvonan.—lt is right that I should bere state why
I omit any consideration of the relation of Pebidian to Arvonian.
The reason is that I have been unable to satisfy myself of the
existence of aseparate and distinct Arvonian system inthe area within
which I restricted my observations. I do not deny the existence of
such a system. But I saw no satisfactory evidence of it in the
immediate neighbourhood of St. Davids.

b. Lhe Dimetian Question—Between the City of St. Davids and
the Crow and Bishop Islands, off Porthlisky Point, there occurs a
granitoid rock, well exposed at Bryn-y-garn and elsewhere. The
question at issue concerning this rock is, whether, in relation to
Pebidian, it is a subseqnent granite-intrusion or a pre-existent
Archeean formation. There are three kinds of evidence bearing on
the question :—(1) that derived from the lithological character of the
rock, (2) that based on the petrological and stratigraphical relation-
ship with the surrouuding rocks, and (3) that afforded by the presence
or absence of Dimetian fragments or pebbles in overlying deposits.

Concerning the first point, the lithological character of the rock,
I have no new facts to communicate. Had I been ignorant of the
controversy on the subject, I should unhesitatingly have pronounced
it a granite or an intrusive rock allied thereto. But since others of
far greater knowledge and experience than myself have held and
hold a different view, I do not presume to suppose that auy opinion
of mine will carry weight.

On the petrological and stratigraphical evidence I may be allowed
to offer a few remarks.

¢, In Porihlisky Bay.—In this locality there is no very satisfactory
evidence of either faulting or intrusion. As before noticed, however,
the strata in this bay have been much altered in some way, and if the
Dimetian be intrusive, one naturally surmises that it may have a
(possibly indirect) connexion with this alteration. It is therefore
worth noting that the Cambrian conglomerate and overlying beds
show a somewhat similar alteration in Porth Melyn, west of
St. Non’s Bay, and here the Dimetian is close at hand. Still, though
this is naturally suggested if the Dimetian be otherwise proved to
be granite, I do not think that by itself it can be taken as satisfactory
evidence of intrusion.

The fault-line, if it exist, is obscured. I found, however, un-

a. 3.G.8. No. 182. T

264 PROF. C. LLOYD MORGAN ON THE PEBIDIAN

doubted Dimetian some distance to the left of the fault-line as drawn
by Dr. Hicks in his figure (Q. J. G. 8. xl. fig. 13, p. 540).

d. In the Allan Valley at Porth Clais.—I have no new facts to
bring forward with regard to this locality, I could find nothing to
convince me of the intrusive nature of the granite in any of the
sections exposed. I am not altogether satisfied with Dr. Geikie’s
mapping of the locality (Q. J. G. 8. xxxix. pl. vii.). There has cer-
tainly been some faulting ; but there is no sufficient evidence of the
faulted patchwork shown in figure 5 of Dr. Hicks’s paper (p. 532).
Such a map, apart from its demonstrable errors (¢. g. the anticline
in the south-west corner, also shown in fig. 5, which has absolutely
no existence in nature), is worthless as a guide on the spot, and mis-
leading to the student in the study. I spent some time in endeavour-
ing to map this locality on the hypothesis of a faulted junction
between Dimetian andCambrian. My complete failure may be due
in part to the want of sufficient data; but it led me to suspect that
the Dimetian is intrusive, notwithstanding the absence of any con-
vincing evidence at the actual points of contact.

e. At Ogof Llesugn.—To this spot the easiest access is by the
Cambrian beds a little to the east of the incoming of the Dimetian.
Clambering down here by the sucking pool, one skirts the upturned
strata—striking N. 85° W. and nearly vertical, but with a slightly re-
versed dip—and descends, at low water, by a cleft opposite the most
easterly of the two faults described by Mr. Blake and Dr. Hicks.
A long cave occupied by water even at low tide runs here some
distance inland. To the west of this is a projecting spur of rock
consisting of Cambrian, with massive conglomerate, and apparently
some Pebidian. The beds strike about N.E. and show again the
inverted dip. There is, to my eye, no indication of the upturning
of the strata figured by Dr. Hicks.

Beyond this spur is the more westerly of the two faults, running
inland about N.N.E. This brings the conglomerate against Dimetian.
On the opposite or Dimetian side of the fault, about west of the
spur, the conglomerate is again seen. It is in contact below with
Dimetian, but there may be a slight slip here. It is overlain, owing
to the reversed dip, by red Pebidian. Then follow eight or ten
feet of green beds which are separated from the Dimetian by a
‘‘diabase ’’-dyke. Itis difficult here and elsewhere at Ogof Llesugn
to separate intrusive diabase from dark green altered Pebidian, and
it may be that all the dark material here is “ diabase.”

South of this, the western shore of the Ogof Llesugn creeks or
bays shows a bewildering confusion of rocks. There are two well-
marked masses of conglomerate, much altered and indurated. On
the outer face of the more southerly mass (that figured, to me quite
incomprehensibly, by Dr. Hicks) there is what appears to be highly
altered Cambrian fine-bedded strata. There is a very large amount
of much altered Pebidian, red, green, and white. Lastly these
rocks are seamed with ‘‘diabase”-dyke material. Here, again, it is
difficult to separate this material from Pebidian. But even granting
(what I am not: prepared to admit) that all the dark green material

VOLCANIC SERIES OF ST. DAVIDS. 265

is “ diabase ” subsequently intruded, it is to me inconceivable that
this alone should have produced the large amount of alteration and
induration in the conglomerate and large masses of Pebidian strata.
I am aware that Prof. Bonney says that he has seen nothing to
lead him to suspect that the Dimetian was intrusive in the Cambrian,
but much to induce him to consider the Dimetian far the older. I
can only say that oft-repeated study. of the locality left me unable
to account for the phenomena there presented, by either faulted
crushing or the influence of the “diabase”-dykes. The view that
the Dimetian was intrusive was therefore forced upon me.

f. General Considerations.—I have already stated that my study
of the Pebidian strata at St. Davids led me to dissent as widely
from Dr. Hicks’s classification and mapping of the volcanic series
as from his conclusions as to their Archean age. Quite apart from
any Dimetian question, I am led to regard the Pebidian beds in
St. Non’s Bay and in Porthlisky Bay as very near the top of the
series. This being so, it is quite impossible to map the Dimetian
on the hypothesis of its Archean age without so extravagant a use
of faulting as to stagger any sober geological surveyor. In any
case, even granting the correctness of Dr. Hicks’s Pebidian con-
clusions, it is exceedingly difficult to realize the sequence of events
which could possibly have given rise to the state of things depicted
in Dr. Hicks’s map.

I venture to think that Dr. Hicks hmself, and some of those
who accept his reading of the St. David’s geology, have failed to
realize what his map commits them to. At Ovof Golchfa, for example,
the conglomerate is stated to rest uncontormably on the highest
visible beds of the Pebidian. These are not necessarily the highest
existing beds. Other higher beds may, on this view, have been
overlapped by the basal conglomerate of the Cambrian. In any
case, however, these Ogof Golchfa Pebidians are, according to
Dr. Hicks, some 8000 feet above the base of the system, which may
have reposed directly on Dimetian, or may have rested on intervening
Arvonian strata. Let us say that it rested on Dimetian, and that
8000 feet represents the thickness of the Pebidians. Now west
of St. Non’s Bay the Cambrian conglomerate rests (see Dr. Hicks’s
map) directly on Dimetian—that is to say, it has overlapped some
8000 feet of upturned strata. Here again I do not press the
eriticism that in St. Non’s Bay the dip and strike of Pebidian and
Cambrian are practically identical—a state of things hard to realize
in connexion with such an overlap. What I wish to draw atten-
tion to is that such an overlap involyes an enormous break in
time,—uplhft, folding, and vast amount of denudation—between
Pebidian and Cambrian. And yet Dr. Hicks remarks in his reply
to the Director-General: “ Whether the volcanic fires had com-
pletely expended themselves or not before the conglomerates were
deposited may be an interesting point; but it is virtually of no
importance in regard to the questions at issue”! and Professor
Bonney says, in a letter quoted by Dr. Hicks (Q. J. G. 8. xl. p. 546),
that ‘“‘we do not efface the limits between Miocene and Pliocene

T2

266 PROF. C. LLOYD MORGAN ON THE PEBIDIAN

because, in a country where there has been great volcanic activity in
the former, some feeble sputterings have occurred in the latter ”—the
implication being that there might: be (though Dr. Bonney is not
satisfied with the evidence of the fact), still there might be some
sputterings of volcanic activity continued from Pebidian into
Cambrian without being utterly and completely subversive of
Dr. Hicks’s Precambrian theory.

Even on Dr. Hicks’s own hypothesis, then, his mapping of the
district, and especially of the Dimetian with its nine-faulted boun-
dary, is, I will not say an impossibility, but, to me, an incomprehen-
sibility.

But great as is the difficulty of mapping the Dimetian as Precam-
brian, on Dr. Hicks’s view of the Pebidian succession and orderly
sequence, it becomes immensely greater if the existence of an isocline
come to be regarded as an established fact. A glance at the diagram-
section (fig. 5, p. 257) will show how considerable a fault there must
be between Dimetian and Pebidian on the hypothesis of the Pre-
Pebidian age of the former. I do not say that the Pre-Pebidian
interpretation is thereby rendered impossible, but I do contend
that the difficulties of this view are thus rendered exceedingly
great.

e. The Evidence from included Fragments.—On this head’ I have
nothing but negative evidence to offer. In Porthlisky Bay there
are Beamtifalliy ‘rounded pebbles of Dimetian, readily recognizable
as such. Not a single pebble in any respect resembling these have
I seen in the conglomerate or elsewhere.

Dr. Hicks lays a good deal of stress on the minute pebbles,
supposed to be Dimetian, in the grit-beds at Chanter’s Seat. Now
from Dr. Hicks’s own statement and from my own observations I
conclude that these Chanter’s-Seat beds are from 800 to 850 feet
above the conglomerate. I find it very difficult to conceive, on
Dr. Hicks’s hypothesis, that any Dimetian—worn down as it had
been by Pre-Arvonian, Pre-Pebidian, and Pre-Cambrian denuda-
tion—could have continued still to afford materials for Cambrian sedi-
mentaries after 800 feet of these strata had already been accu-'
mulated. If the Dimetian origin of these pebbles be thus rendered
improbable, we — search elsewhere for the source of the “ dirty
quartz.”

5. ConcLustion.

It only remains for me to state briefly the general conclusions
that I have reached.

The Pebidian beds constitute a volcanic series, the base of which
is nowhere seen, about 1200 to 1500 feet in thickness. Their age
is anterior to the Harlech (Caerfai) conglomerate, which is, on
many places, locally unconformable tothem. I advocate the reten-
tion of the term Pebidian either as a sub-group of the Cambrian co-
ordinate with Harlech, Menevian, &c., or as a distinct volcanic group
coordinate with Cambrian, Ordovician, &c. (preferably the former),

VOLCANIC SERIES OF ST. DAVIDS. 267

but in any case to be included under the Paleozoic and not under
the Archean category.

These beds, in the western part of the district, where they can be
best studied, are thrown into a series of three folds—a northern
anticline, a central syncline, and a southern anticline folded over to
form an isocline with reversed dips to the south-east. The axis of
folding is roughly parallel with the axis of St. David’s promontory.

There is no evidence in the district of an Arvonian system.

The Dimetian is intrusive in the southern limb of the isocline.

There are no Archean rocks at St. Davids, unless some of the
included fragments in the Pebidian tuffs are to be so regarded—in
any case no Archean rocks in situ.

EXPLANATION OF PLATE X.

Sketch Maps of the North-western and South-western portions of the
District of St. Davids, on a scale of six inches to the mile.

The broken lines between the two Maps unite the points at which they
fit together.

Discussion.

The Presipent commented upon the differences of opinion among
those who had studied the geology of St. Davids, and pointed out
that there were two points of primary importance—the relations of
the Pebidian to the Cambrian, and those of the Dimetian to all the
_ other rocks. The Arvonian question was of less consequence.

Dr. Hicks said that the Author had commenced his paper with a
reference to the Caerbwdy valley, but had not referred to the great
agelomerates at Clegyr, nor to the clearly bedded porcellanites.
Now, there was nothing porcellanized in the Cambrian, and yet
fragments of the Pebidian porcellanite abound in the Cambrian
conglomerate. He proceeded to describe the different beds on which
the conglomerate rests transgressively, showing how the Pebidians
vary in character at different points; he also commented on the
absence of a map, and the paucity of sections. As to that at
St. Non’s Arch, the unconformity on the porcellanites was clearly
shown in both interpretations, and he exhibited photographs in
proof of the correctness of his own reading of thissection. At Ogof
Golchfa the Author had shown the beds as almost conformable, but
photographs were entirely against this interpretation. There might
be a kind of crush here between the Cambrian and Pebidian, as
would happen at the junction of such dissimilar beds; but there
was no fault, only a shearing. At Rhoson and other places large
fragments of Pebidian had been found, which showed that they had
been cleaved before being enclosed in the conglomerate.

Criticizing the diagrammatic section exhibited, Dr. Hicks remarked
that he himself had once given a similar section, but had found that
such a simple interpretation was impossible, and that the beds of
the Pebidian had been greatly broken and, in places, inverted, as the

268 PROF. C. LLOYD MORGAN ON THE PEBIDIAN

result of great thrusts from the north-west, and that they had been.
folded over a crystalline axis (Dimetian) in Pre-Cambrian times. In
Post-Cambrian times there had been a great fold of Cambrian and
Ordovician rocks over the Pre-Cambrian axis, and immense dislo-
cations of the strata had taken place, especially in the arch-limb of
this fold. On the north-west side of the axis the beds have been
intensely cleaved and sheared, and newer rocks have been thrust
for great distances over older rocks; whilst on the south-east side
they have been inverted and faulted so as to cause the older beds to
overlie the newer. On this side the rocks are much less cleaved
and sheared, and the overthrusts are of less magnitude. Faults were
referred to in the fossiliferous strata showing displacements of from
500 to 12,000 feet. A great anticlinal arch bent over a core of
Archean rocks, and broken into a succession of sheared surfaces,
could alone furnish any satisfactory explanation of these conditions.

The Pebidians themselves, both the volcanic and sedimentary
portions, had also been sheared. Whatever might be the relations
in other areas, here there was an immense unconformity. Where
could all these pebbles have come from ? He referred to the existence
of large pebbles of various rocks in the conglomerates in different
areas, and maintained that the Pebidian had been folded, altered,
and cleaved before a stone of the Cambrian had been deposited.

As regards the Dimetian, he was not surprised at the difficulty
the Author found in mapping it. He himself now admitted that
the rock was originally, like the massive Archean gneisses, of
igneous origin. It was of Pre-Cambrian age; but he thought it had
been too much crushed to assume a gneissic character. ‘The pebbles
at Chanter’s Seat were undoubtedly fragments of Dimetian.

Prof. Braxe thought the views of the two disputants were not so
far removed in matters of fact; both agreed that there was a well-
marked overlap or unconformity. In so far as details were concerned,
he could verify the sections given: by Prof. Morgan. The main
question is the importance to be assigned to the unconformity. He
formerly thought it very great; but later work in Caernarvonshire,
and still more recently in Shropshire, had shown that there was a
voleanic series more satisfactorily classed with the Cambrian than
with the underlying series, and of this the St. Davids rocks might
possibly be the equivalents.

Prof. Hucurs regretted the absence of the Director-General, as
the paper seemed to be chiefly a re-opening of the old controversy in
which he had ably expounded the same view as that now put
forward. The paper secondly suggested corrections of details in the .
interpretation of the structure of the district, which, though valuable,
were not of great importance in the general question.

He would have been glad if the six-inch maps on which the
Author had drawn his lines had been produced, if only to be sure
that they were speaking of exactly the same sections.

He gave diagrammatic illustrations of his own view that the
Cambrian was unconformably trangressive across the Archean, and
that the constituents of the conglomerate varied according to the

VOLCANIC SERIES OF ST. DAVIDS. 269

various parts of the Archean from which they were derived, though
that might not be the immediately underlying part, as he had long
ago pointed out in the case of the North-Wales sections.

Appealing to particular sections he explained the proofs, from the
fluting and crushing of the rocks, &c., that the junction seen at
Porth Clais was afault; but at Ogof Golchfa evidence of the original
unconformable junction could still be made out, though the Cambrian
was much crushed and shifted by the coming together of beds of
unequal texture, and the purple ash-like schist on which it rested
was squeezed out during earth-movements by being in contact with
the unyielding conglomerate. There seemed to be here, as at Nun’s
Well, signs of long and deep oxidation of the rock on which the
Basement Beds of the Cambrian rested. At Ogof Llesugn he thought
that an unconformable junction could be seen, though it was tra-
versed by numerous step-faults, so that much depended upon the
position of the observer when drawing the section; while the sup-
posed passage or intercalations in the cliff-section close by he con-
sidered to be only a passage between the gneissic and porcellaneous
felspathic rock, with local changes due to crush and consequent later
alteration, the Cambrian conglomerate being quite distinct, and the
supposed alternation of Cambrian and Archzean only an included
fragment or “horse” of conglomerate caught in a fault and cut
back by denudation.

Mr. H. W. Witttams failed to recognize some of the Author’s
sections, although well acquainted with the locality.

The AvrHor said that the main point between himself and
Dr. Hicks was as to the relations of the conglomerate to the under-
lying Pebidian. He hoped to go over the ground some day with
him and Mr. Williams. He had not worked the section in patches,
but had traced it continuously throughout the whole district. He
had listened with admiration to all that Dr. Hicks had said about
the enormous faulting of the fossiliferous Cambrian, but failed to
see how it bore on the subject. To please Prof. Hughes he was
ready to admit any number of faults, and he also agreed with
Dr. Hicks as to shearage. He was glad to find that Prof. Blake
practically agreed with him as to the relations of Pebidian to
Cambrian. He was well acquainted with the existence of step-
faults, and thought that Prof. Hughes had misunderstood his
meaning ; the overlap of 4 mile was due to step-faulting. He
maintained that his reading of the Ogof Golchfa section was correct,
and spoke of the bevelling-off of the edges of the beds.

The evidence of Carn-ar-wig neither Dr. Hicks nor Prof. Hughes
had touched. It was perfectly clear that “tuffy”’ ash and lavas
might be seen overlying the conglomerate. He submitted a map,
which was on the table; but in a volcanic region it was not easy
to map systematically, since this was not a regular series of beds as
maintained by some.

270 MR. E. WETHERED ON THE OCCURRENCE OF

15. On the Occurrence of the Genus GIRvANELLA in Ooxrric Rocks,
and REMARKS on Ooxitic Structure. By Epwarp WerHernp,
Esq., F.G.8., F.C.S., F.R.M.S. (Read December 18, 1889.)

| Puare XI.]

I, lyrropucrion.

In January 1888 1 commenced a systematic examination of the
oolitic rocks in the Carboniferous and Jurassic series. The subject
was, of course, by no means new, but I was under the impression that
there had been no systematic investigation of the structure of those
rocks, though many authors had referred to the subject. My
attention was subsequently called to Dr. Sorby’s illustrated appendix
to his Presidential Address to this Society, 1879, and I found that
much of the work I contemplated was already done. I had, however,
atan early stage of the work, discovered that the little-known genus
Girvanella was of frequent occurrence in oolitic rocks, which appears
to have escaped the notice of Dr. Sorby. My work then resolved
itself into a search for that organism ; but, as I] had to make over 230
thin slides for microscopic examination, I have been able to work
out the structure of the rocks in greater detail than Dr. Sorby has
done, and J trust that an account of the observations deduced from
those slides may prove a worthy supplement to his work.

The Genus Grrvanetia, Mich. § Etheridge, jun.

This apparently insignificant organism was first noticed by Prof.
H. Alleyne Nicholson and Mr. Robert Etheridge, jun., in their
‘Monograph of the Silurian Fossils of the Girvan District in Ayrshire’
(Part I., 1878), and was described as consisting of ‘‘ Microscopic
tubuli with arenaceous or calcareous (?) walls, flexuous or contorted,
circular in section, forming loosely compacted masses. The tubes
apparently simple cylinders, without perforation in their sides, and
destitute of internal partitions or other structures of similar kind”
(p. 23). The one species established was G. problematica, which
name was given for convenience’ sake *.

In the Geol. Magazine for 1889 +, I have shown that Girvanella
is not confined to the Silurian rocks, and that as a rock-forming
organism it is of more importance than was supposed. In that
communication I established a new species, G'. pisolitica, which
forms the Pea-Grit spherules near the base of the Inferior Oolite in
the northern Cotteswold area of Gloucestershire. I also showed
that a much smaller form built up the pisolite spherules which occur
in the Coralline Oolite near Weymouth; but I did not see my
way to establish a third species. Since then I have obtained in-

* See also Geol. Mag. 1888, pp. 22-24.
t Dee. iii. vol. vi. p. 196.

: Quart.Journ.Geol.Soc. Vol. XLVI. PL XI.
;
{
4
f
i

Mintern Bros. del et litb

Geol Soc Vol

rn

Quart

+f
oo

GIRVANELLA IN OOLITIC ROCKS. ark

formation which I think will justify me in drawing a distinction
between the Coralline-Oolite form and G. problematica, to which I
temporarily referred it.

Il. Tur Carponrrerous Oorrric LIMEstroneEs.

In the Carboniferous Limestone of Gloucestershire oolitic lime-
stone is more common than is generally supposed. Taking the gorge
of the Avon as the typical section, I find oolitic limestone to occur
at four horizons in the middle series. It is also worthy of remark
that in three instances out of the four the oolitic limestones rest on
dolomitized limestone.

1. The first development of oolite occurs at the base of the
Middle Limestones, and the So rane analysis shows the beds to be
dolomitized :—

mete TERING. |. ccc ee we 1°40
Pe OIC Mapet eee ks. kk ee ee 6°20
OL LTD STE NA 15°56
yal 20) MeO Sanna be Vice rrr 32°36
DELO EG (ae Oy AR rr 42°78
Oxides of iron and alumina .....:.... 1:10
REED (OCR. Merete. Succeed ele. 6 Soke oe -60

100-00

2. About 100 feet of oolite follow above the dolomitized limestone,
consisting of well-defined spherules of dark colour and granular
erystalline structure. ‘These stand out in relief against the clear
calcite which occupies the space between the spherules, and average
about *6 millim., but occur as small as-l muillim. in diameter. In
some the main axis has been extended and a spheroidal form has
been developed, which is usually larger than the others. In some
spherules the crystalline radiate feature is seen, but the concentric
arrangement can always be distinguished. In most instances the
original nature of the nucleus cannot be determined, it having passed
into calcite. When a nucleus is preserved in its original form
it is usually a Foraminifer in the spheres, and in the spheroids a
spicular object which could not be definitely distinguished, pro-
bably a portion of a small spine.

3. The next development of oolitic limestone is in what is known
as the Great Quarry, and, like that previously mentioned, it rests on
dolomitized limestone, as the following analysis of the beds shows :—

MMISOINDIE-PERIGME Ty fi. cick ek ed AL 2:70
ING TAD EGRE i. lsacd ies Wee he Haley 6 5°20
RUA M scr uls a pais sev Mls bla Be Wadd 11°86
Perr e MRR RGA eid ai bla hd a dvedd ARETE 49-48
REO ME GLC bys, ig odes aha a Gs. Weg gta 37°40
Oxides of iron and alumina .......... trace.
PAM PRIOOGH IE sc kta ak calle OE eRe 36

100-00

272 MR. E, WETHERED ON THE OCCURRENCE OF

This analysis shows that the amount of magnesia present is less
than in the previous analysis. This is accounted for by numerous
minute veins of calcite which traverse the rock. ‘These are clearly
of secondary origin, and in an analysis would, of course, increase
the percentage of carbonate of lime. The oolitic spherules are
very similar to those which I have described from the base of the
middle series. ‘hey average about ‘52 millim., and are therefore
slightly smaller than those previously described. No sign of Gir-
vanella was discovered in these beds.

4, The next limestone which shows oolitic structure occurs a
short distance below where the New Road from Clifton joins the
road along the banks of the River Avon, and for convenience I will
call it the ‘‘ New-Road Oolite.” The beds differ from those pre-
viously noticed; they do not rest on dolomitized limestone, and are
not so crystalline. The following section shows the character of the

beds :—
Section of the New-Road Oolite.

ft.
1. Oolitic limestone, with corals at the top .......ss.s-+0. os 10 0
2. Dark nodular limestone with argillaceous material ...... 0.2
3. Blue limestone with some oolitic spherules ............... a 6
4, Oolitic limestone) <...cca-aes<neteeintiateewckinea<c geet seen eee 3, 16
5. Grey limestone; oolitic in part ........ ReneS SABE seein 2 tS
6. Base, Coralline Limestone.

Commencing an examination from the top, the sections were
made from specimens collected throughout the 10 feet of rock. The
oolitic spherules are slightly ferruginous, and some of them are as
large as 1 millim. in diameter, and the average may be put at about
‘8 millim. In some the nucleus is well preserved and consists of a
Foraminifer, a joint of a Crinoid, a portion of a spine, or a fragment
of shell. The nucleus is surrounded by a concentric arrangement,
but the crystalline radiate feature is only slightly developed in a
few instances. ;

A form of Girvanella was here discovered to which I propose to
give the name of Girvanella Duc, for reasons to be presently ex-
plained. It consists of an aggregation of tubules similar to those
represented in Pl. XI. figs. 2 a and 6; but in this instance the out-
lines are to a large extent obliterated by mineral changes ; the centre
of the granule has been converted into calcite, and the concentric
arrangement now presents a dark granular crystalline structure.
Throughout the whole of this the tubules of Girvanella Duc can
be seen. The concentric arrangement is similar to that of the
other granules or spherules in the slide, and I have given it very
careful examination with the object of determining whether it
is of organic or of inorganic origin. _ Seeing it for the first time, an
observer would be disposed to pronounce in favour of the latter view:
but after the study I have made of the structure of oolitic spherules
I am disposed to regard it as organic. The apparent concentric
layers may be a series of tubuli, the outlines of which have become
obliterated by mineralization. That some of the spherules in the

GIRVANELLA IN OOLITIC ROCKS, 275

limestone originate from the Girvanella-tubuli there is proof, but
in these the structure, though it can be made out, is almost obli-
terated.

Bed No. 2 consists. of dark nodular limestone and argillaceous mate-
rial. The sections ot the former show it to be extensively crytalline,
the calcite being slightly tinged withiron-oxide. Scattered here and
there are some Foraminifera; but the most conspicuous feature is
formed by some oolitic spherules which measure as much as 3 millim.
in diameter (fig. la). Viewed in a thin section of the rock, these are
seen to be masses of tubuli (fig. 16), measuring only -01 millim.
in diameter, forming a crust around a nucleus. This nucleus is
usually calcite, and probably represents some foreign object which
served as a nucleus to which the organisms attached themselves, and
which has changed into calcite. I propose to distinguish this species
by the name of Girvanella incrustans.

Bed No. 3 is a blue limestone largely made up of Foraminifera,
associated with oolitic spherules. In this bed we again meet with
the organism I propose to call Girvanella Ducii, occurring in loose
aggregations, as represented in fig. 2a. It is aiso found surround-
ing foreign objects, as in fig. 2 6, in which case an oolitic granule is
made up. In fig. 26 there may be said to be three nuclei, which
serve as centres of growth. With the largest of these the very
interesting question is again raised as to whether the concentric
arrangement around the nucleus is of organic or inorganic origin.
The original structure is, doubtless, much obliterated; but the
outlines of tubes can be seen, and I am therefore disposed to regard
it as organic. G, Ducw may be said to be numerous in this bed,
sometimes in loose aggregations of tubules, at other times growing
round some foreign object.

Bed No. 4 consists of an oolitic limestone in which the spherules
are unusually dark in colour. In my slides, made from this bed, I
obtained one specimen of a loose aggregation of G. Ducit, in which
the tests were for the most part well preserved.

The next development of oolitic limestone occurs just above what
is known as the “ Great Fault,” where the Millstone-Grit is thrown
down against the Middle Limestone. ‘These oolites rest on dolomi-
tized limestone, and are like the others previously referred to, which
rest on a like basis. That is to say, the nuclei of the spherules are
seldom preserved, and the concentric arrangement is highly crys-
talline. The radiate crystalline structure is prominent and at times
develops what Dr. Sorby calls the “fan-shaped arrangement of the
small prisms of calcite” *.

The following analysis of beds on which the oolite rests shows
them to be dolomitized :—

a

* Presidential Address, Quart. Journ. Geol. Soe. p, 71, plate x, fig. 1

(1879)

Q74 MR. E. WETHERED ON THE OCCURRENCE OF

Insoluble: residue: : <0 Wik aaa ota ee 3°10
Organie qathen |... % oss 44 tbineaeueeee 3°60
IND ING o),, Seas OA a eee eens ee cee 12-10
ATES 1 Ali ce iss. Shape Bie eal tie oii oe 42°25
Carbonie@eid: 2a. x Seat eee ee ee 38°80
Oxide of iron and ‘alumina. Si. 94. Yee trace.
Alicalites, &e. +2 <x dis taatatevss eae ee 15

100-00

I have also found a good specimen of Girvanella Ducii (fig. 2c) in
oolitic limestone at Tortworth Park, Gloucestershire, the residence
of the Right Hon. the Earl of Ducie. The horizon corresponds
with the Clifton oolite at the base of the Middle Limestones; but
at Tortworth the beds are not so crystalline. As to whether or
not the beds rest on dolomitized limestone could not be ascertained,
as the strata at the base were not exposed. This specimen of
G. Ducit was the first I discovered in Carboniferous rocks, and I
dedicate the species to his Lordship.

In this specimen the central tubuli are surrounded by a radiate
and in part concentric arrangement, which also characterizes some
of the other spherules in the rock; and in this there are the out-
lines of undoubted tubes, which seem to point to the structure being
of organic origin.

So far, then, I have discovered two species of the genus Girvanella
in the Carboniferous Limestone, and these only in rocks of oolitic
structure.

It may at first appear strange that Girvanella has not been
discovered in oolite resting on dolomitized limestone, and a
connexion between the latter and the oolite may be suggested. I
was at first disposed to believe that this was so, but the absence of
dolomitized limestone at the base of the New-Road Oolite dispelled
that idea. It is, however, noticeable that in the Forest of Dean
there is a thick series of oolitic beds, and these also rest on dolo-
mitized limestone. The only connexion between the two types of
rock appear to me to be that both are highly crystalline ; and it may
be due to this fact that we find no reliable signs of Girvanella in
the oolites which rest on dolomitized beds, the structure having been
obliterated in the process of crystallization.

Tur Jurassic OoLrres.

All the specimens I have examined frem the Jurassic rocks were
collected in Gloucestershire or in the neighbourhood of Bath.

Commencing at the base of the Inferior Oolite in the northern
Cotteswold area, we find coarse oolites of the Pisolitic type, which
series are finally brought to a close by the fine development of large
spherules known as the “ Pea-Grit.” These, as I have already
stated, are not concretions but the organism I have named Girvanella
prsolitica*,

* See my paper in the Geol. Mag. dec. iii. vol. vi. (1889), pp. 196-200,
plate vi. figs. 8-11.

GIRVANELLA IN OOLITIC ROCKS. 275

The organisms attach themselves to a foreign substance which
finally becomes a nucleus in the centre of a mass of Girvanella
tubules, and a spherule results, the exact shape depending upon the
form of the nucleus. I am not sure that I should not be justified in
making a new genus out of some forms which occur in the Pea-
Grit. In some spherules the tubes have the appearance of branching,
a feature which is absent in what may be considered the typical
Girvanella. Professor Nicholson remarks * on what he considers to
be a close comparison between Girvanella and the ‘Challenger’
Foraminifer, Syringammina fragilissima (‘ Challenger’ Reports, vol. ix.
p- 242, woodcut, fig. 9). In describing this organism Dr. Brady
says (loc. cit.) :—‘* Test free; consisting of a rounded mass of
branching, inosculating tubes, radiating from a common centre, and
arranged in more or less distinct concentric tiers or layers, which
are marked by the formation at intervals of a network of lateral
branches.”

Dr. Brady, however, appears to take a different view from that of
Professor Nicholson, for under the head of Hyperammina vagans he
refers to Girvanella problematica; and, after quoting the description
originally given by Professor Nicholson and Mr. Etheridge, jun.,
remarks (op. cit. p.261):—‘“ This description applies in every particular
to such specimens of Hyperamnina vagans as are represented in
figs. 7 and 8; and the specific characters which follow agree equally
well, except in a single point, namely, that the diameter of the tubes
in Girvanella is from ~t,th to gj} th of an inch, whereas those of
the present species range from =j,th to ;4,th of an inch. Some
latitude must be allowed in estimating the characters of a minute
fossil belonging to so very remote an age; but it seems scarcely
worth while to recognize these trifling differences as a basis of generic
distinction.” Now, assuming that the genus Girvanella is rightly
referred to the Foraminifera, some forms which I have included
under the head of Gurvanella pisolitica appear to correspond with
Syringammina fragilissima ; but on the other hand the Carboniferous
forms I have mentioned, and some to be referred to further on, are
allied to Hyperammina vagans. In reference to that organism Dr.
Brady further remarks (loc. cit. p. 260) that it occurs ‘‘ spreading in
irregular tortuous lines over the surface of shells or stones, or, in the
absence of foreign bodies, growing coiled upon itself in irregular
masses.” The coiling upon itself is also a feature in Girvanell
pisolitica, as shown in fig. 3, where apparently we get the primordial
chamber at A.

Passing now to the beds of the Inferior Oolite which follow the
Pea-Grit series, we come to the Lower Freestones. There is a con-
siderable amount of calcite present, and some of the spherules are
granular, without any concentric or other structure. At Bull
Cross, near Stroud, the beds appear not to have undergone molecular
change to such an extent as at Leckhampton, near Cheltenham ;
and in my prepared section from these beds I have several spherules
showing the structure of G. pisolitica.

* Geol. Mag. dee. iii. vol. v. p. 23 (1888).

276 MR. E. WEITHERED ON THE OCCURRENCE OF

Following the Inferior Oolite in ascending order, we pass from the
Lower Freestones into the Oolite-marl, and above that -we come to
the Upper Freestones. What I have said with regard to the crys-
talline condition of the Lower Freestones also applies to the Upper
Freestones, when taken as a whole; but a striking exception has
been found to this in freshly exposed beds of this freestone near
Chedworth, about eight miles from Cheltenham. In these beds
there are patches of oolite, of blue tint, which is due to the iron in
the rock being in the state of carbonate, the original condition in
which it existed after the formation of the rock. In the yellow
oolite the iron has been converted into ferric oxide. Where the
original carbonate of iron has not been converted into the ferric
condition the oolite-spherules show their original structure better
than is the case where the iron has been converted into ferric oxide,
and in this the Girvanella-tubuli are clearly made out. The tubes
show a somewhat dark exterior; and, when cut in section; the in-
terior is seen to be filled with crystalline calcite or dark argillaceous
material. They are smaller than G‘. prsolitica as it occurs in the
Pea-Grit spherules, but otherwise similar; and I therefore regard
them as a variety of that species. In Pl. XI. fig. 4 I have represented
a spherule in which tubes are clearly distinguished ; but in parts
the outlines have been obliterated by mineral changes, and we then
get the identical structure which is characteristic of most of the
oolitic spherules in the Upper Freestones. There are others which
show a regular crystalline concentric arrangement, and they may
possibly be of concretionary origin; but I am disposed to regard
them as spherules in which the G'rvanella-tubes have become crys-
talline and the outlines consequently obliterated.

Another form of Girvanella has also been met with in the Upper
Freestones. It consists of a dense mass of tubes, measuring -01
millim. in diameter, which form a crust attached to foreign objects
(fig.5). It is very similar to the Carboniferous G. incrustans, and
might perhaps be regarded as identical with that species. For
reasons to be explained under the head of ‘‘ new species,” I think it
best to regard it as a variety, with the name of G*‘. incrustans,
variety Luci, after W. C. Lucy, Esq., the excellent President of the
Cotteswold Naturalists’ Field Club.

I now pass to the upper divisions of the Inferior Oolite. In the
new railway now in course of construction between Cheltenham and
Cirencester some fine exposures of the Olypeus-Plottiw beds are seen.
In these there are large oolitic spherules which measure as much as
4 millim. in diameter, though the average size may be stated at
about half that. In most of these there is no structure except the
dark granular and occasional streaks and circles of calcite, but in
others the Girvanella-tubules are seen. I have therefore no doubt
that the spherules in this division of the Inferior Oolite are not
concretions, but due to a variety of Girvanella pisolitica.

GIRVANELLA IN OOLITIC ROCKS, O77

THE GREAT OoLiTE.

1. The Stonesfield Slate——Specimens were collected from Eyford
in Gloucestershire, on the eastern side of the Cotteswold Hills, where
the so-called “ slate” has been worked since the time of the Romans.
Dr. Sorby describes the Stonesfield Slate thus *:—‘“ This is a good
example of a fine-grained shell-sand with small grains of quartz.
Most of the fragments are of Brachiopods and Oysters, which are of
flat shape, and thus cause the rock to split easily along the plane of
bedding.” I find this description to apply only to the “‘ Base Bed ”
at Eyford (7. ¢. the lowest which rests on the Fuller’s Karth) and not
to those above. The beds which give the “best slate” are made up
of broken valves of Ostracoda, a few Foraminifera, and a quantity of
undetermined material, which, whatever it may be, does not consist of
fragmentary remains of Brachiopod and Oyster-shells. There is a large
amount of insoluble residue, which includes detrital quartz, zircon,
tourmaline, rutile, and microcline. No oolitic structure was observed
in these beds, nor any sign of Gurvanella.

2. The Bath Oolite—Of this rock it is most difficult to prepare
sections for microscopic examination on account of its softness and
the slight cohesion of the oolitic spherules with the crystalline matrix.
My specimens were collected from Coombe Down, near Bath, and
Cross Hands, in Gloucestershire.

The specimens from Coombe Down show a highly crystalline lime-
stone, and consequently a large percentage of calcite. The oolitic
spherules were so crystalline that in some cases the concentric
structure had disappeared. All the specimens show fragments of
shells, and in some cases Foraminifera are met with. The specimen |
from Cross Hands: showed the same crystalline condition as those
from near Bath, and only a few of the spherules were preserved,
most having been detached during the process of preparing the slide.
No reliable evidence could be obtained as to their origin.

3. Horest-Marble.—The specimens were collected from Langton
Herring, near Weymouth, and from a boring at Swindon, Wiltshire.
In both cases the limestone partook of the Bath-oolite character,
butit is more shelly, and oolitic spherules are not so numerous.
Like the former, too, the spherules are so crystalline that little can
be said as to their origin.

Passing over the intermediate formations, I take next the Coralline
Oolite. All my specimens were collected from near Weymouth, and
reference has already been made to my communication to the
‘Geological Magazine,’ in which I have shown that the pisolite
spherules in the Oolite near Weymouth and at Sturminster Newton
are not concretions but a minute form of Girvanella tT.

I find that preparations of this rock for microscopic examination
are seen to most advantage when not covered with Canada balsam,
It is best to simply polish the surface of the thin sections, and then

* Presidential Address, Quart. Journ. Geol. Soc. p 53, and Appendix, p. 70,
plate vil. fig. 1 (1879).
t Geol. Mag. dee. iii. vol. vi. p. 196.

278 MR. E. WETHERED ON THE OCCURRENCE OF

the structure can be easily made out. It is probably owing to the
fact that slides are generally covered with balsam that the structures
I am about to describe have not before been detected. I have
myself rendered many of my slides almost useless by reason of the
high refractive power of Canada balsam.

The best examples of oolitic structure are to be found in the
“ Osmington Oolite” of Blake and Hudleston*; but there may be
said to be several types of oolitic spherules in the Coralline Oolite.
1. A spherule with a minute loosely aggregated form of Girvanella
tubules as a nucleus, which are surrounded by an irregular sort of
concentric arrangement(Pl. XI. fig.6a). 2. The same form of minute
Girvanella occurs in loose aggregations or surrounding foreign
objects (fig. 6 6); in these instances forming granules or spherules.
3. A spherule or granule made up of a mass of loosely-aggregated
very vermiform tubuli which are larger than the last (fig. 7).
4. A spherule or granule in which the nucleus generally consists
simply of calcite, and the concentric arrangement has a granular
crystalline appearance, in which occasional outlines of tubuli may
be seen. In short, we get in these spherules the same appearance
that we see in those obtained from the Upper Freestones and
Olypeus-Plottic beds of the Inferior Oolite, which I have represented
in fig. 4. 5. A spherule with a clear and well-defined concentric
arrangement around a nucleus (fig. 8).

With regard to the first of the above spherules or granules, in
which the Girvanella-tubules occur in the centre (fig. 6a), I regard
the tubes simply as the nucleus, and the concentric structure as
foreign to the nucleus. That this is so, is proved by the fact that

Girvanella-tubules of the same form are met with apart from the

concentric arrangement (fig. 6, 6). It is then a question whether
the concentric structure is of concretionary origin or a form of
Girvanella. A casual observer would probably either give no
opinion at all, or decide in favour of the concretionary origin.
A careful examination, however, of other spherules in the slides
shows that they exhibit the same structure; and in some there
are unmistakable outlines of tubules. I am therefore obliged to
come to the conclusion that the structure is organic, and the same
may be said of other spherules in the slides which show similar
structure.

With regard to the class of spherules which I have mentioned
under the head of 3, they are simply an aggregation of a species of
Girvanella, which I propose to call G. intermedia. Spherules of this
type are fairly numerous in the bed of Coralline Oolite from which
the slides were taken, and which occurs on the sea-shore at Wyke,
near Weymouth. Ihave not found the tests of this species attached
to foreign objects.

Spherules of the type represented by fig. 8, are quite different from
those before described. They are more truly crystalline, and the
granular crystalline feature is absent. Also the structure around

* Quart. Journ. Geol. Soc. vol. xxiii, p. 265.

GIRVANELLA IN OOLITIC ROCKS. 279
Fd

the nucleus is perfectly concentric. Viewed through a microscope,
spherules .of this type would be regarded, at all events at first
sight, as of concretionary origin, and I am not prepared to say that
such may not be the true interpretation. When photographed,
however, what under the microscope are very obscure dark spots
appear like the extremities of tubes which have been cut across.
These objects occur throughout the concentric layers at short inter-
vals; and it is impossible to resist the idea that the apparent
concentric layers may really be layers of tubuli which were filled
with dark material, and the walls of which have become crystalline.

PortLanpd OoLite.

The beds of the Portland Oolite vary considerably in microscopical
structure. I therefore found it necessary to take a section of a
quarry and examine each bed separately.

Section of the Portland Oolite.
Imosthay Quarry, Portland.
Beds in descending order.

if... int,
MRPA EOD au sse. is oceccacecsoases 2 6 Full of the casts of Cerithium
portlandicum, Trigonia gibbosa.
Chert at the top contains mi-
nute shells.

< (Portland Building-stone ...... 6 QO Fine-grained limestone. Termi-
a | nates in a layer of chert.
+2 4 Portland Stone withnumerous 3 0 Inferior stone on account of lia-
us cracks. bility to split.
= | portion Stone with Chert ... 3 6 Chert nodules most numerous at
the bottom.
PE VOAGH eis cvesesscesessdae 3 O Mass of casts of shells: Zrigonia
incurva(2), Ammonites giganteus,
Cerithium portlandicum.
cc acncce-ccecatnntecses 3 0

Commencing at the ‘“ Base Bed,” we find the rock made up
entirely of dark oolitic spherules, which have been much altered by
erystallization, and nothing can be said as to the original structure.

Curf Roach Bed,—Contains some rather large crystalline oolitic
spherules, numerous granular nodules, and organic detrital material.
The spaces between are filled with small crystals of calcite and a
quantity of dark granular structure, which indicates altered organic
calcareous remains.

Whit Bed.—The last, or top bed, is a mass of small crystalline
organic fragments, with a few oolitic spherules. Dr. Sorby’s*
description and figure of the Portland Stone is not typical of the
Portland Stone of commerce, namely the ‘ Whit Bed,” as it occurs
in the above quarry.

* Presidential Address, p. 50, and Appendix, p. 70, pl. iv. (1879).
GQ. J. G. 8. No, 182. U

280 MR. E. \VETHERED ON THE OCCURRENCE OF

Roach Bed.—A mass of shell-débris ; the structure is often well
preserved in the fragments ; no oolitic spherules appeared.

In none of the slides from the Portland Beds was Girvanella des
tected. As to the origin of their oolitic spherules, it is impossible
to express any positive opinion, on account of the alteration they
have undergone by crystallization.

The New Species.

To make distinctions between organisms such as the Girvanelle
is a task of considerable difficulty, but to do so is a matter of
necessity.

I. Girvanella incrustans, Pl. XI. figs. 1 a, 6.—Occurs only in the
Carboniferous Limestone at Clifton, in spherules as large as 3 millim.
in diameter. When cut in section, the organism is seen to consist
of a dense crust of very tortuous minute tubuli, which measure
‘01 millim. in diameter. They are arranged in rude layers, formed
around a centre, which is usually represented by calcite into which
the original nucleus has probably been converted.

Girvanella inerustans, variety Luci (fig. 3), 1s very similar to
G. incrustans ; but so far I have not found the tubuli to occur in
layers, but as an irregular mass incrusting foreign objects. I have
found G. incrustans only as spherules; but the variety Luci, as
represented in the figure, is not a spherule. The differences between
the two varieties are slight ; but as one occurs in the Carboniferous
Limestone and the other in the Inferior Oolite, I think it better to
give the varietal name of Luci to the latter.

Il. Girvanella Ducii, Pl. XI. figs. 2 a, 6, c—This species is confined
to the Carboniferous Limestone, and has been found at Clifton and
Tortworth Park in Gloucestershire. The test consists of a tortuous
tube, with clearly defined walls of dark granular structure, and
measuring ‘02 millim. in diameter. In some-instances the tubes.
occur in irregular loose agg regations, at other times adhering to
foreign objects, as represented in fig. 2b, when a small nodule or
eranule results. In some instances G. "‘Ducii assumes a more or
less spherical form, and the inner tubes are surrounded by a con-
centric structure. Whether in this case the central tubes are
nuclei and the concentric arrangement concretionary or organic
is doubtful, and worthy of consideration by future observers. I
have not as yet been successful in discovering a primordial chamber ;
but, seeing that in the living Foraminifer Hyperammina vagans,
which G. Ducii resembles, the primordial chamber is “almost inya-
riably wauting”*, it is not surprising that, in the fossil state, it
should be still less easily detected.

Ill. Girvanella minuta, Pl. XI. figs. 6 a, b.—The test consists of a
short minute tube, which measures ‘007 millim. in diameter. These
tubes are enclosed by a thin dark granular wall, and occur in the
centre of oolitic spherules (fig. 6 a), or in aggregations or around
some foreign object (fig. 6 5).

* ‘Challenger’ Report, Zoology, vol. ix. p. 260.

eG:

GIRVANELLA IN OOLITIC ROCKS. 281

IV. Girvanella intermedia, Pl. XI. fig. 7.—The test consists of a
vermiform tortuous tube, which grows in nodular masses. The tubes
measure ‘01 millim. in diameter, and have well-defined thin walls.
I have not as yet found this form adherent.

In concluding this paper I should lke to say, first, that it has
been my object to produce evidence that oolitic structure is not
always of concretionary origin. .That it is all organic I am not pre-
pared to maintain, but it may be. |

DESCRIPTION OF PLATE XI.

Fig. 1a. Spherule of Girvanella incrustans; X 28 diam. Seen in section.
From the ‘‘ New-Road Oolite,” Middle Carboniferous Limestone,
Clifton.

Fig. 1. Portion of fig. ia; x 70diam. Showing the tubules of Girvanella
inmcrustans.

Fig. 2a. Girvanella Ducti occurring as an aggregation; x 70 diam. “ New-
Road Oolite,’ Middle Carboniferous Limestone, Clifton.

Fig. 26. The tubules of Girvanella Ducit attached to foreign objects, which
act as nuclei for the formation of an oolitic granule or spherule.
x 52 diam.

Fig. 2c. The tubules of Girvanella Ducii in the centre of an oolitic granule,
and surrounded by a radiate and concentric structure of doubtful
origin, but probably organic. X 68 diam.

Fig. 8. Girvanella pisolitica, coiling upon itself, with what is suggestive of the
primordial chamber at A.

Fig. 4. Portion of an oolitic spherule from the Upper Freestones of the
Inferior Oolite, from near Chedworth. The spherule is passing
into the granular-crystalline condition. > 50 diama.

Fig. 5. Girvanella incrustans, variety Lucii, attached to a foreign object. From
the same beds as fig. 4. > 70 diam.

Fig. 6 a. An oolitic spherule from the Coralline Oolite at Radcliff Point, near
Weymouth, with the tests of Girvanella minuta in the centre,
surrounded by a concentric arrangement of doubtful origin, but
probably organic. x 70 diam.

Fig.6b. Girvanella minuta, attached to a foreign object, which has been con-
verted into calcite. The latter acts as a nucleus, and an oolitic
granule results. On the left-hand side, and on the outer edge of
the right, the tubuli have passed into the granular crystalline con-
dition. x 70 diam. From the Coralline Oolite, Wyke, near
Weymouth. Only a portion of the granule is represented.

Fig. 7. Girvanella intermedia forming an oolitic spherule. Coralline Oolite,
Wyke, shore near Weymouth. X 70 diam. Around the edge of
the granule the tubules have passed into the granular crystalline
condition.

Fig. 8. A crystalline oolitic spherule, showing perfect concentric arrangement
around a nucleus which has become converted into calcite,
Coralline Oolite, Radcliff Pot, near Weymouth. x 70 diam.

[Most of the figures are represented imbedded in the limestone. |

Discussion.

The Prestrpenr remarked on the importance of investigating the
question whether these appearances are organic or not. We should
take warning from Hozoon as to possible differences of opinion in the

v2

282 MR. E. WETHERED ON THE OCCURRENCE OF

interpretation of tubular structure, though these mystifying appear-
ances seem more common in serpentine and chalcedony than in cal-
cite. In the bodies depicted, the wall, the irregularity, and the
manner in which the tubes curve round each other are in favour of
their being organic.

Prof. Ruprrr Jones thought that these forms were not due to
mineral, but to organic laws. The surrounding enallostegian lines
looked like tubuli (he was not prepared to ignore those of Hozoon),
quite analogous to those mentioned by the Author, and perhaps to
those of the small knots of Serpule in the Chalk; but whether the
latter are continuous or not, is doubtful. As to difference in the
size of the tubules there was not much in that. He referred to the
views of Schafhiutl, who had given distinct names to oolitic granules
from the Alps of South Bavaria. -He suggested that some markings
in flint had been due to thread-like Foraminifera in the chalk.
He congratulated the Author on his successful research ; also on
his not claiming that all oolitic granules were derived from this one
source.

Dr. Evans, while disclaiming any special knowledge of the subject,
suggested that the appearances might be interpreted on the supposition
of an organism boring into a comparatively hard substance. He also
referred to other difficulties in the way of the Author’s interpreta-
tion, though there could be little doubt as to the organic nature of
the structures.

Dr. Htypz, who had seen most of the known species of Garvanella,
spoke of the wide distribution of these organisms. Dr, Bornemann
had found them forming a bed of rock of Cambrian age in Sardinia,
and he referred them to calcareous alge ; Prof. Nicholson originally
noted their occurrence in the Ordovician rocks of Ayrshire ; and he ~
(the speaker) had found them in limestones of similar age in the
Province of Quebec. They are undoubtedly organic ; the tubes have
definite imperforate walls of granular calcite, distinct both from the
matrix and from the calcite infillingthem, and they could not therefore
be mere borings. The ‘Challenger’ Foraminifera, with which they
were compared by Dr. Brady, are considerably larger and are also
built up of arenaceous grains. G'irvanella had been erroneously
described as a Calcisponge, and compared to knots of Serpule, but
we can hardly conceive that worms inhabited such small tubes.

Dr. Hicxs referred to the walls of borings, in the Cambrian and
Silurian rocks, giving an appearance of being distinct from having
been lined with calcite.

Prof. Bonney felt sure the specimens had no place in the mineral
kingdom, and organic fragments were common in them, for there
had been no creat degree of molecular change in these beds. What
organism the Girvanella might be he would not venture to say.

Prof. Jupp referred to the oolitic grains from the coral-reefs of
the Bahamas, which had been described by De la Beche and Sorby.
The study of these recent oolitic grains might be expected to lead to
important results. He had found in them structures similar to
those described by Mr. Wethered, but the structures are finer even

GIRVANELLA IN OOLITIC ROCKS. 283

than that of Girvanella incrustans; the tubuli also anastomose
greatly : the little tubuli are sometimes filled with calcite, at other
times with calcareous mud.

Rey. H. H. Winwoop congratulated the Author and the West of
Hngland on this piece of work. Stoddart, after examination, had
failed to discover any organisms. He referred to Mr. Wethered’s
happy knack of discovery.

The Avrnor said that he prepared his own slides, and that in
some cases it was a mistake to mount them in Canada balsam, as
its high refractive power obliterated the structure. Possibly it was
for this reason that Dr. Hinde had not observed the structure of
Gurvanella to the extent he, the Author, had done in oolitic granules.
Those Fellows who had seen his slides agreed with him that the
Grrvanella-structure was organic, but those who had not seen them
doubted it; clearly those who had seen the slides were the best
judges. To Dr. Hicks he replied that the walls were not formed
of calcite; quite the contrary, it was only the interior of the
tubules which contained it as an infilling mineral. The discovery
made by Prof. Judd in recent oolite from the Bahamas was most
important; and as the tubules were branching he suggested the
possibility of their being allied to Syringammina fragilissiema.

As to Dr. Evans’s remarks, half an hour’s examination of the
actual slides would convince him that he was mistaken in the
views he had expressed. The Author thanked the Fellows who
had discussed his paper.

284 MR. R. LYDEKKER ON A CROCODILIAN JAW

16. Ona Crocopitran Jaw from the Oxrorpd Cray of PrrerBoroven.

By R. Lyprxxer, Esq., B.A., F.G.S., &. (Read March 12,
1890.)

Tar symphysis of the mandible of a Thecodont Reptile recently
obtained from the Oxford Clay near Peterborough, by Mr. A. N.
Leeds, and entrusted to me for description, affords evidence of a
species new to the English fauna, and apparently belonging to a
genus not hitherto recorded from the Oxfordian.

The specimen, which is represented of one third of the natural size in
the diagram (fig. 2), belonged to a comparatively large reptile, and
comprises the anterior portion of the splenial and dentary elements ;
that part of the dentary which still remains including the whole of
the alveolar region. The symphysial portion of the jaw is very
broad and flat, with a rugose inferior surface; but the original flat-
ness has been abnormally. increased by pressure, which has crushed
the oral floor into the dental alveoli, and has thus destroyed the
original circular contour of the latter. The splenials enter exten-
sively into the formation of the symphysis, reaching as far forward
as the seventh tooth on the left side. No traces of teeth remain,
and the empty dental alveoli are thirteen in number on the left, and
twelve on the right side. The alveoli, in their original condition,
must have been nearly circular; and none of them are markedly
enlarged, or separated from one another by spaces in the neighbour-
hood of the muzzle. On the inferior aspect the dentaries and
splenials are completely anchylosed together, this feature, taken
together with the rugose surface of the bones themselves, indicating
that the specimen belonged to a fully adult animal. The length of
the symphysis on the oral aspect is close upon 8 inches, while the
length of the alveolar portion of the dentary is some 9 inches.

The thecodont character of this jaw indicates that its owner be-
longed either to the Sauropterygia or the Crocodilia, and it is neces-
sary, in the first place, to point out why I refer it to the latter Order.
I do not, indeed, know what characters there are by which it is pos-
sible to say at once whether a given thecodont mandible is Sauro-
pterygian or Crocodilian ; and it is therefore necessary to rely upon
empirical means of distinguishing between the two. Now it is
quite clear that the specimen under consideration does not belong
either to Pliosaurus or to Peloneustes; while in the other Sauro-
pterygians of the Oxford Clay, which I have provisionally included
in the genus Cimoliosaurus, the mandibular symphysis is very short,
and the whole jaw very much smaller than in the present specimen.
Compared with Crocodilians, the mandible before us agrees in the
rugose character of its outer surface, and also in the relations of the
splenials to the symphysis; and since, as will be shown below, it
agrees in all essential features with an undoubtedly Crocodilian jaw,
I take it for granted that the specimen really belongs to a Croco-
dilian genus.

FROM THE OXFORD CLAY OF PETERBOROUGH. 285

Figs. 1—-4.—Mandibles and Teeth of Suchodus durobrivensis
and Metriorhynchus Moreli.

1
Ml
eit

Se eS

Fig. 1. Anterior portion of the mandible of Metriorhynchus Moreli; from the
Oxford Olay of Wiltshire. (Brit. Mus. No, 46323.)
2. Anterior portion of the mandible of Suchodus durobrivensis ; from the
Oxford Clay of Peterborough.
3. Outer side of tooth of Suchodus durobrivensis ; from Peterborough.
4. Tooth of Metriorhynchus ; from Willesden. .

286 MR. R. LYDEKKER ON A CROCODILIAN JAW

Compared with the Crocodilians from the Oxford and Kimeridge
Clays described by Deslongchamps, in his ‘ Notes Paléontologiques,’ -
under the names of Stencosaurus and Metriorhynchus, the present
specimen differs, among other features, from all those species of
which the mandible is known, by the smaller number of teeth, this
character alone being quite sufficient to prove its generic distinct-
ness from Stencosaurus. In the mandible of a typical species of
Metriorhynchus, like M. Morelc (Deslongchamps, op. ct. pl. xxil.,
and fig. 1 of the diagram illustrating this paper), there are nineteen
alveoli, of which the first four are larger than the others, and are
separated from one another by considerable intervals, so that the
anterior portion of the mandible is quite unlike the specimen before
us. In M. brachyrhynchus of the Oxford Clay (op. cit. pl. xxiii.)
the number of alveoli in the upper jaw was less than in WW. Moreli ;
but if Deslongchamps is correct in his restoration of the muzzle, the
extremity of the mandible must have been similar to that of /.
Morelt, and in any case the number of lower teeth (judging from
the relative number of upper and lower alveoli in the latter) can
scarcely have been less than fifteen. It may therefore be saiely
considered that the specimen cannot be referred to the genus
Metriorhynchus, and also that it is specifically distinct from all the
forms which have been described under that name.

The genus Teleidosaurus * of the Fuller’s Earth (which in some
respects connects Steneosaurus with Metriorhynchus) makes a deci-
dedly nearer approach to the present specimen, as is shown by the
reduction in the number of the teeth and the great width of the
oral aspect of the skull. In 7. Calvadosi and T. Joberti the num-
ber of lower teeth is, however, 20 or 21; and the anterior alveoli
are spaced, with a very long interval between the 4th and 5th in
T. Joberte.

If, however, our specimen be compared with the large Crocodilian
originally described from the Kimeridgian of France under the name
of Machimosaurus mosey, and to which I have referred + the mandible
and part of the cranium from the equivalent beds of Dorsetshire
figured by Sir R. Owen § as Plhiosaurus trochanterius, we shall find
a marked resemblance between the two. In both specimens the
number of alveoli is very nearly the same, the Kimeridgian one
having 14 on each side ||, and the present one 13 on one side and
12 on the other. In both the splenial extends as far forward
as the seventh alveolus; while the anterior alveoli in both are
not separated from one another by longer intervals. The Oxfordian
mandible is, indeed, rather more pointed at.the extremity of the sym-
physis, and is perhaps more flattened at the symphysis. The total

See Deslongchamps, op. cit. pls. xviii., xix.
See Sauvage & Lienard, Mém. Soc. Géol. France, sér. 3, vol. i. pl. xxiii.
Cat. Foss. Rept. Brit. Mus. pt.i. p. 104.
Reptiles of the Kimeridge Clay (Mon. Pal. Soe. for 1868), pt. 3, pl. iii.
. 3-5.
|| In the British Museum Catalogue it is stated that there are 13 alveoli, but
the anterior one is evidently broken away on either side.

BR emtt > x

fi

—

FROM THE OXFORD CLAY OF PETERBOROUGH. 287

length of the Kimeridgian mandible is 52 inches, the portion of the
symphysis in advance of the extremity of the splenials being one
fifth of the whole length. Calculating the dimensions of the present
mandible on these proportions we should have a total length of
about 25 inches.

The resemblance to the above-mentioned jaw which I have refer-
red to Machimosaurus mose is, indeed, so close, that were it not for
other evidence, I should have been inclined, in spite of its much
smaller dimensions, to regard the present specimen as indicating
another representative of the same genus.

In his collection Mr. Leeds has, however, an imperfect crocodilian
skull from the Oxfordian of Peterborough, which appears, both to him
and to myself, to belong te the same form as the present specimen,
and which certainly cannot be referred to Machimosaurus. The
mandible of that specimen agrees precisely in size with the one
before us, and has a symphysis of just the same length; unfortu-
nately, however, it has been crushed in the opposite direction, that
is to say, the symphysial region has been compressed from side to
side, so as to render comparison of details almost impossible. Ten
alveoli can now be traced in the right ramus, some of which still
retain their teeth; and itis quite probable that there may have
been two or three more. There is no trace of a long interval
between the 4th and 5th alveoli, and I have accordingly little
or no hesitation is regarding this skull as specifically identical with
the detached mandible. The cranium of the second specimen has
the laterally placed orbits characteristic of Metriorhynchus, and it
approximates in contour to the cranium from the Oxfordian of Nor-
mandy, figured by K. Deslongchamps in his‘ Notes Paléontologiques,’
pl. xxii. as Metriorhynchus brachyrhynchus. The English cranium
has, however, a broader muzzle than in the latter, the nasals are
relatively shorter and wider, and do not reach the premaxille, and the
number of teeth was evidently considerably less, although the exact
number cannot be determined. If Deslongchamps is correct in his
restoration of the missing muzzle of M. brachyrhynchus, there must
have been at least 20 upper teeth, while in the present form, cal-
culating from the lower jaw, there were probably only some 15
teeth in the upper jaw. ‘The mandible and teeth of MW. brachy-
rhynchus are unknown, and since the restoration of the muzzle is
conjectural, it is quite possible that it may have differed considerably
in these points from the more typical representatives of the genus, as
it certainly does in the shortening of therostrum. The teeth of the
skull in the Eyebury Collection (diagram, fig. 3) are distinguished
from those of Metriorhynchus (cbid. fig. 4) by their more compressed
and expanded crowns, of which the enamel is nearly smooth, instead
of having the strongly marked vertical stria which are so character-
istic of those of the latter. The teeth of the present form are, indeed,
more like those of Geosawrus (Dacosaurus), although readily distin-
euished by the absence of serrations on the fore-and-aft carine.
These teeth, it may be observed, agree precisely in size with the
alveoli of the figured mandible.

288 CROCODILIAN JAW FROM THE OXFORD CLAY OF PETERBOROUGH.

If, then, I am right in regarding the skull in the Eyebury Collec-
tion and the figured mandible as belonging to one and the same-
species, we have evidence of the existence of a Crocodilian allied in
cranial characters to Metriorhynchus, but with a shorter and wider
skull, furnished with fewer teeth, which have smooth enamel and
compressed crowns like those of Gensante us, While the mandible has
no long interval between the 4th and 5th teeth, and thus approxi-
mates to Machimosawrus. In the width of the palate and mandible
this form also seems to approximate to Teleidosaurus of the Fuller’s
Earth, although the latter is at once distinguished by the greater
number of teeth and the Steneosauroid type of cranium.

The foregoing comparisons indicate that we have to do with a
Crocodilian allied to Metriorhynchus, but certainly distinct from all
named forms with which I am acquainted. The characters pointed
out as distinguishing it from the typical species of Metriorhynchus
seem, moreover, to be sufficiently important to be regarded as of
generic value, when we take into account the distinctions on which
genera are based in the Crocodilian order. JI propose therefore to
regard the figured mandible as the type of a new genus and species
to be named Suchodus durobrivensis, the characters of this genus
being those given above.

I have said that the mandible of Seen differs from that of
Metriorhynchus by the absence of a long interval between the 4th
and 5th teeth, and of a distinct terminal expansion ; and the inter-
alveolar portion is also wider than in the typical forms of the latter
(diagram, fig. 1). When the mandible was in its original shape, it
is, however, probable that the interalveolar portion was raised in
the same manner above the level of the alveoli.

SINOQGOHILNIQAGVT MAN

“YAtL Je ‘Tep -sodg ute puryy

=

ale JO 50g Joon “Utne: 7ren)

ay
n
*
;
.
‘

.
fe
f

ry
a
Aa)
" ' *
® ,
» ’
‘
ms
La +
¥ ‘
‘ -
aime
Di
‘. ~
‘ “
7 '
"4
’
i
<
‘
s
'
. 4
H ei
* ‘
' .,
1 , ,
Wy
\
v
’ '
ye i
"Ee
. iw’
- "
‘
‘
i A
¥ ,
'
'
*
‘
,
-
\! )
‘ '
,
,
% ‘
nan
f
at d A
.
{
-
+ -
, i be
+
. -

ON TWO NEW SPECIES OF LABYRINTHODONTS. 289

17. On two new Srrcrns of Lasyrinrnoponrs. By R. LypexxKer,

Esq., B.A., F.G.8., &. (Read March 12, 1890.)

[Prats XIT.]

A. Mandible from the Carboniferous of Scotland.

Exctustve of the smaller forms like Ophiderpeton, Ceraterpeton, &c.,
the Labyrinthodonts hitherto described from the British Carboniferous
comprise Anthracosaurus, Loxomma, Pholiderpeton, and Pteroplaa.
Of these the type specimen of Anthracosaurus was obtained from
the Coal-Measures (Upper Carboniferous) of Lanarkshire *; while
the types of the second and third genera come from the ironstone of
Gilmerton, near Edinburgh, which is generally considered to repre-
sent the upper part of the English Mountain-Limestone (Lower
Carboniferous). Pteroplax is from the Coal-Measures of Northum-
berland. Several other generic names have, indeed, been applied by
Mr. T. P. Barkasy+ to remains of reputed Labyrinthodonts from
the Coal-Measures of Northumberland; but such of these spe-
cimens as are truly referable to the group in question appear to
belong to Lovwomma and Anthracosaurus. It is important to
observe that a jaw from the Lower Permian (Rothliegendes) of
Bohemia has been referred by Dr. Fritscht to a species of
Loxomma, thus indicating, if the determination be accepted, the
persistence of this generic type from the Lower Carboniferous tu
the Lower Permian. The Northumberland specimens indicate the
occurrence of Lowomma in the Coal-Measures ; while a specimen in
the British Museum leads me to conclude that Anthracosaurus dates
from the Lower Carboniferous of Burdie House.

Of the four genera mentioned above, Pteroplax and Pholidogaster
are represented by species of much smaller size than the others:
and since it is quite evident that they have no affinity with the
specimen I am about to describe, it will be unnecessary to make any
further mention of them.

In Lowomma the teeth are characterized by the large size of the
crowns, which are straight and laterally compressed, with very
prominent fore-and-aft carine, so that they present a striking
resemblance to some types of spear-heads. These teeth have a
highly polished and nearly smooth surface ; and in the lower jaw
their arrangement is very irregular. Further, the outer surface of
the mandible is entirely covered with a net-like sculpture, and the
depth of the ramus is not very great.

In Anthracosaurus, on the other hand, the teeth (as described by
Mr. Atthey) have subcylindrical crowns, without fore-and-aft
carine, and with an oval transverse section at the base, of which the

* See Quart. Journ. Geol. Soc. vol. xix. p. 56, note.
t ‘Coal-Measure Palxontology.’
¢ ‘Fauna der Gaskohle,’ ete. vol. ii. p. 16.

290 MR. R. LYDEKKER ON TWO

larger diameter is placed at right angles to the axis of the jaw. The
mandible is readily distinguished from that of Loxomma by the
slight development of the sculpture on the outer surface, and also
by the great vertical depth of the hinder part of the dentary element,
which causes the inferior border of the ramus to assume a highly
arcuated contour.

Having thus briefly sketched the salient features of the teeth and
mandible of Lowomma and Anthracosaurus, we may proceed to
notice the specimen forming the subject of this part of the present
communication. The specimen in question is a slab of shale,
exhibiting the external aspect of the greater portion of the right
dentary bone of a comparatively large Labyrinthodont from the
Lower Carboniferous of Gilmerton; it is now preserved in the
British (Natural History) Museum, where it bears the register-
number Rh. 310, and was formerly in the collection of the late Karl
of Enniskillen. That this jaw belonged to a Labyrinthodont is at
once evident from the internal structure of the teeth, as shown by
fractured specimens. It is figured on ascale of 2 in Plate XIL. fig. 1.
The portion of the dentary remaining is about 8 inches in length
and contains a number of teeth, some of which are entire, while
others are more or less broken. The jaw is of moderate depth at
the hinder portion of the dentary, and thereby approximates to
Loxomma, from which, however, it is at once distinguished by the
slight development of the external sculpture; so that in this
respect it is more like Anthracosaurus. At the anterior extremity
of the jaw there is the broken base of a large tusk-hke tooth*,
immediately followed by an entire tooth of similar type; then we
have an interval of about an inch and a half, occupied by the
bases of smaller teeth, which are again succeeded by the stumps of
two large tusks. The remainder of the alveolar margin is occupied
by a regular series of small teeth, many of which ure well preserved.
The whole of the teeth have a cylindrical section at the hase, while
their crowns are smooth, with a convex external and a somewhat
flattened inner surface, and there are distinct, although not very
prominent, fore-and-aft carine. Distinct grooves are visible at the
base of each tooth, which tend to become obscure as they approach
the smooth summit; and there is a more or less marked tendency
to a backward curvature of the summit of the crown; while each
tooth has a large pulp-cavity and strongly marked labyrinthic
foldings at the base.

The above description is quite sufficient to indicate that we have
to do with a form which is generically distinct (in the sense in
which generic terms are employed in the Labyrinthodents) both from
Loxomma and Anthracosaurus, and therefore from all British Car-
boniferous representatives of the Order. Among the numerous forms
described by Dr. Fritsch from the Lower Permian of Bohemia, the
genus Macromeriont (or, more correctly, Macromerium), which was
probably allied to Anthracosaurus, presents, however, such a marked

* These broken teeth are not shown in the figured aspect of the specimen.
| Fritsch, ‘ Fauna der Gaskoble,’ ete. vol. ii. pp. 57-41.

NEW SPECIES OF LABYRINTHODON'S. 291

resemblance in dental characters to the specimen under consideration
as to lead to the conclusion that the latter cannot be generically
separated. The teeth of the several Permian species of Macromerium
are described as conical, with the crowns smooth near the summit but
deeply grooved inferiorly, and bearing distinct fore-and-aft carine ;
while they have a well-marked pulp-cavity, and complex labyrinthic
foldings at the base. The figures given by Fritsch, together with a
cast of part of the jaw of the typical M. Schwarzenbergi, now in the
British Museum, show that the outer surface of the teeth was
markedly convex ; while the summits of the crowns were more or
less bent backwards. MW. Schwarzenbergc was a much larger form
than the one under consideration ; but the fragmentary upper jaw
represented in pl. lxvii. fig. 15 of the work cited, under the name of
M. bicolor, has teeth agreeing in size with those of the Gilmerton
jaw. The magnified views of these teeth, given in plate lxx. of the
same volume, show an internal structure which, so far as I can
determine, is very similar to that of the Gilmerton specimen. ‘The
crowns of the upper teeth are, however, more curved baekwards in
M. bicolor ; and if the same condition holds good in the lower jaw,
we shall have a character by which the Carboniferous species can be
readily distinguished from the Permian one, The lower geological
horizon of the Gilmerton jaw is, however, of itself sufficient to
indicate its specific distinctness from VW. bicolor, and I therefore
propose to make that specimen the type of a new species, which I
refer (at least provisionally) to the genus Macromerium, with the
name of J. scoticum. This species may be defined as agreeing in
size with MM. bicolor, but with the crowns of the lower teeth less
recurved than the upper ones of the latter. |

If I am right in the generic reference (and, in any case, the Car-
boniferous form must be closely allied to AMacromerium), we shall
have the same vertical range in the case of Macromerium as is
given by Dr. Fritsch in that of Lowvonma.

B. Mandible and Intercentrum from South Africa.

Among a series of specimens from the Karoo system of South
Africa, presented to the British Museum by Sir R. Owen, is the
greater portion of the right ramus of the mandible of a com-
paratively large Labyrinthodont, together with an intercentrum
which, from its size and mineral condition, appears to have belonged
to the same individual. The precise locality where these specimens
were obtained is unknown; and there is likewise no evidence
to show whether they were derived from the Beaufort or Stormberg
beds of the Karoo system.

The mandibular ramus is in three fragments, which, when put
together, indicate that its entire length was somewhere about
40 centimetres. The portions remaining comprise the entire arti-
cular region and the greater portion of the dentary and associated
elements, together with a fragment of the missing intermediate
portion, The anterior portion of this mandible is represented, from

292 MR. R, LYDEKKER ON TWO

the oral surface, on a reduced scale in Plate XII. fig. 4. The outer
surface of the bone is ornamented with a coarsely reticulate and
ridged sculpture, while the broken teeth show the labyrinthic
internal structure characteristic of the Labyrinthodonts; so that
there is no hesitation in referring the specimen to that group of
Amphibians. The unfigured articular region is fairly well pre-
served, and shows that there was no postarticular process behind
the glenoid cavity—a feature in which this jaw agrees with that of
the North-American genus Hryops and the Kuropean Lowomma. In
the dentary bone the bases of twenty-five teeth now remain, these
bases having an ovoid section, with the longer diameter at right
angles to the axis of the jaw. Externally to this row of teeth
there is a well-marked bony parapet, forming the summit of this
border of the jaw. The most remarkable feature displayed by the
specimen is, however, the presence of a narrow band of about half
an inch in width, situated on the bone of the jaw, immediately on
the inner side of the alveolar area, and covered with a number of
minute knob-like denticles, much resembling in appearance the
so-called ‘ shagreen ” of the Elasmobranchiate fishes. Apparently
this band of denticles stopped short of the symphysial region.
Each denticle presents the appearance of a veritable tooth, having
a distinct pulp-cavity.

The intercentrum, already referred to, is figured of the full
dimensions in Plate XII. figs. 3,4. This bone presents the horse-
shoe-like form characteristic of the “rhachitomous” Labyrintho-
donts, and shows the presence of a distinct facet («) for the articu-
lation of the capitulum of the rib. The absence of ossification in
the axial region of the bone shows that it belongs to a Labyrintho-
dont and not to an Anomodont, since in the latter group the
intercentra always form complete wedges, This is confirmed by the
presence of a rib-facet; since the only known Anomodont with an
intercentral costal articulation is the American genus Hmbolophorus.
I may take this opportunity of mentioning that the evidence
appears to be absolutely conclusive as to the correctness of Prof.
Cope’s identification of the Labyrinthedont intercentrum (hypo-
centrum of Gaudry) with the Anomodont intercentrum, as may be
verified by a comparison of specimens of the vertebral column
of the Labyrinthodont Hryops and the Anomodont HLinbolophorus,
acquired a few years ago by the British Museum.

With regard to the affinities of the form imdicated by these two
specimens, it may be observed, in the first place, that the only
Labyrinthodont hitherto described from the Karoo system, which
can be compared in point of size to the present form is the
imperfect skull described and figured by Sir R. Owen in the
Society’s ‘Journal’* under the name of Lhytidosteus capensis.
Assuming that specimen to be adult, the superior size of the
mandible under consideration would of itself indicate the specific
distinctness of its owner from Lt. capensis. A comparison shows,

* Vol, xl. p. 333, pl. xvii. (1884).

NEW SPECIES OF LABYRINTHODONTS. 293

however, a well-marked generic distinctness in the presence of a
postarticular process to the mandible of the latter. The oral
surface of the mandible of Jthytidosteus is, moreover, characterized
by the absence of the parapet externally to the dental series, which
forms such a marked feature in the present mandible; while, in
place of a band of denticles situated internally to the marginal
teeth, Lhytidosteus has a similar band placed externally to the
latter *. We have, therefore, decisive evidence of the generic
distinctness of the form under consideration from /thytidosteus.

I have hitherto been unable to find among the larger Laby-
rinthodonts any description of a band of denticles situated as in
the figured mandible. In part of a mandible preserved in the
British Museum (No. R. 570, a, 6), from the reputed Permian
of Texas, which appears to belong to Hryops megacephalus of Cope,
there is, however, a precisely similar band of denticles. Now, as
I have already mentioned, Hryups agrees with the present form in
the absence of a postarticular process to the mandible, and also in
having rhachitomous vertebre; and since the above-mentioned
mandible agrees with the African one in the presence of this band
of denticles, and also presents no characters by which it can be
generically distinguished from the latter, there is a presumption
that the Labyrinthodont under consideration indicates either an
African representative of Hryops or a closely allied form. The
African mandible indicates, however, a somewhat smaller form than
the typical HL. megacephalus; and it also seems to differ from the
latter in that the anterior teeth are less enlarged in proportion to
the hinder ones. Again, the African intercentrum differs from the
corresponding element of the American form in the absence of ossi-
fication of the axial region; but it does not seem to me that this
feature is necessarily a generic difference. I therefore propose to
refer the African form provisionally to the genus Hryops, with the
name of 4. Oweni, the mandible being taken as the type.

In conclusion, it may be observed that the reptilian and amphibian
faunas of the reputed Permian of Texas and the Karoo system of
South Africa are both remarkable for the abundance of more or less
closely allied types of Anomodonts; while the first-named fauna
also contains numerous forms of rhachitomous Labyrinthodonts.
The remains of the latter group hitherto described from the Karoo
system are less common ; but it is not surprising to find among them
a form which cannot at present be satisfactorily separated from one
of the American genera. A connexion between the Mesozoic faunas
of Africa and America is already known to us by the identification
of the Brazilian genus Stereosternum with Mesosaurus from the
Kimberley beds of the Karoo system; and the present form adds
further evidence of this community of types. I have recently pub-
lished + the description of a species of Labyrinthodont from the
Karoo system, which is referred to the Australian genus Bothriceps ;

* No mention of this band of denticles, nor of the similar denticles with
which the palate is covered, occurs in Sir R. Owen’s memoir.
t+ Ann. Mag. Nat. Hist. ser, 6, vol. iv. p. 475 (1889).

294 ON TWO NEW SPECIES OF LABYRINTHODONTS,

and this, with the evidence previously recorded, serves to show that
the Anomodonts and Labyrinthodonts of the Permian of Texas, of .
the probably equivalent beds of Brazil, and of the Karoo system of
the Cape were closely related, not only to one another, but also to
those of the Gondwanas of Central India and the Hawkesbury beds
of Australia; while more or less closely allied types also occur in
the Upper Permian of the Urals.

[Since the foregoing was written I have been informed by Dr. E.
Fraas that the Munich Museum possesses some rhachitomous
Labyrinthodont vertebre from the Karoo system, which are pro-
bably referable either to the form described above or to Rhytid-
osteus. |

EXPLANATION OF PLATE XII.

Fig. 1. Outer aspect of the anterior portion of the right ramus of the mandible

of Macromerium scoticwm; from the Lower Carboniferous of Gil-
merton, near Edinburgh. {$uat. size. (Brit. Mus. No. R. 310.)

2. Oral aspect of the anterior portion of the right ramus of the mandible
of Eryops Oweni; from the Karoo system of South Africa. { nat.
size. (Brit. Mus. No. R. 466.)

3, 4. Terminal and left lateral aspects of an intercentrum of Hryops Owent;
from the Karoo system of South Africa. Nat. size. a, facet for
capitulum of rib. (Brit. Mus. No. R. 470.)

Quart.Journ.Geol.Soc. Vol. XLVI. PI XIL.

G.Cole&J.Gregory de]
MPParker lith

West,Newman imp

Igneous Rocks of Mont Genévre

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. | 295

18. The Vartoxrric Rocks of Mont Genivrr. By Grenvitte A. J.
Cort, Esq., F.G.8., and J. Watrur Grecory, Esq., F.G.S., F.Z.5.
(Read February 5, 1890.)

[Puate XIII. |

ConTrENTS.

I. Introduction.
II. Previous work on the Variolite of the Durance.
ITI. General features of the surface.
IV. Rocks found in the Gondran Valley.
V. The Gabbro and associated Serpentines.
VI. The Dykes.
VII. The Variolitic Diabases and Tuffs. :
VIII. Relations of the rocks to one another and to the stratigraphical

series.
IX. Conditions of Formation.
X. Conclusions of previous authors as to the nature of the Variolites

of other localities.
XI. Summary of conclusions.

I. Inrropucrion.

THouen the series of structures found in the acid igneous rocks has
now an almost complete parallel in the basic group, a few gups in
the latter still remain unfilled. The spherulitic and_perlitic
structures of ordinary rhyolites are now well known in the basic
lavas ; but the only rock that seems homologous with the pyromerides
of Jersey and North Wales is that known as the Variolite of the
Durance, which has been described as the selvage of a compact
euphotide. Impressed by the perlitic and other structures of this
rock, one of us suggested in 1888 * that it was a devitrified tachy-
lyte; while a few weeks later, the other attempted to settle the
question of its true nature by an examination .of the rock in the
field. As aseries of heavy sngwstorms prevented anything being
done on that occasion, we visited Mont Genévre together last
August, to examine the igneous mass to the south of the pass,
which had been mapped by Lory as an intrusive euphotide, and
from which it was probable that the variolites of both the Durance
and the Dora had been derived.

II. Previous work ON THE VARIOLITE OF THE DURANCE.

Variolite is a rock that has been of interest since the time
of the Romans on account of its supposed medicinal value;
its Kuropean sources, however, were lost till it was found near
lucea, early in the.17th century; previously the supply had
been drawn from America, where it had long been known as
“gamaicu.” Specimens of the “lapis variolatus ” of Lucca were

* G, A. J. Cole, “ On some additional Occurrences of Tachylyte,” Quart.
Journ. Geol. Soc. vol. xliv. p. 307.

Q.J.G.8. No. 182. x

296 MESSRS, G. A. J. COLE AND J. W. GREGORY

figured and described by Aldrovandus * in 1648, but no definite
opinion as to the nature of the rock of this locality can be obtained
from his work. A figure, however, given by Langius f, in 1705, of
a ‘‘variolites Lucernensis” from the Emmenthal is unmistakable.
The rock was subsequently described from other localities, as by
Bruckmann ¢ in 1734 and by Demeste § from the bed of the Durance
in1779. Wallerius || in 1747, and Bertrand J in 1763, published
classifications of Variolite, as by this time different rocks had been
included under the same name. Hitherto pebbles only had been
found, but in 1775 the Abbé Rozier’s ‘ Journal’ ** announced its
discovery im situ in the “ Servieres” valley, by MM. Faujas de
St. Fond and Guettard ; the former, however, gave in 1781 Tf an
account of his observations, and from this it is obvious that he and
his companion had only found fallen masses of rock on the
talus-slopes; in the same contribution Faujas called the Durance
rock “lapis variolatus viridis verus,” to distinguish it from the
amygdaloids that had been confounded with it. Valmont de Bomare’s
discovery of native silver in the Variolite of the same district led him
to examine it, with the result that he contended for t+ the common
origin of varioles and ground-mass (or “ variolin”’ as it was called
by Delamétherie).

Though Buffon §§ had in 1786 clearly indicated Mont Genévre as
the source of variolite, Morozzo |||| threw doubt on its occurrence
there. Fournet’s elaborate ‘“‘ Mémoire sur la géologie de la partie
des Alpes comprise entre le Valais et |’Oisans,” JJ contained an
important addition to the knowledge of variolite: from his de-
scriptions *** he seems to have collected, probably from the bed
of the Durance, compact diabase, perlitic variolite, and porphyritic
diabase. Elie de Beaumont probably found variolite in situ,
but no record of his observations seems to have been published, and

* Aldrovandus, Ul., ‘Muszum Metallicum in libros iii. distributum ;’
Bononiz : 1648: p. 883.

+ Langius, Carl Nic., ‘Historia Lapidum figuratorum Helvetiz ejusque
vicinie ;’ Lucerne : 1705, pp. 40-1.

¢ Bruckmann, ‘ Centuria Epistolarum Itinerarium,’ vol. i. ep. xxxi. Wolf-
fenbuttele, 1742.

§ ‘Lettres du Doct. Demeste au D. Bernard sur la Chymie, Docimasie,’ &e.
Paris, 1779 (quoted by Buffon).

|| Wallerius, ‘ Mineralogia, Eller Mineral-Riket, Indelt och beskrifvit,’
Stockholm: 1747, p. 409 (French edition, 1753).

*| E. Bertrand, ‘ Dictionnaire raisonné universel des fossiles propres et: des
fossiles accidentels, Le Hage, 1763, t. ii. pp. 238-9.

** “ Observations sur la physique,” t. xvi. (1775) p. 517.

t+ Faujas de St. Fond, ‘ Histoire Naturelle de la province de Dauphiné,’
Grenoble: 1781, t. i. p. 2538. See also Faujas de St. Fond, ‘ Histoire Naturelle
des Roches de Trapp,’ ed. 2 (Paris, 1813), p. 26, footnote.

tt ‘Dictionnaire raisonné universel d’ Histoire Naturelle,’ t. viii. Lyon: 1791.

S$ ‘ Histoire Naturelle des Minéraux; sur la variolite du Piémont,’ t. iv. (Paris,
1786) pp. 395-8.

||| Mém. Acad. Roy. Sciences (Turin), vol. v. 1793, pp. 165-72.

“| Ann. des Sci. Physiques et Nat. Soc. Roy. d’Agric. Lyon, sér. i. t. iv.
Weme ney 105-183, 483-560 ; ix. (1846) pp. 1-112; sér. ii. t. 1. (1849) pp. 185-
aOed, Pl. 1.

wk Fournet, ibid. séy. i. t. iv. p. 155.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 297

his collection from Mont Genévre was described by Delesse * ;
Scipion Gras certainly examined it in situ, and in consequence denied T
the volcanic origin of either the variolite or any of the rocks asso-
ciated with it.

Delesse’s memoir “ Sur la variolite de la Durance” t was the
first serious attempt to treat the rock from a modern point of view ;
the paper was illustrated by a coloured plate, which was supple-
mented by an exquisite lithographic drawing in the same author’s
‘* Recherches sur les roches globuleuses”’ §. Delesse was led by his
examination of the collection and acceptance of the field-work of
M. Elie de Beaumont to accept the passage from euphotide to ser-
pentine, and to regard the variolite as a selvage to the euphotide.

Supplementing the laboratory-researches of Delesse, Lory made
in the field a series of observations which have long appeared to be
conclusive. In 1861 the Geological Society of France, under his
guidance, spent one day in the variolitic area; visiting the Col du
Gondran, they saw the largest gabbro mass, and having probably
met with this rock again in the Chenaillet Valley, they greatly
exaggerated its importance ||, Lory argued on that occasion, in
opposition to M. Hébert, that the melaphyre-like rock was only an
‘“‘euphotide porphyroide, comme la variolite serait une euphotide
globulaire,” and that the latter was a structural modification of the
gabbro on itsselvages. These views Lory indicated clearly in 1863
in his map and sections of the Brianconnais { ; in the latter he repre-
sented this igneous massif as composed of euphotide intrusive in the
surrounding schists, and with a selvage of variolite on the west and
of serpentime on the east. In 1864 he repeated these views in a
rather detailed account of the area in question ** ; in his well-known
memoir he reaffirmed the passage from euphotide to serpentine on
the one hand and to porphyry and variolite on the other Tr.

The first application of the microscope to the study of thin sections
of the variolite of the Durance was made by Inostranzev in 1874,
in his valuable paper ‘“‘ O Variolitye ” tt, in which he described in
detail the variolite of a new locality, Yalguba in Olonetz, and devoted
several pages and figures to the microscopic structure of that of

* Ann. Mines, sér. 4, t. xvii. D: 130;

+ Gras, Sc., “Introduction 4 un Essai sur la constitution géologique des
Alpes centrales de la France et: de la Savoie,” Bull. Soe. géol. France, 2™°
sér. t. i. pp. 723-4.

¢ Ann. des Mines, sér. 4, t. xvii. pp. 116- 131, pl. i. Compt Rend. xxx,

p. 741-743 ; Bull. Soc. géol. Fr. 2™¢ sér. t. vil. pp. 407-431.

§ Mém. Soc. Geol. Franc, 2™ sér t. iv. (1852) pl. xxiv. ff. 18-20.

| “ Réunion extraordinaire a St. Jean de Maurienne,” Bull. Soc. géo}. France,
Qe sér, t. xviii. pp. 779-784.

“| “Carte et coupes géologiques du Briangonnais,” Bull. Soc. géol. France,
2m¢ sér. t. xx. pp. 253-235, pls. ill. & iv.

** Lory, “Description gé Sologique du penine B sei Soe. Shige as er de
l'Isére, sér, 2, t. 2%, (1861) pp. 1- Ns pl. i.; sér. 2, t. 1. (1861) pp. 1-260,
pls. ii., iii. ; sér. 2, t. viii. (1864) pp. 7-252.

th Loe. cit. par. 293; Bull. slant Pat Isére, sér. 2; fn vii. p. 86.

Th Verh. russ. k. min. Ges. St. Petersburg, ser. 2, Bd. ix. (1874) pp. 1-28,
pls. i., 1.

x 2

298 "MESSRS. G. A. J. COLE AND J. W. GREGORY

the Durance. These include an excellent coloured drawing of the
Durance variolite and a figure that illustrates the corrosion of the
varioles by the ground-mass*. Inostranzev fully recognized that
the varioles were closely akin to spherulites; he considered the
two structures to be distinguished by the fact that in the variolitic
the central sphere of radial fibres is enclosed by a series of concen-
tric layers, which do not share in the formation of the black cross
under polarized light. i

Zirkel 7, in 1875, made a detailed microscopic study both of the
variolites of the Durance and of those described by Giimbel from
the Fichtelgebirge; he corrected Delesse’s statement that the
ground-mass of the rock is a felspathic paste, and declared that
microscopic study rendered untenable the view of the connexion of
the gabbro and variolite that had been taught by Elie de Beaumont,
Cordier, Scipion Gras, Roth, and others. In the next year,
however +, he admitted variolite as a contact-product of diabase,
and Senft §, in the same year, described it as a diabase-aphanite.
In 1877 appeared Lévy’s important memoir ||, which embodies the
most detailed study yet made of the microscopic characters of
variolite. Relying on Lory’s map and sections, he described it as
a compact euphotide formed by the rapid cooling of the selvage of a
great euphotide-dyke, thereby differing from Zirkel, and agreeing
with Lory and Delesse. He described the fiuidal structure, and
made the important discovery that some specimens were perlitic, as
is well shown in the figure given subsequently in the ‘ Minéralogie
Micrographique ’ 4.

In 1887, in the second edition of his ‘ Mikroskopische Physio-
graphie,’ Rosenbusch ** redescribed variolite and accepted it as a
selvage-product of a basic rock, analogous to the spherulitic structures
so common in the glasses of the acid series.

In the same year Zaccagna 77, in describing some spherulitic
_ diabases from the neighbourhood of Monte Viso, referred to the
variolites of Mont Genévre as a thin crust on decomposing diabase
spheroids, and we regard this description as the truest that has yet
appeared. ;

Finally, in 1888, the perlitic structure of the rock was again
described and figured tt, accompanied by the suggestion that the
rock was a devitrified tachylyte. .

* Loe. cit. p. 2.

t “Die Structur der Variolite,” Berichte d. k.-stiichs. Ges. Wiss. xxvii (1875)
pp. 209-220.

+ F. Zirkel, Neues Jahrb. 1876, pp. 279-280.

§ F. Senft, ‘Synopsis der Mineralogie und Geognosie,’ Abth. ii. 1876, p. 556.

|| A. Michel Lévy, “ Structure et Composition minéralogique de la variolite
de la Durance,” Comptes Rendus, t. lxxxiv. pp. 264-266 ; Mémoire sur la vario-
lite de la Durance,” Bull. Soc. Géol. France, sér. 3, t. v. (1877) pp. 282-266.

“| Fouqué & Lévy, Minéralogie micrographique, (Paris) 1879, pl. xxiv. fig. 2.

** H. Rosenbusch, ‘Mikroskopische Physiographie der massigen Gesteine,’
ed. 2, vol. ii. 1887, pp. 227 e¢ seq.

“t+ D. Zaccagna, “ Sulla geologia delle Alpi occidentali,” Boll. R. Comit. geol.
Italia, xviii. (1887) pp. 387-8.

tt G. A. J. Cole, Quart. Journ. Geol. Soc. vol, xliv. p, 806-7, pl. xi. fig. 6.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 299

III. Generat FEATURES OF THE SURFACE.

The area occupied by the rocks studied in this paper comprises
some sixteen square kilometres immediately to the south of the
highroad from Mont Genévre to Clavieres. By ‘‘ Mont Genevre ”
we indicate the village of that name, at the summit of the well-
known pass, since the mountain or mountain-group once so desig-
nated is now known under other names. Our authorities in nomen-
clature have been the map on the scale of J : 80,000, published by
the French Dépot de la Guerre, and revised to 1887 (sheet 189), and
that of the Italian Survey, 1: 50,000, sheet 66, division 1, made by
the Istituto topografico militare in 1880.

Three valleys open on the south side of the highroad at a level of
1800 metres, rising towards a line of hills that runs east and west,
beyond which, again, the ground descends rapidly to the valley of the
Cerveyrette, or Cervicres. The westernmost of these is the Gondran
Valley, in which the upper Durance rises ; the floor is grassy, and
covered with pine-woods at the lower end, the stream ramifying
considerably in the more barren upland known as the Prés du
Gondran. On the west rise the grassy Cime du Gondran and the
sheer crags of Mont Janus (2514 metres), formerly spelled Juan,
Jouan, or Joux, and also styled sometimes Mt. Genévre. On the
east, above an intermediate platform used as cow-pasture, lie the
rocky ridge and taluses that run north-west for 1? kilometre from
Le Chenaillet. This peak, the highest point in the area (2634
metres, or 8642 tect), occupies, in fact, the south-east angle of the
bounding wall, and sends out an important spur towards the Col du
Gondran on the south. This col has an altitude of 2350 metres,
lying between the Cime du Gondran and Le Chenaillet.

The second and central valley, which we term for convenience the
Chenaillet Valley, is bounded on the west by the steeper and more
rugged face of the Chenaillet ridge and, further to the north, by a
long fir-clad promontory, the end of which is surmounted by pale
limestone cliffs. On the south is an extremely picturesque col (2500
metres) which we here term the Col du Chenaillet, following the
system adopted in the Gondran Valley. On the east a series of
pinnacled crags, reminding one of the north of Skye, leads up to
Mont La Plane; the valley-floor, at first undulating and containing
several little lakes, falls rapidly on the right, the descent from the
col being over terraced cliffs until the stream is encountered,
runnirg in a deeply-cut gorge. Above this gorge, on the east or
right hand, the slopes are formed of steep taluses, with a smooth
slate-blue exposure of serpentine; on the west rise the walls of
rock that mark off the upper division of the valley.

This upper or western division, into which one looks from Le
Chenaillet, falls much more gradually; it contains no stream in
ordinary weather, and the cattle-track from the col descends along
it over glaciated bosses of gabbro until it reaches a smooth grassy
upland, from which one may cross to the Durance. We are here,
in fact, on the watershed between that stream and the Piccola Dora,
the waters of which fall into the Adriatic.

300 MESSRS. G. A. J. COLE AND J. W. GREGORY

Fig. 1.— Map of the Variolitic Rocks of Mont Genévre.
Scale about 1 : 50.000 (# mile = 1 inch).

ae
GseZC LIVIERES

( ae

Pai Se

Wy _)\
CRENAICET / 29
SSUES

Mz HO} KMONSI /
2 We WINS SS S H
¢ XG l We Miy Of: Se

We aaah
~~’ COL DEXGIMON

ge
a al
xy
xQ

‘ead \ fief, ae
cIMES CoL DULY
DU CONDRANGONDRAN.

The area included by the broken ine — —— ———— =, which is left
open on the south, is occupied by the variolitic rocks.

Variolite-tuffs.

Intrusive porphyritic diabase of Le Chenaillet.

Gabbro.

=— Serpentine.

Brecciated serpentine.

(Heights in metres.)

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 301

If we follow the stream of the Chenaillet Valley, we find it
turning east under a cliff-set mountain-side to Clavicres ; and here
the third valley opens southward. This we have styled, for uni-
formity, the Gimont Valley, since Mt. Gimont forms its south-west
angle and the Col de Gimont (2428 metres) is at its head. Here
the dominant mass is Mt. La Plane, the cliffs and great taluses of
which form the western wall. On the east the slopes are far
smoother, with rounded gabbro-masses and blue serpentine showing
unmistakably at a distance of some miles. ‘The Col de Gimont is
formed by an interesting ridge, scarped to the north, dipping
smoothly and steeply to the south, the boundary between France
and Italy running exactly along its crest. The rocky prominences
of Cima Saurel (2453 metres) occupy the south-east angle.

From what follows it will be seen that the series of variolitic
rocks lies mainly between the Durance and the branch of the
Piccola Dora in the Gimont Valley, and may have an important
extension outside our area towards Cervicres on the south. Pro-
bably one of the most easily attained localities in which variolite
may be studied in situ is the north face of Mt. La Plane, just within
the Italian frontier, and a kilometre south of the highroad. The
whole east front of the same mountain forms one of the most admi-
rable fields for the collector.

LY. Rocks FounD IN THE GoNDRAN VALLEY.

As it is from the bed of the Durance that the principal supply of
variolite has been derived in the past, it is natural to make the first
search for the rock in the upper reaches of thisstream. Proceeding
south from the village of Mont Genévre among the boulders strewn
over the bed, one soon finds plenty of material. Following the
stream up the valley, one notices, scattered over the limestone floor,
great blocks of coarse gabbro (euphotide) and variolite, some of the
latter reaching to 5 feet in diameter and being spherulitic through-
out. Amongst these, but numerically less important, are blocks of
dense fine-grained diabase ; porphyry, with green saussuritic felspars ;
serpentine with or without diallage-crystals and cleavage-flakes ;
great masses of agglomerate containing variolite and diabase; and
finally, dolomite, ‘* cargneules,” limestone, and limestone-breccia. A
closer scrutiny of the gabbro-blocks shows that some of this rock is
fine-grained, and some schistified with large diallage- and felspar-
eyes: it shows no signs of the asserted passage into variolite, but is
traversed by many dykes of diabase as well as by felspathic segre-
gation-veins.

Here in the stream we have specimens of all the rocks of the
district spread out before us: the dykes and agglomerates are sug-
gestive of volcanic origin, but of this there is no hint in the descrip-
tions of Prof. Lory, who records neither of these two rocks. This
author, moreover, regards the coarse gabbro, the fine-grained diabase,
and the porphyrite with green felspars, as only different degrees of
coarseness of the same rock, which he describes as euphotide, and of
which the serpentine and variolite are alike structural modifications.

302 MESSRS. G. A. J. COLE AND J. W. GREGORY

Leaving the stream, then, as it breaks np into the numerous brooks
which drain the peat-bog at the head of the valley, we turn to the.
ridges on the east from which the material has been derived, in order
that we may see what light is thrown on the relations of the rocks
to one another.

V. Tur GABBRO AND ASSOCIATED SERPENTINES.

At the summit of the Col du Gondran, along the ridge that
forms the watershed between the Durance and the Cerveyrette, the
igneous rocks are seen in situ. We here find the gabbro as a series
of rough crags forming the south-west spur of Le Chenaillet. The
rock is usually coarse-grained, the crystals being in places as much
as 60 millim. in diameter; the texture is truly granitic. The rock
is a gabbro (euphotide of French and Italian authors), all the more
typical because its constituents, plagioclase and augite, have been
altered into ‘‘ saussurite ”’ and ‘‘ smaragdite ” respectively. Micro-
scopic examination shows that the rock has undergone considerable
change. In a less coarsely-grained specimen collected from near the
junction with a diabase-dyke, the felspar is often brecciated and
traversed by veins of secondary hornblende. The following analysis
by Delesse* shows that the felspar is labradorite :—

Pe LUCE ds cm aR ee 49-7
SALT RR TENT Met aa usenet gu pee ome le eat 29°65
IProtomide of IrOM ... ....)sscer et oe 8d
Oxide of manganese © 4 .).uu2e <a 6 trace
ee he ye oe a a ee cee eS
Meenas: .5 30 (. aaetetre enema 56
OE sol assSe nc wih eRe ae eee fer ke 4-04
TP ObAISD. fcakient cate emieeen here ace te 24
Water and Carbonic Acid........ 3°75
100:00

The magnesia is to be attributed to the serpentine-veins traversing
the felspar, and Delesse has also noted the presence of veins of cal-
cite, which may perceptibly increase the percentage of lime.
Boulanger ~ has also given an analysis of the felspar, and of what
he describes as a felspathic ‘‘ pate blanche ” in the euphotide; but
the results‘ of this early analysis differ considerably from that of
Delesse, while the silica of the felspar is much higher than in those
occurring in typical gabbro.

The pyroxene is still more altered. There is little of it remaining
even in the form of diallage, since it has been changed into grass-
green masses of ‘ smaragdite;” these on closer examination are

* Delesse, “ Recherches sur I'Euphotide,” Bull. Soc. géol. France, sér. 2,
t. vi. p. 549,

T +O, Boulanger, “Mémoire sur la Composition des roches d’euphotide,”
Ann. Mines, sér. 3, t. viii. (1835), p. 163.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 303

seen to consist of actinolite, uralite, and common hornblende. The
hornblende forms long frayed-out masses, with the fibres bent and
broken, and often surrounded by a zone of radiating needles of
actinolite. As arule, the green amphibolic areas are quite irre-
gular in shape, and often consist of a felt, or of radiating masses of
actinolite-needles.

The third constituent is titanic iron, and this also is decomposing
and passing into leucoxene,

Neither olivine nor pseudomorphs after it appear to be present,
and this forms another of the points of resemblance between this
rock and the saussuritic Cornish gabbros, which rarely contain
olivine*.

Along its western margins on this spur of Le Chenaillet the rock
is of finer grain, and it has not only been altered by the develop-
ment of microlites and decomposition-products, but by the mechanical
rearrangement of the constituents. In the first stage the rock is
schistified into an eye-gabbro, strikingly like that of Karaclews.
The primary felspar is turbid and opaque, and both it and the
pyroxene occur in eyes or lenticles drawn out along the plane 2f
schistosity. Between these are layers of green hornblende and a
mosaic of clearer secondary plagioclase. Actinolite-needles are
greatly developed, and occur in lines sweeping round the felspar and
pyroxene.

Still closer to the margin of the mass occurs an interesting fissile
rock. The felspar, which largely predominates, is far less turbid ;
the pyroxene has all been altered to actinolite which, with the
sphene associated with it, occurs in straight lines through the
rock.

Ascending the ridge, we cross many diabase-dykes in the gabbro,
and finally come to a sudden junction with the rocks of finer grain
that form the main mass of the ridge. From Lory’s description we
had expected a gradual passage from one to the other; on the con-~
trary, the junction is very sharp, and probably faulted. On the
west side of a line that runs straight across the hill, the gabbro is
at its coarsest; on the other side are the normal diabases with
variolitic selvages. ‘There is no sign whatever of a passage; the
general appearance of the junction, which, however, is not well
shown, and the extent to which the rocks have there been slicken-
sided, both suggest a fault.

There are several other outcrops of the same coarse-grained gabbro
in the area. Thus a little to the north, along the line of junction of
the igneous rocks with the calc-schists, it forms the face of the slope
of the platform that runs along beneath the ridge. It is the same
coarse-grained mixture of ‘ saussurite ” and “‘ smaragdite,”’ traversed
by diabase-dykes and serpentinous patches, which will be subse-
quently described. In the upper part of the west Chenaillet valley
there is another exposure which extends from the lowest lake to the °
north bank of the dry basin of a former tarn, where it abuts against

* J. J. . Teall, ‘ British Petrography,’ London: 1888, p. 177.

304 MESSRS. G. A. J. COLE AND J. W. GREGORY

a bank of serpentine. Round the margins of this gabbro-mass,
except where it joins the serpentine, the texture is especially coarse, .
and there is not the slightest sign of a passage into the finer-grained
rocks of which the variolite is a selvage.

The last outcrop of the gabbro is on the extreme east of the area,
where it occurs running from the bottom of the Gimont valley up
the east slope to the level of the platform, just north of Gr. Gimont.
On the lower part of the slope it abuts against the calc-schists that
form the floor of the valley ; but the junctions higher up were not
exposed, and no special attention was devoted to this mass, as it
lies outside the area especially considered in this paper. The usual
diabase-dykes and veins of green felspar occur in it.

Wherever the gabbro is exposed, it is found to be associated with
dark green or black “‘serpentines.” On the south-west spur of
Le Chenaillet these occur in irregular patches in the gabbro, from
which, by the elimination of the felspar and decomposition of the
pyroxene, a gradual and complete passage to the “ serpentinous”
masses can be traced. In the gabbro on the west flank of Le Che-
naillet true serpentine appears as a long dyke traversing the rock. In
the upper Chenaillet valley a similar serpentine runs from the end
of the gabbro on the north slope of the dry tarn-hollow across the
- Col du Chenaillet, where it is covered by tuff (see sketch, fig. 2),
and here, as well as in the ridge that runs south, it is associated
with brecciated serpentine. On the west flank of Mt. La Plane,
that is, on the right slope of the lower part of the east Chenaillet
valley, the serpentine occurs as a dome-shaped mass, irregularly
underlying tuffs; both the face of the serpentine and the layer of
vein-quartz that often marks the junction are greatly slickensided,
and it appears as if the serpentine had been faulted up into the tufts.
Finally, looking east from Mt. La Plane across the Gimont valley,
one recognizes, by the striking slate-blue tint of the talus-slopes of
the upper part of the opposite bank, a still larger development of
serpentine. From the north of Gr. Gimont it extends as a great
band along the side of the ridge, at about the 2200-metre contour,
for some distance to the south. This areais of interest, as it is that
which, by its size and development, is most akin to the serpentines
that crop out as elliptical patches throughout the range of the
Cottian Alps.

It was doubtless on the black patches of ‘‘serpentinous” matter in
the south-west spur of Le Chenaillet that Elie de Beaumont based
his theory of the complete passage from the gabbro to the serpentine,
a theory which was accepted by Delesse * and Lory +, and reaffirmed
by Hébert in 1877 +. Microscopic examination of this “ serpentine,”
however, shows that two very different rocks have been confounded
together. The dark green masses of the spur of Le Chenaillet are

* Delesse, Ann. des Mines, sér. 4, t. xvii. p. 130.

t Lory, “ Description géologique du Dauphiné,” para, 292, Bull. Soc. Stat.
Isére. t. vii. (1864), p. 83.

{ Bull. Soe. géol. France, sér. 3, t. v. p. 266.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 305

thus shown to be due to great aggregations of chloritic decompo-
sition-products, Other patches in the neighbourhood are true
serpentines formed from olivine, and contain areas of felspar, dial-
lage, and bronzite. The structure exactly resembles that of the
ordinary serpentines of the Cottians, one of which is well shown a
little over two kilometres to the north-east, at the upper angle in

Fig. 2.—The Col du Chenaillet, from the north.

a at we fs 5 ian
a ‘ . AP hi Bram , i / ee
=

-

Sea ae ah t

B.S. Brecciated serpentine. S. Serpentine.
V. Variolite-diabase and Variolite-tuff.
X. Point where fragments of limestone occur in the brecciated serpentine.

the zigzag on the road between Clavicres and Cesana Torinese.
This rock was described last year by Prof. Bonney * as a schistified
serpentine. Macroscopically it is almost identical with some from
the variolitic area; under the microscope it is seen to consist of a
light green serpentine with a well-marked ‘‘ Maschenstructur” and
areas of altered diallage ; secondary magnetite, either in the form of
crystals or dust, and actinolite are both abundant, and the rock is
traversed by a complex of chrysotile-veins.

We have thus to deal with a pseudo-serpentine formed from
segregation-masses of diallage and a true serpentine with bronzite.
In the case of the former, the junction with the gabbro is so irre-
gular that the rock certainly does not result from the intrusion of
a dyke richer in pyroxene than the surrounding gabbro. That the
true serpentine was not formed from pyroxene seems clear, as it

* Bonney, “Notes on two Traverses of the Crystalline Rocks of the Alps,”
Quart. Journ. Geol. Soc. vol. xlv. (1889), p. 80.

306 MESSRS. G. A. J. COLE AND J. W. GREGORY

contains an abundance of slightly altered flakes of that mineral, as
in the Wildschénau serpentine discussed by Hatch * and Cathrein +. .
As, however, there is so little olivine in the gabbros and the diabases,
the serpentine must have been formed from great segregation-masses
of this mineral. The existence of such segregations in basic rocks
is well known from the descriptions of Prof. Juddt. But it is
possible that one of the dykes of serpentine in the gabbro on the
west flank of Le Chenaillet, containing as it does evidence of former
felspar, may be due to the intrusion of a gabbro richer in olivine than
is usually the case.

At several points round the margins of the serpentine is found a
serpentine-breccia similar to that described by Prof. Bonney§. The
most striking mass is that on the east slope of the valley that runs
south from the Col du Chenaillet, while a little of it is well shown just’
to the north of the Col. A similar bed occurs above the slicken-
sided serpentine on the east flank of the lower division of the eastern
Chenaillet valley. Examined under the microscope, the rock is seen
to consist of broken pieces of serpentine, the ‘‘ Maschenstructur ”
in which indicates its production from olivine. Secondary horn-
blende in the shape of long wisps, forming lght-green dichroic
areas, indicates the former existence of pyroxene; flakes of altered
felspar also occur. These three constituents, and a multitude of
magnetite-granules, are scattered irregularly through a brown
matrix. In several specimens there are many small grains of calcite
and occasional lumps of limestone; the latter appear in sections as
dusty areas traversed by veins of clear calcite with the usual irre-
gular outlines and polysynthetic twinning. This rock, resulting
from the breaking-up of serpentine with pyroxene and some felspar,
may be named a picrite-breccia.

VI. Tue Dykes.

Though earlier observers have accepted the gradual transition
from euphotide to the variolite-diabase, we have, as has already
been stated, found no sign of such a passage. On all the exposures
examined, the gabbro ends abruptly against the more compact rocks.
In all probability the gabbro was once a deep-seated mass that
consolidated at the base of the volcano; but it now seems to form
a platform under the diabase, exposed where dome-shaped masses
have been pushed through the softer rocks, or where the valleys
have cut down to it. This view is supported by the abundance of
diabase-dykes traversing the gabbro in all its exposures. These
vary in width from half an inch or less to about 4 feet. Their course

* KF. H. Hatch, “ Ueber den Gabbro aus der Wildschonau in Tirol und die
aus ihm hervorgehenden schiefrigen Gesteine,” T'sch. Min, u. Pet. Mitth. Bd. vii.
(1886), pp. 75-87.

t+ A. Cathrein, “ Ueber Wildschénauer Gabbro,” tid. pp. 189-194.

{ J. W. Judd, ‘On the Tertiary and Older Peridotites of Scotland,” Quart.
Journ. Geol. Soc. vol. xli. (1885), p. 358.

§ T. G. Bonney, “ Notes on some Ligurian and Tuscan Serpentines,” Geol.
Mag. 1879, p. 365.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 307

~may be irregular, as they may branch and enclose masses of the
gabbro, or they may form long straight regular dykes, often marked
on the denuded surface by a long gully in the more resisting
gabbro.

The dykes are usually composed of a compact fine-grained rock,
of a dull green colour ; some, however, are more coarsely crystalline,
and the felspars are visible to the naked eye. Under the micro-
scope the coarse-grained dykes are shown to consist of lath-shaped
felspars ophitically included in a ground of secondary hornblende.
The felspar is turbid and worn, and the crystals are often surrounded
by a zone of fresh felspar, which has restored the original crystal-
line form. In many cases a fresh felspar-crystal has been deve-
. loped, surrounding several turbid ones, which appear as if ophiti-
eally included in it. The titaniferous iron is passing into leucoxene,
the white bands of which are very marked. Olivine appears to have

been rarely present, and is indicated by dark brown decomposition-
products. We may therefore fairly call this rock a diabase, using
that ill-defined term in Hausmann’s sense”, that is, for a labradorite-
pyroxene rock with green decomposition-products. A more finely
grained dyke traverses the gabbro on the slope below the west face
of Le Chenaillet, and in this the rock is less altered ; it 1s mainly
composed of a granular aggregate of felspar and pyroxene, with
green decomposition-patches formed from the latter; titaniferous
iron occurs in scattered grains, and there is a little olivine. In
most of the dykes the rock is finer on the margins than in the
centre, and there is a thin devitrified glassy selvage. This is well
‘shown in a specimen collected low on the flank of the Col du Gon-
dran ; the junction is irregular, thin tongues of the diabase pene-
trating the gabbro, while broken fragments of the latter are enclosed
in the diabase. The rock of which the dyke is composed is a finely
erystalline mass of acicular felspars in a basis coloured green by the
predominance of the decomposition-products. Towards the margin
of the dyke the texture becomes finer, till at the edge it passes into
a glass, full of cumulites and some incomplete crystals of felspar.
Epidote-veins traverse the diabase in all directions near the margin
(Pl. XIII. fig. 2). The dykes are usually not spherulitic, the only ap-
proach to this structure being the formation of the cumulites above
referred to. But in one case a huge block of compact diabase has
a distinct variolitic selvage ; along the margin of the diabase there
are many amygdules, some of which are elongated. Though this
specimen was not found actually zn situ, there can be httle doubt from
its position that it belongs to the dykes intrusive in the gabbro.
The rarity of the variolitic selvage in the diabase-dykes is remark-
able, since it is so constant an accompaniment of the great diabase-
masses about to be described. Since, moreover, the dykes are
not seen to run from the gabbro into the upper diabase-series,
they may possibly not be connected with the latter. The spherulitic
and glassy selvages are, however, evidence that they are not mere
i F, L. Hausmann, ‘Ueber die Bildung des Harzgebirges.’ Géottingen :
LOtS.

308 MESSRS. G. A. J. COLE AND J. W. GREGORY

segregation-veins, and the irregular nature of the junction and the
inclusions of the plagioclase- and pyroxene-fragments from the~
gabbro speak unmistakably in favour of their intrusive nature.
The rarity of the glass-selvage products is of interest, since it shows
that even the small intrusive veins could only have solidified slowly ;
the gabbro, therefore, may have been in a heated condition at the
time of the intrusion of the more compact rocks. ‘he fact that the
dykes do not run from the gabbro into the diabase, suggests that
the former was more deeply seated at the time of their intrusion,
and that it was subsequently forced up into the diabase-masses by
earth-movements ; if, indeed, these dykes entered the diabase-masses,
the original junctions have been shifted and destroyed.

Dykes, however, do occur in the great variolitic diabases. They .
may be divided into three classes :—compact diabase; diabase-
porphyrite or altered augite-andesite ; and coarse-grained dolerite.

Commencing with the dykes of diabase, the most important is
one that crosses the ridge of Mt. La Plane, just south of the summit
and on the north side of the east hollow; it is probably continuous
with a similar dyke seen in the corresponding position on the other
side of the ridge in the lower part of the east Chenaillet valley.
The rock is just macrocrystalline, and is jointed into bold columns
which are not perpendicular to the edge of the dyke. Microscopic
examination shows that the rock is composed of augite and plagio-
clase grouped ophitically ; the augite is remarkably fresh, but the
plagioclase is kaolinized. Patches of yellowish-green serpentine
indicate by their structure that they have been derived from olivine.
Biotite occurs as a few small, pale green, fibrous, and slightly ©
dichroic areas. There is a good deal of titanic iron with leucoxene.
The rock may therefore be called an olivine-diabase. It is markedly
scoriaceous, and overlies a thin diabase-ash or mud, which is baked
at the junction, and jointed into irregularly columnar blocks. This
green to purple slate-like rock appears to be unique in the area
under discussion. The dyke has cooled against the ash with a vario-
litic selvage, a fact important in showing the connexion between the
diabase-dykes and the variolitic series. Immediately to the north
of this is a similar but less interesting dyke in the north-east hollow
of Mt. La Plane. A dyke of a similar but more finely crystalline
rock runs up into the porphyritic diabase or diabase-porphyrite on
the west slope of the middle of the Chenaillet ridge.

The “ diabase-porphyrite ” plays an important part in the forma-
tion of the Chenaillet ridge, which it crosses as a saddle-shaped mass
running north-east and south-west. It faces the west as a steep
and rugged crag, whileit presents to the east a slope covered with
spheroidal joint-surfaces. Alongits northern margin it cuts sharply
against a bank of tuff, but its relations to the diabase and. tuff on
the west flank are complicated. In fig, 3 the junction of the
three rocks is shown; the diabase-porphyrite is exposed by the
denudation of the diabase and tuff into which it has been faulted.
It appears here and at other points that the porphyritic rock was
intrusive into and partly faulted up through the diabase-series, of

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 309

which scattered patches occur plastered on to its western face. A
little to the north of this a faulted junction of the compact and the
porphyritic diabase is well shown. The latter weathers into great

Fig. 3.—Rock-face showing relations of Variolitic Diabase (D* and
D*), Diabase Dyke (D'), Porphyritic Diabase (P’), and Tuff (T),
on west slope of north ridge of Le Chenaillet.

VE

The spheroidal porphyritic diabase (P2) is exposed from beneath the variolitic

diabase (D* and D#) and tuff’ (T), and shows faulted junctions with these ;

a fault parallel to the ridge, and giving a nearly horizontal trace, separates

the spheroidal porphyritic diabase (D') from a small patch, broken by

curved joints. The junction of D? and Dis faulted. The tuff overlies

ae variolitic diabase D?, and both are cut by an intrusive dyke of compact
iabase.

F. Faults.

rounded spheroids, the faces of which appear to be surfaces of cooling,
since the masses are often jointed within into radial prisms ; the
master-joints, however, often cut straight through the spheroids.
Microscopic study shows that the porphyritic diabase is composed
of plagioclase, augite, and some decomposition-products, in a granular
base that probably represents a devitrified glass. The plagioclase
belongs to two periods of consolidation ; there are the large saus-
suritic and porphyritic crystals, which are greatly corroded by the
ground-mass, in one specimen all the angles being rounded. These
crystals are traversed by veins of secondary felspar, which are in
optical continuity with the adjacent crystal (Pl. XIII. fig. 1) even
when they extend a little distance beyond it. The augite is mainly
present in the form of granules, which, with felspar ina similar con-
dition, forms the ground-mass of the rock. A large number of clear
isotropic octagonal or rounded masses are to be attributed to the

310 MESSRS. G. A. J. COLE AND J. W. GREGORY

pseudomorphs after augite. Some very similar bodies are, however,
probably amygdules, filled with clear crystals, the single cleavage of.
which is suggestive of epidote. The alteration of the rock is
marked by the development of epidote in the felspars, and of chlo-
ritic and epidotic areas, and minute grains of epidote, in the ground-
mass. There is very little of the original glassy matrix preserved.
The rock was, however, originally an augite-andesite. In most
cases the only signs of radial structure are seen in the chloritic areas,
but in some specimens long rays of felspar are grouped about a
centre; by a gradual increase in this structure a passage from the
ordinary andesite to a variolite-selvage can be traced (Pl. XIII.
fig. 5). In other cases the selvage is full of porphyritic crystals
which seem to have fioated to the margin.

Another coarse porphyritic diabase-dyke, grey in colour, occurs
crossing the south-west spur of Le Chenaillet in the diabase-tutf
above the junction with the gabbro.

The last type of dyke is the dolerite that occurs in a mass on the
south side of the summit of Le Chenaillet, on the side of the valley
running to the Col du Chenaillet. It is a rather coarse-grained
rock, and we considered it in the field as more allied to gabbro. Its
microscopic structure, however, shows that it would be most appro-
priately named a dolerite; the texture is ophitic, and the augite is
not schillerized. Its constituents are augite and plagioclase, with
some green decomposition-products and scattered crystals of titanic
iron and pyrites. The augiteis in fairly large crystals, and, in con-
trast to the felspar, is remarkably fresh; it is, however, much
cracked, and along these fissures decomposition has commenced in
places. In some cases a complete passage can be traced from fresh
augite at one end of a crystal into green decomposition-products at
the other, while in the middle a zone of diallage has been caused by
schillerization. Whether all the green areas are derived from
augite is doubtful, since in some cases, the junction is sharp between
a fresh augite crystal and the “ viridite.” The latter may have been
formed from accessory bronzite. The green areas appear, however,
to be mainly composed of actinolite, and a crystal of secondary
magnetite often forms a nucleus from which radiates a group of
actinolite-needles.

VII. Tuer Varionrric D1aBAsEs AND TUFFs.

We may now proceed from these dyke-rocks, on which variolite
occurs i situ asa selyage, to the mass of the compacter diabases
through which they were intruded. In 1861 * Lory reports that,
starting from near Le Chenaillet, “en avancant de quelques pas
vers lest, on trouve Vewphotide bien caracterisée, 4 élements nette-
ment séparés, qui continue de la jusqu’aux sommités et dans tout
le vallon affluent de la Doire.” The euphotide proper is certainly
visible from this point, but occupies, as has been described, only a

* Bull. Soc. géol. France, 2° sér. t. xviii. (1861), p. 782. “ Descript. géol.
du Dauphiné ” paragraph 293.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. Sih

small part of the floor of the upper and western portion of the
Chenaillet valley; while the summits immediately above, and the
whole upland about the lakelets, as well as all the main walls of
this “vallon affluent de la Doire,” consist of rocks entirely different
in their mode of weathering, colour, and degree of crystallization.

Finding serpentine on the eastern flank, Lory *, in his published
section, filled in the intervening space as ‘ euphotides,” and thus
unconsciously diverted the attention of observers from one of the
richest areas where variolite may be obtained in situ. We must
recognize, however, that the igneous masses extend some way
towards the Cerveyrette, and euphotide may be there more pro-
minent. We hope at some future time to examine this southern
area;. but from the contour we judge that Lory’s section traverses
the high ground near Le Chenaillet, to which his descriptions, as
above quoted, undoubtedly apply.

Fig. 4.—Variolite-diabase. Spheroidal Masses with Variolitic
Selvages. North end of Le Chenaillet Ridge, above the Durance.

aye)
SES.
ENS

WSS
WO

y)

{ >}

ARGS wc!

The prevalent rock of the whole district at present under dis-
cussion is a compact grey-green diabase. The dykes already
described doubtless represent the coarser types of these widely
spread masses. ‘The most striking character of the compacter series
is a tendency to spheroidal jointing. Sometimes, as among the

* “Carte et coupes géol. du Brianconnais,” Bull. Soc. géol. France, 2° sér.

t. xx. (1863) p. 233.
Q.J.G.8. No. 182. yi

312 MESSRS, G. A. J. COLE AND J. W. GREGORY

crags forming the east side of the Chenaillet valley, south of Mt.
La Plane, the spheroids appear piled regularly one above the other,
forming walls as it were, which are divided by conspicuous vertical
joints; but the structure is more commonly irregular, the masses
resembling pillows or soft cushions pressed upon and against one
another, each cliff-face thus exhibiting a number of swelling sur-
faces and curving lines of junction (fig. 4). Examined more
closely, small vesicles are seen in these rude spheroids, especially
towards the margins; and in some places, as on the east of Mt. La
Plane, the whole rock becomes vesicular and slaggy. The surfaces
of the masses are covered by a crust of variolite, from 1 to 7 or 8
centim. thick. The spherulites or “ varioles ” are grouped or drawn
out in bands parallel to the surface, being in some places almost
microscopic, in others 5 centim. in diameter.

The coarsest variolite that we are acquainted with occurs on a
little plateau above the pine-woods on the north end of the ridge of
Le Chenaillet. The ground here, with the large spherules pro-
jecting from the weathered surface, reminds one of the pyromeride-
area of Digoed near Penmachno in North Wales,

Fig, 5.— Variolite-diabase ; north end of Le Chenaillet Ridge.

A and C. Compact diabase.

B. Variolite, 5 centim. thick.

D. Variolite, bent and infolded, 3-4 centim. thick.
E. Compact spherulitic diabase.

This, then, is the typical mode of occurrence of the famous Vario-
lite of the Durance. It is everywhere a selvage to compact and
ordinary basic igneous masses, just as tachylyte so frequently bor-
ders the intrusive basalts of our Western Isles of Scotland*. But in

* See P. F. Kendall, ““On some Occurrences of Tachylyte in Mull,” Geol.
Mag. 1888, p. 555.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 313

the Mt. Genévre area the spherulitic selvage is found on every
conspicuous surface of division throughout the rock, and often seems
to have become infolded when still viscid by the pressure of adjacent
masses (fig. 5). Often a subsidiary jointing has been set up, as
is common in spheroids of contraction *, columns being produced
which radiate from the centre, and produce a tesselated effect on
the outside. This feature is best seen, however, in the globular
masses found in the rocks styled by us variolitic tuffs.

Where very thin, the variolitic crust is liable to become lost by
exfoliation and decomposition ; and its outermost layer is commonly
soft, and coated with dark-green alteration-products. But in the
majority of instances the spherulites are easily recognizable, and
hundreds of specimens might be collected in an hour which would
show the passage from compact grey diabase to typical “ variolite of
the Durance.”

The microscope shows us that the green matrix of the variolite
becomes less and less in quantity as we proceed from the surface
towards the centre of the spheroidal masses of diabase. Thespheru-
lites come into contact with one another, as in the similar ‘‘ apha-
nite” of Liguria f; but even at some distance from the selvage they
are still differentiated. In the interior of the rock their place
is taken by beautiful stellar or brush-like groups of plagioclase, the
rays of which are straight. These rays contain dark axes, occupying
about a third of their bulk, formed of included or impertectly erys-
tallized material ; they often bifurcate at the ends, branches are set
on at intervals, and forms resembling skeleton-crystals are thus
built up, though the individual little rods composing them have
different optical orientations (compare Pl. XIII. fig. 5).

The spherules of the variolite itself are often of a translucent
brown colour, the more characteristic grey appearance being due
to alteration. The rays, moreover, of the brown examples are
pleochroic, as in ordinary tachylytes. .The matrix becomes also
browner in the interior of the spheroidal masses of the rock, resem-
bling thus the residual glass in the great porphyrite dykes.

Porphyritic crystals oceur occasionally in the variolite. We have
not detected olivine, but may record felspar, magnetite, iron-pyrites,
and transparent little pseudomorphs after pyroxene. Not unfre-
quently, embryo prisms of felspar, with characteristic bifurcated
ends, appear in the midst of the spherulites, as if developed at an
earlier stage. We must mention also the “ pseudocrystallites ” so
clearly distinguished by M. Lévy ¢, which occur in so many of the
larger globules, and which we are inclined to regard as little fissures
due to fracture or contraction. Much as they often resemble the
constituents of a crystalline meshwork, there is evidence in many
of our examples of a tendency to branch and become irregular. We
do not find that the rays of the spherulites, as seen in polarized
light, run on without interruption through these lighter areas; on

* See, for example, Scrope, ‘Considerations on Volcanos,’ 1825, p. 140.

+t Mazzuoli and Issel, Boll. R. Comit. geol. d'Italia, vol. xii, (1881), p. 330.

t Bull. Soc. géol. France, 3° sér. t. v. (1877), p. 238.

¥2

314 MESSRS. G. A. J. COLE AND J. W. GREGORY

the contrary, they are broken through, and the “ pseudocrystallite ”
resolves itself into a minute rift filled with colourless secondary
products. The dark granules that abound throughout the rock are
frequently grouped along these transparent lines, so as to suggest
that they also are developed as products of alteration. We feel
that until a similar structure is found in other rocks, so that ample
comparison may be made, the last word cannot be said on these
interesting ‘* pseudocrystallites ;” but in a large spherulite, 2 centim.
in diameter, which we have especially studied in reference to this
question, all stages between the coarser and undoubted cracks and
these little individualized and intersecting rifts can be determined
without any hesitation (Pl. XIII. fig. 6).

While dealing with these structures in the variolite, we would
note the great abundance of yellow epidote as a secondary consti-
tuent, whether in the occasional perlitic lines of separation, or in
the more ordinary fissures, or irregularly developed in the matrix.
M. Lévy’s specimens appear to have been deficient in this mineral,
the importance of which was insisted on by Delesse in 1850, and
again in discussion in 1877. The epidote commonly forms a granu-
lar mosaic, but occasionally occurs in almost colourless prismatic
forms associated with the chloritic areas. It is unnecessary te call
attention to the little bunches and fibres, probably of actinolite, in
the matrix, and to the other mineral features that M. Lévy has so
admirably described.

The more we examine the interesting structures of the variolite,
the more we are convinced that we are dealing with the altered and
devitrified selvages of an ancient basic andesite or basaltic lava.
The matrix of the rock, despite its epidote-veins and granules, and
its action on polarized light, shows so often a perlitic structure that
its former colloid condition seems placed almost beyond dispute*.
The alteration of basic glass to palagonite and to fibrous recrystal-
lized products, has been again and again described ; and the ‘ vario-
lite of the Durance ”’ received, indeed, a normal explanation if placed
in the category of the tachylytes.

The varioles themselves have been already referred to as if they
were ordinary spherulites ; but this is a question that has received
considerable attention. Setting aside the old discussions as to
whether they were included pebbles or concretions subsequent to
consolidation, we note that even Morozzo + compared them to the
*¢ taches variolitiques ” of the lava of Vulcano, although he could see
no proof of volcanic action in the locality of his variolite near Susa.
In far later times, M. Michel Lévyt, while stating that the varioles
have only a superficial analogy to the colloid globules of acid rocks,
fully recognizes their spherulitic character, classing them as erystal-
lized varieties. Geinitz§ also insists that they should be compared

* Mr. Rutley has recently traced in certain ‘“ epidosites” the extreme phase
of alteration of perlitic lavas. Quart. Journ. Geol. Soc. vol. xliv. (1888),
p. 740.

+t Mém. Acad. royale des Sciences, Turin, t. v. p. 171."

t Bull. Soe. géol. France, 3° sér. t. v. (1877), pp. 257 and 263.

§ Tscherm. Min. u. petr. Mitth. Bd. i. 1878, p. 143.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. a1b

with ordinary spherulites. Loewinson-Lessing *, on the other hand,
regards them in a similar rock as globular forms analogous to por-
phyritic felspars, a view calculated to lead the mind away from a
number of most valuable comparisons. It is clear that the varioles
are now largely composed of crystalline fibres ; but 1t is doubtful if
these are all of the same mineral composition. Delesse 7 has given
the following analysis of globules brought by Scipion Gras from 2
kilometres south of the village of Mont Genévre :—

SO a ee on See eee is (ode
MOPIMPMC UNAM cic o's cele s « mias see Shs 17:40
Dane or iron... +. sees ee os C19
Reatge Of CHYOMIUM ...<... sinc Oat
Oxide of manganese............ traces
[NG eo Si hon Ae eR ae 8°74
Sa eget ee nes n'y vee sd 3°41
MM et ech es: eisiste es sieve br: O12
1 RESSUT phlei ha aed Agee el a 0-24
POISON oy ks ee eae: 1:93

99°86

The globules from a similar specimen from the “ torrent de Cer-
vieres” yielded M. Lévy { results agreeing closely with the
above.

With hesitation, Delesse classed the globules as triclinic felspar.
Their specific gravity is given as 2°923; M. Lévy records 2:920;
and we have found a large spherule which has a specific gravity as
high as 2°96.

M. Michel Lévy § concludes that oligoclase-fibres form 60 per
cent. of the globules, the remainder being composed of amphibole
and pyroxene. It is equally impossible for us to refer our own
materials to any one mineral, but rather to a mixture, in which
felspar largely predominates. The varioles may have originally
included only a smal! amount of glassy matter, and nay even have
been among the crystalline ‘“ belonospherites” of Vogelsang; yet
we cannot on this account cut them off from kinship with the more
familiar types of spherulites. Indeed we know how in modern
tachylytes pleochroism and other effects of crystallization are ob-
servable in the fibres of bodies that are exactly comparable in mode
of origin to the spherulites of pitchstone or obsidian. The whole of
a basic rock, even to the vitreous selvage, becomes, under similar
conditions, more crystalline than the corresponding acid type. The
variolites of Mt. Genevre have undergone, in addition, the very
extensive secondary devitrification of which the epidote-veins and
microlites of actinolite afford such abundant evidence.

* Tscherm. Min. u. petr. Mitth. Bd. vi. 1885, p. 208.

t+ Ann. des Mines, 4° sér. t. xvii. (1850), p. 116. Also Comptes Rendus,
t. xxx. (1850), p. 741.

t Bull. Soc. géol. France, 3° sér. t. v. (1877), p. 248.

§ Ibid. p. 250.

316 MESSRS. G. A. J. COLE AND J. W. GREGORY

If, then, the variolite represents a vitreous selvage-product, how
comes it to be so widely diffused among the masses of the diabase-
lavas? It is possible that the surfaces of ordinary spheroids of
contraction, even in the heart of a cooling mass, may differ appre-
clably from the more central portions, and, consolidating more
rapidly, exhibit a vitreous structure. Delesse * thus concluded,
from a number of determinations of specific gravity, that the centres
of prisms and spheroids in igneous rocks are denser than the ex-
ternal layers. If denser, even a glassy crust may occur outside
while the core is fairly crystalline. But we prefer to read in the
irregular shape and involuted surfaces of the diabase-masses of Mt.
Genévre evidence of the rolling over of lavas among themselves ;
and we are led to regard the presence of variolitic selvages through-
out such great thicknesses of rock as largely due to movements
taking place within a crater, a point to which we shall revert in
Section IX. That the mode of occurrence of the variolite of Mt.
Genévre is paralleled at other places may be seen by the descriptions
of Mazzuoli and Issel of kidney-shaped masses of aphanite near
Bonassola in Liguria, which have variolitic surfaces of junction.
Zaccagna ¢ also records similar phenomena in a spheroidal diabase
near Mte. Viso.

A glance at the sketch-map of the district (p.300) will at once show
the large area covered by the variolite-diabases. When we add that
the thickness of these compact rocks often amounts to 300 metres,
and appears to reach 500 metres in the neighbourhood of Mt. La
Plane, some idea may be formed of the importance of the series. In
places both folds and faults are traceable; but we believe that the
thicknesses here stated are not the result of actual repetition.

Our map also indicates the occurrence, particularly upon Le Che-
naillet, of rocks styled by us Variolite-Tuffs. These, as has been
stated, readily attract attention among the pebbles in the bed of
the Durance, though, with an exception in the Museum of Grenoble,
we have not found specimens of them in any public collection.
Delesse §, however, cites Elie de Beaumont as stating (probably in
conversation) that ‘‘ Veuphotide formant le massif central du Mont-
Genévre est encore accompagnée ou entourée par des roches bréchi-
formes variées, ainsi que par des roches probablement métamor-
phiques.” Cordier || has, moreover, in his classification the heading
*‘ Bréche variolitique,” and he describes one of his specimens as
follows :—“ Bréche de variolite embryonnaire. Cette roche, trés-
curieuse, ayant la méme origine que toutes celles que j’appelle
Bréche de froissement, sert d’éponte a ia variolite qui forme des amas
transversaux dans les serpentines des parties supérieures de la
vallée de Serviéres (Hautes Alpes).” It is possible that the pou-

* «Métamorphisme des Roches,’ Paris, 1858, pp. 371-4.
t Boll. R. Comit. geol. d'Italia, vol. xii. (1881), p. 329.
t Lbid. vol. xviii. (1887), p. 387.

§ Ann. des Mines, 4° sér. t. xvii. (1850), p. 130.

| ‘ Description des Roches,’ 1868, p. 1738.

——_—

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. $17

dingue with variolitic rocks recorded by Morozzo* from near Susa
was a rock similar to those of Mt. Genévre. We fail to see, how-
ever, that Geinitz tT has established satisfactorily that the schistose
variolite described by him from the Col de Sestricres is a tuff and
not merely a metamorphosed portion of the diabase.

We have not mapped the boundaries of these fragmental rocks on
account of their intimate association with the variolite-diabase.
They may, indeed, be friction-breccias, or lavas broken up while
viscid, or volcanic tuffs. Careful consideration inclines us to the
last-named of these views, and we regard them, as will be seen in a
later section, as the products of local explosive action. Against the
view that they are friction-breccias, we would urge that slickensides
are rare in their material, though common enough in the brecciated
serpentines ; that the dykes which must be practically contempora-
neous with them have not suffered from any similar crushing ; and
that we have found no admixture of gabbro, serpentine, or limestone
in these diabase-“ breccias,” even when they are hundreds of metres
in thickness. The smaller particles appear, moreover, to represent
the glassy types rather than the compacter diahase-lavas ; while
spherical “‘ bombs” are abundant, which remain unbroken and are
beautifully coated with uninjured variolite. Nor, on the other hand,
do we think that the characters of the matrix in these fragmental
rocks, when little altered, can support the suggestion that they are
lavas which became brecciated during flow. In such a case at least
some of the instances examined should betray, by spherulites or other
signs of imperfect crystallization, the former molten nature of the
ground-mass. The slaty bed against which the great dyke of Mt.
La Plane’has cooled is also some evidence of the existence of ashes
and tuffs among the lavas at the time of their formation.

A striking feature of these fragmental deposits is, as we have
hinted, the abundance of globose masses of compact diabase, their
surfaces being thickly coated with variolite. Although only slightly
vesicular, these appear to be of the nature of volcanic bombs. The
smaller ones are spherulitic throughout, and in almost all cases the
old glassy crust is exceedingly well marked. Some of these sphe-
roidal specimens, with their concentric coats, resemble the well-known
globes from the pitchstone of the Chiaja di Luna of Ponza, The
largest that we have measured was on the western slope of Le
Chenaillet, and was partly broken, showing within the characteristic
radiating columnar structure. The dimensions of this imperfect
mass were 70 centim. by 43 centim. by 45 centim. We believe
that the large and beautiful specimens of variolite, spherulitic from
one side to the other, which are obtainable in the upper Durance
are residues from the breaking-up of the volcanic agglomerate rather
than from the massive diabase-lavas. ‘The blocks thrown out into
the tuffs would naturaliy be at times completely vitreous.

The smaller fragments are often scoriaceous and very angular,
and consist of variolite and more ordinary diabase in about equal

* Mém. Acad. royale des Sciences, Turin, t. v. (1793), p. 169.
Tt Tscherm. Min. u. petr. Mitth. 1878, pp. 146-152.

318 MESSRS. G. A. J. COLE AND J. W. GREGORY

proportions. Microscopic sections reveal a number of transitional
forms, with delicate radial groups of felspar and brown interstitial
glass, such as have been referred to in our description of the diabase-
lavas. We have also found fragments of the porphyritic andesite or
diabase of the aréte of Le Chenaillet—a fact that confirms the
practical contemporaneity of the great dykes and these agglomerates.
Of course, on the other hand, these fragments would by themselves
support the view that the agglomerates are friction-breccias. The
matrix of the tuff has generally been extensively altered, and a zone
of epidote and other clear secondary minerals, accompanied by opaque
granules, has often formed around the inciuded fragments. Par-
ticles of basic glass, rich in globulites and minute stellar aggregates,
are freely scattered; and many even of the stony-looking and
darker fragments prove, between crossed nicols, to retain their
original amorphous character (Pl. XIII. fig. 4).

Fig. 6.— West Slope of Le Chenaillet, showing dyke-like forms
of the Variolite Tuff.

—____ a

Le Chenaillet. Gabbro of the
Col du Gondran.

The secondary mineralization of the matrix has given rise to a
handsome rock on the west of Mt. La Plane, where dark-green
particles of variolite lie in a ground of bright yellow epidote.
Where, moreover, the tuffs come in contact with the serpentine,
hydrous magnesian silicates have permeated the mass, and even the
variolitic fragments have become softened and decomposed. The
resulting serpentinous tuff is, on Mt. La Plane and at the Col du
Chenaillet, difficult to distinguish from the breccia of the serpentine
itself; but we have found no passage between these rocks, the
variolite never occurring in the breccia, and the wisps of diallage or

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. olg

bronzite being entirely absent from the tuff. The microscope easily
distinguishes between the particles of serpentine, with their veins of
magnetite, in the breccia, and the fragments of diabase in the green
and metamorphosed tuff.

It is remarkable, indeed, that the serpentine should have thus
yielded to earth-movement without a real intermingling of the rocks
at contact. We presume that, at the period of brecciation, the
variolite-tuff had become as tough and hard as its unweathered
masses are to-day.

The great locality for the tuff is Le Chenaillet itself; and on the
western slopes the characteristic mode of weathering is admirably
displayed. The roughly piled masses are divided, not by stratifi-
cation, but by vertical joints, and form, under denuding influences,
great dyke-like spurs running out towards the valley at right angles
to the ridge (fig. 6). As is common in ancient volcanic agglome-
rates, there is also a marked tendency to the formation of pinnacles
and spires.

VIII. RELATIONS oF THE Rocks TO ONE ANOTHER AND TO THE
STRATIGRAPHICAL SERIES.

To summarize, then, the relations of these igneous rocks to one
another, we may safely assert that the gabbros and serpentines, so
intimately connected, form a floor or undulating platform on which
the variolitic series has been piled. The gabbro is exposed at four
distinct points :—-above the forks of the Durance, at a height of
2250 metres; on the south-west angle of Le Chenaillet, at 2450
metres ; in the floor of the upper Chenaillet valley (2350 to 2550
metres); and on the east flank of the Gimont valley, among the
limestones, as low down’as 2100 metres. Serpentine occurs inde-
pendently at 2200 metres on the west slope of Mt. La Plane and
along the ridge north of Cima Saurel, some 200 metres higher.

While, then, the true euphotide seems to have at the surface little
of the importance assigned to it by earlier observers, it none the less
forms a base to the eruptive series and is probably of similar age.
But the original junctions of the highly crystalline rocks with the
diabase-series, or the passages from one type to the other, have been
lost during subsequent earth-movements, the gabbro being often most
coarsely developed at its present margin, and exhibiting there the
eye-structure of gabbro-gneiss. These facts, and the abundant
slickensides in the gabbro, show that the upper series may have been
shifted over the hard crystalline masses, leaving us in doubt as to
their contemporaneous origin and connexion.

The gabbros, however, were broken through in places by eruptive
rocks, which form numerous dark dykes and veins.. We are led to
regard these as representing either the last upwelling of molten
material through the cracks of the consolidating gabbro, or as the
lines of fissure through which the variolitic rocks attained the surface.

We have, however, been unable to detect the passage of these
dykes, so numerous on the west flank of Le Chenaillet, into the

320 MESSRS. G. A. J. COLE AND J. W. GREGORY

upper diabase series. Where the variolitic tuffs are in direct
contact with the gabbro, such dykes ought to form prominent
objects. The great porphyritic diabase, however, that crosses the
ridge of Le Chenaillet is certainly intrusive in the tuffs, and pro-
bably has similar relations to the gabbro; but the gabbro does not
reappear to the north of it, and thus even here the evidence is
inconclusive. There are abundant dykes of diabase in the variolitie
lavas and tuffs, and their characters link them closely with those
traversing the gabbro. Yet we find no evidence of passage between
the gabbro itself and this compacter group. An observer intent on
establishing the sedimentary or metamorphic origin of euphotide and
serpentine might, indeed, accept the eruptive character of the diabases
without prejudice to his views of the more crystalline series.

The age of the variolitic group and associated gabbros has been
generally accepted, on the authority of Lory*, as later than the
Infra-Lias. We have observed something like contact-alteration
where the variolitic diabase abuts on limestone north of the fork of ,
the stream in the Chenaillet valley. Here, and also against the
gabbro in the Gimont valley, the limestone is broken and traversed
by abundant calcite-veins ; but this brecciated condition of the rock
precludes accurate determination of the existence of contact-meta-
morphism. Gastaldiy has, indeed, denied such alteration at the —
junction of the ‘“ pietre verdi” and the overlying limestone. Simi-
larly, the interesting limestone-fragments in the eruptive rocks at
the Col du Chenaillet occur, not in the massive serpentine, but in
the brecciated variety ; and it may therefore be urged that they
have become included as the result of subterranean crushing. We
think, however, that their distinct removal from the limestone of the
lower valley is fair evidence that they were SS up during the
intrusion of the igneous mass.

But doubts now arise as to the real age of the stratified rocks
regarded by Lory as Liassic. The obscure fossils picked up on the
talus of Mt. Chaberton appear to have formed the basis of this con-
clusiont. Gastaldi and his collaborators, who believed in 1876 that
they had found evidence here of Cambrian and Silurian strata,
abandoned this view later, on the determination of their specimens
as Mesozoic. But Gastaldi claims to have proved the existence of
the Trias within the limits of Lory’s “ Caleaire du Briancgonnais” § ;
while it is clear that he would sweep the whole of the euphotide and
diabase group down into the “ pietre verdi,” and thus relegate them
to the pre-Paleozoic. That this view was influenced by the gene-
ralization he had adopted with regard to serpentines in the abstract
may be seen by his refusal to admit the Eocene age of any of these
rocks in Tuscany |}.

* “ Descript. géol. du Dauphiné,” paragraph 290, Bull. Soc. Stat. Isére,
2° sér. t. vii. p. 79.

+} Boll. R. Comit. geol. d'Italia, vol. vi. (1875) pp. Bony

; - Bull. Soc. géol. France, 2° sér. t. xviii. (1861) p. 770

“Sui rilevamenti geologici fatti nelle Alpi piemontesi, 1877,” Mem. R.

eae dei Lincei, Rome, ser. 3, vol. ii, 1878, p. 959.
|| Letter in 1878 to Sterry Hunt, Geol. Mag, 1887, p. 536.

—————

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 321

Zaccagna*, however, agrees that the ‘“‘massa diabasica” of
Mt. Genévre is intercalated in the cale-schists below the limestones
of Mt. Chaberton. He states that various authors have treated the
mass as Permian; but against this view he urges that the calc-
schists cover it upon the French or western side. It is clear, how-
ever, that this reasoning, and that of other Italian geologists, will
only hold good if we regard the series as sedimentary. Moreover,
Zaccagna himself would seem to assign an eruptive origin to the
diabase-groups of the Val de Chabricre and of Mt. Geneévre.

The age of the calc-schists themselves has not been satisfactorily
determined. As early as 1850 Fournet? pointed out the existence
of this zone of the “ roches pennines ” at Mt. Geneévre, and suggested
that they were of Carboniferous or earlier age. Lory ¢, selecting
the band of ‘“ Gypse et cargneules” below Clavieres as the top of the
Trias, included in that system the mass of the ‘“schistes lustrés
calcaréo-talqueux ” and much of the ‘“ pietre verdi” of Gastaldi.
Though strongly opposed by Italian writers, he issued a sketch-map
in 1881, in which the base of the Trias is still carried out to meet
the ancient gneisses along a line as far east as Susa§. This seems
a logical consequence of the acceptance of any part of the ‘‘ schistes
lustrés ” as Triassic ; and in almost his latest scientific utterance he
affirmed the accuracy of these views ||.

Notwithstanding his great breadth of vision, the balance of recent
evidence seems in this matter opposed to Lory. Zaccagna, for
example, states that the zone which he regards as Permian, and
which underlies dolomitic limestones with Gyroporella, was deposited
in inequalities of the calc-schist series 4] ; and in his section of the
Pointe de Mary he shows an unconformity of the most decided cha-
racter between the two **,

Zaccagna and Mattirolo, indeed, in the beautiful map appended to
the paper cited Tr, carry their Triassic rocks from the frontier to
Briancon, entirely excluding the Lias from the neighbourhood
of Mt. Genévre. Strips of Permian appear above the. diabase
group and on Mt. Chaberton.

Gastaldi hesitated to divide up definitely the ‘‘ Calcaire du Brian-
connais” of Lory; but on the frontier itself his map tt, if more
detailed, would probably agree with that of Zaccagna. We have

* “Sulla geologia delle Alpi occidentali,” Boll. R. Comit. geol. d'Italia, xviii.
1887, p. 388. Cf. ibid. p. 377.

+ ‘“ Notes sur une excursion dans les Alpes en 1849,” Ann. des sciences phys,
et nat. Lyon, 2° sér. t. iii. (1850-51) p. 37.

t “ Descript. géol. du Dauphiné,” 1864, paragraphs 256 and 286, Bull. Soc.
Stat. Isére, 2° sér. t. vii. pp. 14 & 72; “Stratigraphie des Alpes Graies et
Cottiennes,” Bull. Soc. géol. France, 3° sér. t. i. (1873) p. 278. Cf. ibid.

. 269.
i § Bull. Soe. géol. France, 3° sér. t. ix. p. 655.

|| “‘ Etudes sur les schistes crystallins,” Congrés géol. internat. London, 1888,
pp. 26 and 28.

@ Boll. R. Comit. geol. d'Italia, vol. xviii. (1887) p. 389.

** Thid. tav. 1x.

tt Ibid. tav. xi.

tt Mem R. Accad. dei Lincei, ser. 3, vol. ii. tay. ii.

. MESSRS. G. A. J. COLE AND J. W. GREGORY

Fig. 7.—Part of Professor Lory’s Map. (Scale 1: 250,000.)

Alluvions modernes.

Alluvions anciennes.

Lias compacte, Calcaire du
Brian¢onnais.

Gypse et cargneules.
Schistes lustrés. TRIAS.

Gres blancs ou
bigarrés.

Serpentine, Variolite de la
Durance, et Euphotide.

Fig. 8.—Part of Map by Zaccagna and Mattirolo.
(Scale 1: 1,000,000.)

Triasico.
Permiano.

Calcescisti, Micascisti, Quarziti.

Roccie serpentinose, Eufotide,
Diahase.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 323

here traced portions of the two first-mentioned maps, which will
illustrate the position better than any words * (figs. 7 & 8).

Prof. Bonney + also declines to accept the ‘ schistes lustrés ” as
Triassic. He regards them as schists which have retained their
original stratification, and as forming the uppermost member of his
three Archean groups. If, then, the euphotides and diabases are
subsequent to the “ schistes lustrés,” they may still be of very con-
siderable geological age.

At its northern end, however, the variolitic series of Mt. Genévre
abuts against a normal compact limestone, the ‘“ Calcaire du Brian-
connais,” which is certainly above the horizon of the anthracitic
Carboniferous strata. Accurate paleontological evidence being
still wanting, even on Mt. Chaberton, we cannot state with cer-
tainty that this limestone is either Triassic or Liassic, but we
believe with Lory that our series has been erupted through it, as
well as through the dubious “ schistes lustrés ” or “‘ calcescisti” of
Zaccagna. ‘The eruptive group has suffered from folding, faulting,
and in some places from brecciation; but the earth-movements
that took place in this area at the close of the Eocene period would
amply account for these phenomena. In fine, we observe that
throughout Liguria and the western Alps the distinction between
the pre-Tertiary and Kocene serpentinous groups is becoming a
matter of pure stratigraphy t+. The existence of, at least, two
groups has been again and again accepted; but, in the absence of
the direct evidence afforded by the presence of derived pebbles of
these rocks in subsequent formations, the age often assigned to the
older masses may be looked upon with considerable caution. The
admitted exact resemblance of the igneous rocks themselves at
different horizons makes the most careful investigation all the more
desirable before an age is affirmed in any instance. As long as the
view that diorite, euphotide, and serpentine are formed by meta-
morphism from contemporaneous muds continues to be prominently
put forward, so long must the true stratigraphical position of Italian
and Alpine “ greenstones” be involved in considerable obscurity.
While we may accept with Lory a maximum age for those of
Mt. Genévre, we must in fairness merely style them Post-Carboni-
ferous until further evidence is forthcoming.

LX. Conprrions oF ForMATION.

In dealing with the question of the physical conditions that gave
rise to the variolitic series and its associated rocks, it is only fair to

* Tt is unfortunate for purposes of reference that the topographers have in
Gastaldi’s map written ‘‘ Mt. Genévre ” in place of “ Claviéres,” while precisely
the reverse mistake has occurred in that of Zaccagna and Mattirolo. In our
copy from the latter the name is omitted, the frontier being sufficient guide,

+ “On two Traverses of the Crystalline Rocks of the Alps,” Quart. Journ,
Geol. Soc. vol. xlv. (1889) pp. 96 and 80.

t See, for example, Mazzuoli and Issel— Sulla zona di coincidenza delle
formazioni ofiolitiche eocenica e triasica della Liguria occidentale,” Boll. R.
Comit. geol. d'Italia, vol. xv. (1884) p. 2.

324 MESSRS. G. A. J. COLE AND J. W. GREGORY

bear in mind that, even at the present day, there are numerous
authors who would question their eruptive origin. Scipion Gras* -
in 1844 went so far as to assert that dykes and veins were unknown
in connexion with the variolites, spilites, euphotides, and serpentines
of the Alps, which in Dauphiné and Savoy “ particularly affect the
anthracitic formation.” A more detailed examination of the base
of Le Chenaillet, however, would probably have modified this
opinion. When the French Geological Society visited the area in
1861, M. Hébert +, supported by M. Studer, maintained that the
compact rocks seen on the east side of the Val de Gondran (7. e. the
variolitic diabases) were nearly horizontal sediments which had been
metamorphosed by injections of serpentinous matter. This view,
however, was strongly opposed by Lory, and was certainly held by
only the minority of the members present in the field. We have
aiready referred to the opinion of some geologists as to the stratified
character of various ‘‘ pietre verdi.” It is not for us to enter into
the vexed question of the origin of serpentine and euphotide or of
other “‘ greenstones”; and we must content ourselves with a passing
reference to some of the more recent literature on this subject,
selecting papers that deal with the area of the Apennines and the
Alps. :

Prof. Bonney +, for example, has carried his studies on serpentine
as far as the masses of Liguria, and strongly insists on their intrusive
character. He also opposes the view that serpentine can be derived
from gabbro. In 1880 Issel $ criticized these opinions, and shortly
after published, with Mazzuoli ||, a paper in which it is suggested
that the serpentines were poured out as a warm impalpable mud on
the sea-flocr, where they underwent slow internal changes through
the action of vapours and liquids. The authors hold that such
changes would be competent to produce the diorites, euphotides,
granitones, and variolites so constantly associated with the ser-
pentines. Lotti 4], on the other hand, acknowledges and helps
to demonstrate the igneous origin of euphotide, and recognizes this
rock as the deep-seated type of diabase and basalt. But he differs
from Prof. Bonney when he asserts that serpentine may be derived
from ordinary basic rocks by alteration, through the permeation of
magnesian waters from below.

In connexion with this point it will have been seen that the
apparent passage from altered gabbro to serpentine at the Col
du Gondran is deceptive, and that we regard the serpentine as
resulting from an exceptionally basic mass formed in intimate
association with the normal and felspathic igneous rock.

* “Oonstitution géologique des Alpes centrales de la France et de la
Savoie,” Bull. Soc. géol. France, 2° sér. t. i. p. 728.

+ Bull. Soe. géol. France, 2¢ sér. t. xviii. p. 782.

+ “Notes on some Ligurian and Tuscan Serpentines,” Geol. Mag. 1879,
p. 362.
§ Boll. R. Oomit. geol. d'Italia, vol. xi. p. 183.

| ‘‘Relazione degli studi fatti per un rilievo delle masse ofiolitiche nella
riviera di Levante,” 2bid. vol. xii. (1881) p. 313.

“| “Contribuzione allo studio delle serpentine italiane e della loro origine,”
ibid. vol. xiv. (1888) p., 281.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 325

Turning to the compacter series, the abundant dykes show that
considerable activity was going on during the formation of the
variolitic lavas. In the field we pictured to ourselves a huge
volcanic cauldron, its centre being most probably among the great
intrusive masses of Mt. La Plane; in this basin, excavated in the
calcareous schists, the viscid lavas would heave and seethe upon one
another, the surfaces of junction between them. becoming coated
with spherulitic glass, the product of their more rapid cooling. A
crust would form from time to time across the crater, to be torn
through again by occasional explosive action. Hence agglomerates
would be formed intimately connected with the lavas, and spherulitic
glassy fragments would be abundantly thrown up, together with
globular masses of compacter rocks. As the andesitic lavas became
piled thickly upon one another, the new material would burst up
through rocks already solid, and would form the more crystalline
dykes of the Chenaillet ridge and Mt. La Plane. But even these
would prove their affinity to the earlier lavas by consolidating
against them with a vesicular and spherulitic selvage.

Indeed, it is this abundance of basic glass, now devitrified and
furnishing the “ variolite,” that makes the area of Mt. Genévre
remarkable among volcanos old or new. While it is probable that
many such centres may be recognized in Piedmont and the northern
Apennines, similar occurrences are rare in other parts of Europe;
and we believe that the best modern analogue is to be found in the
great craters of Hawaii. Although we do not pretend that the
compact andesites of Mt. Genevre possessed the marvellous fluidity
of the lavas of Kilauea, yet they must have borne, when fresh,
a remarkable resemblance to the well-known pahochoe of the
Sandwich Islands. The engraving in Dutton’s ‘ Hawaiian Vol-
canoes ’*, and the exquisite photographic view of the lava-floor of
Kilauea which accompanies a recent article by Prof. J. D. Danarf,
restore for us, as it were, the surface of our ‘ variolite-diabases ;”
while the vertical joint-faces in the foregrounds of these illustrations
hint at structures precisely similar to those seen on the aréte of
Le Chenaillet. Prof. Dana’s articles, indeed, considerably strengthen
the impression made upon us in the field. At Kilauea the lavas
have a glassy crust, which is often scoriaceous, and half an inch to
two inches thick. ‘The crust is a crater-feature,’ writes Prof.
Danas, ‘‘ for I have not seen it on the lavas outside....The lavas
exuded through the crust from the liquid mass below, above alluded to
as making seams, streamlets, and knobby surfaces, are covered some-
times with separable scoriaceous glassy crust, though commonly
having a solid glassy exterior half an inch or so thick.” At Mt.
Genévre, even allowing for the crushing and obliteration of delicate
scoria during earth-movements, the more solid glassy selyages
appear to have been everywhere predominant. But the scoriaceous
character of the diabases, and even of the edges of the massive
dykes, bears ample witness to the vapours that escaped throughout

* U.S. Geol. Survey, 4th Annual Report, publ. 1884, p. 98.

+ Amer. Journ, Sci. vol. xxxiv, (1887) pl. iv. p. 364.
t Ibid. pp. 354 and 355.

326 MESSRS. G. A. J. COLE AND J. W. GREGORY

the mass. Moreover, we probably find preserved for us only the
lower layers of the volcanic cauldron, and any pumiceous matter
of the final surface must have been removed by early denudation.

It is only natural that spherulites should occur in the glasses of
the Sandwich Islands, although they may not be on so bold a seale
as at Mt. Gencvre. Mr. E. 8. Dana* has recently described
spherulitic structure in a lithoidal lava from Mauna Loa; the rock
contained olivine, and the spherulites were of two kinds, light-brown
ones being set in a “nearly opaque spherulitic ground-mass.” On
pp. 451 and 459 of the volume quoted, Mr. E. 8. Dana mentions
similar structures in other rocks from Mauna Loa and Kilauea.
Moreover, his beautiful “fan-shaped or feather-like” groups of
augite in the ‘clinkstone-like basalt’ appear to be sections
of interesting, if imperfect, spherulitic aggregations.

Cohen + has also described a tachylyte from Hawaii with a
spherulitic ground-mass; and a specimen in the collection of the
Normal School of Science and Royal School of Mines shows small
brown spherulites, clustering more and more closely until the glass
passes into the almost opaque matrix of the basalt.

It would have been a harmonious conclusion to this comparison
if we could have classed our agglomerates as ancient aa lava-streams,
that 1s to say, as brecciated, rugged, and scoriaceous flows. But
neither the arrangement of the masses nor the globe-like bombs
correspond with the features so clearly described and figured by
Prof. Dana §, and we are led to treat these deposits as produced by
true explosive action. ‘The compact non-scoriaceous character of
the vast majority of the ejecta is paralleled, curiously enough, in
the “stones ” of the tuffs on Kilauea ||.

While the extent of these fragmental rocks does not seem to have
been sufficiently insisted on in the past, authors have often stated
their views as to the origin of the variolite itself. The great
advance in the discussion of this question appears to us to have
been made by Lory4], when he so clearly recognized the variolite as
a product of the rapid cooling of an igneous mass. After this
statement the various accounts of its discovery as a selvage to
diabase dykes in other districts have seemed in the highest degree
natural, and have met with ready acceptance.

Finally, if it is granted that the variolite of Mt. Genévre
represents a glassy lava-crust which has been deyvitrified by
slow secondary action, is there anything in the nature of the
compact diabases that will explain its relative abundance? If
the lavas were unusually fusible, the glassy condition might be
retained over large areas; but it is unfortunately impossible to
argue as to the exact original characters, chemical or physical,

* “Qontributions to the Petrography of the Sandwich Islands,” Amer.
Journ. Sci. vol. xxxvii. (1882) p. 452.

t Lbid. p. 448.

+ Neues Jahrb. fiir Min. &c. 1880, vol. 1. p. O1.

§ Amer. Journ. Sci. vol. xxxiv. (1887) pp. 362-364. | Zoid. p. 860.

{ Bull. Soc. géol. France, 2° sér. t. xviii. (1861) p. 782.

EE

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 327

of rocks so highly altered. The analysis made by Delesse * of
the variolite of Mt. Genevre corresponds closely with the average
composition of a number of Hawaiian lavas, as already quoted
in this Journal from the work of Coheny. But an average of
twelve analyses by Silvestrit differs in many respects from that

_ derived from Cohen’s figures, the percentages of silica and magnesia,

for instance, being distinctly lower. It seems, moreover, from the
experiments of Silvestri, that ease of fusion or a refractory cha-
racter cannot be ascribed to the predominance in these lavas of
any particular base$. We quote these averages for comparison
with the variolite, but fully recognize the extensive alteration
of the latter. We have excluded the two most altered examples in
dealing with the analyses of Silvestri.

i: EE, Il
Average Average

composition of | composition of

Variolite. Hawaiian lavas. Hawaiian lavas.

(Delesse.) (Cohen.) (Silvestri.)
eee. ss 52°79 51°71 48°25
PRONE cnae s,s os ss Li6 11°44 15:65
Oxides of Iron .... 11:07 12°62 : 16°59
Oxide of Manganese. trace — —
oo 5°90 10°75 8°40
Mjenesia ........ 9:01 7°59 3°70
REM, ons y+ 3°07 3°47 3°62
on) 116 0°67 1:57
Oxide of Chromium. trace _ —
Loss on ignition... 4:38 0-98 0-41

99°14

It is probable, then, that complete fusion, arising from abundant
access of water || or unusually high temperature, rather than any
chemical peculiarity, will best explain the wide extension of glassy
selvages in our area. But the occurrence of the variolite, with its
detailed analogy to the tachylytes of the present day, forms the best
proof, if proof were needed, of the igneous origin of the diabase-
series of Mt. Genevre.

X. Tue Conctustons or Previous AuTHoRs As To THE NATURE OF
THE V ARIOLITES OF OTHER LOCALITIES.

Though variolite is rare and local, a fairly long list of its oecur-
rences can be compiled. Of these, however, a considerable proportion
may be at once dismissed. as there are several very different rocks

* Bull. Soc. géol. France, 2¢ sér. t. vil. (1850) p. 480.

+ Quart. Journ. Geol. Soc. vol. xxxix. (1883) p. 457; Cohen, Neues Jahrb.
fiir Min. &c. 1880, vol. i. p. 41.

t “Lave del vulcano Kilauea,” Boll. R. Comit. geol. d’Italia, vol. xix.
(1888) p. 194.

§ Jbid. pp. 135, 141, 171, &e.

|| See Prof. Judd, “ The Natural History of Lavas,” Geol. Mag. 1888, p. 11,

Q.J.G.8. No. 182. ‘i

328 _ MESSRS. G. A. J. COLE AND J. W. GREGORY

included under this name. Thus, according to Valmont de Bomare*,
some of the specimens of West-Indian ‘‘Gamaicu” are pieces:
of madrepore ; possibly it has an oolitic structure. A second group
that must be removed is a series of hornblendic and actinolitic
schists; such are the variolites of the Varaita and Upper Po
valleys described by Gastaldi +, those from the Pellice valley near
Turin ¢, and the variolitic hornblende-schists of Transylvania §.
The third group to be removed are those amygdaloids known as the
‘‘ variolites of the Drac”||; they were rightly regarded as volcanic
by Lamanon{, who, having been persuaded by Faujas and others
that he was wrong, destroyed all but twelve copies of his work.
Brongniart ** has described from Pietra mala, and Mattirolo ++ from
Pria Borgheise, other variolites that are apparently amygdaloids ;
in the latter case the rock contains globules of calcite and chlorite,
without radial structure.

In most of the localities from which true variolite has been
recorded only pebbles of it have been found, and these may be
summarily dismissed as likely to throw little or no additional light
upon the nature of the rock. Such are the pebbles at Le Chatelard,
in Savoy $+; in the Emmenthal, in Switzerland $§ ; at Hausdorf and
other localities in Silesia||||; in the Remigiusberg, near Cusel in
Bavaria J]; in the valley of the Inn, at Braunau***. In Italy
they have been discovered at Chaumont near Susa Trf, at Fenes-
trelles *, Exilles ttt, Frejus $$$, Sestri near Genoa *, Monte Catini
near Volterra *, near Pietra Mala *, the Dora near Turin ||\\||, Ses-
triéres [J4J, near Monte Viso ****, &e. In the collection of the
Normal School of Science and Royal School of Mines there is a

* Valmont de Bomare, ‘ Dictionnaire raisonné universel d’Histoire Natu-
relle,’ t. viii. Lyon (1791), pp. 272-4.

t B. Gastaldi, Boll. Com. geol. Italia, vol. vii. (1876) p. 106. _

t Geinitz, Tsch. Min. u. petr. Mitth., Neue Folge, Bd. i. (1878) p. 152.

§ F. yon Hauer and Guido Stache, ‘ Geologie Siebenbirgens, Wien, 1863,
p. 209.
|| Gueymard, Ann. Mines, sér. 4, t. xviii. (1850) pp. 41-59.

€ De Lamanon, ‘ Mémoire Litho-Géologique sur la vallée du Champsaur et
la montagne de Drouvaire dans le Haut Dauphiné,’ Paris, 1784.

** A, Brongniart, Ann. Mines, vol. vi. (1821) p. 198, pl. i. fig. 4.

tt E. Mattirolo, Rend. Accad. Lincei, Roma, ser. 4, vol. ii. pt. 1. (1886) p. 646.

+t P.L. A. Cordier and Ch. d’Orbigny, ‘ Description des Roches,’ Paris, 1868,
9. 165.
‘ §§ Longius, /.c.; J. F. Kaufmann, Beitr. z. geol. Karte Schweiz, xi. 1872,
9. 375.
|||| E. Dathe, Jahrb. d. k. preuss. geol. Landesanst. fiir 1882 (Berlin, 1883),
p- 228-62 ; “ Variolite der Gabbrogruppe in Schlesien,” Zeitschr. deutsch. geol.
Ges. Bd. xxxiv. 1882, pp. 432-4.

44, A. Leppla, N. Jahrb. 1882, Bd. ii. pp. 134-5.

*** Chierici, Ann. Mines, vol. v. 1820, pp. 397-400.

ttt Morozzo, Mém. Acad. roy. Sci. Turin, vol. v. 1793, p. 165.

ttt Fournet, Ann. des Sci. phys. et nat. Soc. roy. d’Agric. Lyon, sér. 1, t. iv.
(1841) p. 156.

§§§ H. B. de Saussure, ‘ Voyages dans les Alpes,’ t. v. (1796) pp. 415-417.

|| ||| Eug. Geinitz, Tscherm. Min. u. petr. Mitth. i. (1878) pp. 186-153.

“44 Ibid. p. 146.

**** Robilant, Mem. Ac. Roy. Sci. Turin, i. 1786, p. 242.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 329

specimen of typical variolite, brought by the late Prof. Carvill
Lewis from Masasco, in Liguria; and we have recently received

from Mr. F. B. Parkinson, A.R.S.M., an excellent example from

Monte Penna, on the western frontier of Emilia.

Though this does not exhaust the list of recorded localities of
variolite as pebbles, there are but very few cases known of its
oceurrence in situ, viz.: the Fichtelgebirge *, Schonfels in Voigt-
landy, and the Harzt in Germany; Yalguba, near Olonetz, in
Russia ; Mont Genévre, Cesana Torinese §, Monte Loreto ||, the
Rochers de Rioubrent §], south-west of Monte Viso, and a few
other Italian localities.

Most authors agree that it is a structural modification of a basic
rock, whether euphotide, as was maintained by many French
geologists, as Fournet, Lory, Hébert, Gras, Cordier, d’Orbigny, and
Lévy, or of aphanite or diabase, as was held by Haiiy, Lossen,
Gimbel, Loewinson-Lessing, Rosenbusch, and others.

As to the nature of the modification, opinions differ materially.
The most unsatisfactory modern theory is that which regards the
varioles as included and metamorphosed fragments—a view advanced
by Giimbel **, and still held by him +7 in spite of the criticisms of
Zirkel $f and others. Chierici $$ maintained that the varioles were
formed by decomposition of garnets, which at first broke down into
black granules, and these, in a later stage, were bleached into the
typical varioles. The opinion, however, that is most generally re-
ceived regards variolite as the product of contact-alteration—a view
that has been accepted by, amongst others, Lory, Lévy and Fouqué,
Dathe, Leppla, Zirkel, Teall ||||, and Rosenbusch 94]. The last-
named author concludes that the opinion that variolite arises as an
“endomorphe Contactform der Diabase” hardly requires repe-
tition. There can be no doubt that many variolites have been
formed in this manner; but some, no doubt, have arisen as a
erust on lava. Loewinson-Lessing clearly recognizes *** that both
methods of formation have been in operation, as he divides the
variolites into two classes. He includes among the first group, or
contact-modification products, those of the Fichtelgebirge, Franken-

* ©. W. Giimbel, ‘ Die palaolithischen Eruptivgesteine des Fichtelgebirges,’
Miinchen, 1874, p. 31; N. Jahrb. 1876, pp. 42,43 ; Geognostische Beschreibung
des Konigreichs Bayern, Abth. iii. (Gotha, 1879), pp. 215-8.

t F. Zirkel, Ber. d. k.-sachs. Ges. d. Wiss. xxvii. (1875) p. 211.

¢ K. A. Lossen, Jahrb. d. k. preuss. geol. Landesanst. fiir 1880, pp. 10-12.

§ B. Gastaldi, Descriz. della Carta geol. Italia, ii. pt. 2 (Firenze, 1874), p. 28.

|| Mazzuoli and Issel, Boll. Comit. geol. Italia, vol. xii. (1881) p. 329.

“| D. Zaccagna, Boll. R. Comit. geol. Italia, xviii. (1887) p. 387.

** CO. W. Gimbel, N. Jahrb. 1876, p. 42.

tt C. W. Giimbel, Geologie von Bayern, Th. i. Lief. 1, 1884, pp. 78, 79.
tt F. Zirkel, Ber. d. k.-sachs. Ges. d. Wiss. xxvii. (1875) p. 211.

§§ Chierici, Ann. des Mines, v. (1820) p. 398.

||| J. J. H. Teall, ‘ British Petrography’ (London, 1886) p. 134.

“|4| H. Rosenbusch, ‘ Mikroskopische Physiographie der massigen Gesteine,’
Aufl. 2, Bd. ii. (1887) p. 227.

*** Ft, Loewinson-Lessing, “ Olonetzkaya Diabazovaya Formatziya,” Trud.
St. Peterburgskagho Obshch. Estest. xviii, (1888) p. 169.

330 MESSRS. G. A. J. COLE AND J. W. GREGORY

wald, and Voigtland, and doubtfully those of the Durance; the
second division, or the spherulitic augite-porphyrites, 1s constituted
by the variolites of Yalguba and some described by Geinitz. As will
have been seen by our previous description, the variolites of Mont
Genévre mainly belong to the second class.

Owing to the looseness with which the name “ variolite” has
been used, it will be advisable in this connexion to repeat our
definition of the term, although from the modern point of view
the rock would scarcely require a distinctive name. As the
variolite of the Durance was the first scientifically studied and
described, we think it ought to be regarded as the type, in preference
to the obscure ‘“ Variolites Lucernensis,” or the unknown Italian
rock described by Aldrovandus. We therefore define ‘ variolite ”
as a devitrified spherulitic tachylyte, typically coarse in structure.

The unaltered rock that is probably most closely related to
variolite is the spherulitic augite-andesite of the Vashegy mountain
near Telkibanya, in Hungary. For interesting information re-
specting this rock we are indebted to Dr. J. de Szddeczky, of
Budapest. .

The variolite of Yalguba, in Olonetz, also closely approaches that
of the Durance, and is of interest from the occurrence in the
matrix of small patches of a brown glass which have escaped
devitrification. This rock has been described in considerable
detail by Inostranzey * in 1874, by Loewinson-Lessing 7 in 1884,
and again by the latter author in his elaborate memoir “ Olonetz-
kaya Diabazovaya Formaziya” +t. Loewinson-Lessing seems in-
clined to abandon variolite as the name of a rock-species in favour
of spherulitic augite-porphyrite, retaining it, however, in the form
of “ variolitism ” for that of a process §. As variolitization seems
to have resulted from the same causes that have built up ordinary
spherulites, we do not see the necessity for the new term, especially
as its introduction would obscure the identity of the results that
have been produced by the action of similar causes on both the acid
and the basic rocks.

The above definition of variolite, however, excludes several rocks
that have been regarded as variolite; thus, that found by Dathe||
in the Culm Conglomerate of Silesia contains 75 per cent. of silica,
and certainly cannot be regarded as a basic rock, unless a considerable
proportion of the quartz is secondary. ‘The close association of this
variolite with gabbro and gabbro-conglomerate suggests that such
may be the case, though Dathe has abandoned his original view of
the connexion of the variolite and gabbro. Neither do we see any

* A. Inostranzev, “O Variolitye,” Verh. k. russ. min. Ges. St. Petersburg,
1874, pp. 1-28, pls. i. & ii.
te F. Lewinson-Lessing, Tsch. Min. u. petr. Mitth. vi. (1884) pp. 281-300,
pl. iv.
{ Trud.St.Petersburgskagho Obshch. Estest. xviii. (1888) pp. 29-896, pl. i—v.
§ Lbid. p. 169.
|| J. Fr. E. Dathe, Jahrb. k. k. preuss. geol, Landesanst. fir 1882 (Berlin,
1883), p. 254.

ON THE VARIOLITIC ROCKS OF MONT GENEVRE. 331

reason for regarding the spherulitic tachylyte of Carrock Fell * as a
variolite, since the basis is not devitrified. The minute size of the
spherulites would also debar Sordawalitey from ranking among the
true variolites ¢.

XI. Summary of THE CoNCLUSIONS ARRIVED AT IN THIS PAPER.

We believe, finally, that the discussion of the observations of
others and of ourselves justifies the following conclusions :—

The gabbro or euphotide south of Mt. Genévre j is associated with
serpentines, which were originally peridotites, and were not derived
from the alteration of the gabbro. These coarsely crystalline rocks
probably form a considerable subterranean mass, but have little
importance at the surface.

They were broken through by dykes of dolerite and augite-
andesite, and are now overlain by a great series of compact diabases
and fragmental rocks, which has no direct connexion with the
gabbro.

The variolite of the Durance occurs in situ as a selvage on the
surfaces of these diabases among themselves; as blocks in the
fragmental rocks, which are regarded by us as tuffs; and occa-
sionally as a selvage to the diabase dykes.

This product of “rapid cooling was originally a spherulitic tachy-
lyte, and has become devitrified by slow secondary action. Variolite
stands in the same relation to the basic lavas as pyromeride does to
those of acid character.

The eruptive rocks in the Mt.-Genévre area are probably post-Car-
boniferous; but their exact age cannot at present be determined.

There are several other areas of similar variolitic rocks among
both the Alps and the Apennines of Piedmont and Liguria.

The best modern representative of the conditions that produced
these rocks is to be found in the great volcanoes of Hawaii; and there
is nothing, either in their fundamental characters or in their mode
of origin, that cannot be paralleled among the products of causes
now in action.

In the preparation of this paper we have been guided at many
points by the kind advice of Prof. Bonney and Prof. Judd. We
have thus also been able to avail ourselves of several specimens and
sections in the collections of the Normal School of Science and Royal
School of Mines. Our indebtedness to those who have preceded us
on the classic ground of Mont Genévre is, we trust, fully apparent
‘in the paper.

* T, T. Groom, Quart. Journ. Geol. Soc. vol. xlv. (1889) p. 303.

+ F. Lowinson-Lessing, ‘‘ Die mikroskopische Beschaffenheit des Sordawa-
its,” Tsch. Min. u. petr. Mitth. ix. (1887) pp. 61-76.

t [By the kindness of Prof. Blake we have been enabled to examine the vario-
lite found by him near Careg Gwladys in Anglesey (Brit. Assoc. Rep. 1888, p. 11,
pl. v. fig. 22) ; as this is the first discovery of the rock in the British Isles, we
hope it ‘will be more fully described. |

oon ON THE VARIOLITIC ROCKS OF MONT GENEVRE,

EXPLANATION OF PLATE XIII.

[The numerator of the fraction expressing the degree of enlargement of an
object represents the magnifying-power of the objective with which it was
viewed. ]

Fig. 1. Crystal of plagioclase in the great porphyritic diabase on ridge of Le
Chenaillet, traversed by a crack and subsequently restored by mate-
rial optically continuous with the original crystal. x %.

2. Junction of diabase-dyke and gabbro, 8.W. spur of Le Chenaillet. The
diabase has a selvage of formerly glassy matter, green and somewhat
altered, and showing black globulitic aggregates. x 3.

3. Tuff containing fragments of altered scoriaceous glass and variolitic
rocks. ValduGondran. x 23.

4. Tuff containing fragments of greenish altered glass and of compacter
lavas with radial groups of plagioclase. Hast ridge of Gimont
Valley. x 23.

5. Porphyritic diabase of ridge of Le Chenaillet, some inches from its

variolitic selvage, showing radial grouping of the plagioclase. x 3%.

6. “ Pseudocrystallites ” and curving cracks intimately associated in large
spherulite in the variolite. North end of ridge of Le Chenaillet.
Xe: )

Discussion.

Prof. Bonney had been over the Mont-Geneévre, but had not reached
the exact area described by the Authors, though he had seen some of
the rocks mentioned. From his general knowledge of the district,
he appreciated how careful their description had been, and believed
with them that the variolites merely represented the pyromeride-
stage—a feature which, in his experience, was very rare amongst
the basic rocks. He stated that the Authors were correct in assign-
ing the gabbros and serpentines of the region to the ordinary Alpine
types, and was interested to learn that the variolite had nothing to
do with the gabbros.

Prof. Jupp also congratulated the Authors on their thorough
treatment of an interesting subject. He wished to correct a
mistake of his own: judging from specimens of Hawaiian rocks
which he had seen, he was led to suppose that the tachylytes of
Kilauea occurred in extensive masses; but Dana had shown that
the crusts of glass were never more than two inches thick.

Prof. Brake compared the variolite of the Durance with a rock in
Anglesey occurring in a similar way.

Mr. Gregory, in reply, said that though much of the old variolite
came from the north side of the ridge, nevertheless some of the rock
probably occurs in the valley to the south. It would be extremely
interesting to find a true British variolite in Anglesey. One of
the type-places in the Alps where there was supposed by E. de
Beaumont and others to be a passage from gabbro to serpentine
was this valley. The supposed serpentines which gave rise to this
ylew were not really examples of that rock.

A DEEP CHANNEL OF DRIFT IN THE VALLEY OF THE CAM, ESSEX. 333

19. On a Deep Cuoannet of Drirt in the Vatuny of the Cam, Essex.
‘By W. Wauiraxer, B.A., F.RS., F.G.8S. (Read March 12,
1890.)

For many years the rising-up of older rocks beneath the Cretaceous
beds of the London Basin, and beneath the Jurassic rocks to the
north and to the west, has been brought in evidence before us by
means of deep wells and borings. It may therefore be a welcome
change to notice an occurrence of an opposite kind, the evidence of
which is, in like manner, almost wholly owing to the well-sinker.

_ In Scotland long and deep channels, filled with Drift, have been
noticed, and have been referred to river-action*. In the northern
part of England, too, the like has been observed t+; but I am not
aware of the occurrence of such channels in Southern England,
except on a small scale, having been described. It is perhaps well,
therefore, to bring before the Society evidence that shows a sudden
and deep extension downward of beds of late geologic age, namely
the Glacial Drift, which are usually of no very great thickness, and
which, in the tract in question, occur chiefly on the higher grounds.

In the Geological Survey Memoir that treats of the part of
Essex that borders on Hertfordshire and Cambridgeshire, there is
an account of a well-section at Wenden, showing an unexampled
thickness of Drift at a comparatively low level, and also a descrip-
tion of two railway-sections that show the Drift abruptly abutting
against the Chalk +.

Although my former colleague, Mr. Penning, who mapped the
tract in question, near Audley End, wrote that “The Drift here-
abouts fills an old channel, one slope of which is shown in [one]
section, whilst another slope in a different direction, and at a
distance of half a mile, is exposed near the station,” he did not
then think the evidence clear enough to warrant further remark.

Lately, however, a good deal more evidence has turned up, for
which we have to thank Mr. G. Ingold, well-sinker, of Bishop
Stortford. It is not proposed, however, to lay before the Society
tne detailed accounts of the various new wells, these having already
been more fitly given to the Essex Field Club §. i

In the well-sections to be referred to there is, in some cases, a
certain amount of Post-Glacial Drift at the top; but this is com-
" paratively small (in no case, for certain, more than 20 feet thick),
so that it may be disregarded as a separate feature, and may be
massed with the underlying Glacial Drift. This latter consists

* A. Geikie, ‘‘Ancient River-courses underneath the Boulder-clay,” Trans.
Geol. Soc. Glasgow, vol. i. pt. ii. pp. 49-52 (1863). J. Croll, “River Channels
Buried under Drift,” 2bid. pp. 830-345.

+ T. M. Reade, “ The Buried Valley of the Mersey,” Proc. Liverpool Geol.
Soe. Session 14, pp. 42-65 (1873), &e.

t “The Geology of the N.W. parts of Essex,” &e., pp. 38, 39, 80 (1878).

§ See ‘ Essex Naturalist,’ vol. ii. pp. 49-54 (1889).

334 MR. W. WHITAKER ON A DEEP CHANNEL OF

mostly of loam and sand, more or less bedded, with clay (sometimes
apparently a Boulder-clay, full of pieces of chalk) and gravel.

It will be convenient to take the localities in order from south to
north, beginning at the head of the valley of the Cam, in the higher
part of which they all are (with a range of little more than six
miles), and working downward.

Quendon and Rickling.

Although the evidence here is of a far less striking character
than at the places to the north, and, indeed, might be passed over
did it stand alone, yet it may be well to note what has been
proved by well-sections, namely, that there is a greater thickness
than would have been expected of those beds of Glacial Drift that
crop out from beneath the great sheet of Boulder-clay, the sandy
and gravelly beds that Mr. 8. V. Wood called Middle Glacial. —

Thus, near Brick Kiln Cottages, N.W. of Rickling Green, just
above the 300-feet contour, the Chalk seems to have been reached
at a depth of about 83 feet, whilst it comes to the surface some
550 feet N.N.W. at about the same level. Again, in a well at the
south-western end of the Green, the depth to the Chalk is 60 feet,
at a level perhaps a few feet higher.

At the public well, by the side of the highroad opposite Quendon
Farm, and just below the 300-feet contour, a depth of 794 feet did
not reach the Chalk. An old well at “The Views” near by, but
rather higher, is 100 feet deep, and about 3 feet in Chalk. On the
eastern side of Quendon Hall Lane, some way below the 300-feet
contour, and some 400 feet from the highroad, the Chalk was
reached at the depth of only 18 feet ; but at Quendon Hall, further
north, the well ends in sand at 90 feet, the level of the ground
being about 300 feet.

On the east of Quendon the Chalk crops out, rising, at one part
of the western slope of the valley, to about the 300-feet contour.

Newport.

It is here that we have the greatest thickness of Drift hitherto
recorded, not only in Essex, but in the South-east of England, and
even there its base has not been reached.

At the southern end of the village, a well at Mr. Shirley’s
Malting, on the marsh just east of the stream, reached the Chalk
at the depth of 75 feet. On the eastern border of the narrow
marsh the Chalk seems to crop out at a distance of about 150 feet,
so that the westerly underground slope of the Chalk-surface is not
less than 1 in 2,

The most interesting well, of all that have to be referred to, is at
the other end of the village, and was made for the Grammar
School, on the site of the Castle, a little above the 200-feet contour
on the north of the Wicken Water. This boring begins just below
the boundary of the great sheet of Boulder-clay, and therefore we
have here to deal only with beds beneath that division of the

DRIFT IN THE VALLEY OF THE CAM, ESSEX. 335

Glacial Drift. Instead, however, of the usual comparatively thin
sand or gravel being found, the boring-tool, after passing to a depth
of 340 feet, chiefly through loamy beds, did not succeed in reaching
the Chalk, and the work was abandoned. The Drift, therefore,
must here go down to a depth of about 140 feet below the level of
the sea; how much deeper we know not.

As on the other, or eastern, side of the main stream, the Chalk
crops up at a distance of about 1000 feet, or a trifle more, and
only a little below the 200-feet contour, we have here, allowing a
difference of level.of 15 feet between the two sites, an easterly rise
of the underground Chalk-surface of at least 825 in 1000, on the
presumption that the Chalk would be touched at once on deepening
the bore, and that the Drift occurs right up to the eastern edge of
the marsh. We may fairly, therefore, call this a slope of about 1 in
3, over a long distance, and it may, of course, be steeper.

Wenden.

Hitherto we have been dealing with tracts where the great sheet
of the Drift spreads down to the bottom of the valley, though at
last on the western side only. From Wenden northward, however,
this sheet of Drift is cut through by the valley, the flanks of which
are then chiefly of Chalk.

It is at and near this place that the abrupt way in which the
Drift lies against the Chalk has been seen, in open sections, as
figured by Mr. Penning; and turning again to the evidence from
deep borings, we have here two sections showing a great depth of
Drift. |

One of these, at Mr. Collins’, north-eastward of Audley End
Station, and, measuring on the six-inch Ordnance Map, about
550 feet eastward of the “ Neville Arms,” reached the Chalk at the
depth of 220 feet. The other, which is somewhat nearer to the
outcrop of the Chalk, was made for some cottages belonging to Lord
Braybroke, and is on the southern side of the road, a little north
of the “* Neville Arms,” and about 650 feet W.N.W. from the former
well. In this case the Chalk was not reached until the boring had
been made to the depth of 296 feet.

As, by a measurement made by Mr. Ingold, the Chalk occurs at
only 3 feet below the ground (the 3 feet probably being soil)
at the railway, only 140 yards N.N.W. of the second boring, it
follows that, between these two places, there must be a fall of the
Chalk-surface of 293 feet. Presuming that they are at about the
same level (the site of the boring is probably a trifle the lower), this
is a slope of 1 in 1°43.

Mr. Collins’ well, though at a slightly lower level, seems to show
the beginning of the easterly rise of the Chalk, which rock is bare
at the lower part of the slope on the other, or eastern, side of the
valley, the Drift coming on again higher up, at about the 200-ieet

Q.J.G.8. No. 182. Da

336 MR. W. WHITAKER ON A DEEP CHANNEL OF

contour, whilst on the western side the mass of the Drift is at a
higher level.

Lnttlebury.

According to the Geological Survey Map (Sheet 47) this village
is on Chalk, capped in the eastern and lower part by River Gravel,
which, in its turn, sinks below Alluvium close to the river. There
was nothing, however, at the time when this map was made to
show the presence of Glacial Drift, or of anything more than a thin
narrow sheet of River Gravel over the Chalk; nor, indeed, is there
now any sign at the surface; the mapping is right, for the narrow
tracts of River Gravel and of Alluvium wholly hide the deep mass of
Glacial Drift which has been unexpectedly proved.

The position of various wells in the village and their depth to the
Chalk are shown in the map (fig. 1), which is from the new
Ordnance Map (Essex, Sheet 8).

Fig. 1.— Outline Map of Littlebury, with Sites of Wells.
(Seale 6 inches to a mile.)

SECTION /[j

4a
WI ‘
Tunnel

The figures stand for the depth to Chalk, in feet, at the wells.
The Geology has been indicated from the one-inch map (Sheet 47).

From this it will be seen that in five wells the depth to the{Chalk
is from 3 to 6 feet only, that being taken up merely by such top-
earth, soil, or trace of gravel as might be expected. In two other
wells, however, the Chalk was not touched for 15 feet, perhaps
from the occurrence of a pipe or small hollow of gravel. Another
well, the second to the north, ends in sand at a depth of 22 feet,
and therefore gives little information.

When, however, we turn to the one at about the centre of the
village, where the road to Saffron Walden leaves the highroad, we

7

DRIFT IN THE VALLEY OF THE CAM, ESSEX. 337

find that, after boring to the depth of 218 feet, the Chalk was not
reached, the whole being in Drift. Now, as in the next well to the
west, only 60 yards off, and at a slightly higher level, Chalk was
touched at the depth of 6 feet, it follows that there must be a fall
of the underground Chalk-surface of more than 212 feet in a
distance of 180, or about a slope of 1:2 in 1 (adding only 4 feet to
the 212).

As the last well was only carried 6 feet into the Chalk, it may be
thought that this might be merely a boulder; but it should be
noted that its evidence to the presence of Chalk in place 1s supported
by the other wells. Thus the one where the road to Royston
branches off, and which is only 125 yards from the deep Drift
boring, reaches the Chalk in 3 feet, and is carried 121 feet into
that rock. Again, the most northerly well, which is probably at
much the same level as the deep boring, reaches the Chalk in 6 feet,
and has been carried 19 feet into it, and this shows a fall of the
Chalk-surface of more than 212 feet in 270.

Turning to the other side of the valley, we find that the Chalk
rises up from beneath the Alluvium, and is bare of Drift until
reaching the higher ground, from which it follows that the under-
ground Chalk-surface must again rise abruptly eastward. A section,
therefore, through Littlebury from east to,west would be as in
fig. 2, presuming that the Chalk would soon be met with by

Fig. 2.—Section across Littlebury, from a little S. of W. to a little
NV. of £. (Scale 6 inches to a mile, or 880 feet to an inch *.)

Village.

3
~

|= a rama

— ;ij| —1_} :

1. Alluvium (and River Gravel).
2, River Gravel.

3. Glacial Drift.

4, Chalk.

* * Ordnance datum,
deepening the 218-feet boring, and giving the greatest possible lateral
extension to the channel of Drift: in other words, the slopes of the
underground Chalk-surface cannot be less than as shown, but may
be greater ; and it should be remarked that the vertical scale is not
exaggerated.

* Ordnance Datum (mean sea-level), The thickness of 1 and of 2 exaggerated
slightly, of necessity.

338 - MR. W. WHITAKER ON A DEEP CHANNEL OF

This section has been taken to about the 200-feet contour on
either side of the valley, and it should be noted that, whilst the-
boundary of the high mass of Glacial Drift just touches that con-
tour on the east, and then only just by the spot to which the
section has been taken, on the west that boundary is above the
300-feet contour, far beyond the limit of the section.

Nature of the Channel.

It may be well to notice three explanations of the channel that
certainly suggest themselves. ‘These are disturbance, sinking-in of
the Chalk, and erosion.

As to the first, there seems to be strong imagination wanted for
the acceptance of the idea of a fault of the throw and extent needful,
and that must have been brought about during or since Glacial
times. Moreover, there are no signs at the surface of such a fault,
which must affect the Chalk. The Drift beds, too, that fill the
channel are not such as occur on the higher ground around.

On the other hand, Mr. Ingold, to whom we owe our information
about the borings, asks ‘“‘ If the Chalk at Wenden has been ploughed-
out, how do you account for the soft white Upper Chalk with flints
being found at from 300 to 350 feet below the level of the same
kind of chalk at the outcrop near by? It seems to me more like a
settlement.” As, however, the Middle Chalk has a few flints in
part, there is some doubt whether Upper Chalk is present beneath
the thick Drift in the Wenden borings, though this pay pro-
bably goes down some depth in that neighbourhood.

To explain the occurrence of so deep a hollow over sae a length
of country by sinking-in of the gravel from dissolution of the Chalk,
is open to the objection that the infilling Drift differs from that on
the neighbouring hills, which, too, in most cases comes near or close
to the borings. Deep pipes in the Chalk we know to occur, but
these are very different things.

I can see therefore no other explanation than a cutting-out of
the channel by erosion of some sort, the effect being perhaps
strengthened by later dissolution of the Chalk, which might take
place more readily here than elsewhere. It is this explanation
only that gets over the difficulty of the peculiar character of the
Drift in the channel.

It would seem that the channel was cut out before the deposition
of the Boulder-clay over the higher ground, for we have no such
beds as those in the borings anywhere above the Boulder-clay, and,
on the other hand, they are more like the loams, &c. that occur
beneath the Boulder-clay elsewhere. The deepest boring of all,
too, at Newport, begins just at the base of the Boulder-clay.

Mr. Ingold thinks that the channel reaches northward to Whittles-
ford, the loam of the deep Newport boring being like that at
Whittlesford Bridge, near the station. This would add about 5
miles to the length of the channel, making it 11 miles. It is to be
noted,. however, that on the Geological Survey Map (Sheet 47) there

a

DRIFT IN THE VALLEY OF THE CAM, ESSEX. BI 3tY)

are two breaks in the continuity of the Glacial and River Drift
along the valley, bare Chalk being mapped between Wenden and
Newport, and again south of Littlebury. Whether further exami-
nation, with fresh evidence, may show the Drift to be continuous is
a question to be decided. If the Chalk in the parts mentioned be
really bare of Drift, then the channel is not continuous, or, at all
events, was in parts so shallow as to have been destroyed in the
erosion of the present valley. Between Littlebury and Whittlesford
Bridge, a narrow channel, filled with Glacial Drift, may occur
beneath the River Drift and the Alluvium, and may be proved by
future wells; but we may perhaps have a set of long narrow basins
instead of one more even and continuous channel.

[ Postscripr.—A well-section at Whittlesford has been given on
page 20 of the Geological Survey Memoir, ‘The Geology of the
Country between and south of Bury St. Edmund’s and Newmarket”
(1886). Specimens, since seen, show that the bed described as
blue clay is a hard grey calcareous band, like some of the loams in
the borings alluded to above. |

Discussion.

Dr. Evans thought the Author’s conclusions would generally
commend themselves to Fellows. He gave reasons for rejecting the
supposition that these particular depressions were due to chemical
solution of the Chalk, and believed that, at the time the depressions
were formed, the district was more elevated than it is at present.
Under such conditions valleys would be rapidly denuded with an
increased rainfall. There was one curious feature, viz. that the old
configuration of the country was sufficiently distinct for the existing
valleys to follow the same lines as those of an earlier age. This ele-
vation of the country to some extent corresponds with that required
py Mr. Prestwich in connexion with the Westleton Beds, and the
axis might well have taken the direction which that Author had
inferred.

Mr. Crpmenr Rem had found several of these old valleys in the
North of England, but felt some diffidence in comparing an old valley
in hard rocks with one in soft rocks. He suggested as a possibility
that the Essex depression might not be a river-channel but a lake-
basin, and was desirous of knowing whether it corresponded with
the general direction of movement of the ice.

Mr. Tortry was inclined to think that the Preglacial-channel
explanation was the most likely one. In Northumberland, the
Blyth was, in Preglacial times, a tributary of the Wansbeck, and a
deep Preglacial valley, which was filled with Glacial drift, occurred
between the present valleys.

Mr. J. Arren Brown asked why such hollows were called Pre-
glacial, rather than Glacial.

Dr. G. J. Hiypr asked whether there were any striated or foreign
pebbles to be met with in the lower beds of the Drift in the
depression.

Q.J.G.8. No. 182. 2B

340 A DEEP CHANNEL OF DRIFT IN THE VALLEY OF THE CAM, ESSEX.

The Avrnor, in reply, maintained that the occurrence of deep
Drift at various places along the valley-bottom pointed to the
existence of a more or less continuous channel or line of basins with
the longer axis along the valley. He had not asserted that the hollow
was Preglacial, but that it was either Preglacial or early Glacial.
There was no evidence of striated pebbles, which could hardly be
expected in the materials brought from a small bore-hole; still the
deposits were of the nature of Glacial accumulations.

Quart.Journ.Geol See Vol. XLVI PL XIV.

Sait

; aoe ho” F
Pay ORS Deon >

M P Pex ker delet iit! We NITLa

Ncottish Andesites and Propylites.

Quart.Journ Geol. Soe Vol. XLVI. PI XV

West, Newman im

AW 3 | -/
Varieties of Andesite, [en Hiant.

ON THE PROPYLITES OF THE WESTERN ISLES OF SCOTLAND. b41

20. The Propyuires of the Wustern IsiEs of Scornanp, and their
Retation to the Anpestres and Diorrres of the District. By
Prof. Joun W. Jupp, F.R.S., F.G.S. (Read February 5, 1890.)

[Puares XIV. & XV.}
I. Introduction.
II. Previous Literature.
Ill. Physical Characters and Chemical Composition of the Scottish Pro-
pylites.
IV. Microscopical Characters.
V. Relations of the Scottish Propylites to the other Rocks of the District.
A. Geological Age.
B. Structure.
C. Nature of Roch-masses.
1. Lava-streams,
2. ‘ Cupolas.”
3. * Laccolites.”
VI. Nature of the Original Rocks from which the Propylites haye been formed.
A. Amphibole- and Mica-andesites and Diorites.
B. Pyroxenc-andesites and Pyroxene-diorites.
VII. Causes by which the Propylitic Modification of these Rocks has been
brought about.
A. Solfataric Action.
B. Contact-Metamorphism.
VIII. Light thrown by the Study of these Tertiary Layas on some of the Older
Volcanic Rocks (Porphyrites, Felstones, &c.).
IX. The Younger Augite-andesites (‘‘Tholeites,” “ Pitchstones,”’ &c.) of the
Western Isles of Scotland.
X. Summary of Results.

I. Lyrropvucrion.

THERE exists in the Western Isles of Scotland a great series of lavas
which, for the most part, underlie the ophitic olivine-basalts, and
constitute the oldest of the ejections of the great Tertiary volcanoes
of that district. These rocks were distinguished by me in 1874
under the old English field-name of “ Felstones,” and it was stated
that they “ vary in colour from black, through various shades of
green and grey to white; but in almost all cases their surfaces
acquire a white crust in consequence of weathering action ”*.

In attempting, at that date, to define more exactly the characters
of these lavas, by studying them microscopically in thin sections, I
was confronted by two difficulties. In the first place, it soon be-
came manifest that these more acid lavas of the Western Isles in-
clude a great variety of types—differing widely from one another in
mineralogical constitution and in structure; and in the second
place it was found that the minerals of which these rocks were
built up were in a remarkably altered condition.

In both these respects, the ‘felstones” present a very striking
contrast to the overlying series of ophitic olivine-basalts. The latter,
as I have shown 7, are remarkable for their uniformity of composition

Q.J.G.8.. No. 183. 2¢

342 PROF, J. W. JUDD ON THE PROPYLITES

and character, and, except where influenced by surface-agencies,
seldom present any great signs of alteration; they are indeed,
as a rule, singularly fresh and unchanged in their appearance.

But in the “ felstones ” which underlie the basalts the most ex-
treme metamorphism is seen to have taken place; the felspars are
found to be so completely kaolinized that it is sometimes impossible to
decide whether they should be referred to orthoclase or to plagio-
clase; the pyroxenes, amphiboles, and micas are converted into iso-
ropic mixtures or into minerals of the chlorite group; while in
many cases the formation of epidotes and other secondary minerals
at the expense of the original constituents of the rock has gone on
to such an extent as to completely obliterate their distinctive charac-
ters. It may be safely asserted of many of these rocks that they
are at the present time entirely made up of secondary minerals, the
porphyritic constituents being represented by pseudomorphs, while
the ground-mass has been completely recrystallized.

In 1874 I had been able to study only a few of the leading types
of these rocks microscopically, and consequently did not feel justified
in attempting a complete diagnosis of their varieties ; therefore I con-
tented myself with the grouping them under a convenient field-
name.

During the last fifteen years, however, I have devoted much time
to the study of these rocks both in the field and in the laboratory.
The result of these studies is to show that among these “felstones ”
there are presented to us many interesting types of rhyolites, dacites,
and sanidine-trachytes, intercalated with which are a few basalts,
some of them of the same ophitic type as those so abundantly poured
out at a somewhat later date. . With these there also occur certain
rocks which are so remarkable in their mineralogical constitution
and structure that they do not seem capable of being referred to
any of the accepted petrographical ty pes ; and these anomalous
rocks I hope to describe on a future occasion.

But the great majority of these Hebridean “felstones ” prove to
belong to the family of the andesites, and to that ‘‘ pathological
rene ”* to use Rosenbusch’s expressive term, to which the name
of “ propylite ” has been given.

The delay in publishing the results of .my researches upon these
curiously altered rocks has not been unattended with advantage.
Many interesting details concerning the propylitic rocks of other
areas have been published in the interval both in Europe and in
America: and during the same period there have appeared several
very important memoirs on the rocks of the Faroe Isles, Iceland, and
Greenland—districts in which the Tertiary igneous rocks present the
most marked analogies with those of our own Western Isles t. The
comparison of the much altered Scottish rocks with the very fresh
examples in these several districts has often afforded valuable aid
in the interpretation of the former.

* Rosenbusch, ‘Massige Gesteine,’ Ond ed. p- 691.
t See Q.J.G.S. vol. xli. (1886) p. 53.

OF THE WESTERN ISLES OF SCOTLAND. 343

II. Previous Literature.

In his great work on the Geology of Hungary, Beudant, as early
as 1822, distinguished a series of rocks presenting very well-marked
features, to which he gave the name of “‘ porphyres trachytiques ”’*.

In 1860, Baron von Richthofen proposed to separate these rocks
from the ordinary trachytes (andesites) of Hungary and Transyl-
vania under the name of “ greenstone-trachytes ” t; and this term—
indicating their analogies both with plutonic and with volcanic
rocks—was very generally accepted by von Hauer, Stache, and the
other geologists of Austria.

In 1868, however, von Richthofen was led by his study of the
voleanic rocks of California and Nevada to abandon the term
“‘ oreenstone-trachyte” in favour of that of ‘propylite;” he was
induced to make this change from his conviction that, in Hungary
and Transylvania, as well as in the western districts of the North-
American continent, the rocks in question were the earliest
erupted of the whole series of Tertiary lavas ¢.

In 1875 the late Mr. Poulett Scrope, who was well acquainted with
the Hungarian rocks, pointed out to me the close similarity between
many of the features exhibited by the volcanic rocks of that country
and those which I had described in the Western Isles of Scotland.
In consequence of his advice, and with his friendly assistance, I
visited Hungary and Transylvania in that year, and some of the
general results of the comparisons then made were submitted to this
Society shortly afterwards. The conclusion at which I arrived with
respect to the ‘*‘ greenstone-trachytes” or ‘“ propylites ” of Eastern
Europe was that, while they have intimate relations on the one
hand with the andesites, and on the other hand with the diorites
of the same district, yet many of their peculiarities are certainly
due to their having undergone great alteration, especially in con-
sequence of having been acted upon by acid vapours §.

The name “ propylite,” as distinctive of a well-marked group of
rocks, was adopted by Mr. Clarence King and other members of the
United-States Geological Survey engaged in the exploration cf the
Western Territories, and the term thus became familiar to all stu-
dents of American geological literature, while its use in Europe still
continued to be very restricted.

In 1876, however, Prof. Zirkel published the results of his micro-
scopical study of the North-American rocks; and in this work he
endeavoured to define the particular characters which seemed to
justify the retention of the ‘“‘propylites” as a distinct type of
rocks ||. Dr. Zirkel pointed out that, while in their geological re-
lations the propylites are clearly associated with the Tertiary

* Voyage Minéralogique et Géologique en Hongrie, tome iti. p. 344,

+ Wien. Geol. Verhandlungen, xi. (1860) pp. JL 94, and Jahrb. k.-k. geol.

Reichsanstalt, Wien, xi. (1860) pp- 154-276.
+ Mem. California Acad. of Sci. vol. i. (1868).
y Q.J.G.S. vol. xxxii. (1876) p. 298.
| Microscopic Petrography, vol. vi. of the U 8, Geol. Expl. of the Fortieth

Parallel (1876), pp. 110-121.
202

344 PROF. J. W. JUDD ON THE PROPYLITES

lavas, yet in the characters of their constituent minerals and in the
enclosures which these minerals exhibit they present the most —
remarkable analogies with some. of the older dioritic rocks. Vom
Rath also adopted the same view as Zirkel as to the close relations
existing between the propylites and plutonic rocks and their dis-
tinction as a group from the andesites.

In the first edition of his very valuable work ‘ Mikroskopische
Physiographie der Massigen Gesteine, published in 1877, Professor
Rosenbusch not only refused to accept the term ‘‘ propylite” as dis-
tinctive of a group, but classed many of the rocks that had been
described under that name by other authors among the andesites.
In 1879, Dr. Doelter showed that the Hungarian rocks which pre-
sent the peculiar features held by von Richthofen and Zirkel to be
characteristic of the propylites, could be seen to pass by insensible
gradations into ordinary andesites *; and the view that the propy-
lites were really altered forms of the andesites, was very forcibly
upheld by Rosenbusch in a review of Doelter’s memoir, published
shortly afterwards f.

In the same year Dr. Wadsworth strongly insisted that the dis-
tinction between propylites and andesites could not be maintained
in the case of the North-American rocks ¢.

Dr. Szabo of Buda-Pest, Dr. Anton Koch of Klausenburg, and
Dr. KE. Hassak of Gratz, have all expressed the opinion .that the
propylites of Eastern Europe are really altered forms of the an-
desites.

The publication in 1882 of Mr. George F. Becker’s “ Geology of
the Comstock Lode and the Washoe District” marks an important
epoch in the history of the propylite controversy §. Mr. Becker,
while still continuing to classify the diorites and other plutonic rocks
as Pre-Tertiary, maintained that the propylites could not be regarded
as a distinct group of rocks, but only as a distinct “facies” or
“‘ habitus” of the andesitic lavas. As the result of a microscopic
study of a large series of specimens obtained during the construc-
tion of the Sutro Tunnel, and the numerous deep workings of the
Comstock Lode, Mr. Becker was able to show how, by the gradual
alteration of their constituent minerals, the hornblende- and augite-
andesites could be seen to gradually acquire those peculiar cha-
racters which had been held to be distinctive of the propylites. —

Not less important as a contribution to this interesting question
is the very remarkable memoir of Messrs. Arnold Hague and J. P.
Iddings, ‘On the Development of Crystallization in the Igneous
Rocks of the Washoe District ”||. The authors of this memoir,
while fully accepting the conclusions of Mr. Becker that the pro-
pylites of the Washoe district are simply altered forms of the
andesitic lavas, went much further, and proceeded to show that the

* Verhand. d. k.-k. geol. Reichs. 1879, p. 27.

| Neues Jahrb. fiir Min. &e. 1879, p. 648.

t Bull. Mus. Comp. Zool. vol. v. (1879) p. 285.

§ United States Geol. Surv. Monograph iii. (1882).
|| Bull. of the U.S. Geol. Surv. No. 17 (1885).

OF THE WESTERN ISLES OF SCOTLAND. 345

distinction between the Tertiary hornblende- and augite-andesites
and the supposed older diorites and diabases could no longer be
maintained. This conclusion they were able to establish by acaretul
examination of the extensive materials collected by the officers of
the United-States Geological Survey. They proved that the diorites
are only deep-seated portions of the rocks, which are poured out at
the surface as hornblende- or mi¢a-andesites, and that both alike are
of Tertiary age; the differences between them were shown to be
due, not to the period of their formation, but to the more perfectly
developed crystallization in the deeply seated masses. ‘The “ dia-
bases ” of the district were also proved to be similarly related to
the augite-andesites.

In the second edition of his ‘ Massige Gesteine,’ published in
1886 and 1887, Professor Rosenbusch admirably summarizes the
results which have been obtained by the study of both the European
and the American propylites. Admitting, with von Richthofen and
Zirkel, the extreme modification of the constituent minerals, and
the frequently well-developed crystallization, that recall so strik-
ingly the characters of the diorites and diorite-porphyrites, he shows
that the former characters are unquestionably due to the peculiar
kind of alteration that the rocks have undergone. The term “ pro-
pylite ” is therefore accepted only as serving to distinguish a well-
marked and interesting facies of the andesitic type of rocks—“a
pathological variety,’ employing Rosenbusch’s apt designation.
Used in this way, the term propylite may still be of great service
to petrographers and field-geologists as a descriptive name ; just as
the terms shale, melaphyre, and porphyrite are convenient, and
even necessary to us, for describing peculiar modifications of clay,
basalt, and andesite respectively. It is in this sense that I propose
to use the term propylite in the present memoir.

I shall be able to show that a careful study of the oldest Tertiary
igneous masses in the Western Isles of Scotland makes us acquain-
ted with a series of rocks presenting all the distinctive features of
the “ greenstone-trachytes” of Hungary and Transylvania, and of
the “ propylites ” of California and Nevada.

I shall endeavour to illustrate the exact nature of the processes
by which ordinary andesites (and rocks which in their structure
and degree of crystallization are intermediate between andesites and
diorites) have been converted into the curious varieties that present
all the characters of the “ greenstone-trachytes” or “ propylites ”;
and it will be my especial aim to investigate the exact causes to
which these peculiar modifications must be assigned.

~

Ill. Puysican Cuaracrers AnD CuHemicat Compostrion OF THE
Scorrisn PRopyrires,

In colour these rocks vary from a very dark grey, almost black
tint, through many lighter shades, to varieties that are nearly white.
Usually, however, more or less marked green tints are exhibited by
them, and in some cases this colour becomes very pronounced.

346 PROF. J. W. JUDD ON THE PROPYLITES

Though often very dark-coloured, their lustre is usually dull, and
they seldom if ever exhibit the jet-black tint and velvety aspect so-
often found in the olivine basalts of the district. The rocks are
usually, though by no means invariably, of porphyritic structure, and
the crystals of felspar have the opacity and the absence of vitreous
lustre so often seen in the more ancient and plutonic rock-masses.
Not unfrequently rocks that appear at first sight to be perfectly
compact.are shown by their mode of weathering to have been
originally made up of angular or rounded fragments, a conclusion
which is confirmed by microscopic study. Under the microscope,
indeed, many compact and seemingly homogeneous rocks are seen to
present all the characters of volcanic agglomerates and tufts, and are
found tio be composed of a great variety of ejected fragments.

On freshly fractured surfaces or on faces that have been weathered,
these rocks often exhibit evidence of possessing a strikingly banded
and fluidal structure, and, under the same conditions, the porphy-
ritic habit which is so general in these rocks becomes very con-
spicuous. It is very remarkable to find that many rocks which
are of a uniform dull grey colour, and apparently quite homogeneous
or compact in texture, must originally have presented all the charac-
ters which distinguish flowing lava-streams or beds of scorie and
lapili. These conclusions as to the original characters of the vol-
canic materials are fully confirmed, as we shall see when we come to
study their microscopical characters. It is evident that the altera-
tion, attended in many cases with an almost complete recrystal-
lization of their materials, has effectually masked their original
characters.

Many of these rocks were evidently originally scoriaceous ; and, as
the result of weathering, these often assume at the surface their
pristine slaggy appearance. In many cases the cavities are occupied
by aggregates of epidote- (pistacite) crystals usually enveloped in
zeolites ; and these clusters of green crystals, by the weathering-out
of the surrounding zeolites, stand up in relief on the exposed surfaces
of the rocks. Veins and nests of epidote also abound in many of
these rocks. In other cases the black enclosures (originally green)
to which Macculloch gave the name of Chlorophaeite are very con-
spicuous. 7

Vitreous varieties of these rocks sometimes occur, and such per-
fectly glassy parts of the rocks often exhibit but little alteration.
The same fact is illustrated in the andesites of the Cheviot Hills,
where the glassy portions are far less altered than the associated
stony portions of the same mass. It would seem that these glassy
varieties resist the percolation of solvents through their mass to a
much greater extent than rocks made up of aggregates of dissimilar
particles, and thus remain in a comparatively unaltered state.

The white crust which covers the weathered surfaces of the Scot-
tish propylites has been already referred to as one of their most dis-
tinguishing characteristics. The origin of this white crust appears to
be as follows:—by changes, which will be hereafter described,
much of the iron has separated as secondary magnetite. Almost

OF THE WESTERN ISLES OF SCOTLAND. 347

everywhere in the Western Isles the rock-surfaces are acted upon
by peaty waters; and just as brown sandstones and other ter-
ruginous rocks become bleached by this action, so do the igneous
masses, which have been rendered more permeable by the extensive
alteration of their constituent minerals, become bleached to the
depth of a few millimetres from the surface. That this is the true
explanation of the phenomenon is confirmed by a microscopic study
_ of these white crusts themselves, and of the parts of the rock where
they graduate into the dark-coloured mass.

Another distinguishing characteristic of the Scottish propylites is
the presence of considerable quantities of pyrite and other sulphides
diffused through their mass. Certain rocks about Salen in Mull,
and in Ardnamurchan, for example, when broken, are seen to be
studded all through their mass with pyrite-crystals. In other cases
marcasite and chalcopyrite are found, and these sulphides are often
present in such quantity as to constitute an important constituent
of the rocks. All who are acquainted with the ‘“ greenstone-tra-
chytes ” of Eastern Europe and the ‘“ propylites” of the Western
Territories of the United States will recognize this as a feature
which they present in common with the Scottish rocks. In one case
I have found metallic copper forming thin plates scattered through
the rock.

One of the readiest means of distinguishing the dark-coloured,
much-altered andesites from the overlying olivine-basalts is by a
determination of their specific gravity. While the gabbros, dolerites,
and basalts have a density which always approaches to and some-
times exceeds 3, the propylites and their deep-seated representatives
have a distinctly lower specific gravity, ranging from 2°4 to 2-9 *.

During the last fifteen years, I have been able to compare the
results of a great number of determinations of the specific gravities
of the Scottish propylites, which have been carried out by various
methods, in the geological laboratories of the Normal School of
Science and Royal School of Mines. Some of these determinations
have been kindly made for me by Mr. Grenville Cole, F.G.S., or by
students working under his supervision ; others have been contri-
buted by Mr. W. B. D. Edwards, Mr. T. H. Holland, Mr. J. W.
Evans, F.G.S.,and Mr. W. F. Hume, F.G.S., working in the Research
Laboratory of the school, and these gentlemen have spared no pains
in obtaining and verifying their results.

A comparison and analysis of the great mass of specific-gravity
determinations thus placed at my disposal shows that the propylites
of the Western Isles of Scotland may be roughly classed in two
great groups-—those in which the specific gravity ranges from 2:4 to

* Shortly after the appearance of my first memoir on these rocks in 1874,
Mr. W. Walker, F.G.S., wrote to inform me that, having visited the district
described by me, in company with Mr. James Durham, he had been led to devise
a portable balance for the purpose of obtaining rapid and approximately accu-
rate determination of the specific gravity of rock-specimens. ‘This balance proves
to be of great service, as it can be employed by the geologist when he is far

away from the resources of a laboratory. (See Geol. Mag. dee. ii. vol. x. p. 109,
and Proc. Geol. Assoc. vol. viii. p. 278.)

«
348 PROF. J. W. JUDD ON THE PROPYLITES

2°7, and those in which the limits are 2°7 and 2°9. As a general
rule (though colour is often a very unsafe guide) the former group.
comprises pale-coloured rocks, while the latter are generally dark-
coloured.

The less dense, pale-coloured rocks, we shall presently see, were
originally hornblende- and mica-andesites, and the heavier dark-
coloured rocks are, for the most part, pyroxene-andesites,

Looking more closely into the results, we find that differences in |
specific gravity in each of these classes of rocks is dependent first,
on the degree of development of crystallization in them, and secondly
on the amount of chemical alteration which they have undergone.

As an example of difference of density in the more acid types, I may
cite the case of the hornblende-propylite of Beinn Talaidh (Beinn
Talla) in Mull. In the deep Corry of Tomsléibe the rock is highly
crystalline, and, indeed, approaches a diorite, having a specific
gravity of 2°68; while in the upper and superficial portions of the
mass the rock is compact, and has a density of 2°60. Glassy
varieties of the amphibolic rocks have a density of only a little over
2-4, :

Among the more basic types, I may cite the pyroxene-propylites
of Mingary Castle in Ardnamurchan. Highly crystalline forms of
this rock have a density of 2°88, while the specific gravity of the
compact varieties of the same rock is only 2°75. At Bealach a’
Mhaim, in Glen Brittle, we find a rock of this type with a specitic
gravity of 2°89, which passes locally into a glass with a density of
only 2°63.

The effect of the processes of alteration upon these rocks is
generally to lower their specific gravity. Thus the much altered
horublende-propyhites, with abundant chlorite and epidote developed
in their mass, are found to have a density of 2-5, or even less, while
the similarly altered pyroxene-propylites have a density which
seldom much exceeds, and sometimes does not reach 2°7.

In cases where it is not practicable to make a complete chemical
or microscopical study of the rocks, a determination of specific
gravity affords a much safer criterion for their discrimination than
colour. Some of the hornblende-propylites are of a very dark grey,
and indeed almost black colour, though seldom exhibiting the lustrous
jet-black of the olivine basalts ; while, on the other hand, extreme
alteration may sometimes cause the pyroxene-propylites to assume
a pale grey and almost white colour.

The distinction of the Scottish propylites into two groups is borne
out when we examine their chemical composition. A number of
chemical analyses have been made for me by Mr. T. H. Holland in
the Geological Research Laboratory of the Normal School of Science,
and for some silica determinations I am indebted to Mr. Grenville
Cole, F.G.S., and Mr. J. H. Power. J am also under great obliga-
tions to my colleague Professor Thorpe, F.R.8., for allowing a number
of analyses of these interesting rocks to be carried out under his
direction in the chemical laboratories of the same Institution. ‘These
analyses enable us to make comparisons between the different types

OF THE WESTERN ISLES OF SCOTLAND. 349

of propylites of the Western Isles of Scotland and those of Hungary
and Transylvania, on the one hand, and of the Western States of
North America, on the other, the chief districts in which they have
been studied.

_ Asa type of the analyses of the more acid varieties of the Scottish
‘propylite we may cite that of the rock of Beinn Talaidh—a horn-
blende-andesite passing into a diorite—placing side by side with it
a European and an American rock of analogous constitution.

dis due Ty,
BOA sy, dex ae ¢) ara ni 62°89 63°05 63:13
J 14°84 14:18 16:00
Peencoxide. .... 9:20 Wes vy 434
IBETVOUS OXIDE seis, soya due 6°71 1°52
Manganic oxide ..__ trace
| 3°61 o-t0 445
PIES. a... 5 4 a0 0:37 1-12 2°07
is og in ani) 4-01 5°65 3°87
[oe 2°91 349 2°65
Loss on ignition... I-41 2:04 2:00
car 99-24 101-64 100:03

I. Analysis of highly crystalline hornblende-propylite from the
deep Corry in Beinn Talaidh, Mull, made by T. H. Holland, 1889.

IJ. Analysis of hornblende-andesite (propylite) from Tokay
(Banhof), Hungary, by K.v. Hauer, Verh. k.-k. geol. Reichsanst.
1869, p. 146.

Itt. Analysis of hornblende-mica-andesite (propylite) from Cross
Spur Quarry, Washoe, made by R. W. Woodward, 1875.

A good type of the more basic pyroxene-propylites of the Western
Isles of Scotland is found in the much altered rocks exposed on the
western slopes of the Beinn More in Mull, and between that moun-
tain and‘A Chioch. Analyses of European and American rocks are
added for comparison with it.

Ti. ive i it 9

oo) a 58°07 59°56 58°44.
oo ———a 17°62 20°38 SS gl Ay
Ferric oxide .... 4°07 ST
Ferrous oxide .... 3°09 nai 6°03
Manganic oxide .. traces
ES cr, a. ase! ons 5°23 6°82 6-19
Magnesia........ 146 x71 2°40
oh 33] 1-49 3°20
oS) 2°15 1°25 1:97
Loss on ignition.. 4:15 1°85 3°63*

Total. :<«x«.eckhOusue L00°93 100-03

* Including 2°87 per cent. of Carbonic Acid.

350 PROF. J. W. JUDD ON THE PROPYLITES

I. Analysis of much altered pyroxene-propylite from Beinn More,
Mull. Made by G. H. Perry in the Chemical Laboratory, Normal:
School of Science.

II. Analysis of augite-andesite, Gyetva, Hungary, by Wymietal
in T'schermak, Min. Mittheil. 1868.

III. Analysis of pyroxene-andesite (containing hornblende) from
the north-east of American Flat, Washce. Made by W. G. Mixter,
PASTS.

While, however, it is convenient to make a broad general distinction
between the usually pale-coloured and lighter amphibolic varieties
and the dark-coloured and heavier pyroxenic forms of these rocks,
it must be confessed that the division into acid and basic types of
propylite is of no great value. Even when there is no free quartz
present, either of primary or secondary origin, the variations in the
proportion of porphyritic crystals to base lead to wide variations in
the ultimate chemical composition of the different rocks. In this
way we often find that pyroxenic rocks are of more acid character
than amphibolic ones. The extreme modification, too, which many
of these lavas have undergone leads to most remarkable changes in
their colour, specific gravity, and chemical composition, and still
further leads to breaking down the distinction between the two types
which, for convenience of description, we have sought to institute.

IV. MicroscorrcaAL CHARACTERS.

The microscopical characters presented by these lavas may be
summarized as follows :—

Although many of the rocks must have originally contained much
vitreous or uncrystallized material in their ground-mass, yet in
almost every instance this glassy substance has disappeared through
secondary devitrification. In the majority of cases, the development
of secondary minerals in the substance of the ground-mass has
completely obliterated the original micro-structure of the rock; but
in some instances we find traces of spherulitic, fluidal, and perlitic
structures ; while in others the structures known as “ grapophyric ”
can be detected—such as the micro-pegmatitic, the centric, and the
pseudo-spherulitic.

As a general rule, it may be said that the ground-mass is the
most highly altered portion of these rocks, this being doubtless due
to the fact that the glassy matrix is less stable than the crystallized
constituents of a rock. The matrix frequently acquires a green
colour from the development of minerals of the chlorite group, and
is sometimes studded with crystals of the metallic sulphides.

The porphyritic crystals of felspar, though so greatly altered,
can usually be found to show, here and there, traces of the pla-
gioclastic twinning. They are never, however, in the vitreous
condition of the felspars of ordinary andesitic rocks (microtine),
but exhibit the opacity and dull lustre characteristic of the diorites
and other deep-seated rocks. It was this condition of the porphy-
ritic felspars, with the state of the ground-mass and the features

OF THE WESTERN ISLES OF SCOTLAND. 3p

presented by the ferro-magnesian silicates, that led von Richthofen
and Zirkel to insist on the analogies of these rocks with plutonic
rocks, which were, at the time when these authors wrote, generally
believed by Continental petrographers to be of Pre-Tertiary age. Any
glass-inclusions that the felspar-crystals may once have contained
have, of course, like the glass in the matrix, undergone devitrifi-
cation, while, as Zirkel has shown in similar rocks in North Ame-
rica, bands of cavities containing liquids are abundant. This
character is also conspicuously exhibited by the quartz, which either
as a primary or secondary constituent is not unfrequently found in
these rocks. I have already stated the grounds that lead me to
conclude that these bands of liquid-inclusions are of secondary
origin. In many cases, however, the felspar-crystals, while pre-
serving their outward form, have been completely transformed, and
now only exist as pseudomorphs. The minerals which replace the
original substance of the plagioclase felspars are pistacite, zoisite,
and other minerals of the epidote group, with some new felspars of
secondary origin. Occasionally quartz and calcite have resulted
from the extreme alteration which the felspars have undergone.

The ferro-magnesian constituents of these rocks,—whether pyro-
xenes, amphiboles, or micas,—are almost always in a more or less
altered state. A fibrous structure and a green colour have been deve-
loped in them, and, as this change goes on, curious modifications of
the optical properties of the minerals are brought about. Frequently
we find, as the result of this action, green isotropic materials are
formed to which the name of “ Viridite ” may be properly applied.
But, in most instances, we find that from the products of the decom-
position of the original ferro-magnesian silicates, various minerals
of the chlorite group are developed, and crystallize out from the
mass. A still further change is marked by the destruction of these
chiorites, and the formation at their expense of various epidotes,
among which the varieties known as pistacite and a lime-epidote with
a little manganese are conspicuous.

The pyroxenes of these rocks are usually the monoclinic forms
or augites; the rhombic enstatites, though not unfrequently pre-
sent, being, as in the case of the associated basic rocks of this
district, usually subordinate and seldom, if ever, a predominating
constituent of the rocks. The amphiboles were probably horn-
blendes, long acicular and tufted forms abounding. It is clear that
in the unaltered rocks these crystals of amphibole and those of
biotite were surrounded by zones (resorption-halos) composed of
pyroxene and magnetite grains, the latter mineral onl} remaining
in the altered state of the rock. Many of the rocks contained biotite
as an original constituent; but I shall show in the sequel that much
biotite has been developed in these rocks as a secondary constituent.

That titanoferrite was often present in these rocks, as well as
magnetite, is shown by the forms of the opaque crystals and by the
way in which, as the result, of alteration, they become surrounded
by the dense white product and the colourless substance derived
from it, known as “leucoxene.” Sometimes the abundant magne-

one PROF. J. W. JUDD ON THE PROPYLITES

tite, much of which is of secondary origin, has been converted into
various forms of hydrous brown oxide, and not unfrequently we-
find great quantities of pyrite and marcasite developed, doubtless at
the expense of the magnetite and ilmenite. In the thin white crust
that so constantly covers these rocks the iron has been reduced and,
in some cases, removed in solution by the action of water containing
organic matter, as already pointed out. In some cases this removal
of iron-oxides has gone on throughout the whole substance of the
rocks, which become completely bleached.

While in most cases the alteration of the ground-mass and the
conversion of the porphyritic constituents of the rock into pseudo-
morphs has not wholly destroyed its original aspect, yet, under
certain circumstances, as I shall point out, the whole structure and
character of the mass is found to be completely transformed. This
is effected by the crystallizing-out of different minerals (among
which the epidotes and chlorites are the most conspicuous) at the
expense of the various secondary minerals that have been deve-
loped in the mass by the alteration of the felspars and ferro-
magnesian silicates. ‘These excessively altered varieties frequently
constitute rocks of very great beauty and interest*.

From this general account of the chemical, macroscopical, and -
microscopical characters of these Scottish rocks every one familiar
with the accurate descriptions given by von Richthofen, Zirkel,
Doelter, Becker, and other petrographers of the “ greenstone-tra-
chytes” of Hungary and Transylvania, and of the “ propylites” of
California, Nevada, and Utah, will at once perceive their complete
identityy.

[Since this paper was read I have had an opportunity of showing
Mr. J. P. Iddings, of the U.S. Geological Survey, a series of speci-
mens and sections of the Scottish propylites. He was able to
satisfy himself of the close similarity between these rocks and those
of the Washoe district in Nevada, which he has so carefully studied ;
and he has permitted me to state his conviction of their identity in
character. |

I shall show that, as in the districts mentioned, the curiously
modified propylites of the Western Isles of Scotland bave been
produced from davites and andesites, and from the deeper-seated.
and more highly crystalline representatives of those rocks, by the
operation of certain well-defined agencies.

* Dr. Hatch, to whom a number of sections cut from these rocks were
submitted by Dr. A. Geikie, has fully recognized the completely altered cha-
racter of the materials he examined. Unfortunately he had no means for
judging of the real nature of the rocks from which these were derived (Trans.
Roy. Soc. Edinb. vol. xxxv. 1888, pp. 77, 167).

+ See the excellent summary of these results given by Rosenbusch, ‘ Massige
Gesteine ’ (1887), pp. 690-693.

©9
Or
Su)

OF THE WESTERN ISLES OF. SCOTLAND.

Y. RELATIONS OF THE ScoTTISH PROPYLITES TO THE OTHER
Rocks oF THE DistRIct.

A. Geological Age.

That the great mass of “ felstones ” or propylites (as I have now
shown they ought properly to be called) were the earliest erupted of
all the rocks in the Western Isles of Scotland, I have already pointed
out in my memoir of 1874.

That the propylites are older than the granitic masses of the
district (“ granophyres ” of Dr, A. Geikie) is shown by the fact that
the latter are seen to send off numerous veins into them, and to enclose
portions of them in their mass, producing all the phenomena of
contact-metamorphism where in apposition with them. These are
all facts that I strongly insisted upon in the memoir referred to.

That the gabbros are younger than the propylites is equally ob-
vious. Sheets and dykes of gabbro and dolerite connected with the
mountain-like masses can be traced traversing the propylites in all
directions, and also giying rise to the phenomena of contact-meta-
morphism.

That the ‘“ felstones ” of the Western Isles of Scotland are invaded
by the extrusions of granite (‘“ granophyre ”) and of gabbro is con-
firmed by many sections described by Dr. A. Geikie*: but, in con-
sidering the descriptions given by this author, it must be borne in
mind that under the same general name “ bedded basalts” he has
confounded two totally distinct petrographical types, namely, the
ophitic olivine-basalts of the plateaux, which I described in detail
before this Society in 1886, and the andesites and associated rocks
of the central areas, of which I am treating in the present memoir.
He has supposed that the rocks which we are now considering are
really basalts which have acquired their peculiar and distinctive
characters as a consequence of the metamorphism they have been
subjected to through contact with great intrusive igneous masses f. |

It will thus be seen that the great cause of the conflict of
opinion between Dr. A. Geikie and myself, concerning the relations
of the igneous masses of the Western Isles of Scotland, is to be found
in the different interpretation we place on these propylitic rocks.
Dr. Geikie has clearly noticed these propylites, which he describes in
such a way as to avoid possibility of doubt concerning what he
refers to. He states that they weather, not like the basalts, but
with a “thin white crust, beneath which the rock appears dull,
black, and splintery. ‘They are generally veined with minute threads
and strings of calcite, epidote, and quartz, which form a yellowish-
brown network that projects above the rest of the weathered surface.
Where they are amygdaloidal, the kernels no longer decay away or
drop out, leaving the empty, smooth-surfaced cells, but remain as if
they graduated into the surrounding rock by an interlacing of their
crystalline constituents” t. Unfortunately, however, Dr. Geikie

* Trans. Roy. Soc. Edinb. vol. xxxv. pp. 151-181. + Ibid. pp. 167, 168.
+ Ibid. p. 107, and pp. 77 & 168.

304 PROF. J. W. JUDD ON THE PROPYLITES

appears to have left all exact petrographical study of the materials till
after the completion of his field-work, and this led him to the erro-
neous conclusion that the propylitic rocks were simply the platean-
basalts altered by contact-metamorphism. ‘Two dozen slices made
from specimens collected by Dr. Geikie were placed in the hands of
Dr. Hatch for microscopical study, and that gentleman’s notes are
characterized by his usual accuracy andacumen. He noticed the ex-
treme alteration of the originally glassy base with the development
of secondary felspars, the complete change of the porphyritic crystals,
and the development of chlorite, epidote, and other secondary
minerals in the rock at the expense of the original constituents.
But Dr. Hatch’s notes afford no support whatever to the idea that —
these rocks are simply the plateau-basalts altered by contact-meta-
morphism,

B. Structure.

That the rocks which in their altered form we now refer to the
propylites were, some of them, effusive (lavas and cupolas), while
others were intrusive (laccolites, sheets, and dykes) there cannot be
the smallest doubt. No warrant can be found from the study of
these rocks for making a fundamental distinction of certain petro-
graphic types, as belonging to the effusive or volcanic series (Erguss-
gesteine), and others as belonging to the intrusive or Plutonic series
(Tiefengesteine). On the contrary, the central portions of some of
the very thick lava-currents poured out at the surface are more
highly crystalline than the rock of many eruptive masses. Still less
eround can I find, in this district, for instituting a class of ‘“ dyke-
rocks ” ( “‘ Ganggesteine ”’) ; for while dykes and veins are sometimes
found exhibiting very coarsely crystalline texture, others finely
grained and even glassy may be seen side by side with them.

C. Nature of Rock-masses.

The rocks of the Western Isles of Scotland now referred to the
group of propylites are found exhibiting three kinds of relations
to the surrounding rock-masses :—

1. Lava-streams.—That these rocks often constituted ordinary
lava-currents there cannot be the smallest doubt. Flat masses
covering considerable areas and presenting at their upper and under
surfaces the most strikingly scoriaceous and slaggy appearance
abound, and are found piled one upon another to the depth of many
hundreds or even thousands of feet. As a general rule, to which,
however, there are a few exceptions, the lava-currents composed of
porphyritic rocks are sbort and bulky, and they can seldom be
traced to a distance of many miles from their point of emission. In
this respect they present a most striking contrast to the olivine-
basalts, which, as a rule, must have been poured out as lavas of
ereat liquidity, and probably flowed distances of twenty, thirty, or
even forty miles from their points of emission.

Professor J. D. Dana, in his suggestive memoirs on the Hawaiian

OF THE WESTERN ISLES OF SCOTLAND. 355

volcanoes, has clearly pointed out the important consequences which
follow from the extreme liquidity of certain types of basalt; and in
the Western Isles of Scotland, as in Iceland, we find many illustra-
tions of the contrast between the features arising from the outflow
of viscous lavas of acid and intermediate composition, on the one
hand, and extremely fluid basic lava-currents on the other.

There is every reason for concluding that the ejection of the more
acid lavas which constitute thick and bulky currents, and surround
the five great centres of igneous action in the Western Isles of
Scotland, took place, as a whole, before the appearance of the mass
of the ophitic olivine-basalts which form the mass of the great
plateaux. But, as 1 have already pointed out, we have evidence
on the one hand that occasional streams of olivine-basalt were poured
out during the earlier eruptions of the andesites; and, on the other
hand, we find that occasional but very interesting outflows of
andesite occurred during the ejection of the olivine-basalts; and
such sheets of andesite-lavas are now found intercalated among the
basalts of the plateaux. One such outflow of andesitic lava was
referred to by Dr. A. Geikie in 1871 as occurring in the Island of
Kigg, and I have noticed several similar in the same island. In
Mull they also occur ; and in the district of Mishnish, which I have
somewhat closely studied, a very considerable number of such ande-
sitic lavas have been detected by me intercalated with the basalts
of the plateaux, The same is also the case in Skye, and about
the other centres of igneous activity.

2. “ Cupolas.”.—Under the name of ‘“Quell-Kuppen,” Dr. E.
Reyer* and other authors in Germany are in the habit of describing
more or less dome-shaped masses of lava, like the domitic-puys of
Auvergne, the phonolite-hills of Bohemia, and the Chodi-Berg and
similar andesitic massesin Hungary. Such “ cupolas,” ‘* domes,” or
‘*mamelons” may vary in size from mere hummocks with an area
of only a few square yards, to mountaim-masses of the grandest
dimensions. Externally such masses may have entirely lost the
scorlaceous covering with which, in all probability, they were ori-
ginally invested. But internally they often exhibit a markedly
concentric structure; and there is a striking gradation from the
true lava-type: (‘“ hyalopilitic”’ texture of rock) in the exterior
portion to highly crystalline (‘* hypidiomorphic-granular ”) varieties,
approaching Plutonic types, in the interior. Dr. Reyer has shown
by plaster models how such masses were probably formed by a kind
of endogenous growth. Dr. A. Geikie refers to some of those
masses under the term ‘ bosses.”

Among the largest and most striking of these “ cupolas” is that
which constitutes the grand mountain of Beinn Talaidh (Beinn Talla)
in Mull, which, rising to the height of 2496 feet above the sea, is
remarkable for its smooth and graceful outlines. Specimens taken
from the flanks and summit of this mountain show the rock to be a
hornblende-andesite in a more or less altered condition. But examples

* Theoretische Geologie, pp. 79-99.

356 PROF. J. W. JUDD ON THE PROPYLITES

obtained in the deep Corry of Tomsle¢ibe, on the north-western side of
the mountain, are found to bea true diorite; and a series of specimens-
can easily be obtained exhibiting every gradation from the one type
to the other. Some of the intermediate types exhibit the various
kinds of ‘‘ granophyric ” structure in a very beautiful manner. The
composition of this dioritic mass, which, in its upward development,
gradates into a hornblende-andesite, is illustrated by the analysis
given at p. 349.

3. ‘* Laccolites.’—In 1874 I described acid, igneous rocks
as being intruded among the strata of the Western Isles, and
stated that they tend to form thick, lenticular masses, which are
generally confined to within moderate distances from the great
centres of eruption*. Mr. Gilbert has since proposed to call |
intrusive masses of this type by the name of Laccolites t. Like the
“cupolas” they are much more highly crystalline in their central
than in their peripheral portions; the outside of such masses may
be a true andesite, while the central portions exhibit the holocrys-
talline or granitic structure of a diorite. Where the country has
undergone much denudation, it may often be impossible to state if a
particular mass should be referred to the class of “ Quellkuppen” or
of ‘* Laccolites,” but that both types occur in the Western Isles of
Scotland, there cannot be any doubt.

VI. Narvre oF tHE OrnIGINAL Rocks FROM WHICH
THE PROPYLITES WERE FORMED.

In endeavouring to determine the exact nature of the rocks grouped
under the general name of “ felstones,” in the Western Isles of
Scotland, very great difficulty is experienced owing to the excessively
altered state both of the “ phenocrysts” (to use Iddings’s useful
term) and of the.ground-mass in which they are imbedded. Deter-
minations of specific gravity and the partial or complete analysis of
the rocks are, of course, of much value in deciding the place of
the several varieties in a classificatory system, yet it is chiefly upon
other methods that I have been led to rely in making a study of
these very obscure rocks. The alteration which has gone on in
them, though often extreme, is not unfrequently found to be more
more or less local in character; and, in the same mass, portions
exhibiting very different stages of the change may often be found.
It has been my object, in the repeated visits I have paid to the
district during the last fifteen years, to trace the much altered and
obscure rocks to points where their phenocrysts and ground-mass can
be studied in a less altered form; and although in some instances it
has been long before I was able to resolve all the difficulties that
have presented themselves, yet in the great majority of cases this
method has led to more or less satisfactory results.

Fortunately, too, several very able investigators have been en-
gaged, during the same period, in the investigation of the very

* Quart. Journ. Geol. Soc. vol. xxx. (1874), p. 268.
+t Geology of the Henry Mountains, U.S. Geol. Survey, 1877.

oa ‘-

OF THE WESTERN ISLES OF SCOTLAND. aor

similar rocks which occur in the Faroe Isles, in Iceland, and in
Greenland,—districts in which the volcanic products present such
remarkable analogies with those of the Western Isles of Scotland.
The results of some of these researches have afforded me invaluable
aid, for they deal with materials some of which are almost abso-
lutely unaltered, belonging to the same types as those which we
find in such an altered condition in our own country.

In 1874 K. Vrba described some rocks from Southern Greenland,
and among them certain diorites of somewhat remarkable character,
which may not improbably be of the same geological age with rocks
to be referred to in the present paper*.

In 1882, P. Schirlitz published the result of his studies, in the
Petrographical Laboratory of Leipzig, of the Icelandic rocks collected
by Professor Zirkel in 1860. In addition to the basalts and rhyo-
lites, a number of very interesting rocks, called by Zirkel augite-
andesites, was described by this author. He rightly insists, how-
ever, on the distinction between these and the Santorin lavas and
the glassy andesites of Java (the vitrophyric augite-andesites of
Rosenbusch), and is in favour of grouping them with the basalts 7.

In 1884, Dr. A. Osann undertook an examination of the series of
specimens from the Faroe Islands contained in the collection of the
University of Heidelberg. He showed that, besides the black
lustrous olivine-basalts, there exist dark grey rocks of very different
aspect, containing an augite of a somewhat remarkable character,
and he is disposed to place these among the andesitest. The
distinction of these dark grey rocks, poor in olivine, which Osann
pointed out in the case of the Faroe Isles, and Schirlitz in the case
of those of Iceland, was also made by H. Reusch in the case of the
Jan-Mayen rocks §, and by Nauchoff in the case of the Greenland
lavas ||.

a and most important of all, must be mentioned the very valu-
able researches made upon the rocks of Iceland and the Faroe Islands
by M. Rene Bréon4]. These researches were carried on in the Labo-
ratory of Prof. Fouqué in the Collége de France. M. Bréon has
described a number of lavas of intermediate composition which pre-
sent the most striking analogies with some of the rocks now found in
such an altered condition in the Hebrides. The wonderful freshness
of the Icelandic rocks enables us to explain many points of diffi-
culty which confront us in the case of their greatly altered British
representatives, and I am much indebted to M. Bréon for his kind-
ness in sending me a series of specimens of his Icelandic types for
comparison with the rocks of Scotland.

* Sitzungsb. Wien. Akad. lxix. (1874), pp. 109-115.

t+ Tschr. Min. und Petrogr. Mittheil. iv. (1812), p. 414.

+ Neues Jahrb. fiir Min. &e. 1884, i. pp. 45-49.

§ ‘The Norwegian North-Atlantic Expedition of 1876-78’ (Christiania,
1882).

I rin. Mittheil. 1874, pp. 109-176.

«| Notes pour servir 4 l'étude de la Géologie de l’Islande et des Iles Feeroe,
par R. Bréon, 1884.

Q. J. G8. No. 183. op

358 PROF. J. W. JUDD ON THE PROPYLITES

Without laying any great stress upon the value of the distinction,
it may be convenient to group the propylites of the Western Isles.
of Scotland in two series. In one of these, the prevailing ferro-mag-
nesian silicate was originally hornblende or biotite, and this we may
speak of as the ‘“‘ Amphibolic Series.” In the other group a pyro-
xene (augite or enstatite) was the predominating ferro-magnesian
silicate in the original rock, and this may be called the ‘* Pyroxenic
Series.”

The rocks of the Amphibolic Series include most of the types
already spoken of as being distinguished by a paler colour, a lower
specific gravity (ranging from 2°4 to 2°7), and a higher silica-per-
centage. The rocks of the Pyroxenic Series are usually darker-
coloured, have a higher density (2°6—2°9) and a lower percentage of
silica. But many varieties occur in which both pyroxenes and
amphiboles or mica are present, and in the case of the very highly
altered forms it is difficult and sometimes impossible to refer the
rock to either of these series.

In both of these series we find rocks of highly crystalline cha-
racter (true diorites) passing through various hypocrystalline (“ pilo-
taxitic”’ and “ hyalopilitic ”’) varieties, into perfectly vitreous rocks.
Both the amphibolic and pyroxenic rocks sometimes contain free
quartz, and then pass into quartz-andesites and quartz-diorites.

The chief types of the andesites and their Plutonic representatives
in the Western Isles of Scotland may be conveniently grouped as
follows :—

A. AMPIIIBOLE- AND MICA-ANDESITES.

Hornblende-andesites.
Hornblende-mica-andesites.
Hornblende-mica-andesites with enstatite.

Diorites and Quartz-diorites.

B. PyroxENE-ANDESITES.

1. ‘‘ Vitrophyric ” Pyroxene-andesites.
2. “ Trachytoid” Pyroxene-andesites.
a. Stikkisholmur Type.
b. ‘‘ Diallage-andesites.”
c, Labradorite-andesites.

Pyroxene-diorites and Quartz-pyroxene diorites.

A. Amphibole- and Mica-andesites and Diorites.

The hornblende- and mica-andesites are perhaps more numerous
in the Western Isles of Scotland than the pyroxene-andesites.
While the former most commonly exist as quellekuppen and lacco-
lites, the latter more frequently constitute lava-schists and intrusive
sheets (“ sills” of the miners of the North of England); but this
distinction is far from being an absolute one, there being not a few
lava-streams, some broad and far-spreading, composed of hornblende-
and mica-andesites, at the base of, or intercalated among, the plateau-

tr

OF THE WESTERN ISLES OF SCOTLAND. 359

basalts. It is among these lava-sheets, at a considerable distance
from the great eruptive centres, that these rocks can be studied in
their least altered condition. Around the great igneous centres the
extreme of alteration is seen to have taken place, not one of the
original minerals of the rocks being recognizable except as pseudo-
morphs. ‘The felspars are usually completely kaolinized, the ferro-
magnesian minerals represented by chlorites, while even the titano-
ferrite is converted into white opaque products, and finally into the
transparent leucoxene or titanomorphite (sphene ?).

Rosenbusch has proposed to divide the amphibole-andesites into
two groups—those which in addition to the amphibole or mica, also
contain a pyroxene, and those in which pyroxenes are absent. Both
of these groups appear to be well represented in the Western Isles
of Scotland. Rosenbusch has also proposed to divide the amphibole-
and mica-andesites containing pyroxene into two groups—those in
which the pyroxene is an augite or monoclinic variety, and those in
which it is an enstatite in rhombic form. The latter type, which
is so abundantly represented in the recent volcanic rocks of the
Western Territories of the United States, and southward in the
Republic of Salvador, according to Hague and Iddings *, is beauti-
fully illustrated in the district which we are describing.

In the Hornblende-andesites proper we find a ‘“ microlitic felt” of
felspar needles, through which are scattered groups of green horn-
blende crystals, often assuming sheaf-like and tufted groupings.
In most cases it is clear that each hornblende crystal or group of
erystals was originally surrounded by a resorption-halo, that is, a
sheath composed of pyroxene and magnetite, the result of the action
of heated magma on the hornblende. But in most cases the
pyroxene has been converted into isotropic viridite or into a chlorite
of feeble double refraction, while the granules of magnetite still
surround the more or less altered hornblende. In many instances,
the hornblende can be seen to have been completely changed into a
chlorite, with the separation all through its substance of granules of
magnetite. These chlorite-pseudomorphs after hornblende, with
granules of magnetite crowded along their sides and also scattered
through their midst, are very characteristic of the propylites which
are derived from the hornblende-andesites (see Plate XIV. fig. 7).

One of the best types of this group is found in the rock of
Beinn Talaidh (Beinn Talla) in Mull. This rock varies in specific
gravity from 2°60 in the least crystalline types to 2°68 in those
more highly crystalline. In the deeper corries of the mountain,
andesites are found exhibiting a distinctly dioritic habit. The
chemical composition of this rock is shown by the analysis given
at p. 349.

The hornblende-andesites of the Western Isles of Scotland
exhibit the widest diversity in the proportions of their constituent
minerals, Some of the rocks of this class, good examples of which
may be seen near Salen, Mull, consist very largely of felspar crystals

* Amer. Journ. Sci. vol. xxvi. (1883) p. 233, vol. xxvii. (1884) p. 460,
yol. xxxii. (1886) p. 28.

2D 2

360 PROF. J. W. JUDD ON THE PROPYLITES

and a little glass, with only a few scattered crystals of ferromag-
nesian silicates. These rocks are usually pale-coloured or nearly
white and have a low specific gravity (2°55). Other hornblende-
andesites, like those of Mhaim Clackaig in Mull and of Glen Brittle
in Skye, exhibit a dark green, often nearly black colour, and have
a much higher specific gravity (2°7 to 2°8).

I have not detected any completely glassy forms of these rocks,
nor any examples in which primary quartz occurs. Some of the
more highly crystalline types, however, exhibit the granophyric
structure and contain free quartz, which I believe is of secondary
origin.

Hornblende-mica-andesites, with or without pyroxenes, are very
abundant in the district. They constitute rocks of a pale grey
colour and a more or less fissile character, which form well-marked
lava-streams, some of which are found intercalated among the
basalts of the plateaux.

In some of the best-preserved of these rocks, crystals of unmis-
takable enstatite (bronzite) make their appearance; and, as what
may be the products of alteration of this mineral are seldom absent
in the more altered varieties, it may probably be assumed that the
majority of the rocks of this type in the Western Isles of Scotland
must be referred to the hornblende- and mica-andesites containing
enstatite.

Some of these rocks exhibit a character lately referred to by
Dr. Osann* and by Mr. Teall‘?. Gas-cavities are found filled with
glassy matter that seems to have oozed out of the ground-mass of
the rocks into these empty cavities. In the case of some of the
Scottish rocks it is curious to find that the glass in these cavities
exhibits a markedly banded structure.

Mica-andesttes.—W hile there are probably some examples of true
mica-andesites 1t must be remembered that a dark brown biotite is
among the commonest of the secondary minerals in these propylitic
rocks. Good examples of true mica-andesites occur at certain
points at Mull and also in Higg. These biotite-andesites pass by
insensible gradations into the hornblende-andesites ; in some cases
the amphibole being the predominating constituent, in others the
mica. As arule among the altered rocks, the hornblendes tend to
disappear by passing into chlorites, with or without the separation
of magnetite, while the biotite seems to increase in amount, either
by the growth of original crystals of the mineral or by the develop-
ment of new secondary crystals.

Diorites—Of the common or hornblende-diorites we cannot find
better examples than those which occur in the deep Corry exposing
the central mass of Beinn Talaidh in Mull. From an almost
perfectly holocrystalline rock every gradation can be traced, through
beautiful granophyric varieties, into the lava constituting the peri-
pheral portions of the mass, which is, as we have seen, a typical
hornblende-andesite.

* Zeitschr. d. deutsch. geolog. Gesellsch. xli, (1889) p. 304.
t Geol. Mag. dee. iii. vol. vi. (1889) p. 481.

‘im 7 O-

OF THE WESTERN ISLES OF SCOTLAND. 361

Quartz-diorttes have a tolerably wide distribution in Mull and
some of the other centres of eruption; the rocks in it, frequently
exhibited granophyric structures and other peculiarities, recalling
in the most striking manner the quartz-diorite of Doire na Kach
and other bosses in Arran so well described by Professor Zirkel *.

B. Pyrowene-andesites and Pyroxene-diorites.

These rocks contain as phenocrysts (or minerals of the first con-
solidation) felspars which are always plagioclastic, and which, by
their characteristic extinctions, their specific gravity, and their flame-
reactions, are shown to belong to labradorite or to a variety between
labradorite and anorthite. These porphyritic crystals are note-
worthy as very constantly displaying a zoned structure, and are
usually full of glass and stone-enclosures, for the most part arranged
parallel to the sides of the crystals. The crystals often exhibit the
evidences of growth after the consolidation of the rock, a phe-
nomenon which has been already described. Sometimes in addition
to porphyritically developed felspars we find large crystals of
augite, belonging to a variety very rich in magnesia and iron, and
often exhibiting the structure to be hereafter described as the
*‘ pseudo-diallagic ;” enstatite not unfrequently accompanies the
augite, a ferriferous variety—between bronzite and hypersthene—
being the most common form of the mineral. Olivine is either
entirely absent or is so rare in these rocks that it must be regarded
as an accessory or accidental constituent only. Magnetite, however,
is always present, though in very varying quantities.

The minerals of the ground-mass, or those of the second period
of consolidation, consist of felspars (usually showing lath-shaped
sections and more or less lamellar twinning), which by their extinc-
tions are referable to oligoclase, but may sometimes be orthoclase ;
intercrystallized with the rod-like felspars is a pale brown variety
of augite, usually occurring in more or less rounded granules, and
many opaque magnetite grains.

The glass, which sometimes is almost absent in these rocks, and
at other times forms the greater part of their mass, is usually full of
erystallites, and in the arrangement of bands and flecks of different
colours, or the distribution of the crystallites, shows striking evidence
of flow-structure. This is especially manifest in the varieties
which contain porphyritic constituents and much glass. Skeleton
crystals and rods of magnetite are very abundant in these glassy
bases of the andesite-rocks.

The pyroxene-andesites of the district fall naturally into two
groups, between which, however, many connecting-links may be
found.

Those rocks in which the quantity of glassy base is reduced to a
minimum, and which consist largely of the minerals of the second
period of consolidation, with or without porphyritic constituents,
undoubtedly approximate to the basalts. But their real analogies,

* Zeitschr. d. deutsch geol. Gesellsch. vol. xxiii. (1871) p. 30,

362 PROF. J. W. JUDD ON THE PROPYLITES

as I shall show in a subsequent part of this paper, are so clearly
with the vitrophyric pyroxene-andesites, that it 1s quite impossible
to remove them from the group of the andesites. We must regard
them therefore as the most basic type of the andesite series,—forms
which constitute a real connecting-link between the andesites and
the true or olivine-basalts. J am still inclined to follow Zirkel’s
original rule of confining the name basalt to those rocks of which
olivine forms are essential constituents. This plan is followed by
Rosenbusch in the case of the leucite and nepheline-bearing rocks,
though of late years he has departed from it in the case of the
felspar-bearing types.

Augite-andesites of the vitrophyric type of Rosenbusch appear at
many points in the Western Isles of Scotland, and are particularly
abundant about the north-western part of Beinn-’-Ghraag in Mull.

In these we find crystals of augite and enstatite, of a felspar
allied to labradorite, and of magnetite, embedded ina glassy ground-
mass, which may be large or small in quantity compared with the
crystalline constituents of the mass. As in almost all similar rocks,
we may notice that the crystals are often by no means uniformly
scattered through the glassy base, but are collected into groups
which often appear like portions of a holocrystalline mass.

At Mhaim Clackaig in Mull I have found a vitrophyric augite-
andesite in which crystals of labradorite (usually much rounded on
the angles and sometimes corroded), of a brown augite, and of mag-
netite are somewhat sparsely scattered through a glassy base. This
glassy base is crowded with black rods (trichites), much twisted
and bent, which in places become so abundant as to render the
glass nearly opaque, except in very thin sections. This rock has a
specific gravity of 2°64 (see Plate XIV. fig. 3).

In Beinn-a-Ghraag similar glassy rocks are highly spherulitic, the
spherulites being arranged in definite bands, evidently produced
during the movement of the viscous mass (see Plate XIV. fig. 4).
One of these spherulitic rocks has a specific gravity of 2°49. In
other cases, the fluidal structure, indicated by the way the micro-
lites of the second period of consolidation are arranged around the
porphyritic felspar and pyroxene crystals (see Plate XIV. fig. 6), is
very strikingly shown.

For the determination of the specific gravities of a series of the
vitrophyric augite-andesites I am indebted to my assistant, Mr. F.
H. Hume, F.G.S.

Although no augite-andesites with free quartz have been detected
in the district, yet some of these very glassy varieties must have a
silica-percentage as high as that of the quartz augite-andesites or
augite-dacites.

The best type of the more basic, stony pyroxene-andesites (“ tra-
chytoid andesites ” of Rosenbusch) is afforded by the rocks which
exactly resemble the lavas of Stikkisholmur and other points in
Iceland, and are so well described and figured by Bréon*. The rock

* Loe. cit. pp. 23 & 24, pl. iii. fig. 1.

OF THE WESTERN ISLES OF SCOTLAND. 363

consists essentially of a mesh of oligoclase and perhaps of anortho-
clase microlites entangling granules of augite (with some enstatite)
and of magnetite, glass being present in small quantities only and
quite inconspicuous.

This Stikkisholmur type is well represented at many points in
the Western Isles of Scotland. Good illustrations of the type occur
in the promontory stretching out to Salen Pier in Mull, at Beinn
Uaig, and Creagach Beinn, in the same island, in Ardnamurchan, and
in many other places.

Like the Icelandic rocks, those of our Western Isles are “ com-
pact and dark-coloured . . . the fracture is often nearly conchoidal,
and certain specimens present a semi-vitreous appearance ” (Bréon,
loc. ctt. p. 23).

In his reference of these rocks of the Stikkisholmur t ype to the
augite-andesites, Bréon is supported by Rosenbusch, who, in the
last edition of his ‘ Massige Gesteine’ (p. 682), refers to these rocks
as presenting some analogies with the augite-andesites described
by Foerstner as occurring in Pantellaria, and containing anortho-
clase and the triclinic amphibole—cossyrite (znigmatite).

Some of the augite-andesites of the Stikkisholmur type contain
large scattered crystals of anorthite or labradorite, and thus pass
into the labradorite-andesites.

Another variety of the “trachytoid ” pyroxene-andesites is pre-
sented when, in addition to the porphyritic crystals of felspar, large
phenocrysts of augite make their appearance. ‘These augites appear
to belong to a variety rich in iron and magnesia, but which, con-
sidering their composition, are of remarkably stable character, often
remaining comparatively unaltered when all the crystals in the
rock have been profoundly changed. Such porphyritic augites often
show a tendency to assume the form of stellar aggregates, and
sometimes are of such dimensions as to be quite conspicuous on the
fractured surfaces of the rocks. Beautiful examples of lavas of this
type are found about Mingary Castle in Ardnamurchan, and I have
also detected them at many other points in the Western Isles.

The porphyritic augites in these rocks present a character of very
considerable interest, which it is necessary to notice here, though I
have discussed it in detail in another place (Min. Mag. vol. ix. ‘i

The augite-crystals exhibit lamellar twinning and subsequent
schillerization parallel to the basal plane (001). Similar varieties
have been described by William Phillips, Osann, and by Mr. Teall.
The forms found in the Western Isles of Scotland differ from those
described by the first and last-mentioned authors in not exhibiting
simple twinning parallel to the orthopinacoid (001), but in showing
some traces of lamellar twinning and subsequent schillerization
parallel to that plane. (See Plate XIV. figs. 1: & 2.)

The occurrence in certain andesites of augite crystals exhibiting
lamellar twinning with schillerization has led toa group being estab-
lished by some authors bearing the name of “ Diallage- andesites.
It is probable that, in many, perhaps in all, of the cases in which
diallage is stated to exist in andesitic lavas, augite twinned and

364 PROF, J. W. JUDD ON THE PROPYLITES

altered on the basal plane has been mistaken for true diallage with
schillerization on the orthopinacoid.

The rocks called by the French geologists labradorites, and which
I propose to term ‘‘ labradorite-andesites,” consist of a base which
is, in all essential respects, identical with that of the last-described
rocks; but they contain numerous and sometimes very large por-
phyritic crystals of labradorite, or of a felspar which is intermediate
between labradorite and anorthite.

Good types of such rocks may be found at Dun-da-Ghaoith (Dun-
da-Gu) in Mull, around the southern flanks of Glamaig in Skye,
and at Beinn Suardil in the same island. ‘They agree in every
respect with the Icelandic varieties so clearly described by Bréon.
The general features of these rocks, and the evidence they afford of
the growth of the felspar crystals subsequently to the consolidation
of the rock, have been discussed in a previous communication to this
Society *.

In their altered condition these labradorite-andesites present the
most complete analogy with the labradorite-porphyrites, such as the
Verde antique of Greece, and the Lambay-Island porphyrite so well
investigated by Von Lasaulx.

Occasionally rocks of the “‘ trachytoid” type are found passing
locally into a perfect glass. An example of this was discovered
some years ago by the late Mr. Grieve, and I am indebted to my
friend Professor Bonney for calling my attention to it. The locality
where this is found is at Bealach a’ Mhaim, at the head of Glen
Brittle in Skye. The mode of occurrence of this glass is somewhat
obscure, but it appears that the glass does not exist like the tachy-
lyte-selvages to basalt-dykes, but as local patches in the midst of
the andesite. Probably in this, as in cases to be more fully de-
scribed in a later portion of this paper, a separation has occurred
between the glassy and the crystalline portions of the andesite.
The glass has a specific gravity of 2°63, while that of the labradorite-
andesite in which it is enclosed is 2°89.

By the kindness of Prof. Thorpe I have been supplied with
analyses of the glassy portions of this rock made in the Chemical
Laboratory of the Normal School of Science and Royal School of
Mines.

if AWE III
SeluGas de at Boleee olaL 62-10 61°80
PN ihrbitt: eee eee 14°83 15-00 14-91
Ferric oxide .... 8:41 8:14 8:27
Hest ee iy Bee 3°58 3°07 Soe
Maenesia: ) ss/vacides 0:28 0:27 0:27
Bodacious a ae 6°58 6°42 6°50
Potagh:cnx Soeee 5:17 Bid 5:19
Loss on ignition 0-88 0-86 0°87

101-24 101:07 101°14

* Quart. Journ. Geol. Soe, vol. xlv. (1889) pp. 175-186.

OF THE WESTERN ISLES OF SCOTLAND. 365

J. Analysis of glass in labradorite-andesite from Bealach a’ Mhaim,
Skye, by S. Parrish.

II. Analysis of second specimen of the same rock by H. J.
‘Taylor. :

III. Mean of these two analyses.

It appears from these analyses that this glass is richer in silica
than the andesite (a labradorite-andesite) in which it occurs.

Studied microscopically, this vitreous rock is found to consist of a
glassy base, less black and opaque than ordinary tachylyte, through
which porphyritic crystals of plagioclase (labradorite) are somewhat
sparsely scattered. The glass often contains incipient and some-
times well-formed spherulites, and the arrangement of these and of
darker streaks of glassy material give it a marked fluidal structure.
The felspar phenorysts are remarkable for the amount of corrosions
by the fluid magma which they have undergone, and spherulitic
fringes have often been developed all round the edges of the
erystals. Sometimes the incipient spherulites are seen to yield to
weathering influence much more readily than the enclosing glass,
and a peculiar banded appearance then becomes very conspicuous
on weathered surfaces (see Plate XIV. fig. 5).

The Augite-diorites—In 1866 Zirkel* proposed the use of this
term, and in 1877 Strong described an important class of rock of
this type as occurring in Minnesotay. Mr. Cole has also strongly
advocated the use of this term +, which has, moreover, been adopted
by Rosenbusch, in the last edition of his ‘ Massige Gesteine.’

The type is beautifully exemplified, especially in Ardnamurchan,
where great mountain-masses, like that of Meal nan Con, are made
upofit. The augite often exnibits, partially or throughout, the dial-
lagic striation, and the rocks differ from the gabbros only in the
absence of olivine and magnetite. Every gradation can be followed
from rocks with a glassy magma, though various granophyric types,
into a perfectly holocystalline rock.

Quartz-augite-diorites occur at several points, as in the great sheets
under Beinn More. ‘They contain both rhombic and monoclinic
pyroxene, and also quartz, both primary and secondary.

As it has been asserted that the “felstones” or propylites of the
Western Isles of Scotland are really nothing more than basalts
altered by contact-metamorphism, I may point out that, asso-
ciated with the andesites and more acid rocks, are a few ophitic-
olivine-basalts, which have been subjected to the same kind of
modiiication as the propylites. These are found to exhibit cha-
racters very strongly contrasted to those of the rocks in question,
In all, or nearly all, these cases the distinctive characters of the
basalts can still be clearly recognized, namely, the olivine grains,
reduced to pseudomorphs, and the ophitic structure, traces of which
can be detected even when both the felspar and the pyroxenes have
undergone the most profound change.

* Lehrbuch der Petrographie, vol. ii. p. 7.
t Neues Jahrb. fiir Min. &e. 1877.
t Geol. Mag. dee. iii. vol. iii. (1886) p. 225,

366 PROF. J. W. JUDD ON THE PROPYLITES

VII. Causrs BY wHicu THE ** Propyiiric”” MoprricatTrIon OF THESE
Rocks HAS BEEN BROUGHT ABOUT.

In studying the relations of the propylites to the other rocks of
the Western Isles of Scotland no fact strikes the observer more
forcibly than that of their being constantly invaded by igneous in-
trusions, composed of granite and felsite on the one hand, and of
gabbro and dolerite on the other hand. Beautiful examples may
be studied, at many points, of the ramification of granite veins
through the propylites, and portions of the propylite may even be
seen caught up in the midst of granite. On the other hand, the
currents of propylite may he seen to be broken up by numerous sheets
of gabbro and dolerite, which are generally intruded between them ;
and from these sheets numerous veins and dykes of dolerite and
basalt can often be traced intersecting the propylite masses. In
places the intrusions, indeed, outbulk the rocks among which they
have been thrust. These relations were fully explained by me in
1874 *, and have been confirmed by numerous illustrative examples
given by Dr. A. Geikie in 1888 7.

Impressed by the number of these intrusions among the pro-
pylite- (‘‘ felstone ”-) lavas I was led, in 1874, to refer the re-
markable alteration which they have undoubtedly undergone to
contact-metamorphism t, and the same view was adopted by Dr.
A. Geikie in 1888 §.

But subsequent und more detailed study of the propylites has
convinced me that contact-metamorphism, while producing very
striking results close to the planes of junction of the lavas and the
intruded sheets, has seldom operated to any great distances from the
latter, and that the widespread modifications which have been
effected in the minerals and the ground-mass of the propylites must
be referred to a widely different cause. In the case of the analogous
rocks of Eastern Europe and North America, it has been abundantly
proved, by the researches of geologists in these districts, that the
cause of the curious alteration of the andesitic and dioritic rocks
and their impregnation with metallic sulphides (some of which are
of great commercial value in those two districts) must be referred
to the action of steam and of various acid gases, which have per-
meated the whole substance of the lava-masses, giving rise to pro-
found chemical alteration of their constituents.

At the same time the contact-metamorphism, to which I called
attention in 1874, has undoubtedly been a noteworthy and, in some
instances, an important contributory factor in bringing about the
results. Ishowed that ‘in proximity to the gabbros, these felstone-
lavas are seen . . . to have acquired a peculiar platy structure and
splintery fracture, combined, in many cases, with the development
of a probably preexisting banded coloration ” ||. I particularly dwelt

* Quart. Journ. Geol. Soc. vol xxx. p. 246.

t Trans. Roy. Soc. Edinb. vol. xxxy. (1888) pp. 165-171.
+ Quart. Journ. Geol. Soe. vol. xxx. p. 251.

§ Trans. Roy. Soc. Kdinb. vol. xxxv. (1888) p. 167.

|| Quart. Journ. Geol. Soc. vol. xxx. p. 251.

OF THE WESTERN ISLES OF SCOTLAND. 367

upon the evidence of the contact-metamorphism produced around
the intrusive mass of 8. Airde Beinn (Sarsta Beinn), and the facts
then pointed out have been confirmed by Dr. Geikie and Dr.
Hatch *.

In many cases the solfataric action and the invasion of the lavas
by great molten masses of rock can be shown to have produced
effects which are strikingly contrasted. The effect of the contact-
metamorphism is to induce a remarkable splintery fracture and
jointed structure in the rocks affected. But this effect is only seen
to extend to the distance of a few inches, or at most feet, from the
actual planes of junction. As the result of the contact-metamor-
phism the rocks acquire, in a very remarkable manner, a power of
resisting denudation; and in consequence of this, we find sheaths
of altered rock standing up above the general surface, and enveloping
the intrusive masses 7.

The more widely spread changes which have affected the oldest
Tertiary andesites and diorites are of a totally different kind. The
action appears to have taken place in a sporadic and seemingly
capricious manner. Highly altered rocks may sometimes be found to
pass into comparatively unaltered rocks, within a few feet or yards,
and no direct relation can be detected between the greatly altered
masses and any particular intrusions of either acid or basic rock.
The effect of the chemical changes in the rock is usually to disin-
tegrate its constituents, and thereby render it less able to withstand
the action of denuding agents upon the mountain-sides. The che-
mically altered rocks, rendered soft and porous and coated with a
friable white crust, are often covered up and concealed by peat and
vegetation, while the intrusions among them, and their surrounding
sheaths produced by contact-metamorphism, retain the marks of
glacial action, and stand up prominently above the peat and
heather.

In many places it can be clearly shown that the widely spread
chemical action has preceded the action of contact-metamorphism,
while in other instances the opposite may perhaps have been the
case. As might be expected, the results of these two kinds of action
are often curiously complicated and involved. Microscopical and
chemical study enable us, however, in most cases to define and ex-
plain the exact nature of the results which follow from either kind
of action, and these I now propose to consider.

A. Hffects of Solfatarie Action.

To this cause must be assigned the alteration both of the pheno-
erysts (“ Kinspreninge”) and the ground-mass of the propylitic
rocks already described.

The order in which the several changes take place is often
capable of exact definition, when a large series of sections made

* Trans. Roy. Soc. Edinb. vol. xxxv. (1888) pp. 103, 104.
t Q. J. G. 8. vol. xxx. (1874) pp. 265-266, figs, 4, 5, & 6.

368 PROF. J. W. JUDD ON THE PROPYLITES

from carefully selected specimens, and taken from different portions
of a propylite-mass, are examined microscopically. |

We are able to see how clear plagioclase with vitreous lustre
(microtine) becomes gradually clouded and opaque, and in the end
completely kaolinized; the changes being, in the first instance,
developed along the planes of chemical weakness between the twin
lamelle ; but the extension of this action very frequently results in
the complete obliteration of all traces of the original twin-lamellation.
In some instances the felspar substance then breaks up into a
mosaic of different minerals, among which zoisite and a secondary
felspar usually appear to play the most important part. But in other,
and perhaps the majority of instances, the results are modified by the
impregnation of the products of the felspar alteration with ferro-
magnesian secretions derived from the decomposition of other
minerals in the rock. The consequence of this is that the necessary
materials for the formation of an epidote are brought together and
tufted masses of pistacite, or some other variety of that species, are
formed and replace a part or the whole of the felspar crystal.

The ferro-magnesian silicates at the same time lose their dis-
tinctive character, and green isotropic products (viridite) are formed
at their expense. Out of these decomposition-products various
chlorites are formed with the separation of secondary magnetite.
These, in turn, yield to further chemical action, and pistacite and
other epidotes are produced, forming more or less distinct pseudo-
morphs after the pyroxene, amphibole, or mica *.

The ground-mass is often one of the earliest portions of the rock
acted upon. Any glassy matter that may be present disappears as
the result of secondary devitrification, and the whole matrix of the
rock is frequently converted into a mass of secondary minerals.
Among these, various metallic sulphides are often very conspicuous.

When steam-holes abound in the rock the epidotes and other
secondary minerals crystallize out freely ; and in these situations
they are conveniently displayed for careful study and determination.
Beautiful amygdules, composed of epidote and other secondary
minerals, and filled in with still later deposits of zeolites, calcite,
and chalcedony, are, indeed, among the most conspicuous features
presented by the surfaces of such of these propylitic rocks as have
originally possessed a scoriaceous character. .

There are localities in which the kind of change which I have
been describing seems to have been carried to its farthest ex-
treme. In these cases epidote has been developed to such an extent,
at the expense of the other constituents, that it is now quite im-
possible to determine the original mineralogical constitution and
structure of the rock. The most marked example of this is seen in
the eastern spurs of the great mass of Beinn More in Mull, and
around ‘A Chioch. Here the epidotization of the rock-constituents
and the formation of numerous volcanic minerals has gone on to

* Compare Q. J. G. 8. vol. xlii. (1886) pp. 430, 431.

OF THE WESTERN ISLES OF SCOTLAND. 369

such an extent that it is often impossible to distinguish between *
lavas and tufts.

The characters of the propylites of this particular district, as we
now see them, are most remarkable, not one of the minerals of the
original rock being present in it. The ground-mass has been com-
pletely altered, all traces of glass having disappeared by secondary
devitrification, and many secondary minerals being developed in it.
The outlines of the original felspar-crystals can sometimes be made out,
but this is all. Their substance has been converted into aggregates,
among which epidote, zoisite, secondary felspar, and even quartz,
play the most important part. The ferro-magnesian silicates usually
appear as pseudomorphs in isotropic ‘“ viridite” or in some species
of chlorite. The resorption-halos of the hornblendes and micas can
often be detected by the clustered magnetite grains; and certain
forms of biotite may be seen developed at the expense of the secon-
dary chlorites. Lastly, in addition to the original magnetite grains
of the rock, we find enormous quantities of the same material pro-
duced during the breaking up of the ferro-magnesian silicates, a
process which is so frequently attended with the separation of mag-
netite grains (see Plate XIV. fig. 7).

As “ epidotization ” is the ulterior and most marked change of
which the propylite rocks exhibit evidence, it may be well to consider
the nature of the mineral species which result from the change.

From one of the extremely altered augite-andesites of Beinn
More, in Mull, Mr. W. B. D. Edwards isolated, by means of Klein’s
solution, a considerable quantity ot the beautiful green epidote, the
material proving, on microscopic examination, to be remarkably free
from foreign admixture. The specific gravity of the mineral proved
to be 3°42, and a partial analysis made by Mr. Edwards showed it
to be a lime-iron-epidote or pistacite. I find that all the optical
characters confirm the identification of the epidote in question with
this variety.

Besides the beautiful deep green epidote which is most abundant,
pale-coloured lime-epidotes occur, and some which have a pale pink
colour, probably due to manganese. ‘The highly coloured withamite,
however, has not yet been detected in these rocks.

It is a most suggestive circumstance that this solfataric action is
found to have been developed around each of the five great centres
which I have identified as the sites of the great volcanoes of the
Western Isles of Scotland. In most cases where this action cau
be shown to have taken place intrusive masses of granite and
felsite can be shown to be in tolerably close proximity to the altered
rocks. »

In a very interesting memoir, M. de Lapparent has insisted on

* I believe that there cannot be any reasonable doubt that the district lying
immediately to the east of the summit of Beinn More must have existed under-
neath what was the great central active crater of the Mull voleano, and in this

way the excessively altered condition of its rocks and the production of the
remarkable volcanic minerals described by me in 1874 is accounted for.

370 PROF. J. W. JUDD ON THE PROPYLITES

the close connexion that always appears to exist in different vol-
canic regions between solfataric action and eruptions of rock of acid
composition *. The same fact has also been pointed out by Schmidt f.
While the ejection of basaltic lavas is followed by actions that lead
to the formation of carbonates, the extrusion of great masses of highly
silicated materials is attended and followed by the escape of steam
containing sulphurous and other gases, which give rise to the
phenomena of solfataric action.

The rocks of the Western Isles of Scotland afford a very striking
illustration of this connexion between solfataric action and the
ejection of highly silicated rocks.

B. Contact-Metamorphisn.,

Studied microscopically, the sheaths of altered “ felstone ” that
surround the intrusion of granite or gabbro enable us to understand
the succession of changes which place as the result of the contact
of these rocks with great bodies of fused materials. As already
pointed out, these effects are strikingly contrasted with those re-
sulting from solfataric action.

We are, in the first place, forcibly reminded of the resorption-
halos which are seen surrounding hornblendes, micas, and other
minerals as the result of the action of a heated magma upon them.
But this action, instead of being confined to the immediate proximity
of the crystals affected, may extend to the distance of some inches or
even feet from the planes of contact.

All the ferro-magnesian silicates—pyroxenes, hornblendes, and
micas—break up into finely granular aggregates, which seem to
consist of an almost colourless pyroxene and of magnetite grains,
though other minerals may not improbably be present. In some
cases, however, the very minute granules appear to have the colour,
pleochroism, and other optical properties of melilite (see Plate XLV.
dig. 8).

te midst of these granular aggregates we sometimes find
scales of a deep brown, highly pleochroic biotite making their ap-
pearance ; and these increase in size and in number as the igneous
mass is approached. Clear colourless needles can also be detected,
and these may not improbably be referred to some species of secon-
dary felspar.

In these greatly altered rocks it is only possible to state what
was the nature of the original rock, by tracing the alterations step
by step from the comparatively unchanged mass at a distance from
the intrusions right up to the planes of contact.

VIII. Lieut tHrown By THe Srupy oF rHese Tertiary Lavas on
SOME OF THE OLDER VoLcaNnic Rocks (Porruyrires, FELSTONES,
&c.),

It was pointed out, in my former memoir, that in Scotland we
have brought close together remarkable masses of voleanic materials

* Bull. Soc. Géol. Fr. sér. 3, vol. xvii. pp. 282-290.
| Zeitsch. d. deutsch. geol. Gesellsch. 1885, p. 737.

OF THE WESTERN ISLES OF SCOTLAND. OTe

of very different geological ages. We can readily compare the
altered or unaltered rocks of the Tertiary periods with Paleozoic
lavas like those of Lorne, and of the great Central Valley of Scotland.
At the time when I wrote, all these Paleozoic lavas were generally
considered by geologists to be of Devonian age; but since the
publication of my paper in 1874 I have had the opportunity of
studying the remarkable volcanic rocks and conglomerates of Ballan-
trae in Ayrshire, and I cannot help thinking that a part at least
of the Lorne rocks may prove to be of the same age. I am at all
events fully prepared to subscribe to the opinion so clearly expressed
by Mr. Dugald Bell, namely, that the question of the age of the
Lorne lavas is still sub judice *.

Among these Paleozoic lavas we find just the same contrast
between almost wholly unaltered and greatly altered rocks, as in
Skye, Mull, or Rum in the case of Tertiary voleanic rocks. Mr.
Teall has shown that the glassy rocks of the Cheviot Hills are
really enstatite-andesites, which differ in no essential respect from
the recent lavas of Santorin and Krakatoa. Mr. Durham and I
have described in Fifeshire enstatite-andesites and glassy dacites,
which, though as old as the Carboniferous, are as fresh and unaltered
as the modern enstatite-andesites of Japan. In the Garlton Hills
near Haddington there occur sanidine-oligoclase-trachytes, of Pre-
Carboniferous age, which are strikingly analogous with those of the
Siebengebirge.

On the other hand, we find in the Pentland and Braid Hills
rocks, which, while of the same general ultimate chemical composi-
tion as the modern andesites, are remarkable for their obscure
structure and peculiar mineralogical constitution. A comparison of
these with the Tertiary propylites of the Western Isles of Scotland
is most instructive, for it shows that some of the “ porphyrites ”
are really andesites that have been subjected to the propylitic
modification, and then further modified by surface-agencies. It may,
indeed, be asserted of many of the propylites of Mull that, if their
abundant magnetite-granules, some of which are original and others
secondary, were changed to a red colour by peroxidation, they would
be quite undistinguishable from the obscure porphyrites to which
I have referred. These latter have such a peculiar constitution
that they have been classified by Dr. A. Geikie as “ felspar-magnetite
rocks.”

IX. Tur Younerr Avairp-AnDesires (‘ THOLEITEs,”
“¢ Prrcustones,” &¢.) oF THE WusreRN Isis oF Scornany.

While the older Tertiary andesitic rocks which we have been
describing are remarkable for the extraordinary and often extreme
changes which they have undergone, there exist other lavas of
similar composition in the district, which present the most marked
contrast with them, by the wonderful freshness of their appearance.
That these lavas are younger than all the plateau-basalts is shown

* Trans. Geol. Soc. of Glasgow, vol. viii, (1886) p. 116.

872 PROF, J. W. JUDD ON THE PROPYLITES

by the fact that they are found intersecting the basaltic sheets as

veins or dykes, while at other times they can be shown to lie upon.
their greatly eroded surfaces, as lava-currents. Of the same late age

are certain other rocks, some of more basic and others of more acid

composition, which will be considered in greater detail hereafter.

The whole of these rocks belong to the latest of the three periods to

which, as I showed in 1874, the Tertiary volcanic rocks of the

Western Islands must be assigned.

The lavas in question are of very considerable interest as having
been undoubtedly the iatest-erupted volcanic masses in the British
Islands. A careful study of them shows that they present the most
striking resemblances to some of the recent volcanic rocks of
Iceland. Dykes and veins of these lavas are found traversing the
thick ophitic olivine-basalts of the Western Isles of Scotland and of
Antrim. But other dykes of remarkably similar rock occur cutting
through the Paleozoic rocks of the lowland districts of Scotland,
and these reappear in the north of England, where some of them
can be shown to intersect Jurassic strata. Some of the Scottish
examples of these rocks have been well described by Dr. A.
Geikie*. The English examples have been admirably studied by
Mr. Teallt.

I have already pointed out< that along these lines of fissure now
occupied by dykes there is evidence of the outburst of a volcanic
material giving rise to lines of volcanic cones, which bore the same
relation to the great volcanoes of the Western Isles, that the chains
of “*puys” in Auvergne did to the great volcanic mountains of
Mont Dore, the Mezen, and the Cantal.

At two points only, so far as 1 know, have the lava-currents and
tuffs of this period been preserved. Thisis accounted for by the fact
that the amount of denudation in the district since the formation of
these small, subsidiary volcanic cones has been excessive ; and only
where the lava-currents were of unusual dimensions, or were of such
a character as to resist the action of denuding agencies in an
exceptional manner, was there any chance of their being preserved
for our study at the present day.

The first case of the kind noticed was that of the Sgurr of Higg,
which was so well described by Dr. A. Geikie in 1871 §. His
explanation of the mode of preservation of several successive lava-
sheets, by their being poured out into a valley that had been eroded
in the basalti¢ plateau, is one that must commend itself to every one
who has studied the district. Equally convincing is the evidence
he adduces of the enormous amount of denudation that has taken
place since the formation of these laya-flows, seeing that the basalts
forming the sides of the valley have all been removed, leaving the
later lavas as a mass crowning the summit of a long ridge.

* Proc. Roy. Phys. Edinb. vol. v. (1878-80) pp. 219-254; and Trans. Roy.
Soc. Edinb, vol. xxxv. (1889) pp. 24-73.

t Q. J. G. 8. vol. x1. (1884) p. 209.

t Q. J. G.S. vol. xxx. (1874) pp. 260-272.
§ Quart. Journ. Geol. Soe. vol. xxvii. (1871) pp. 303-309.

OF THE WESTERN ISLES OF SCOTLAND. 310

Not less interesting and remarkable are the sheets of lava with
the great masses of underlying tuffs that form the mountain of
Ben Hiant (Beinn Shiant) in Ardnamurchan. The general struc-
ture of this mountain will be understood from the accompanying
map and section, which have been constructed on the basis of the
recently published 6-inch maps of the Ordnance Survey (figs. 1 & 2),
see pp. 374 and 375. |

Lying in part upon the much eroded basalt of the plateau, in part
on the underlying Jurassic strata, and in part on the fundamental
erystalline schists, we find thick masses of volcanic agglomerate.
These volcanic agglomerates can be especially well studied on the
northern face of the mountain, and on the southern sea-washed
promontory known as Sron Mhor, or Maclean’s Nose. ‘They
vary in character from ordinary andesitic tuffs, to very coarse
breccias made up of fragments derived from all the underlying rocks
(crystalline schists, liassic shales, sandstones, and limestones, and
andesitic and basaltic lavas), with varying quantities of other vol-
canic materials.

The preservation of these agglomerates has been clearly due to
the fact that they were covered by currents of a peculiar lava, often
of a columnar habit, which cap all the spurs of this singularly
outlined mountain ; only the lower and more crystalline portions of
these laya-currents having in most cases escaped removal by denu-
dation. These lavas are found by careful study to be an andesite
presenting many remarkable varieties, to which I propose to call
especial attention in the sequel *.

The rocks of Ben Hiant find their closest analogues in the
augite-andesites of the Tertiary dykes of the north of England
(‘‘ tholeites” of Rosenbusch), so well described by Mr. Teall, and in
the rock of Eskdalemuir, for a very careful and accurate account of
which we are indebted to Dr. A. Geikiec. Mr. Grenville Cole, F.G.S.,
has kindly supplied me with a series of specimens collected by him
from the Eskdalemuir rock, which have proved of great service
to me in my comparisons.

Dr. A. Geikie has shown that in the case of the Eskdalemuir
dyke a marked separation has often taken place between the more
acid, vitreous parts of the rock and the more basic, crystalline
materials. In consequence of this, as shown by Mr. Grant
Wilson’s analyses, different portions of the dyke come to present
wide divergencies in composition and appearance 7.

* 'The main features of the remarkable mass of Ben Hiant were accurately
described by me in 1874. Dr. A. Geikie, asthe result of what must surely have
been a superficial examination of the locality, asserts that the lava of Ben Hiant
is a single intrusive sheet, and that it consists of the ordinary ophitie dolerite
of the “sills” that were erupted at the same time as the plateau-basalts. My
statement of 1874 that the rocks consist of a very remarkable augite-andesite
is borne out by the microscopic study of a very large series of specimens
derived from various parts of the mountain ; and the statement that the rock
is neither glassy nor vesicular is contradicted by the study of this large series
of rocks (see Plate XV.).

+ Proce. Roy. Phys. Soc. Edinb. vol. v. (1850) p. 256; and Trans. Roy. Soc.
Edinb. vol. xxx. (1888) pp. 40-44.

Q.J.G.8. No. 183. a

374 PROF. J. W. JUDD ON THE PROPYLITES

Fig. 1.—Sketch-map of Ben Hiant, Ardnamurchan.

LD

in
ZZ ,

GALI:

Sin
GLEE
tivis5

LEZ Ze tg
ld

Gp
LIE GE Zs

‘ort a Cham ais———~

zIMile

EAA) Augite-andesite lavas, passing into glassy varieties
ty a
LEZEZE, (‘‘ pitchstone-porphyries”) at x.

TERTIARY.
Volcanic agglomerates.

|
\ NEWER
|
)

Basalts &c. overlying propylites. OLprEr TERTIARY.

Sandstones and clays (altered). JuRAssic.

\. WS Crystalline schists &c.

375

nN
. my . . . a . =>)
Fig. 2.—Profile Diagram, illustrating the Structure of Ben Hiant, Ardnamurchan., ou
a (Viewed from the South.)
E
<
i)
=I
S 1729 ft.
RM
& a
° WYNNE
ie) i 4 \
&
4
mM
Loa
ve SNe
>] ANG I Fee SAA
: LL SS
2p Bree —————————— — —
= ee SSS AMAiAiA w@Q@X&s5
= Rudha Ailean Maclean’s Nose. Port a’ Chamais.
i)
&
io)

The shading of the different rocks is the same as in the Map (page 374).

* The glassy varieties of andesite (“ pitchstone-porphyries”) are well seen at this point.

376 PROF. J. W. JUDD ON THE PROPYLITES

Now the separation that has taken place within the Eskdalemuir
dyke, on asmall scale, has evidently gone on on a grand scale beneath .
Ben Hiant. The result of this has been that, while in some of the
laya-sheets of the mountain we find a glassy lava through which
porphyritic constituents are somewhat sparingly distributed (the
result being a “ pitchstone-porphyry ” similar to that of the Sgurr of
Eigg), in other cases masses of crystals with only a comparatively
small matrix of glass have been poured out, giving rise to a rock of
far more basic character than the pitchstone varieties.

In studying the Krakatoa lavas I was led to point out the
remarkable differences in the composition and appearance of rocks
resulting from variations in the proportion of acid ground-mass to
basic phenocrysts in a rock. My examples in illustration of this
principle were taken from Santorin, the Cheviot Hills, and Krakatoa*.
But here in Ben Hiant we find, among the ejections of the same
vent, the most wonderful illustrations of the same principle, one that
has been too much overlooked in our petrographical studies.

I shall show that among the lavas of Ben Hiant we have
varieties that are distinctly basic in composition, with a specific
gravity of over 3 and a silica-percentage of a little above 50. But
among the same rocks are others with a distinctly acid character,
having a density of only 2°45 and a silica-percentage of over 65.
Yet the minerals in all these rocks are identical; the same fel-
spars, the same pyroxenes, magnetite, and a similar glass, are
found in all; it is the variation in the relate proportion of these
several mineralogical constituents which gives rise to the very
wide diversity alike in the aspect and in the ultimate chemical
composition of these rocks.

Mineralogically these rocks exhibit, as I have said, a remarkably
uniform character. They consist of :—

1. Felspar, which is almost always either anorthite or labradorite,
or some form intermediate between these species. This is proved
by the extinctions which they give in the several zones, and is
confirmed when we examine specimens of them, isolated by the use
of heavy liquids, for their specific gravity, and the flame-reactions
which they give by Szabo’s method. The felspar-crystals are often
zoned, the different zones giving evidence of being of different com-
position, the more basic being in the centre. Inclusions are often
arranged parallel to these zones, and the first traces of schilleri-
zation are sometimes exhibited. Although the twin striation is
often very marked, cases of simple Carlsbad-twinning are not un-
common.

2. Pyroxene, an augite, sometimes of a green colour, at other times
brown. There is almost certain evidence that the brown augite is
an altered form of the green; indeed every gradation from the one
kind to the other can be found, and crystals occur which are in one
part green and one part brown. The original colour is certainly

* «The Eruption of Krakatoa and subsequent Phenomena ’ (1888), pp. 80-35 ;
and Geol. Mag. dee. ii. vol. v. pp. 1-11.

OF THE WESTERN ISLES OF SCOTLAND. OTT

green, and the brown tint is the result of alteration. Only the
faintest trace of pleochroism can be detected. Some of the crystals
show the beginning of the development of a structure lke that
exhibited by the augites in the older andesites of the district, which
is described at page 363. Osann has described and analyzed a
very similar augite from the augite-andesite of Kolter, in the, Faroe
Islands *. Its composition is as follows :—

“TL a tbe at )een D
RET a ch kx na tans ela 8 3°24
MV GTEOWUS ORIG): 50 hand os dach ound 17°40
RO, Ni screpart xc sbh shakes 13°92
POMS ST cai d. @ absiaeo' aloha 14:05

98°82

Rhombic pyroxene occurs in these rocks, but in small quantities,
and it must be regarded as an accessory constituent.

3. Magnetite occurs in distinct individuals, as skeleton-crystals,
or in roundish grains, and is in some cases remarkably abundant.

Olivine, like enstatite, is an accessory constituent and is very
variable in quantity. In some varieties of the rock it is not
rare, while in most cases it is wholly wanting.

Brown glass containing microlites of different minerals and often
corroding and forming enclosures in the felspars is usually present.
Sometimes, when it is present in considerable quantities, this glass
exhibits traces of both the spherulitic and the perlitic structure.

The best way of illustrating the remarkable varieties of struc-
ture and chemical composition which can be produced by combining
the same mineralogical constituents in varying proportions, and
with modification of internal arrangement, will be to describe some
of the leading types of the Ben Hiant rocks, and show how they
pass into one another by insensible gradations.

1. Typical Pyrowene-andesites.—These consist of a more or less
perfectly glassy ground-mass crowded with microlites of felspar and
augite, and grains of augite, the whole forming a “ microlitic felt.”
Through this base are scattered crystals of plagioclase, usually
abounding with glass-inclusions, and with remarkable zoned struc-
ture. Pyroxene is represented by both augite and enstatite, the
former being always the most abundant, though the latter mineral
is sometimes by no means rare. Magnetite grains also occur
scattered through the base (see Plate XV. fig. 2).

This rock not unfrequently contains vesicular cavities, which are
usually filled with concentric deposits of various secondary minerals.
The whole rock presents the most remarkable analogy with some of
the well-known pyroxene-andesites of Hungary. Indeed, if some of
my Ben Hiant and Hungarian sections were accidentally mixed,
I know of no characters by which I should be able to separate

them.
* Neues Jahrb, fiir Min. (1884), i. p. 48.

378 PROF. J. W. JUDD ON THE PROPYLITES

2. At some points, especially near the east side of the mountain,
lava-currents composed of a compact rock are found. ‘These, when -
studied microscopically, are seen to consist of a microlitic felt, in
which the large porphyritic crystals are wholly wanting. The rock
is vesicular, and the contents of the vesicles appear to be an
altered glass. The specific gravity of this rock was found to be
2°89 (see Plate XV. fig. 1).

3. Glassy (Vitrophyric) Andesite.—-At certain points, especially
on the eastern side of the mountain, the rock is found to become
perfectly vitreous and to pass mto a “ pitchstone-porphyry.” In
this the proportion of the glassy base to the porphyritic crystals
is sometimes very great, but the latter present all the characters of
the minerals found in the stony types of the rock (see Plate XV.
fig. 3).

It is interesting to note that im these glassy forms of the rock the
plagioclase crystals only show slight lamellar twinning in many
cases, and some of the types of the rock appear to approximate very
closely to the pitchstone-porphyry of the Seurr of Higg.

The glass sometimes exhibits the perlitic structure, and it varics
in density from 2°52 to 2°62.

4, When the glassy or microlitic felted base becomes small in
amount, it forms isolated masses which are caught up between the
crystals, and the rock exhibits the ‘“ intersertal structure” of
Rosenbusch in a very striking manner, the rock becoming a
typical ‘“ tholeite” of that author. In many cases the glass of
these ‘ tholeites” is crowded with skeleton-crystais of magnetite,
as in the case of the rocks figured and described by Mr. Teall *
(see Plate XV. fig. 4).

5. Highly Crystalline Andesites—In places, especially in the
great central mass of the mountain, in some of the dykes, and in
the deepest part of the thick lava-streams, the rock loses almost all
trace of glass, and passes into a holocrystalline mass. ‘These holo-
crystalline varieties sometimes exhibit the ophitic structure ; while,
as in the case of the ophitic basalt of the same district, the
breaking up of the augite and felspar crystals into rounded gra-
nules, leads to a more or less perfectly developed granulitic struc-
ture (see Pl. XV. figs. 5 & 6).

6. New varieties make their appearance in consequence of
differences in the proportion of the several porphyritic constituents
to one another. These varieties are especially seen in the dykes,
some of which contain the plagioclase felspar almost to the exclu-
sion of the pyroxenes and magnetites; while in other cases the
augite and magnetite are present in preponderating quantities,
and a rock of abnormal density and basicity is the result. (See
Pl. XV., compare figs. 7 & 8.)

The wonderful variation in chemical composition which may
result from admixture in varying proportions of the same mineral
constituents is illustrated in the following table of analyses :

* Quart. Journ. Geol. Soe. vol. xl..(1884) pp. 209-246, pls. xii. & xiii.

La

OF THE WESTERN ISLES OF SCOTLAND. 379

Analyses of the Later-Tertiary Augite-andesites (Pitchstone,
Tholeites, &c.).

. id's III. IV. \ VI.
SUG 52°68 57°57 58°67 65°49 66°62 65°81
RIA 855) 00.000. 12°66 14-42 14:37 14°66 14-02 14:01
Ferric oxide ......... 17°34 6°04 1°64 73 4-43
Ferrous oxide ...... AN 3°95 694 5:44.
Manganic oxide ... trace 0:27 trace
1S ea 11-45 6:87 7:39 3°72 2°74 2:01
Maenesia ............ 0:93 4-24 4:65 1:57 0°33 0°89
Oy 2°49 2:98 301 6°93 4°15
Li ee 1:91 1:08 1:42 151 6°08
Loss in ignition ... 0°70 L50 2-02 2°83 2°70

I. Analysis of augite-andesite (tholeite) with very little glass,
from N.W. spur of Beinn Hiant, by W. Tate. Made in the Chemical
Research Laboratory of the Normal School of Science, 1888.

II. Analysis of Cleveland Dyke (tholeite), made by Stock.

III. Analysis of crystalline portion of the Eskdalemuir dyke, by
Mr. Grant Wilson, 1880.

IV. Partial analysis of kernels of glassy rock in the Eskdalemuir
dyke, by Mr. Grant Wilson, 1880.

V. Analysis of glassy andesite from west side of Ben Hiant,
made by Mr. T. H. Holland in the Geological Research Laboratory
of the Normal School of Science, 1889.

VI. Analysis of the glassy andesite of the Sgurr of Eigg, made by
Mr. Barker North in the Chemical Research Laboratory in the
Normal School of Science, 1888.

These younger augite-andesites seem to be remarkable for the
tendency of the crystalline to separate from the glassy portions of
the mass. This is illustrated in the several ejections from the same
volcano, as in the case of Ben Hiant, and even in different parts
of the same dyke as shown by the interesting observations of Dr. A.
Geikie on the Eskdalemuir dyke, and in those of Mr. Clough in the
case of other dykes in Scotland. According to Professor Ditmar’s
analyses, the mass of the Dunoon Dyke contains only 47°36 per cent.
of silica, while the glassy segregation-veins contain 68-05 per cent.
of silica*. The contrast in chemical composition between some
of the Ben Hiant rocks, which are composed almost wholly of
erystals, and others made up almost entirely of glass, must be
equally great.

The tendency of the ground-mass in rocks of this kind to ooze out
from among the crystals and fill up vesicular cavities in the rock
has already been pointed out, and has been remarked upon by
Osann * and Teall +.

The dykes of pitchstone which traverse the basalt of Mull, near
Carsing and elsewhere, and also of the well-known dykes with the
same relations in Eigg, are usually glassy andesites, the porphyritic

* Trans. Roy. Soc, Edinb. vol. xxxy. (1888) p. 44.
t+ Neues Jahrb. fiir Min. &e. 1889, vol. i. p. 304.
t Geol. Mag. dec. 3, vol. vi. 1889, pp. 481-483.

380 PROF. J. W. JUDD ON THE PROPYLITES

crystals being plagioclase. In this connexion it may be mentioned
that -recent researches show that many of the rocks of Iceland
formerly regarded as rhyolites must really be referred to the group
or the very ‘acid andesites.

We have seen that the most glassy varieties of. the Ben Hiant
rocks have a very close analogy to the so-called “ pitchstone-
porphyry ” of the Sgurr of Eigg. This latter rock, from the presence
of Carlsbad-twins, has usually been regarded as a purely ortho-
clastic rock. But careful examination in polarized light often
proves that some of these felspars show undoubted evidence of
plagioclase-twinning. I have already remarked upon the fact that in
the glassy variation of these rocks the lamellar twinning of the
plagioclase often remains undeveloped. The quantity of glass
present as enclosures in these felspars would vitiate any result
obtained by their isolation and analysis.

Nowhere can we find such clear evidence as in the rocks of Ben
Hiant of the truth of the conclusion that the phenocrysts of such
lavas as these were formed under Plutonic conditions, and that there
is no direct and necessary relation between the porphyritic crystals
of a volcanic rock and the magma by which they are enveloped.

In the case of the glomero-porphyritic rocks, I have shown that
the evidence points to the existence of a holocrystalline mass having
been broken up and its fragments enveloped and carried up in a
magma of different composition. In certain pitchstones from Colo-
rado, for specimens of which I am indebted to Mr. Louis, I have
found fragments of micro-pegmatitic rocks enveloped in a perfectly
glassy magma. In hornblende-andesites from Auvergne I have
found glomero-porphyritic fragments of an enstatite-andesite, and
in the case of the Krakatoa lava I have shown that the crystals
are not scattered at random, but really form groups derived from
a preexistent nearly holocrystalline mass.

Now some of the porphyritic crystals of the Ben Hiant rocks
show all those features which I have already pointed out as being
characteristic of deep-seated rocks. Both the felspars and the augites
show incipient schillerization, and this is found to be the case even
in crystals enveloped in a perfectly glassy and vesicular matrix.

In the face of all these facts, I believe that it will be found
impossible to maintain that the porphyritic constituents of such
rocks as these could have been formed except under Plutonic condi-
tions ; and their present condition of corrosion and partial resorp-
tion proves that, in the voleanic masses as poured-out on the earth’s
surface, these materials of the Plutonic consolidation are in a con-
dition of instability—very different indeed.from that in which
they were originally formed.

[Since the reading of this paper I have had the opportunity of
studying the remarkable work of Mr. G. F. Becker on the rocks of
California. He has shown that, closely associated with the ande-
sites and basalts of the district, are great masses of glass, contain-
ing few crystals or none at all, and. presenting therefore a higher

OF THE WESTERN ISLES OF SCOTLAND. 381

silica-percentage and lower specific gravity than the rocks with
which they are associated. These cases, though on so much grander
a scale, seem comparable to those of the Eskdalemuir and Dunoon
dykes and the rocks of Ben Hiant. (See the Quicksilver Deposits of
the Pacific Slope, U.S. Geol. Survey, Monograph xiii. pp. 153-162.) |

X. SumMMARY oF RESULTS.

The oldest of the Tertiary volcanic rocks of the Western Isles of
Scotland (which were provisionally classed as ‘‘ felstones ” in 1874)
prove on closer study to belong, for the most part, to the group
called by von Richthofen ‘‘ propylites.” This term is used in the
present memoir in the sense proposed by Rosenbusch, namely, as a
“pathological variety” of the andesites and of their Plutonic
representatives. |

The rocks from which these “ propylites” of Scotland have been
formed find their exact analogues among the andesites of Iceland
and the Faroe Islands, which have been so well described by Zirkel,
Schirlitz, Osann, Bréon, and other authors. But in their present
condition the Scottish propylites agree in all essential respects with
the altered andesites of Hungary and Transylvania, which have been
described by Délter, Szabé, Koch, and other petrographers, and no
less strikingly with the rocks bearing the same name in the Western
Territories of North America—the rocks which have been so well
illustrated by the researches of Zirkel, Wadsworth, Becker, Hague,
and Iddings.

These Scottish propylites are distinguished by their dioritic
aspect, the alteration which their minerals have undergone, and the
development of metallic sulphides in their mass. In this way the
original characters of their constituent minerals is often completely
lost ; various epidotes and chlorites with much secondary magnetite,
biotite, and other minerals being formed at the expense of the
original constituents. In their general aspect, in their specific
gravity, and in their chemical composition, the propylites of
Scotland strikingly agree with those of Europe and North America.

The propylites are shown to be the oldest of the Tertiary lavas of
the district ; as a mass, they underlie the ophitic olivine-basalts of
the plateaux, though a few lava-currents of andesitic type are
found intercalcated with the latter. These propylite rocks form
lava-currents, which are generally short and bulky as compared
with the basaltic flows ; they also constitute ‘ cupolas” or ‘* quelle-
kuppen,” and lenticular intrusions (* laccolites ”).

By tracing these much altered rocks to points where the changes
produced in them have been less extreme, it can be shown that
they represent various types of andesite and of the deep-seated
representatives of those lavas, the diorites. Among the amphibolic
and mica-rocks, we find hornblende-andesites, hornblende-mica-
andesites containing enstatite, mica-andesites, and also true diorites
and quartz-diorites. Among the chief types of the pyroxenic rocks
described are glassy augite-andesites, labradorite-andesites, stony

382 PROF. J. W. JUDD ON THE PROPYLITES

augite-andesites, the so-called ‘“ diallage-andesites” with augite
diorites and quartz-augite-diorites. }

The causes by which the ‘ propylitic modification” of these
rocks has been brought about are two-fold ; namely, solfataric action,
which produces widely spread results, and contact-metamorphism,
which is strictly local in its effects. By microscopic study of the
rocks, the actions produced by each of these causes can be
discriminated and severally studied. The solfataric action appears
to have accompanied the intrusion of the highly acid masses
(granites and felsites) of the district, and is shown to have taken
place at each of the five great volcanic centres previously described.

The study of these greatly altered Tertiary rocks throws much
light upon the mode of origin of some of the most obscure among
the Paleozoic lavas—rocks to which the names of ‘“ felstone ” and
““porphyrite” have been applied. It is shown that while in some
cases these rocks are simply andesites which have undergone slight
alteration from the action of surface-waters, in other instances the
rocks in question must have been profoundly changed by solfataric
action and converted into propylites before the alteration from the
surface commenced.

In striking contrast with the older Tertiary and much altered
-andesites (propylites) of the district are the remarkably fresh
volcanic rocks which are everywhere seen to intersect and overlie
the eroded masses of the plateau-basalts, and are therefore of much
later age than those rocks. These younger rocks which are only
preserved as surface lava-flows at the Sgurr of EHigg and at Ben
Hiant in, Ardnamurchan are of much interest, as constituting the
most recent volcanic rocks of the British Islands. They are shown to
have the most striking correspondence in their petrographical cha-
racters with the rocks of the Tertiary dykes that traverse the south of
Scotland and the north of England, which have been described by
Dr. A. Geikie, Mr. Teall, and other authors. These rocks, which were
in 1874 referred to the augite-andesites, are shown, both at Ben
Hiant and in some of the dykes, to illustrate in a remarkable way
the influence produced on the characters and chemical composition
of rocks when the same mineralogical constituents are united m
varying proportions. In this case we find every gradation from
highly basic holocrystalline rocks, through various “ ophitic,” ‘“ in-
tersertal,’ and “ pilotaxitic” types of augite-andesite, into quite
acid “ vitrophyric” andesites (pitchstone-porphyries).

EXPLANATION OF PLATES XIV. & XV.

|The system of notation here adopted to indicate the magnifying-power used
for the rock-sections is explained in the Quart. Journ. Geol. Soe. vol. xlii.
(1886), p. 88.]

Puare XIV.

In this Plate an attempt has been made to illustrate the chief characters of
the Older Tertiary Propylites, and of some of the Andesites, of which they are
the altered representatives.

sag

OF THE WESTERN ISLES OF SCOTLAND. 383

Fig. 1 shows a twinned group of Augite-crystals, exhibiting partings, produced
by schillerization, along planes parallel both to the orthopinacoid
and the basal plane. ‘The crystals occur in a type of rock to which
the name of “ Diallage-Andesite”’ has been given by some authors.
It is from Mingary Castle, Arduamurchan. The specimen is shown
as seen with a magnifying-power of 100 diameters. (See p. 863 and
‘ Mineralogical Magazine,’ vol. ix.)

Fig. 2. Transverse section of a prism of the same Augite, showing the cleavage
and the secondary twinning parallel to the orthopinacoid, the planes
of the latter being crowded towards the centre of the crystal.
Showing, as magnified, 250 diameters.

Figs. 3, 4, 5, and 6, represent a few of the most striking types of the Older
Tertiary Andesite Lavas, as seen in parts of the rock-masses that
have undergone a minimum amount of chemical alteration. (See
p- 356.)

Fig. 3. Vitrophyric Augite-andesite, showing groups of crystals of plagioclase,
augite, and magnetite (with some apatite), sparsely scattered through
a glassy base, which is crowded with beautiful trichites. The latter
are in many cases resolvable into globulites. The rock is from
Mhaim Clackaig, in Mull, and is shown as viewed with a magnifying-
power of 25 diameters. (See p. 362.)

Fig. 4. Spherulitic Augite-andesite, from Beinn-a-Ghraag, Mull. Crystals of
plagioclase, augite (much altered), and magnetite are scattered
through a glassy base, showing incipient spherulites. These spheru-
lites are seen to affect a parallel arrangement, due to the movement
of the mass. Magnified 25 diameters. (See p. 362.)

Fig. 5. Glassy Andesite, from Bealach a’ Mhaim, Skye. The black glass is
almost as opaque, in thin sections, as that of the basalts (Tachy-
lyte). There are many spherulites, consisting each of two concentric
zones; and also spherulitic fringes around the much-correded
plagioclase crystals. This glass is associated with a ‘‘labradorite-
andesite.” Magnified 25 diameters. (See p. 364.)

Fig. 6. Banded Augite-andesite, from Beinn-a-Ghraag, Mull. The fiuidal
structure in the base of this rock is very beautifully exhibited, and
is rendered conspicuous by the manner in which the bands of
microlites are seen to curve around the porphyritic crystals.
Magnified 25 diameters. (See p. 362.)

In figs. 7 and 8 an attempt has been made to show the character-
istic differences in the effects of solfataric and contact alteration.

Fig. 7 is the Hornblende-propylite of Beinn Talaidh, in Mull. Scarcely a trace
of the original glassy base and plagioclase crystals can now be seen
in it; the colourless ground-mass consisting of secondary felspars
and epidotes, in which only occasionally the outlines of the pseudo-
morphs of original constituents of the rock can be detected. The
hornblende has been converted into mixtures of chlorite and
magnetite ; but in these pseudomorphs traces of the “ resorption-
halos” originally formed of pyroxene and magnetite, and consti-
tuting sheaths around the crystals, can still be detected. The
section is shown as magnified LOO diameters. The peculiarities of
the alteration of this rock are undoubtedly due to sodfataric action.
(See p. 369.)

Fig. 8 is the Augite-andesite from a point near its junction with the intrusive
granite (‘“‘granophyre’’) of Beinn Uaig, in Mull. Scareely a trace
of the original crystals of the rock can be detected. Ina colourless
and structureless base, which is anisotropic but not individualized,
we find numerous minute rounded granules of a colourless mineral,
usually taken for Augite, with many grains of magnetite. A little,
strongly pleochroic, brown biotite makes its appearance, and in-
creases rapidly in quantity as we approach the intrusive rock.
Magnified 100 diameters. (See p. 570,)

384 PROF. J. W. JUDD ON THE PROPYLITES

Priate XV,

In this Plate an attempt has been made to illustrate some of the varieties of ©
the Pyroxene-andesite of Ben Hiant. In these rocks the minerals and glass
composing the different masses are identical; but the proportions in which they
are combined and their structural relations are so different as to give rise to
some very strikingly contrasted rock-types. They are shown as seen magnified
25 diameters. (See pp. 373-880.)

Fig. 1 is a compact Augite-andesite from the south side of the mountain, and
under the microscope is seen to be a “ microlitic felt,” consisting of
lath-shaped felspars, with granules of augite and magnetite, imbed-
ded in a glassy base. The rock contains numerous small vesicles,
which are sometimes filled with glass, as described by Osann and
Teall. (See p. 378.)

Fig. 2 isa rock with a similar ground-mass, through which numerous porphy-
ritic crystals of plagioclase, with some of augite and magnetite, are
scattered. The plagioclase crystals contain many glass- and magne-
tite-inclusions; and in the ground-mass there are a few vesicles
filled with secondary products. In all its essential characters the
rock is quite undistinguishable from the Augite-andesites of Hun-
gary. (See p.377.)

Fig. 3. “ Pitchstone-porphyry” from the east side of the mountain (at the
point marked x on the map and section), In this rock the quantity
of glassy base becomes very large, and the crystals of felspar, augite,
and magnetite occur in sparsely scattered groups. The felspar-
crystals are sometimes much corroded. The brown glass of this
rock is traversed by many cracks, showing a distinct approximation
to a perlitic arrangement. (See p. 378.)

Fig. 4. Augite-andesite with portions of glass full of magnetite needles caught
up between the numerous crystals, giving rise to the “ imtersertal”
structure of Professor Rosenbusch. (See p. 378.)

Fig. 5. Augite-andesite in which the “‘intersertal”’ structure of the last type is
combined with the ophitic structure. (See p. 378.)

Fig. 6. Rock differing from the last by the almost complete disappearance of
the glassy material, so that the ophitic structure dominates through-
out the whole mass. (See p. 378.)

Fig. 7 is a rock in which a glassy base (with a few vesicles in it) encloses nume-
rous large crystals of labradorite (or of a felspar near that species).
Augite and magnetite are present only in comparatively small quan-
tity and as minute individual granules in the ground-mass, and the
whole rock becomes a good example of a “ Labradorite-andesite.”
(See p. 378.)

Fig. 8 forms a striking contrast to the last. There is little glassy matter and
the felspar is present in small proportions. The bulk of the rock
consists of augite and magnetite, and, though so closely related with
the other types, is remarkable for its low silica-percentage and high
density. (See p. 378.)

Discusston.

The Presipent said that papers like the present were difficult to
discuss. They required to be read and reflected upon.

Mr. Barrow, referring to the amphibole- and pyroxene-andesiest,
remarked that, in mapping some of the dykes in Scotland, he had
come across cases where amphibole prevailed in an acid matrix ;
secondly, where the prevailing mineral was mica; thirdly,
pyroxene; and fourthly, that the three minerals would occur
together, All these dykes were parallel to one another, and often
formed double dykes with the apophyses of tne Dee-Side granite.

OF THE WESTERN ISLES OF SCOTLAND. 385

He inquired if it were possible to get a connecting-link between
the amphibole- and pyroxene-andesites.

Mr. Cots, speaking of the dykes and sheets traversing the
plateau-basalts, inquired whether those with selvages of tachylyte
might be related to the later andesitic eruptions.

The Avurgor, in reply to Mr. Barrow, said that the existence of true
amphibole-andesites was shown, even when the change was most
complete, by the chlorites &c. occupying the place of the original
hornblende-crystals showing: traces of the ‘‘ resorption halos” so
characteristic of that mineral. He had described rocks which
contain amphibole, mica, and pyroxene; but in the district under
consideration the distinction between amphibole- and pyroxene-
andesites may be fairly made out. In reply to Mr. Cole, he was
not aware of any andesitic dykes traversing the basalts which
put on a selvage of tachylyte.

386 PROF. J. F. BLAKE ON THE MONIAN AND

21. On the Montan and Basat Camprian Rocks of Surorsurrn. By
Prof. J. F. Braxz, M.A., F.G.8. (Read March 12, 1890.)

[Pirate XVI.]
ConTENTS.

§ I. Inrropucrion.

§ 11. Srrarigrapuy or THE Lonemynp Hits.

1. General.

2. The Junction-line between the two Series (Lower and Upper)
in the Longmynd.

3. Constitution of the Western Part of the Longmynd Massif.

4, The Western Boundary of the Longmynd Massif, with the sup-
posed Archzxan Masses.

5. Summary of the Stratigraphy of the Longmynd.

§ III. Srraticrapny or run Voucanic Hitts.
§IV. PossiBLE MORE ANCIENT Rocks in tux Disrricr.

§ V. REeLations or THE OvERLYING ForRMATIONS.
1. The Quartzite.
2. The Succeeding Formations.

§ VI. GenuraL ConcLusions.

§ I. Inrropvucrion.

In my memoir “ On the Monian system ” as developed in Anglesey *,
I suggested that the Longmynd rocks might belong to the Upper
Monian, on account of their general similarity to those of Bray Head,
and that the Uriconian rocks of Dr. Callaway might be Middle
Monian, because they were at once Precambrian and Volcanic. As
these suggestions, which would be of some importance if true, were
matters of conjecture only, I have taken the first opportunity to
examine the district with care in order to arrive at a definite con-
clusion.

At the time of my writing, it was the universal opinion that the
Longmynd series were essentially, even if not typically Cambrian ;
but about the same date Dr. Callaway was suggesting to the local
geologists of Shropshire that in view of the break that existed be-
tween his “‘ Hollybush Sandstone,” which he regarded as Meneyian,
and the Longmynd series, it was doubtful if the latter were really
Cambrian, and he proposed that till this was decided, they should be
called Longmyndian t. The same argument was more strongly en-
forced last year by Prof. Lapworth, who writes, “the presence of

* Quart. Journ. Geol. Soe. vol. xliy.
t Trans. Shrops. Archzol. Soc. 1887.
¢ Geol. Mag., Nov. 1888.

Quart. Journ. Geol. Soc. Vol.XLVI. Pl. XVI.

77.5

,

REFERENCES.

HIGHER CAMBRIAN

QUARTZITE

CAMBRIAN GRIT

", 28°ONRD0
it] CAMBRIAN CONGLOMERATE |°2° 00°

PURPLE SLATES & GRITS|/|/////| HARD GREYWACKE ET EEE

PURPLE SLATE

] ESSSSS
DARK THIN SHALE P 4 DARK ALTERED SHALE |

VOLCANIC ACID ROCKS

HOLOCRYSTALLINE ACID AAA VOLCANIC BASIC ROCKS

CRYSTALLINE BASIC | we

19778 FRED* DANGERFIELD, LITH. LONDON

MONIAN & CAMBRIAN ROCKS

= tlle

SHROPSHIRE.

MINDTOWN

SMETHCOTE

CAMBRIAN

MONIAN

Quart Journ. Geol Soc. Vol. XIV. PIXVI

REFERENCES.

HIGHER CAMBRIAN

QUARTZITE HARD PURPLE suare[ |

CAMBRIAN GRIT CAMBRIAN CONGLOMERATE

HARD GREYWACKE uaa

BANDED GROUP

ae

DARK THIN SHALE OARK ALTERED sHALE| ||

VOLCANIC ACID ROCKS PORPHYRY Pau

HOLOCRYSTALLINE ACID VOLCANIC BASIC vocrs
CRYSTALLINE BASIC =

19778 FRED™* DANGERFIELO, LITH LONDON

PURPLE SLATE

ea a
! ’ *
7 4 ree her’
‘ ot -
A ; ue
. 7
¥ ves ice | P) . -
ay ’ ® ’
’ \ ‘ ' : , i
: . Lae, ;

' i nS , \
fi oe "an 4 § 1 tae
ae

7 bg de we he
i
i ‘ ss bo
» 4 sp Y a7
+ VSI SNE
‘ : 19% : ‘ov Bi:
j a uc r euhaw ew Lint!
’ wy
f ie ‘
"es ‘ i ye Py ue
i , ’ yioth i » cay " ee ih “i hal
4. Vout f ak : Ves
NT GTA re : ee
Te cit de aed al ; i . ae! a oe vn an
p = ; 1 2 ale Ae ; we 7
(ae } j
b :
F ‘ f
rt p
: lat it
\ “ my.
vy : VN Gag ete
‘ ms 4
‘ hy . of |
' at . bf
4 ; Ay
ay . ine
‘
| \
i i"
ey
.
,
7
a:
' Th
|
f
1
ye
at ‘
? , ? ;
t a
|
t ;
¢ ;
: ies
’ ’
ie
: ,
* ; "
r j %
: il
’ Sy ‘4 ‘ i
“4 4!

= ail Ad
ae = .
\

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 3ST

Olenellus in the (Comley) Sandstone appears at first sight to fix dis-
tinctly the Precambrian age of the so-called Uriconian rocks of the
Wrekin and their English equivalents, and even to render the Pre-
cambrian age of the Longmynd a matter of fair probability.” It
will be seen that in both these cases the age of the Longmynd
rocks was made to depend solely on their relations to the fossiliferous
sandstone; my suggestion, on the other hand, had arisen from en-
tirely different considerations.

In any definite attempt to determine the age of a group of rocks
like those of the Longmynd, it appeared to me to be a necessary pre-
liminary to obtain a thorough knowledge of the rocks themselves ;
but I had not the slightest idea where their examination would lead
me.

In their original description by Sir R. I. Murchison, in his ‘Silurian
System,’ they are treated as forming a continuous sequence, whose
base is to the east and whose summit is to the west, where they
are said to pass up into Lower-Silurian rocks. In this description the
lower part of the series is treated with care, but on the horizon of the
grits and conglomerates being reached, the remainder is lightly dis-
patched in the following words :—‘‘ These conglomerates and grits
form the central masses of the Longmynd, and are succeeded on the
west by alternations of similar strata. They are again followed
on the N.W. by various alternations of strata identical with those
described. Still further to the west, the purple-coloured grits and
sandstones and slaty schists prevail. The red grits are evidently of
regenerated origin, and often contain many small fragments of older
slate in a quartzose cement.”

Tt is the same with Mr. Salter in 1857 *. He divides the beds
below the red grit into eight groups, but the entire remainder
is classed as No. 9. His eight subdivisions are not very easily made
to fit with the six of Sir R. I. Murchison; but this is not to be
wondered at, both are quite true and are a matter of more or less
arbitrary grouping. He also shows in asection a perfect conformity
from the bottom to the top and a passage upwards into Lingula-
flags. The Survey section is practically identical with this.

But geologists have been staggered at the enormous thickness
that such a section indicates—some 26,000 feet, the beds being, in
the lower part at least, highly inclined. And this result it has been
hoped to avoid by introducing one or more synclinals. But whether
such synclinals exist or not, no evidence has been adduced except by
Dr. Callaway. In a paper by that author entitled ‘‘The Precambrian
Rocks of Shropshire, part ii.” +, a series of supposed Archzean masses
along the western boundary of the Cambrian grits is described.
From their occurrence it is presumed that we are here at the base
of the Cambrian instead of its summit, and it is stated that on the
east side of the line the Longmynd rocks dip easterly, of which one
example (but one only) is given near Lyd’s Hole.

As far as I ean gather, the memoirs and maps above referred to

* Quart. Journ. Geol. Soc. vol. xiii.
+ Ibid. vol. xxxviii.

388 PROF, J. F. BLAKE ON THE MONIAN AND

constitute the sum total of our available knowledge of the Long-
mynd group of rocks. It will be observed that they present us with
two views, partly discordant and partly concordant. According to
Murchison, Salter, and the Survey, these rocks form the base of a con-
tinuous series, and are of Cambrian age. According to Dr. Calla-
way they are isolated by faults from every succeeding rock (below
the Ordovician), and, if of Precambrian age, are at least younger than
the Uriconian, cf which they contain fragments. Both views agree
in considering them as a single series, and in denying that there is
amongst them anything older than both Cambrian and Uriconian.

Now the totally unexpected result of my examination is to show
that within the Longmynd area there are two unconformable groups,
one of which is older than the Uriconian, and the other of basal
Cambrian age. I must admit at once that this result is by no means
immediately obvious, and that there are many difficulties to be over-
come, principally arising, I think, from the way in which the rocks
have been squeezed together; but while the many points which
make against this view can all be explained away, those which make
for it can in no wise be accounted for in any other way that is in
the least degree acceptable. To avery large extent the whole question
is one of detailed stratigraphy.

SIL. SrrarigrarHy or tHE Lonemynp Hitts.

1. General.—lt has been noted above that in describing the Long-
mynd rocks Murchison and Salter made respectively six and eight
subdivisions of the rocks below the red grits, which form the
upper part of the series. In taking a single section, such as that
of Carding-Mill Glen, or the Ashes Hollow, we might, if we
pleased, make twenty or thirty subdivisions. The whole series
consists of well-stratified rocks in conformable succession, made
up of various-coloured slates and grits, and greywackés of various
hardness and coarseness. but I have not found it possible to trace
across the country more than five groups, and even with these it
would in many cases be impossible to say of an isolated exposure to
which group it should belong. In all of them there are bands of
hard grit, which may occur anywhere, in most there are small masses
of purple-looking slate, which, if more abundant, would indicate per-
haps another group (see figs. 1, 2, 3).

The five groups I have adopted are as follows:—On the
eastern side we have (1) a series of dark thin shales, which
are usually very soft, and contain bands of calcareous matter, corre-
sponding apparently to Nos. 1 & 2of Salter. To the west of these
succeed (2) a series of more solid rocks, many of them hard grey-
wackés, but many pale-coloured slates. When these are seen well
preserved, as in Minton Batch, they show a beautiful banding, being
composed of innumerable small beds, 2 or 3 inches in thickness,
with a fine ripple-drift lamination; but very often they seem so
compacted together that bedding is difficult to perceive at all. These
I call the “ banded series.” Further west comes (3) a mass of purple

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 389

slate of very schistose character, but soft. There are some bands of
grit, but on the whole it is very free from them. ‘This is No. 4
and part of 5 in Salter’s list. Following on we find (4) a large quantity
of hard and often micaceous greywacké, seen in Carding-Mill Glen
to contain many intermediate bands of slate, but the greywacké,
being in greatest abundance, almost always forms the isolated ex-
posures. This is Salter’s No. 6. Lastly we find (5) a pale greenish
slate which weathers purple, and is easily taken for No. 3 till a
fresh fracture is obtained. Associated with this are bands of purple
grit and greywacké, often micaceous. There is so intimate a mix-
ture in some places of these two kinds of rock, and such a segrega-
tion in one place of slates and in another of greywackés, that I
cannot separate them into two. They correspond to Nos. 7 and &
of Salter, and 5 and 6 of Murchison, whose descriptions of them, no
doubt taken in different glens, do not coincide in details, because
they both are true of particular sections.

Practically the above description is the same as Murchison’s, with
the exception of the last item.

The subdivisions in the lower part of the Longmynd rocks, which
I have here enumerated, are given in geographical succession, because
it may be doubtful which is their order of succession in time. This,
however, is the first point to settle. Murchison and every one else
reckons No. 1 the lowest, and I think it is so, but it requires defi-
nite proof. In the first place there is a pretty uniform dip towards
the west, only locally disturbed, and then so very irregular as to be
obviously accidental. Thus if the rocks do not succeed in time as
we pass west, they must be throughout inverted. Again, there are
numerous surface-markings in some of the groups, especially in the
purple and pale slates, the best known of these are the little hollows
referred to the borings of Annelids. Now wherever these are seen
it is the hollows that face west and the elevations which fit into
them that face east. If they were really Annelid-burrows, it would
prove the point, but this is by no means certain. However, the
specimen in the Museum of Practical Geology collected by Mr.
Salter, and figured by him in his second paper (Q. J.G.S. vol. xiii.
pl. v. fig. 1), supplies the required evidence. On this there
are at the same time ripple-marks, rain-spots, and the minute
depressions. Now of rain-spots we can be in no doubt, the con-
cavity must be on the upper side, and in the specimens the
depressions are on the same side as the rain-spot concavities. Hence
the upper side of the rock faces west. A third reason for believing
this arises from the nature of the rocks. Those on the east are en-
tirely unlike the overlying purple grits; but the group which lies
most westerly is so like the succeeding beds, as to give rise to great
difficulties, and suggest in some places almost a passage between the
two. It is far more probable that this is a true appearance than
that the basal beds of two groups should be so much alike; and if it
should be accepted that the overlying grits are unconformable to
the whole of the series, we may expect the included fragments at
the base to have been derived from the uppermost rocks. Now

i.a.G. 8. No, 183, QF

390 PROF. J. F. BLAKE ON THE MONIAN AND

these fragments are of purple slate, such as the western part of the
series alone will yield.

These considerations make it, I think, pretty certain that in going
from east to west we are passing over an ascending sequence. Nor
is there the slightest trace of a synclinal, anticlinal, or any other
folding. There are disturbances here and there, but they have very
little effect, and are mostly confined to the eastern slopes. Except
for being compressed and hardened, they are very little altered, and
if there is any cleavage it must affect the slates only, and be there
confounded with the bedding; only in one place, in Stony Batch,
did I observe an oblique cleavage.

The distribution of the various groups on the surface is indicated
on the map. Itis very possible that the lines of separation there
marked do not always indicate the same horizon in the series as they
should do, but the general tendency of all the rocks in one direction,
wherever their strike can be observed, and the remarkable scoring
of the hill-sides by the parallel crests of the harder strata, leave no
doubt that the whole is an ordinary sedimentary series, simply
turned up on end so as to dip at an average of about 80°, the lowest
dip being seen generally on the west, though it is seldom if ever
lower than GO°. This will give the series a total thickness of not less
than 3 miles.

The careful lithological description given of the series by Salter
relieves me from the necessity of saying much on this point, which
is pretty familiar to geologists; but there are one or two obser-
vations of importance.

It is plain that the oldest member of the series in this locality is
not a basal deposit. Its uniformity, the fineness of its material, and
its caleareous bands, all give it great resemblance to the higher
Welsh Cambrians, and show it to be the product of very settled con-
ditions, and to represent the most tranquil portion of the period of
the general formation. It must in fact be the upper part of a series
whose lower part is not revealed within the district. It could not
possibly be derived from the washing down of such volcanic rocks
as are found on its eastern border, nor without many intermediate
siftings from any series of gneissic or granitic rocks. If therefore
these rocks be Monian, as I hope to show, they must belong to the
upper part of it. The gradual coming on of coarser rocks indicates
a rising of the area of deposition, with the denudation of new and
less distant masses. First we have the fine banding which indi-
cates perhaps a littoral condition of things, and then an alterna-
tion. The greywackés and grits are at first of a finer character,
with very little mica, but the upper parts of groups 4 and 5 are often
coarser and more micaceous, and they gradually put on a purple
hue, but are invariably well bedded. As we approach the top, this
last fact is about the only reliable character, and it is extremely
hard, if not impossible, to distinguish some hand specimens of the
hard greywacké from the overlying grits. One well-marked band at
the top of Ashes Hollow is far coarser than these grits, and contains
abundance of small purple fragments, as though it had been derived

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 391

from the denudation of the slates amongst which it lies. This is
one of the difficulties, but the bedding is very clear, and there is no
proof that these apparent slate elements were ever hardened and
formed into rock before being imbedded with the other ingredients to
form agrit. The same similarity is seen in an outlier near Smeth-
cott; and near one south of Woolstaston the red grits of the under-
lying series are indistinguishable in hand-specimens from those of
the overlying. In the absence of any other evidence, this might
well be thought to indicate a passage, but it is equally well accounted
for by the latter being derived from the former and redeposited.

With regard to fossils, the lowest beds look by far the most pro-
mising, but the only evidence of life I have seen is some impressions
of Lingule found near the Church-Stretton Gasworks, but which
were unfortunately broken in removal. The purple slates of No. 3,
and the pale slates of No. 5 also look hopeful, and it is from these
that Salter obtained his best specimens. Rain-spots and ripple-
marks are undoubted, but it does not seem to me certain that the
small depressions were burrows made by Annelids, they certainly
have no signs of such burrows underneath them. They may, how-
ever, have been hollows occupied by coiled-up worms. ' In examining
the large specimen figured by Salter (Quart. Journ. Geol. Soc.
vol. xiii. pl. v. fig. 1) with me, Mr. E. T. Newton made a curious
discovery. The surface of the slab is covered with very fine discon-
tinuous curling tube-like bodies, which resemble exactly the castings
of minute worms; indeed I cannot doubt that such is their charac-
ter. In these then we have good evidence of the presence of minute
Annelids. As to the supposed Trilobites, the evidence is hostile.
The slates from whence they are derived are divided by irregularly
undulating, overlapping, intermingling surfaces along which they
split. These surfaces are remarkably smooth when compared with
one produced by fracture. In breaking open the slates, these smooth
surfaces come to be bounded by their junction-lines with old fracture-
surfaces, and these have often a pseudo-regularity. This, combined
with the peculiar undulation of the smooth surfaces, gives rise to a
hundred fantastic shapes, and it is one of these surfaces that has pro-
duced the specimen figured by Salter as the tail of Palewopyge, and
another the specimen referred by him to the head of Dikelocephalus
(Mus. Pract. Geology). No Trilobitic remains have as yet been
made known. What has given rise to these curious smooth surfaces
of separation it is difficult to say; possibly it may be an excessively
fine sediment coating a series of ripple-surfaces, or possibly, but not
probably, fragments of some kind of laminarian alga. They may
even be structural surfaces produced after the consolidation of the
rock,

The area assigned to these rocks in my map extends a less distance
to the north than is indicated on that of the Survey, because I have
taken notice of the thick masses of drift which conceal what may
lie beneath; and, though the underlying rocks may belong to the
same series, it is impossible to draw the lines between subdivisions
where nothing is seen. ‘The mass exposed to the North of Smethcott

2F2

392 PROF. J. F. BLAKE ON THE MONIAN AND

thus appears as an outlier. The eastern portion of this is composed
of mixed masses of purple-weathering slate and purple greywacké,
very much in the same way as No. 5, whose strike it continues and
to which it is referred. Several miles to the North-east is the small
inlier of Pitchford, surrounded by basal Carboniferous rocks. This
inlier is exposed along a stream, and consists of well-bedded ver-
tical glistening purple slates with hard greywacké bands. It is
not remarkably like any of the subdivisions ; but of all of them it
is most like the banded series whose line of strike it continues.
Further North still, but more to the West, stands the great inlier of
Haughmond Hill. Dr. Callaway has shown that the long line of
** oreenstone ” marked on the Survey map is really a conglomerate ;
the rocks to the East of the line consist mainly of hard greywackés,
but with occasional masses of pale slate. These alternations and
bedding are well seen in a quarry on the eastern slopes, where the
rocks are more micaceous than usual. This series represents No. 5
extremely well; and, as in the Longmynd and by Smethcott, is
easily confounded with the overlying rocks.

2. The Junction-line between the two Series in the Longmynd.—

We now pass to consider the junction of this lower series
of five groups with the conglomerates and grits which form the
upper part of the Longmynd massif. This is one of the most critical
matters in the whole question. As just noted, we may often think
we see a passage from one to the other, and if without due care we
assign an isolated exposure of purple grit to the overlying beds in-
stead of to No. 5, we may well believe they are interbedded.

The first point to be noted is that the great conglomerate, which
les towards the base of the upper series, seldom forms the actual
basal bed, there is almost always a mass of reddish-purple grit below
it (see figs. 1, 2). The true basal bed seems to be that referred to
by Sir R. I. Murchison, as containing small masses of purple slate.
These, usually about 4 inch in diameter, are angular and very dis-
tinct from the enclosing grit. These fragments are very like the
underlying slates, and suggest immediately a derivation from them,
which seems to be what Murchison means by saying the grits are of
regenerative origin. This special slate-conglomerate is not always
present at the base, but is found nowhere else within the eastern
band of grit with which I am now dealing. The second point to be
noted is that these Kastern grits never show any bedding,—a mark
of distinction, when the exposure is large enough, between them and
any similar grit belonging to No. 5 of the lower group.

Coming now to the line of junction between the two series, the
main feature in its great irregularity. The subdividing lines be-
tween the groups of the lower series are not quite straight, but they
have a remarkable general parallelism. This will be much impressed
on the observer’s mind if he fix their limits in each valley indepen-
dently, and discover that when these points of division are joined,
they form nearly uniform lines. But when we come to the line of
junction now under consideration, it is wholly different. This was
first seen by me in the patch marked as an outlier to the south of
Woolstaston (see fig. 1).

Q@. J. G.S. vol. | To face p. 392.

el

Finch to a mile.)

E.S
aes a Ragleth

Fehes to a mile.)

The Moile Slate,” “‘ Banded Series,”
and ** Dark S

Q. J. GS. vol. xlvi.] i [To face p. B82.

Fig. 1.— General Section across the Northern Part of the Longmynd and the Voleanic Hills, (Seale 1 inch to « mile.)

Wotatt y sos Gthevat Hit Pretest? Hs
MEE Tort

ey id

lak han Fle rtf Coro
s ss, ML Soetton 3

Duck sales “
SIP AEY sae /1E 1

Tig. 2—Geneval Section across the Southern Part of the Longmynd and the Volcanic Hills. (Scale 1 inch to a mile.)

Reant Lill ‘B.S Ex
Beghik

WNW: Adstene Till
2

a
Erolle Fi “ lor
ORM Linley MillIinet ; Lip eras Dae

Tig. 3.—Svetion across the extreme South Part of the Longmynd to the Iforderley Intier. (Scale 13 inches to a mile.)

The Monian Rocks in these Sections are those named “Pale Slates and Grits,” “Hard Greywacké,” “ Purple Slate,” “ Banded Series,”
and “ Dark Shales.”

aie ea) Aa ee

A. 4 ’
en ‘
A oa vi Cat ve
walks) ; Pe
yal) ge ?
*
’ tia
* j 4 ‘ * é
4 s ®
L ‘ ‘ t ’ * f
/
*%, r) t 7 %A he
vig i | ONL MODES ail lieea (OR Sato
: Gal Jyvetty «ial

Bisa ace SRA

f
}
i

a at aha ee

BASAL CAMBRIAN ROCKS OF SHROPSHIRE, 593

On leaving the Drift, west of Colliersley, we come upon some
rugged masses composed of purple-weathering slate in a nearly ver-
tical position, and with the usual N.N.E. strike. On reaching the
summit of the crest, the purple slate suddenly gives place to a great
mass of purple grit without bedding and full of large fragments of
slate. The line of junction is not very clearly seen, but seems to be
a little transverse to the line of strike in the slates. Other beds of
slate, however, in the road to the south strike directly at this mass.
There is slate on the other side of it in the road to the west, and
only a feeble indication of the grit is seen at the cross roads, appa-
rently superficial. Thus if the purple grit be not here unconform-
ably overlying the slate beds, it must be a local band within them.
But this last appears impossible, as it lies across their strike. From
this point it seems obvious that the junction sought is to be traced
at the base of the mass of purple grit.

From the cross roads the purple grit may be traced towards the
S.W. by the farm of Queensbounty by the entire covering of the fields
with its fragments, till we reach the eastern slope of High Bank
Hollow, where quarries are worked in it, and crags of it are exposed
for a certain distance along the slope; while to the base to the
south and on the western slope, there is nothing but the purple-
weathering slate, which lies below, many of the strikes of which, if
continued, would cut through the purple grit. These strikes are
everywhere nearly the same, and yet not in the direction of the
band of purple grit, which here is seen only on the higher parts of
the ground. ‘The mass of purple grit, which we have thus traced
from near Colliersley, thus appears to be an isolated patch, not,
indeed, actually seen lying on the edges of the slate, but whose main
direction crosses the line of their strike; it dies out along a nearly
horizontal line at a high level, and is without any stratification, and
its basal portion, if it be horizontal, contains many slate fragments.
I cannot see how such a mass can be anything than unconformable.

From this outlying patch it is some half a mile west before we
reach the main mass of the purple grit, on the western slope of
Hawkham Hollow. Here the line of junction, if not actually seen,
is strictly limited for a long distance within a yard or two of
breadth. Itis not, however, a straight, but a crooked line, though the
bedded slates, as seen, are everywhere nearly vertical, and parallel to
each other. If part of the line of junction coincides with the strike,
as it seems to do, the rest does not and cannot; and in one place
there are two crags not many yards apart of which one is slate,
striking directly at the other which is unbedded grit. There is here
no evidence of either twisting or interbedding, but the junction
appears to be an irregular surface both vertically and horizontally.

In these localities which lie on the valley-worn northern slopes,
the exposures are pretty clear; but, when we get upon the rolling
summit of hill-country, the relations of the beds become obscure.
From the sigmoid curve depicted on the map, it might be thought
that the irregularity of junction is thereby demonstrated, but it is
not so; the necessity for this curve is one of the difficulties. All
that can be seen is on the surface of the road. As we walk along

394 PROF. J. F. BLAKE ON THE MONIAN AND

towards the west, we pass from irregular grits of the older series to
purple grits with fragments of slate, thence to well-bedded vertical
pale slates, exactly like those of No. 5, and then on the descending
slope of the hill to the grit with slate fragments again. As far as
this spot would show, there might therefore be an interbedding, but
evidence elsewhere necessitates another reading which is indicated
by the curve on the map.

A little to the south of this the line of junction becomes very
nearly parallel to the Portway, along which for a couple of miles
there are occasional exposures of the purple grits and fine conglo-
merates. If this line were continued northward, it would nearly
coincide with the eastern boundary of the patch of purple grit south
of Woolstaston,—a fact which certainly suggests that the great area
of purple slates and greywackés now exposed to the west of this
patch has been laid bare by the denudation of a superficial continu-
ation of the purple grit.

On and near the roads into which the Burway branches on reach-
ing the hill-summit, are seen other exposures requiring explanation.
On the western slope of a small depression at the bend of the north-
ern road is seen a crag of purple slates and greywackés, with the
usual high dip and ordinary strike, but on the eastern slope of the
same depression is a mass of unbedded conglomerate, seen in several
crags on about the same level, and this is followed by coarse purple
grit, till the line of the regular junction is reached 3 of a mile to the
east. What happens to this patch of slate and greywacké to the
north is not seen, but it 1s cut out by purple grit on the south, and
reappears a little further on in surface-exposures over a limited
area. The great regularity of the slates and greywackés, and their
numerous alternations in the crag, forbid the idea of a local deposit in
the midst of the conglomerates and grits. The very limited develop-
ment and absolute absence of any indication negative the notion of a
fold; but all of this combined with the fact that the relations are
not here with the basal grits, but with the higher conglomerates,
point to an unconformity and an irregular surface, in other words
that these two patches of the older slates are ordinary inliers.

About ? of a mile to the south of these inliers, we have the con-
verse phenomenon to deal with,—the conglomerate and grit form a
well-marked outlier (see fig. 2). The northern end of this is seen
in Ashes Hollow, along the south-western slope of which it forms
near Narnells rock, which is also composed of purple grit, a horizontal
crag. Now if we work aloug the valley-bottom of the Ashes Hollow,
and examine only the rocks which are abundantly exposed all along
the stream and pathway side, we shall emerge on the Portway, by
Pole Cottage, without seeing anything else than purple-weathering
pale slates and greywackés, or having any notion afforded of the
presence of massive purple grits or conglomerates. It is only when
we climb to the crag which overhangs the southern slope, and which
has an unusual appearance even at a distance, that we find these grits,
so far away from where we should expect them. On the northern
slopes there are numerous exposures of rock, but not one of them is of

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 395

the purple grit, all are of banded greywackés. This shows first
that the outlier is here at its end, and secondly that it lies, not upon
No. 5 but upon No. 4 of the older series. In this locality, on the
S.E. of Narnells rock the actual junction of the purple grit with
the underlying rocks is seen (see fig. 4). This line of junction has

Fig. 4.—The Junction of Slate and Grit South of Narnells Rock.

here itself a dip towards the west of about 75°, showing that the
outlier is more or.less folded in with other rocks. The surface is
somewhat slickensided, and the line is slightly irregular and cuts the
edges of the underlying slates very obliquely. This grit is therefore
here seen to lie unconformably, but the evidence is scarcely satis-
factory or conclusive. If it had been conformable, the motion
which is indicated by the slickensides might easily have produced
the amount of unconformity apparent.

The eastern boundary of this outlier can be fairly well traced,
but the western which runs across heath-covered moorland is en-
tirely conjectural. But in the next depression we get its southern
termination, and the same phenomena are repeated. Here in Cal-
low Hollow, as before, if attention is confined to the stream-section
where almost every yard of rock is exposed, we find nothing but a
succession of bedded slates and greywackés, with the usual constant
dip and strike, carrying them straight across the valley, but the
moment we climb the slopes we come upon conglomerate. On the
northern side this may be traced in a horizontal line trending 8.F.,
each exposure facing a different rock in the series below. On the
southern side the same thing is observable. So too in the next hol-
low to the south, 7. ¢. Minton Batch, the boundary of the purple grit,
some of which has the purple-slate fragments, follows the contour
of the country, but the purple slates below are vertical and cross
the valley. If there is such a thing as local field-evidence for an
unconformity, I think we have it here.

Passing still to the south, we find ourselves approaching the
western slopes of the Longmynd proper, and no more dependent on
stream-sections and valley-sides. As soon as we descend these
slopes we come again upon purple slates and greywackés, and the
line of junction is seen to rise gradually towards the south, so that

396 PROF. J. F. BLAKE ON THE MONIAN AND

near Asterton we walk round an amphitheatre, crossing all the
while the strike of anything that has a strike, and always with the
slaty series below and the conglomerate occupying the crest of the
hill, The meaning of this still seems pretty plain. From hence to
the south all that is seen of the upper beds is a long tongue of con-
glomerate, with minor beds of grit, which except at one point per-
sistently keeps to the top of the hill. At the one point, however,
where it descends to the level of the road, there is the greatest diffi-
culty that anywhere may be felt about the unconformity. There is
here a great quarry opposite Mindtown Farm, and in this there are
vertical beds of slate with the usual strike, showing beautifully
ripple-marked surfaces, but far more solid than anywhere else. In
the higher portion of the same quarry is seen the conglomerate; in
one part it is evidently disturbed, but in the least disturbed por-
tion the two rocks have a great appearance of conformity, the con-
glomerate being to the east of and therefore below the slate. Still
further up the slope of the hill slate is seen again, and finally the
continuous mass of conglomerate. This appearance of conformity
is very staggering, but we know how easily such an appearance is
produced when rocks have been squeezed together, and this, I think,
is the only interpretation available in face of the facts already
adduced. It is the more easy to accept, because the conglomerate is
not usually the base of the series, it is nowhere else followed by
purple slate, and disturbance and squeezing have evidently taken
place. The purple slate here is much more like the upper mass of
that rock to be presently described, and it continues to have this
resemblance for some distance to the south, so that I am by no
means sure that it does not belong there. Yet in the same direction
the rocks become gradually more like the series No. 5, till at the turn »
of the hill by Hill Cottage there is no mistaking them. It is, however,
quite possible that the map may be here tinted wrong, especially
as the band of hard greywackés No. 4 cannot here be recognized.
Whichever way it is, it will scarcely affect. I think, the main con-
clusion as to the unconformity of the conglomerate.

On the other side of the tongue matters seem clearer. Along the
crest of the hill the hard greywackés are well seen in numerous
crags, till they are cut out by the crossing of the conglomerate, and
from thence the neighbours of the latter are the purple slates of
No. 3, well cleaved, in thin masses and very characteristic. Finally
along the southern margin we find the same phenomenon (see fig. 3)
as is so conclusive further north. Taking the low path, the innu-
merable exposures manifest an apparently continuous sequence with
constant strike of purple and pale slates, with occasional greywacké
bands, without a sign of conglomerate; but mounting the hill the
conglomerate is seen again, and the line that must be drawn to
separate its exposures from those of the slates is approximately
horizontal and entirely transverse to the strike of the latter*.

* It may be noted that the conglomerate seen does not resemble the Llan-

dovery conglomerate of the neighbourhood, which has a special character of
its own.

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 397

Such is the evidence that may be obtained from the Longmynd
hills themselves of unconformity between the two series. It will be
seen that the upper series has relations in different spots to 3 distinct
members of the lower series No. 3, 4, and 5. It would be still
more satisfactory if similar relations were established with Nos. 2
and 1. ‘There is little hope of this with regard to No. 2, but the
great outlier which lies to the south by Horderley shows the grit
and No. 1 in contact. On the side of the road from Horderley to
Marsh Brook, there is a long cliff of dark shale of exactly the same
character as No. 1 at Church Stretton, and at Horderley we find
in it the same calcareous bands. Behind this and above it comes
the purple grit as seen at the two ends of the mass. Capping
all is a cliff of Caradoc grit, which often by its screes obscures the
beds below. This sequence is repeated a second time to the east
by means of a fault as represented on the map. Passing south
the dark shale is soon lost sight of, and the purple grit swells out
into the bulky hill which stretches from Wartle Knowl to Aston.
The actual present position of these rocks in their relation to
each other, is doubtless due to faults (see fig. 3), but the presence
of the purple grit at all in this neighbourhood in association with
the lowest member of the lower series, 1s inconsistent with its
being conformably situated above No. 5. The only question is, are
these rocks rightly identified, seeing they are isolated in a faulted
outlier? As to the dark shales, they lie in the continuation of the
same band; and, though on the opposite side of a fault, this fault near
Church Stretton is seen to make no difference in their horizontal
position, because the beds are nearly vertical. Moreover there is no
other known rock below the Caradoc which they can possibly be.
As to the purple grit, there is nothing to distinguish it lithologically
from the western mass, the nearest exposures in the two areas are
less than 12 miles apart, and when last seen it was creeping east-
wards. It does not correspond to any other known bed below the
Caradoc, and the only alternative is that it is lower even than No. 1.
This, I think, would be a very rash hypothesis, resting absolutely on
no proof, and rendered extremely improbable by the phenomena of
the Caradoc and other volcanic hills, as will be seen in the sequel.
Rejecting this, then, the proof of unconformity between the purple
grit and the underlying series is complete.

I have gone into full details with regard to this point, because it
seems to me to furnish the key to the whole problem of the rela-
tions of the various Pre-Ordovician rocks of Shropshire.

3. Constitution of the Western Part of the Longmynd Massif.
I must now pass on to the questions raised by the western part
of the Longmnyd massif, viz., that which lies between the series
already described and the Stiper stones. This western part is con-
stituted by three members,—a lower series of grits and conglomerates,
a middle mass of slate, and an upper mass of grit. In the lower
mass of grit it has already been noticed that the conglomerate does
not usually lie at the base, but towards the southern part of its
range in the Longmynd it does. So it does also at the extreme

398 PROF. J. F. BLAKE ON THE MONIAN AND

northern end at Houghmond Hill, though at Lyth Hill it lies in
the middle, and a smaller conglomerate band and a mixed series of _
grits and slates form the base. In the southern outlier, near Hope-
say, there is an almost entire absence of conglomerate ; the only
places where I have seen it being the summit and slopes of Wartle
Knowl, where it is apparently at the base. From these facts I
conclude that the conglomerate has no chronological significance,
but is a mere accident in the formation of the purple grits, de-
pendent on the part of the surrounding country which at different
epochs supplied material to different districts. ven where the
conglomerate does not occupy the nearest position to the line of
junction, and there seems to be a great mass of purple grit between
it and the lower series, we cannot assume that this underlies it,
since the inliers in the middle of the Longmynd, unless brought up
by faults, have nothing between them and the conglomerate. More-
over, the absence of bedding prevents our knowing anything of the
dip, while the fact of the purple grit overlapping the slates and
greywackés seems to show that it is, on the whole, not far from
horizontal. It was therefore laid down subsequently to the primary
disturbances which set the slates on end.

With regard to the contents of the conglomerate, we have already
a valuable account from Dr. Callaway *, who, in association with
Prof. Bonney, describes eight examples, together with two specimens
from Haughmond Hill, belonging to the lower series, which are not
described in the same terms as the others, but-are supposed to have
been derived from the denudation of mica-schists. Four others are
from the grits, in which it is noted that many fragments are those
of voleanic rocks, a conclusion which I can confirm.

The nature of the conglomerate at Haughmond Hill scarcely re-
quires the microscope to demonstrate, the bulk of the pebbles being
of purple rhyolite. Dr. Callaway also notices a pale green felsite,
and I can add a fine-grained altered ash. But this conglomerate,
so obviously derived from the ancient volcanic rocks of the neigh-
bouring Wrekin, is exceptional. So also is the conglomerate of
Wartle Know], which is largely derived from an associated rhyolite.

The main conglomerates of the Longmynd are, on the contrary, —
principally composed of quartzite. The bed which lies to the east,
whose range I have been hitherto describing, contains, I should
think, about 95 per cent. of quartz- and quartzite-pebbles. The
question is, whence were these pebbles obtained? ‘There is, to my
knowledge, absolutely no quartzite in the volcanic series (the over-
lying quartzite is obviously of later date than the conglomerate),
nor do granitic rocks readily yield such fragments. Yet, from their
abundance, we are certain that there must have been a large mass
of quartzite, or quartz-veins, in the neighbouring Pre-Cambrian
rocks. The only indication of such rocks that I have met with has
been the abundant quartz-veins which render some portions of No, 4
and 5 almost a breccia. If the quartz-pebbles were not derived from

* Quart. Journ, Geol. Soe. vol. xhi.

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. B99

these, they must have come from some mass of quartz now hidden
from view. Now we know that the Monian rocks of Anglesey and
Ireland are richly provided with masses of quartz; and these
abundant quartz-pebbles may indicate, I would suggest, the presence
of similar masses in the neighbourhood, now hidden by later deposits.
With regard to the remaining 5 per cent., Dr. Callaway has de-
scribed two, one a devitrified rhyolite, and the other a perlitic quartz-
felsite. I have examined thirteen of these pebbles, in fact an
example of every variety which I could recognize as distinct in
the field, in hopes of finding amongst them some of the underlying
greywackés or slates. Most of them were so much altered before
they were imbedded that they are now difficult to recognize. The
first group consists of granitoid and gneissoid rocks; a specimen
from Lyth Hill is a typical gneiss, apparently resulting from the
deformation of a granite ; another, from Pole Bank, is a typical
mica-schist, also very much pressed, and showing everywhere micro-
spectral polarization asin some of the more alter ed schists of Angle-
sey ; a third, also from Pole Bank, is a holocrystalline rock of large
elements, of which only quartz and felspar are now recognizable,
though there are dark patches which from their shape suggest a
derivation from mica. It is brecciated in parts and generally calls to
mind some of the more altered granites of Anglesey or the eurite
of the Wrekin.

A second group consists of felsitic or rhyolitic rocks. One is a
very typical rhyolite, showing flow-structure to perfection. Another
is darker in aspect, but is full of well-marked spherulites, and its
insets are mostly of felspar. A third is also obscurely spherulitic,
but the secondary crystallization is carried so far as to make it
almost a macrofelsite. A fourth has decayed spherulites of irregular
outline now marked by irregular radiating lines of dark dust, and
between them are numerous irregular cavities as in an amygdaloid,
now filled with radiating zeolites (?). A fifth is nearly black, and
the numerous spherulites are almost entirely obscured by the
abundant dark amorphous dust which colours the rock. Different
as these rocks are to the naked eye, their insets in every case
declare them to be essentially quartz-felsites which had suffered
much alteration before they were imbedded.

A third group consists of the doubtful rocks, whose external aspect
suggests that they are bedded; one of these is a fairly coarse quartz-
felspar grit, obviously derived from a granitic rock, and which may
in fact be a fragment of greywacké. A second is a finer-grained,
more quartzose grit full of dust, and with nothing to suggest its con-
nection with a rhyolite. The other three are very plainly banded ;
one, which to the naked eye looks exactly like a slate, has broad
parallel bands of dark amorphous dust, the clearer spaces being ex-
cessively fine polarizing material, which resembles very closely the
material of a slate from near All Stretton. There are, however, in
this rock several large isolated fragments of quartz and felspar which
resemble insets, and. it is possible therefore we have here only a
banded ash. Another also contains irregular bands of dust, and

400 PROF. J. F. BLAKE ON THE MONIAN AND

innumerable grains of uniform size following more or less the appa-

rent stratification, but it contains too some larger crystal fragments _

of felspar and zircon. A third, which is very dark, has the uniform
grains still better stratified in the midst of diffused dust. The grains
appear to be of felspar rather than quartz. This group does not,
as I expected it would, leave absolute conviction on the mind that
it is derived from the neighbouring underlying series; but this
much may be safely said, that no such rocks have been found as yet
forming part of the volcanic series of the neighbourhood, and they
are very like the neighbouring slates and grits. Certainly the
evidence of these contained pebbles is favourable rather than other-
wise to the unconformity observed in the field.

To return to the stratigraphy proper. After passing the con-
glomerate in a journey towards the west, we come again to a vast
mass of purplish grit, which, as before, shows little sign of stratifi-
cation, but is much intruded upon by masses of greenstone. Where-
ever any bedding is seen, as east of Church Pulverbatch, the strike is
still to the N.N.E., and the dip nearly vertical. After passing a
varying breadth of this grit, we come upon the mass of rock which
forms the middle portion of the series. This, though mentioned by
Murchison as “ alternations of strata identical with those described,”
seems generally to have been overlooked. If we make a traverse in
various latitudes, we find towards the south more than two miles’
breadth of solid purple slates, always dipping at a high angle
towards the west, and with an average N.N.E. strike. The whole
hill on which Wentnor stands is composed of this rock, and it
may be traced in numerous exposures as far as Norbury. The
breadth is little less in the traverse through Medlicott farm and
Gravenor, though many thin bands of grit are hereabouts inter-
calated. Near Ratlinghope the breadth is reduced to about a mile,
but the rock is admirably seen in the highroad at Bridges, and a
little further N. on the hill above Stitt Farm, though everywhere
within its range it may be easily traced. In the neighbourhood of
Cothercott it is reduced again to about a quarter of a mile, which it
never again exceeds. No exposures of the slate are seen north of
Castle Pulverbatch, but the last relic of it may be recognized in the
quarry north of Longden Common. This slate may be easily dis-
tinguished from those of the older series (except in the neighbourhood
of Mindtown) by its greater massiveness, and by the absence of the
numerous subdividing, cleavage-like planes. Its occurrence in the
middle between two masses of grit may seem to indicate a synclinal,
but the dips observed give no countenance to this idea; there is not a
single reversed dip in the whole area. We may perhaps think of an
isoclinal, bat in such a case we should expect the boundary to be
more regular than it is; the eastern boundary, in particular, is by
no means a straight line. In tracing these boundaries, however, a
new feature occurs which is very instructive when contrasted with
the inferior limit of the grit, where, as has been seen, it is also in
contact with slate. On both sides of this upper mass of slate there
is abundant evidence of its intercalation with the grit, so that the

sr
7 a

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 401

boundary has to be drawn as a zigzag-line. This is best seen near
Norbury and Cothercott on the western boundary, and near Church
Pulverbatch on the eastern, and many sections show intermingling
of the two kinds of rock. The phenomena are thus quite distinct
from those of the unconformable junction, and I judge they are
entirely due to an intercalation of deposit which thickens rapidly
towards the south, and dies out towards the north. It is obvious
that if there were here a synclinal and it actually died out, we
ought to be getting to its base, in which case the isoclinal expla-
nation fails, in face of the still nearly vertical position of the alter-
nating strata.

The western purple grit, which constitutes the third member of
the upper series, is very similar to the eastern, and, like it, contains
sporadic bands of conglomerate. As every available exposure has
been examined, I am prepared to say that the extent of its con-
glomerates cannot well be much greater than is marked on the
map, which indicates that they are less continuous and narrower
than in the other, and occur on several distinct horizons. I have
sought in this conglomerate also for fragments other than of quartz,
but they are far more rare, only three specimens in all the expo-
sures having tempted collection. These are all quartz-felsites, one
of them very spherulitic. The contents are therefore not so various
as in the lower bed; and the upper one may be properly termed a
quartz-conglomerate. In the grit itself there are more signs of
bedding, and in most places the dip is still high towards the west.
However, at the northern end, in the neighbourhood of Pontesford
Hill, we find the only examples of reversal of dip in the whole area.
Thus in the great crag of conglomerate in Oaks Hill, though the beds
are nearly vertical, they do incline towards the east; and in the
river-section above Lyd’s Hole there is an undoubted easterly dip
of about 60°. It is very tempting to consider these to be the true
dips as Dr. Callaway has done, and to infer that the rocks which
succeed them to the west are of an underlying series. But we are
here in the presence of a large mass of igneous rock, which at least
may be intrusive, and therefore we should be cautious, and take our
observations, as far as may be, away from such possible disturbers.
Leaving, then, this Lyd’s Hole district for the moment, we will go to
the extreme south,—to the other end of the range. Now here we
may observe numerous dips throughout the whole extent of Linley
Hill, and they are always rather low and to the west, no dip being
above 60°, and one as low as 20°. It is in this district also that we
meet with other rocks which, from their intercalation with the purple
grit, seem to follow it in regular sequence. ‘This, I take it, supplies
us with the true reading, and proves that there is no synclinal.

It may seem remarkable that the beds of the upper series, if it be
unconformable to the lower, should nevertheless have the same ap-
proximate strike. But this is easily accounted for. Where the grits
and conglomerates mount on to the summit of the Longmy nds, they
do not possess the same strike; but when developed in the already
denuded yalley to west, the subsequent pressure has pushed them up

402 PROF, J. F. BLAKE ON THE MONIAN AND
into a nearly vertical position against the buttress formed by the
older Longmynd rocks, and the directions of the earlier and later
pressures have been approximately the same.

4. The Western Boundary of the Longmynd Massif with the supposed
Archean Masses—We now come to consider the western margin of
the Longmynd grits. Ifthe account already given of the rocks of
this massif be accepted, and an upward succession broken by an un-
conformity be traced all the way from Church Stretton, we are here
well up in the Cambrian, as represented by Murchison, Salter, and the
Survey, and this western margin has little interest in relation to the
older rocks. But Dr. Callaway has here described a “ second area of
Archean rocks,” * and his proofs of their occurrence must therefore
be examined. He states that the eastern margin of the Longmynd
grits is formed by a fault, indicated on his sketch-map by a straight
line; and immediately to the west of this, and in contact with the
fault, come the masses referred to the Archean. If there were
really Archean exposures here, with the Longmynd rocks dipping
away from them, as stated, it is essential to the proof of their age
that they should be thus in contact. This, therefore, is the first
point to examine.

In the extreme north of the range is Pontesford Hill. All of
this, with the exception of the central dolerite, is referred by
Dr. Callaway to the Archean, the proof assigned being the simi-
larity of the rocks to the Wrekin lavas, and particularly that of
Lea rock. ‘There is, indeed, a remarkable pyromeride on the north-
western border, as noted by Murchison; but, as we are scarcely
justified in assuming that all such rocks, even in the same district,
are of the same age, the question must be determined by the strati-
graphy. The igneous portion of the hill consists of two masses of
acid rock everywhere separated by a mass of basic rock. Now this
igneous portion is xot in contact with the purple grits. These latter
are limited to the eastern slopes of Habberley Brook, while the
whole of the western slope, which is formed by Pontesford Hill, is
occupied by well-bedded, soft, compact pale slate with a moderate
dip of about 30° to the west. It is above these slates, on the higher
slopes of the hill, that the igneous rocks are met with. On the
other, or western, side of the hill only part of the slopes is occu-
pied by a spur of decomposed basic rock; the rest of the ground
between the two masses of acid rock shows numerous exposures ot
pale slates and grits of varying coarseness, with the usual high dip
and strike of the district. As we descend the hill from the doleritic
summit we cross the strike of these rocks, and at a lower level come
upon the pyromerides. In the neighbouring Lyd’s Hole section we
obtain further information. Of the section here seen we have had
two descriptions, of which that by Sir R. I. Murchison seems to me
to render the true interpretation. The slates and grits which here
alternate above the falls are very much altered as they approach the
igneous rock, the grit being rendered micaceous and the slates

* Quart. Journ. Geol. Soc. vol. xxxviii.

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 403

chiastolized, and both are indurated. Below the falls there is
another mass of micaceous altered slate; and irregularly related to
this is seen a mass of pyromeride on its western side. The igneous
rocks appear to have run in among the slates along their bedding,
and their flow-lines, like the crystals in many dykes, are naturally
parallel to the sides of the path. ‘The whole of the grit that is seen
in Radlith is also very much altered. In any case the acid igneous rock
is In association here with purple slates and grits, which are recog-
nized as Cambrian. On the other, or eastern, side of the hill, the
associated slates and grits are of a different character. The area is
certainly a faulted one, and the unusual dip of the conglomerate and
erit may be thus accounted for, if the igneous rocks are of later
date. Rhyolite pebbles are doubtless found in the conglomerates,
but not abundantly, and they do not specially resemble and need
not have been derived from the rock here exposed. JI can find,

‘therefore, no Archean rock here, but conclude we are altogether far

above the base even of the Cambrian.

In the next locality referred to, near Gatten Lodge, there is nothing
very peculiar to be seen. ‘The western side of the Longmynd grit in
many parts of its range is marked by veins of baryta, sometimes
associated with copper, as at the old workings at Westcot; and
Gatten Lodge is a spot where these veins are abundant and have
been worked. ‘heir presence indicates doubtless some disturbance,
and the grits do put on a very compact and irregular appearance; but
under the microscope they are grits still, as will be seen by Prof.
Bonney’s description of the rock submitted to him, and which I
entirely confirm. ‘There is nothing Archian here.

The locality referred to as Knolls Ridge and Cold Hill is par-
ticularly instructive (see fig. 2). On the north of the Farm of
Squilver commences an acid igneous rock, of rather varying cha-
racter, but mostly of grey felsite, which can be traced uninter-
ruptedly as far as Cold Hill Farm. At first it is in contact with
a bed of conglomerate ; a little further south there is a mass of grit
intervening in the valley-sides between the felsite ridge and the
conglomerate ridge, which come together again at the southern end.
The felsite ridge then leaves the conglomerate, and is separated
from it by a valley of pale slate. At Cold Hill Farm the con-
glomerates are seen dipping westerly at 60°, They are followed
by the pale slates seen in the road to dip at the same angle, and
further to the west comes the exposure of felsite. This proves that
the felsite ridge is transgressive across the edges of the strata, which
are here pretty nearly in their natural succession. This conclusion,
perhaps, is made more certain by the occurrence of two masses of
similar compact felsite in the heart of the Cambrian grits, as marked
on the map. Here, then, there is nothing Archeean.

As we trace the pale slates to the south, we see them rise at last
into a conical elevation called Chittol Hill. Here they are more
compact and greener, and the bedding is somewhat difficult to make
out. They appear to be not far from horizontal. The cause of
their elevation and compact appearance may be connected with some

404 PROF, J. F. BLAKE ON THE MONIAN AND

copper vein in the neighbourhood, as the fragments are all tinged
with the green salts of that metal. But the rock is unquestionable ;
it is the ordinary follower of the grits throughout the district. -
This, then, is not Archean.

At the southern base of this hill there is a transverse fault
bringing up the conglomerate alongside of the slate. This con-
elomerate is followed to the west in the south end of Chittol Wood
by a mass of compact felsite, very like that of the Knolls Ridge,
whose relative position it occupies, and whose interpretation it will
therefore follow.

On the western banks of the West Onny river, by the side of
Linley Drive, we have a series of very instructive sections. All the
rocks have a dip of about 60° to the W. by N., and the river crosses
them successively. They consist of a series of alternations of
rock, some of which exactly resemble the purple grits, and others
the compact Chittol slates, and others are of intermediate character ;
we could not desire a better illustration of the passage upwards
from the grits into the slates. But these beds, though quite con-
formable in their strike with the grits of Linley Hill itself, are so
situated that if continued either way they would run into the masses
of felsite exposed in the neighbourhood. They would equally run
into the associated greenstones, and we have no reason in either
case to assume these igneous rocks to be anything than intrusive.
Whatever, therefore, the exposures of acid rocks at Knolls Wood
and Oldmoor Wood may be, there is no reason to call them Archean,
unless we are prepared to maintain that every acid rock of volcanic
origin, or composed of volcanic fragments, is ipso facto, Archean,
The supposed ridge of Pre-Cambrian rocks in this district is there-
fore non-existent; the whole is of Lower-Cambrian age.

5. Summary of the Stratigraphy of the Longmynd.—The results
obtained up to this point may be summarized as follows :—There
are two series of rocks in the Longmynd; the lower series is divi-
sible into five portions, which may be traced across the country and
into the outliers. The upper series les on this unconformably, and
is seen in various parts in relation with four out of the five sub-
divisions of the lower series. It consists of three main members,
which are reduced to one in the north by the dying-out of the
middle one. There is no sign of a synclinal in the whole range,
but the normal dips get smaller to the west. The rocks succeeding
this tripartite series are pale hard slates, whose normal succession
may be seen in the south, but elsewhere may possibly be obscured
by a fault, near which several masses of acid igneous rock have
intruded transversely. The pebbles in the conglomerate may pos-
sibly have been partly derived from some portions of the older
series, but it certainly contains pebbles not only of quartzite unseen
in the neighbourhood, but of acid volcanic rocks also.

Now Dr. Callaway has irresistibly argued from finding such
acid igneous rocks in the neighbouring hills of the Wrekin, Caer
Caradoc, and others, that we must regard the conglomerates as
derived from them, and therefore as of later date than they, pro-
vided the stratigraphy permits it. |

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 405

If the Longmynd conglomerates are Cambrian, the volcanic hills
themselves must be in some sense Pre-Cambrian, so must they be
also if the conglomerates are Pre-Cambrian. To use Dr. Callaway’s
names, so long as the Longmynd series was undivided, it was certain
that the “‘ Longmyndian” must be younger than the “ Uriconian.”
But now that I have shown that there are two unconformable
series, this argument only applies to the upper series which contains
the conglomerates; and the relation of the older series to the
Uriconian is left entirely undecided, and must, if possible, be deter-
mined by details of stratigraphy. To this I now apply myself.

§ III. Srrarierarny or ran Votcanic Hits.

It is not my intention to go into all the details of these hills ;
they have been already described by Dr. Callaway, and are now
receiving the attention of Prof. Lapworth. To him the many points
of general interest in their structure may be left, and those only
attended to which have some bearing on the age of the rocks. The
place to commence our examination of these hills in their relation
to the Longmynds is obviously where the two come closest together
in the neighbourhood of Church Stretton.

The first question to deal with has relation to the fault that is
there drawn between the two. In the south of this district, from
Aston-on-Clun by Hopesay, Hordeley, and Marsh Brook, this fault
may be traced without a shadow of doubt. It has here a re-
markably straight course with only a general curvature to the east.
Leaving it now for the moment from the southern end of Ragleth to
that of Caer Caradoc, we find the western boundary of the latter a
remarkably straight line, as is that of the Lawley; and the suc-
cession of beds on the west: proves this to be a continuation of the
fault. Thence it is traced on the Survey Map as far as the Severn,
near Cound Villa, and if still continued it would form the approxi-
mate western boundary of the Wrockwardine mass. It is therefore
a very continuous fault. But it does not appear that its throw is
very great; Professor Ramsay estimates it at 2000 feet; but, con-
sidering the overlap of the Llandovery which reaches the Longmynd
slopes, and must be thinning out, this would appear to be a maximum.
If now we continue the line of this fault across the interval
omitted, 2. ¢. from Ragleth to Caer Caradoc, we must either assume
that it zigzags about just here in an unaccountable manner, and as
it does nowhere else, or we must leave some of the Longmynd
shales on the eastern side of it, as is done by the Survey. With the
high dip of these dark shales to the west, an upthrow of 2000 feet
on the east would not cause a loss of more than 200 feet on the
surface, so that we should still be probably in the dark shales on
the eastern side of the fault. Now all the slopes of Ragleth are in
the dark shales. They are seen very near the line of fault at the
crossing of Watling Street and the Church-Stretton road, from
which spot there is an almost continuous section exposed up two

Q.J.G.8. No. 183. 2G

406 PROF. J. F. BLAKE ON THE MONIAN AND

roads to Ragleth Wood and Hazler, over a horizontal breadth of
2000 feet. Further north, on the road from Church Stretton to
Caer Caradoc, they are exposed with their usual dip and strike be-
neath the Drift; and on the southern slopes of Caer Caradoc, they
occupy a band running transverse, and almost perpendicular, to the
line of fault. All these exposures being to the east of the fault, it
is obvious that this last has no connection here with the relations
of the dark shales to the igneous rocks, and we cannot solve
the question by saying that the junction is a faulted one. It does
not, of course, follow that the great fault is the only one; indeed,
we know that there are several others on the N.E. side of Caer
Caradoc, and the whole area on the eastern side of the main fault
is greatly disturbed and dislocated. This fact is of use in accounting
for certain difficulties, but will not solve the question as to the
relation of the rocks before they were locally faulted.

Eliminating, therefore, the influence of the main fault, we must
now inquire into the relative age of the adjacent volcanic group and
dark shales. If the dark shales be the younger, and are merely dis-
placed by local disruptions, we ought somewhere to find their basal
beds. They are not at all the sort of rock to show basal beds or to
be derived from volcanic débris—indeed the actual result of the
denudation of the rhyolites is seen in the Longmynd conglomerates.
There are indeed grits and conglomerates which may be considered
basal on these hills, but their relation to the igneous rocks and
shales is nowhere such as to indicate that they lie between them, being
usually found remote from the junction, so that they are the basal
beds of another formation. On the other hand, if the volcanic
rocks be the younger, however much clastic material they may
contain, they must somewhere break through the dark shales and
alter them. The very faulting of the district would make the con-
tacts scarce, and mingle up adjacent rocks confusedly. Yet almost
all the puzzling rocks, that may be either altered slate or banded
compact lava, are found at the lines of junction, and each one ex-
amined with the microscope has turned out to bea slate. Such
rocks are well seen on the north-eastern slope of Ragleth. Their
bedding is here across the hill, and makes an angle of quite 45°
with the normal strike of the slate. This is only natural, if it be
pushed aside, as it must have been, by the igneous rock.

From Hazler Hill we can learn ‘nothing, as there is only dolenie
in it, which may be of later date; but Helmeth is full of interest.
All along the lower path on the western side we walk on slightly
altered slate; but along the crest we find the southern half is all
rhyolite, and the northern half yields successive exposures of rhyo-
lite, slate, and dolerite. The boundary of the slate must there-
fore zigzag amongst the igneous rocks, and in fact at one spot a
coarser rock than usual, almost like a eurite, is seen intruding into
a true slate. Most of the southern slopes of the hill are also
occupied by slaty rocks. The character of these slates does not,
indeed, remain absolutely constant, but there are bands of hard
greywacké, seen at Hazler, and inferred from fragments here.

ei kk

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 407

In Caer Caradoc the unaltered adjacent patch at the south-west
is very probably faulted. On the southern slopes is a band which
we should call either halleflinta or altered slate, according to the
series to which we supposed it to belong; and near. the summit is
another band which can hardly be anything but the latter; but the
most remarkable is in Little Caradoc. Here, crossing the hill be-
tween the rhyolite on one side and the dolerite on the other is a
very clear band of not much altered slaty greywacké, clearly bedded,
and impossible to imagine to be in its natural position. Under the
microscope it is seen to be marked with transverse cleavage-lines of
sericite, parallel to which the long axes of the quartz fragments have
been turned so as to lie across the bedding. From its position and
outcrop it is rather difficult to get it here by faulting, but easy to
explain as the solid underlying rock on either side of which the
igneous extrusions have been made. A very similar band, about
which the same may be said, occurs in the Lawley.

It is a remarkable circumstance that all the localities of these
altered slates are connected with the western margin of the range ;
and there is nothing like them in the whole of Cardington Hill.
The same may be said of the Wrekin area. Nothing that can be
thought to be altered slate is found in the Wrekin itself, and the
only rock of the kind is at Wrockwardine village, near the western
border of the exposure of old rocks.

The first conclusion, then, at which I arrive 1s, that the volcanic
rocks are younger than the slates, and have been extruded from
their midst.

The next point to be considered is the age and character of the
masses of coarse crystalline rock, of acid type, called granitoid by
Prof. Bonney and Dr. Callaway. The principal mass of this type
occurs in the Wrekin, where the former author says of it ‘ there
can be no doubt that it is far older than the rhyolite, and thus we
may regard it as, in general terms, a representative of the Dimetian
series.” The distribution in the district, however, of this class
of rock, presuming it to be all of one age, is very much against its
being older than the rhyolite. Besides the main mass in the Ercal
there are two small patches of it in the midst of the rhyolites near
the south-eastern end of the Wrekin, whose mode of occurrence
suggests intrusive bosses. At Primrose Hill it is likewise entirely
surrounded by the rhyolite, into which, indeed, it almost seems to
pass, and strongly suggests a neck, to which other phenomena point.
Holocrystalline rock also occurs at the extreme N. of the Lawley,
where. it passes gradually into the rhyolite. Similar rock is referred
to by Dr. Callaway near Wallsbank, Cardington Hill. It is here
at the edge of the rhyolite, and is cut off by a fault from the
Caradoc shales. Some connection may here perhaps be suggested
with the porphyry to be presently noted in this hill.

These isolated occurrences only swggest intrusion on the part of the
eurite (as we may call it), and not on the part of the rhyolite; but
in the Ercal Quarry there is a pretty long line of junction, and
this ought to tell us whether there is any intrusion or not, and by

262

408 PROF, J. F. BLAKE ON THE MONIAN AND

which rock. Unfortunately it leaves the matter doubtful after all.
The line runs in general along the face of the quarry, turning -
westwards towards the southern end; but slips, for the most part,
cover it. The rhyolite below has irregular flow-lines, and contains
clastic portions, so that it does not look like intruding on anything.
In one spot beneath a tree the solid eurite and compact rhyolite are
brought side by side with a vertical dividing line, but the line is so
decayed that nothing can be made of it. Hard by are soft bedded
shales, evidently of rhyolitic material, which rest on and enter
the wide cracks of the eurite, and contain numerous nodules of the
latter of all sizes and shapes, which have evidently decayed in situ.
If we could only persuade ourselves that these shales are rhyolite
tuff, the question would be settled; but they are not in the least
like the rocks anywhere else, and are scarcely consolidated. I take
them therefore to be merely stratified débris, probably first formed
within the fault, and therefore proving nothing. I did, however,
obtain a specimen on a former visit, under the guidance of Dr.
Callaway, which seemed to me an intrusive junction of the eurite,
but I cannot confirm the observation. From all available evidence,
it would, on the whole, appear that it is highly improbable that the
eurite is the older, and highly probable that it is, on the contrary,
intrusive in the rhyolite, but I cannot absolutely prove it.

I must next pass to the conglomerates and grits which are met
with in these hills, the age of which is of supreme importance in
connection with the general interpretation of the district. In several
spots they have been noticed by Dr. Callaway, but have been taken by
him to be part of the volcanic series, and to prove the clastic origin of
the latter. If we commence on the south, we must probably consider
the conglomerate and grit of Hopesay Common the first member of
this group, for the summit of Wartle Knowl, at its termination, is
composed of a mass of rhyolite, with which a dolerite is associated
after the manner of an intrusive rock. This association of two
kinds of igneous rock, which recalls what we see universally in
these volcanic hills, and the position of this elevation in relation
to them and to the boundary-fault, indicate that we have in Wartle
Knowl the summit of a hidden Caradoc, enveloped by undenuded
Cambrian grit. The next hill is Ragleth ; along the western slope
of this is seen a red grit of rather mixed character, but recalling
very closely the Cambrian purple grit. It does not run trans-
versely to the hill, as the dark shales do when pushed aside, but
forms a longitudinal patch, which, from its easily determined limi-
tations, must be superficial and deposited where we find it. On
Cardington Hill there are two patches; one is noticed by Dr. Calla-
way on the slopes of the Gaer Stones, and the other is a large one
at a lower elevation, situated to the east, where the hillis crossed by
the footpath. The exposures of this and of the surrounding rocks are
numerous, and the exact limit of the red grit can be easily traced,
It is seen to be superficial. Besides these two masses of grit, there
is on the same range, near the summit called Willstone Hill (see
fig. 5), a very small and local patch of. conglomerate occupying

aS

s ope Bowdler

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 409

part of the western slope. It has a dirty-looking muddy matrix,
and contains various fragments, quartzose, micaceous, and rhyolitic.
On Caer Caradoc there are two patches of red grit. One is at

Fig. 5.—Section across the Volcanic Hills near Church Stretton.
(Seale 13 inches to a mile.)

2 Sel,
elie Zettle Caradoc
erry Red Grit Dourtze
: ae Quirlzite => Sled:
Shirebere Shalc 77s ~~ Nie a Fs | \ >
Wf, Nw aS L

4
ral

the southern end, where it is noticed by Dr. Callaway and described
microscopically by Prof. Bonney, who says it contains fragments
which closely resemble the Wrekin rhyolite, and that its material
has probably been derived from this and the granitoid rock, which
is exactly the character of the Cambrian conglomerates. The other
is on the north side, where only fragments are found, but their
position is such as to suggest, though not to prove, that the rock
is overlain by the Cambrian quartzite. On the summit of the
Lawley there is also an entirely isolated patch of grit, which may
belong to the same group, but it is not very like the other exposures.

If we pass on to the neighbourhood of Wellington, there are again
conglomerates and also grits, but it does not appear that their age
is necessarily the same as those already mentioned. There is first
the conglomerate of Charlton Hill, which Dr. Callaway regards as
of Uriconian age, on account of the stratigraphy of the spot. By
the aid of the 6-inch map, and the numerous exposures, I have been
able to lay down pretty accurately the actual position occupied by
the conglomerate and associated beds on the surface, and to show
that it is entirely isolated and surrounded on all sides by igneous
rocks. There is also a second patch at the northern-road junction,
whose relation to the other rocks is not made out. On Charlton Hill
itself the conglomerate is quite local (see fig. 7, p. 410). Towards
the north-eastern end, where the band crosses the roadway, there

Fig. 6.—Section seen in Charlton Lane, showing the Relations of
the Grits. (Scale about } inch to 90 feet.)

are some slaty grits, with high dip striking N.W. and pointing
directly on one side to diabase, on the other to rhyolite. In the
road-section, which Dr. Callaway regards as conclusive (see fig. 6),
we find in the northern bank two masses of grit, each with a dip

410 PROF, J. F. BLAKE ON THE MONIAN AND

6 Street

Nn.

Han

ef

WELLINGTON.
i

JWatl

Mm,

ACID VOLCANIC.
RUSHTON ROCKS’

BASIC JGNEQUS

CONGLOMERATE

1 the Wrek

KG

U

line

1

INTERMEDIATE
GNEISSOSE ROCKS #7 FAULTS EXPOSURES o

| Reservoir

J

ngton,

a

COMLEY SANDSTONE QUARTZITE
SNVapWrekin Farm

N

Il to Well

7

wr

Wreh

from Charlton H
oe

strict |

of the di

al Map

% -
TMNT HY
iy WILLE 7

f

Me
Witty

a
Up,

4,
Z
Vie

Ogu

SSy
SS aS
SSE fii)\\| 4

Sy

INOWOoU

™S
e
Ec

— Geol

}

= 74 >
Oa f=
md i
=> Cm
= sz
= —
= } ~
4: Ge
\= aa-~
\S
} \
if :
— }
/ a
a . f

“~~

of Mites

Scale

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 411

in certain parts towards the west, but becoming almost horizontal
through disturbance. The compact halleflintas show no bedding,
but lie on all sides of the masses of grit, some of whose beds, if con-
tinued, would run into them. No grit is visible on the other side of
the road. These masses seem to be portions of later deposits caught
up and folded in with the older rocks, both here and on the summit
of the hill. They do not, therefore, form part of the voleanic series.
Nevertheless, since these foldings took place before the deposition of
the quartzite, these grits must be older than the latter. On the next
bare boss to the west there is another mass of grit intervening
between rhyolite breccias and quartzite on the surface, but the
relations of this are not very clear.

On the southern end of the Wrekin, east of Primrose Hill, there
is a considerable mass of conglomerate rock forming an elevation
and bearing considerable resemblance to that on Charlton Hill. It
also appears to lie between the quartzite and the rhyolite (see
fig. 8). It has, however, so mongrel a matrix that we seem to be

Fig. 8.—Section from Charlton Hill to the South end of the Wrekin.
(Scale about 14 inches to a mile.)

Wrekin
ake

Lrimyrase Hell
Cony lomer

Rarrblende Scie Ofes aah
eur <t¥

Doterile
g
Ss

oss) A 2 eed

Charltory Ab ie A Hace
Conglomerdte
PB gn ell

ne ee
err rats

n=)
Dolinte Rhyorctes fF Rushton. Schtals t Rhyoites

approaching the agglomerates of Lawrence Hill. With these latter,
however, we should have to compare, not the red grits of Cardington,
but the great breccias there exposed at Woodgate quarry and fully
described by Dr. Callaway, who ascribes them and, I think, justly,
to the true volcanic series ; but which, it must be noted, occur only
on the edge of the mass, and may therefore be the youngest, in spite
of their actual dip.

I think we may reconcile all these observations by looking on
the Lawrence Hill and Woodgate deposits as the earliest results
of denudation of the volcanic products, and almost belonging to
their epoch. Then come the Charlton-Hill and South-Wrekin
conglomerates, and possibly that on Willstone Hill, which is very
like them; and lastly, at a later stage, the conglomerate of Wartle
Knowl, followed by the red grit of all the localities that have been
mentioned. We must conclude also that all this took place before
the deposition of quartzite. The explanation involves, however,
three conclusions, which rest, of course, on independent evidence,
which will be strengthened, if this be accepted as reasonable. These
are:—1l. That the Cambrian grit lies unconformably, not only on
the slates and grits of the Longmynd, but on the volcanic rocks on the
east of the fault. 2. That these volcanic rocks are younger than the
Longmynd rocks. 3. That all of these are anterior to the quartzite.

I pass next to the porphyry of Hope Bowdler and Cardington

412 PROF. J. F. BLAKE ON THE MONIAN AND

(see fig. 5). This occurs in isolated and irregular masses of consider-
able size, and might at first be thought to form only an integral portion

of the volcanic series of the hill. It is red in colour and has~

abundant felspathic insets. There are three reasons for consi-
dering it intrusive. First, the character of the rock is different
from any rock met with in the other volcanic hills, and is therefore
not an ordinary constituent of the series; but it resembles more a
superficial form of the eurite, which has already been regarded as
intrusive, and, moreover, porphyries are more naturally intrusive
than more glassy rocks. Secondly, because in the Gaer Stones plan-
tation we find the ordinary grey and pink rhyolite becoming very
much discoloured on approaching it, turning to a bright red hue
owing to the oxidation of the iron. And thirdly, because one of the
masses of red grit already described, as seen in a crag on one side of a
valley, actually has a large vein of this porphyry intruded into its
midst (see fig. 9). If, therefore, the porphyry was of the same age
as the whole of the acid rocks of the hill, this grit would be earlier
in date than the hill on which it rests, which would be very difficult
to conceive of.

Lastly we come to the basic rocks, which seem to be everywhere
present, mixed in the most intimate manner with the acid types.

Fig. 9.—Porphyry intruswe in Red Grit at Cardington.

There is seldom anything to indicate whether these are of later date
or contemporaneous with the acid rocks. They are usually less in
quantity than the latter ; but in the Lawley the proportion is reversed.
The great majority show no crystals, but are decayed into a dark
irregular mass. There are other associated rocks, as at the north
of the Lawley and in Hazler Hill, which appear to be the unstra-
tified ashy representatives of this kind of rock, such as I have called
pelite in Anglesey, and which would indicate that these basic rocks
are not in the form of intrusions, but are eruptive. If all the basic
rocks of the district are of the same age, they must be later than the
agglomerates of Lawrence Hill, and therefore one of the last to be
formed. Negative evidence to the same effect is afforded by the fact
that the conglomerates and grits, wherever known, always lie upon
the rhyolites and never on the basic rocks (unless Wartle Knowl be
an exception). Even at the spot where the porphyry intrudes in
the grit on Cardington Hill there is a crystalline dolerite which is

a a

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 413

close at hand, but is not overlain by the grit. They may have once
been overlain by grit, but have afforded it a less secure foundation,
so that it has been more readily denuded. The absence of pebbles
of this rock in the Cambrian conglomerates is not conclusive, since
there is nothing in the majority of exposures that could produce a
pebble; and the crystalline portions may be of a different and later
date. We can thus get no nearer to the date of the basic rocks than
that they are anterior to the quartzite which lies upon them, and
that some of them, at least, are posterior to all the acid rocks.
Their position at the present moment in relation to the rhyolites is
very complicated: but this is due quite as much to later foldings
and squeezings, possibly subsequent to the formation of the quartzite,
as to the location of their. original eruptive centres.

§IV. Posstste more Ancrent Rocks tn tHE District.

The rocks already dealt with form the principal portion of the
Pre-Cambrian rocks of the district ; but there are two other groups
to which Dr, Callaway has already assigned a similar antiquity, viz.
the Rushton schists and the gneiss of Primrose Hill (see fig. 8).
With regard to the former there is little or no stratigraphical evidence
available, and I have nothing to add to Dr. Callaway’s petrographical
descriptions * ; I must only remark that the mica-schists and asso-
ciated rocks are more altered by pressure than any other rocks of
the neighbourhood, and call to mind many of the schists of the
eastern district in Anglesey. Such strike as they show is more or
less concordant with the strike of the Longmynd rocks ; but they
lie on the eastern side of the fault. It is very possible, considering
the great exposure of the quartzite and the higher elevation of the
Wrekin on the one side, and the coming in of the Trias on the
other, that the throw of the main fault may be increased before
reaching Rushton, and therefore that there may be a greater interval
between the lowest accessible rocks. The Rushton schists may
therefore be far lower in the series than the dark shales of the Long-
mynd border, and may actually represent some of the rocks of
Anglesey, and this, at all events, is their most probable position ; and
if this correlation is correct, it would indicate a continuous deve-
lopment of the Monian series in the district.

The second mass, the gneiss of Primrose Hill, is intimately as-
sociated with the eurite and is considered by Dr. Callaway as forming
part of the same group. This is not very likely to be the case if
the latter is an eruptive rock, as I believe it to be ; but independently
of this the mode of occurrence of the gneiss is very peculiar.
Towards the bottom of the western slope of the hill there is a small
mass of it not many yards square, and there is another narrow
patch of it, about 2 feet broad and a few yards in length, quite
close to the summit, and this is all that can be called true gneiss,
though some portion of the eurite is slightly gneissose. There is

* Geol. Mag. 1884.

414 PROF, J. F. BLAKE ON THE MONIAN AND

also a narrow band of hornblende-schist ef about the same size
as the gneiss on the summit, and near and parallel to it, in con-
nection with which may be mentioned a non-foliated diorite on ~
the slope. These patches are so small and so isolated that it is im-
possible to regard them-as exposures of bands in a gneissose series,
especially as they are surrounded by non-foliated eurite; but if the
latter be of the nature of a neck, these fragments may very well re-
present the underlying rocks, pieces of which have been torn off and
carried up with the eruptive rock. ‘he gneiss is foliated on a large
scale, after the manner of the most mylonized gneisses of Anglesey,
and the hornblende-schist is practically identical with the foliated
diorite of that island. The occurrence of pebbles of gneiss and schist
in the Longmynd conglomerates proves that there were large masses of
such rocks exposed at the time of their formation ; and the other in-
teresting varieties recorded by Dr. Callaway * prove that other rocks
which might belong to the same series accompanied them. The horn-
blende-schists, however, which would perhaps decay before forming —
pebbles, have not as yet been recognized.

These observations therefore tend to show that, as in crossing
the Longmynds from west to east we come on ever lower rocks, so
if the country still further east could be laid bare, we should find
still lower rocks of the same system following in their proper order,
the western and all other of the volcanic hills being later outbursts
from the uptilted ground and having their own independent bedded
pyroclasts.

$V. Rerarions oF tHE OverLyING ForMATIONS.
1. The Quartzite.

Leaving on one side the Cambrian conglomerates and grits as
already dealt with, the oldest of overlying formation is undoubtedly
the quartzite. With regard to this rock, the first point to be noticed
is that it never occurs on the west side of the fault. It is, moreover,
limited on the south by Cardington Hill, so thatit occurs, as it were,
only in a bay on the north-east side of the district It does not even
mount on to the extreme west of the volcanic hills. It climbs up the
sides of Caradoc and occupies the summit of the crest between this and
little Caradoc. It laps round the eastern side of the Lawley. It over-
passes the Wrekin, it is true, but this hill is not in a geological line
with Caradoc, but with Cardington Hill; and, though it reaches Charl-
ton and is found as a capping on the slopes of this elevation, it neither
reaches the western boundary nor appears at allin the Wrockwardine
mass, which has the main fault on its western side. The extreme
edge, therefore, of these volcanic hills appears, as far as we can tell,
to have formed also its boundary, and they must therefore have been
erected into a barrier at the time of its deposition. The occurrence
of the Cambrian grit to the east of this boundary, and in fact to the
east of the quartzite itself, on Cardington Hill, shows that the barrier

* Q. J. G.S8. vol. xiii.

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. A415

did not exist when the grit was being formed. This grit must, there-
fore, antedate the quartzite, and the elevation of the hills into a
barrier must have occurred during the interval between them. And
this is consonant with what we find elsewhere. Much of this grit
lies below the conglomerate of the Longmynd, which was derived
from the volcanic hills when first they came under the action of the
denuding forces. As they rose they supplied the materials for the
deposits on the west and formed the boundary of a quiet sea on
the north, where organic life began to flourish. The fauna of the
quartzite and the Comley sandstone, which everywhere succeeds
it, and which is, therefore, probably only its continuation, is believed
to be the oldest in the British Isles, except the fauna of the Monian
rocks; but this does not. necessitate its development at the earliest
portion of the Cambrian period, when we remember how vast an
amount of unfossiliferous Cambrian there is in North Wales, and
how far above the base the Puradowides-zone is at St. Davids.

2. The Succeeding Formations.

This barrier, once established, continued to be an important
feature in the district through many subsequent ages. Now it is the
character of Cambrian rocks, whenever we find them, to form the
base of a continuous series which succeeds in regular order in the
same district. On the other hand it is the character of Pre-
Cambrian rocks to form the nuclei down to which the denudations
of later ages have cleared away the rocks, so that they constantly
form limits to later formations. This they do in Anglesey, at
Charnwood, and here. For example, the next group above the
primordial beds is the Caradoc. Towards the north this is separated
from the volcanic hills by an expansion of the former ; but it reaches
them at the Lawley and Caer Caradoc, where it is faulted again,
then on the other side of Cardington Hill the conglomeratic and
gritty base of the Caradoc Series may be traced running nearly east
and west in bay-like curves as far as Hope Bowdler, and showing
large rhyolite pebbles where it crosses the Church-Stretton road.
Another conglomerate, probably referable to this series is seen at the
south end of Ragleth ; coarse Caradoc bounds also all the southern
injier towards the east, but it never crosses the main fault. This
fault, then, must lie also near the boundary of the Caradocian sea,
since the beds of the same age in the Shelve district have not the
same character. ‘The existence of this boundary is probably con-
nected with the Post-Cambrian squeeze which gave the dip to the
purple grits and slates and placed them in a position for denudation.

The next formation which comes up to the nucleus is the Silurian
with its basal Llandovery beds. ‘The much wider range of these
indicates that a depression had set in, Nevertheless the nucleus
appears to have formed their northern boundary. They commence at
Little Stretton and may be traced continuously, clinging to the
Longmynd rocks, all the way to Plowden. They are mostly lost
sight of in the succeeding valley, but are clearly seen all the way

416 PROF. J. F. BLAKE ON THE MONIAN AND

from Wentnor to Lydham, dipping at a gentle angle from the Cam-
brian rocks on which they rest. 7

Many changes doubtless took place in this district during Devonian —
times, but these changes did not result in its submergence, since
the Old Red Sandstone is only found in the south. More probably
they resulted in its greater elevation; and the main fault, which
did not exist during Silurian times, may now have been produced.
The area of deposition was then transferred to the north ; and from this
direction came the later Coal-measures to abut naturally against the
old rocks with an outline produced by denudation. In the same
direction followed the Permian, then the Trias, which envelops the
still remaining peaks of the ancient rocks, by Haughmond and the
Wrekin; and even the Lias at Whitchurch is tending towards the
same point: and none of these rocks have any representatives south
of the Longmynd. -Finally, even in the Glacial epoch, there appears
to have been nosubmergence. The lower valleys on all sides are
filled with Drift, but there is none of it on the surface of the hills ;
only on the northern side, whence the boulders travelled, do we find
it, as it were, forced up-hill in the direction of its course. Here the
boundary rises from a level of about 700 feet near Lebotwood to as
much as 1050 feet on Picklescott' Hill, descending to about 500 feet
again to the east of Church Pulverbatch. In this direction a few
boulders have even reached the summit of the hills, as at Church Pul-
verbatch itself and on Cothercott Hill. The boulders, as far as I have
seen, are all of northern origin. None of them are of the Longmynd
rocks, and the ice which thus pushed forward up a hill has left its
strie on the rocks of Charlton Hill, at a height 340 feet above the
sea.

We thus perceive that the ancient rocks of the Longmynd have
been exposed to denudation ever since the middle of Lower-Cambrian
times, and the valleys we now see cutting across the vertical strata
of the hardest and most insoluble grit, and carrying water remarkable
for its clearness and purity, are the end result of its work.

$ VI. Grnerat Concrusions.

We are now in a position to determine how far my suggestion
that the Longmynd rocks are not Cambrian, but Upper Monian, was
correct. It is obvious that here, where the succession of the later
rocks is so well made out, we are in the most critical locality for
settling the existence or not of a system of ordinary stratified rocks
subjacent to the Cambrian.

In the first place, in the face of the fact that the rocks hitherto
comprised under the term Longmynd are not homogeneous, but
consist of two distinct and unconformable portions, every state-
ment made up to this time regarding them must be modified. Thus
it is no longer permissible either to say the Longmynd rocks are
Upper Monian or to give one name, such as that of Longmyndian,
to the whole. Again the proofs that have hitherto been given that

- BASAL CAMBRIAN ROCKS OF SHROPSHIRE, 417

the Longmynd rocks are derived from, and therefore later than, the
Uriconian, will now only hold good for the upper of its two series.

We shall find it best, in considering what must be the result of
the present observations, to commence at the top of the succession.
The lowest beds that are continuous throughout the area, 2. e. those
found on both sides of the Longmynd hills, are the Shineton shales,
and these have been determined to belong to the Upper Cambrian.
Below these on the east there is the Comley sandstone and quartzite,
enclosing a fauna which does not elsewhere characterize the beds
immediately below the Upper Cambrian, but which forms the lowest
fossil group of that system. Whether the Cambrian series is here
complete and the intervening fauna lies yet hidden in the rocks,
whether there is a yet unrecognized break between them, or whether
such intervening fauna ever existed, it is not for me to decide. It
is certain, however, from what is known elsewhere, that we cannot
expect to discover here any truly Cambrian fauna below that of the
Comley sandstone. On this side, therefore, of the Longmynd Hills
we are at ‘the base of the ordinary Cambrian development. On
the other side we find an enormous thickness of grits and slates
bearing no resemblance to the quartzite * and totally devoid of
fossils. These grits and slates, though doubtless deposited with
much greater rapidity than the rocks on the eastern side, must yet
have required an enormous length of time for their formation, and
starting at the top in Upper Cambrian, the base must belong to a
very early, if not the earliest possible, portion of that series. The
series must therefore, to some extent, be synchronous with, and to
some extent earlier than, the quartzite, and have been formed in a
different basin.

It is to be regretted that the relations of the two groups of rocks
to one another are not as yet indubitably settled. Nevertheless such
indications as there are, and which have been enumerated above,
point with some force to the conclusion that the lower part, at
least, is anterior to the quartzite, and is therefore the oldest repre-
sentative of the stratified Cambrian rocks in the whole district. For
these rocks, inasmuch as they still form the bulk of the Longmynd
Hills, whose highest summits they actually occupy, the name of the
Longmynd series can still be retained, and this series will therefore,
in this district, be the base of the Cambrian.

On the eastern side of these hills, however, we must now recog-
nize a comparatively narrow band, which belongs to an older series.

It is this band, and not the conglomerates, grits, and western
band of slates, which has been studied by Salter and in which he
discovered organisms totally unlike, so far as they go, the fauna of
the Cambrian. It is this that shows a resemblance to the rocks of
Bray Head, containing somewhat similar organisms, and it is this
that has been compared with the schists of S. Lo, which are admitted
to be unconformably overlain by the ‘ conglomerat pourpré ”

* The only exception to this is a reef of quartz running fairly parallel

to the bedding at “ Roch,” near Medlicott, in the midst of the purple slates;
but this appears to be rather of the nature of a vein.

418 PROF. J. F. BLAKE ON THE MONIAN AND

of Brittany, referred by French geologists to the Cambrian. This

band must therefore belong, by all the tests at our disposal, to a_

system which is at once of considerable thickness and wide distri-
bution, and I venture to suggest that this can be none other than
that system whose lower parts we see in Anglesey, in other words
the Monian ; and the portion of that system thatis here represented
must certainly be an upper part. So far, then, my original sug-
gestion has been justified.

But, in view of what is seen in this locality, my former suggestion
that the Uriconian rocks were Middle Monian cannot be adhered to.
If there be any Middle Monian in this district it must be the
Rushton schists; and if any Lower Monian, the fragments of gneiss
and hornblende-schist caught up in the outburst on Primrose Hill.
In fact, the proof that these volcanic hills are of later date than
the Longmynd slates has entirely nullified all my previous con-
clusions as to the age and position of this and other volcanic Pre-
Cambrian groups, which have been too rashly assumed to belong
necessarily to the underlying subdivision called the Middle Monian.

What, then, are we to do with these Uriconian rocks? We have
three alternatives to choose from. Hither we must class them with
the Monian, or we must assign them to an intermediate system, or
we must class them with the Cambrian.

The uptilting of a group of rocks and the formation of fractures in
its base, out of which a volcanic eruption may take place, indicates
a great change of physical conditions, and probably a lapse of time
equivalent to an unconformity. Can rocks formed after all this
still belong to the same system? Moreover, the various conglomer-
ates which cap them, some forming actually part of their mass,
others worked up with them, show a gradual change of character
into those which lie upon the surface, and which resemble the Cam-
brian grits. These considerations seem to associate these rocks, in
spite of the unconformable quartzites, more with the rocks above
than with those below.

Again, to class them as a separate system under the title of Unri-
conian is little more than a confession of ignorance. Such a system
has been nowhere worked out, and we might have to create a new
system on the same principle for every locality. Probably, however,
this is what we shall have to do temporarily till more is known of
the relations of these old rocks.

But if neither of these alternatives be acceptable, can they be
classed with the Cambrian? I shall not, with our present infor-
mation, attempt to answer this question definitely, but only throw
out a few suggestions. In the first place, the behaviour of the over-
lying quartzite does not prove that they cannot properly be called
Cambrian. On the one hand, it is very probable that the grits
which lie upon them are also overlain by the quartzite, and yet that
this grit is Cambrian. On the other hand, these conglomerates and
grits, though derived in part from them, need not be of much later
date, considering the rapidity with which volcanic rocks consolidate
and are broken up, and considering the connection, as noted above,

BASAL CAMBRIAN ROCKS OF SHROPSHIRE. 419

of some of them with the actual volcanic débris. Again, if we go
further afield, in North Wales, as I have shown *, the rocks which
overlie the Monian unconformably, and are so well developed between
Bangor and Carnarvon, are very volcanic in character, yet they form
the base of the Cambrian and have several well-marked conglomerates
in their midst, up to the one that overlies the felsites of Llyn Padarn.
It may be that the Uriconian rocks are of the same age as these,—
they have both been thought to be the same as the Pebidian. And
this takes us to St. Davids. There is certainly there an entire
unconformity and independence between the Cambrian conglomerates
and the underlying series, and therefore I so unhesitatingly classed
the voleanic group of St. Davids with the Middle Monian, that I
gaye as an alternative name for that subdivision *“‘the St. Davids
group.” But there is no special similarity between the rocks there
and the Middle Monian of Anglesey; there is quite as much resem-
blance, if not more, to the rocks between Bangor and Carnarvon.
It is possible, therefore, that Dr. Geikie may be right after all, and
that sufficient allowance has not been made, in estimating the signi-
ficance of the unconformity, for the volcanic nature of the underlying
rocks. Again, in the Midlands, the Nuneaton quartzite les upon
the volcanic rocks of Caldecott: and at Charnwood the Swithland
slates have great conglomerates associated with them and pass down,
without any discovered break, into the volcanic ashes and lavas of
the western portion of the Forest. If, on further knowledge, it
should turn out that all these must be referred to the Cambrian, it
would be certainly a remarkable circumstance, amounting to a
generalization, that wheresoever we reach the base of that formation
we find it formed of volcanic débris, which is not, perhaps, an
unnatural commencement of a system formed under new physical
conditions.

And if this should turn out to be the case, which as yet is far
from proved, then would the Monian system be entirely cleared
from the Pebidian and its associated Arvonian and Dimetian, and
stand firmly as a distinct system founded entirely on independent
observations.

EXPLANATION OF THE MAP, PLATE XVI.
The Monian and Cambrian Rocks of Shropshire.

This Map is traced from the l-inch Ordnance Survey Map; the geological
lines being reduced from the 6-inch Survey Map. Consequently, if this
Map be retraced on the Ordnance Map, the exact positions of all lines will
be found.

Discussion.

Dr. Hicks said it was greatly to be regretted that Dr. Callaway,
who had done so much in unravelling the geology of the district
referred to was unable to be present to reply to the Author's
remarks. In his absence, he (Dr. Hicks) desired to say that, in the

* Q. J. G.S. vol. xliii.

420 MONIAN AND BASAL CAMBRIAN ROCKS OF SHROPSHIRE.

main, his own views were much more in accord with those of
Dr. Callaway than with those of the Author. He failed to see any
reason why the Author should call any of the Longmynd rocks —
(which already had local names given to them) by the name
‘* Monian,” especially since they were entirely unlike the rocks in
Anglesey, which the Author had recently called by that name.
Dr. Hicks had examined most of the sections, referred to by the
Author, last autumn. He believed the Longmynd rocks to be
mainly Cambrian, and the two series to represent the Caerfai
and Solva groups of St. Davids, which contained similar fossils to
those of the Longmynd rocks. Between the Caerfai and Solva
groups there were well-marked grits and conglomerates. The
materials composing the Lower Longmynd series had undoubtedly
been derived by denudation from volcanic rocks, such as those now
forming the Pre-Cambrian rocks of Caer Caradoc, hence the Long-
mynd rocks were clearly newer than the Uriconian (Pebidian) rocks
of the area. The sections, on careful examination, showed that the
Lower Longmynd rocks had formed an arch over the Caer Caradoc
rocks, that the limb on the west side had been greatly broken by
reversed faults, and that the limb on the east had been broken by
great thrusts which had caused newer beds to be pushed over and
hide the older. The Author, Dr. Hicks believed, had here, as he
had done at St. Davids and in Caernarvonshire, entirely failed to
realize the true interpretation by overlooking the effects due to
thrusts and faults. In those areas he had also attributed contact-
changes to Pre-Cambrian rocks, when entirely due to dykes which
penetrated the Pre-Cambrian and overlying series. There was no
evidence to show that the Bray Head rocks were of the same age as
the Pre-Cambrian rocks of Anglesey.

Mr. Waurraxer asked whether the Author’s results were in
accordance with those of Prof. Lapworth.

Mr. Marr objected to the use of the term Monian for a system
whose upper and lower limits were not defined. He pointed out
the discrepancy between the supposed basal Cambrians on either side
of the ridge.

The Avruor replied that the Bray Head rocks followed naturally
upon the Howth Head rocks which were continued into Anglesey.
The statement that the purple slates were derived from older acid
rocks might be equally true of any other slates, and did not prove
that they were derived from any definite volcanic series. He had
seen no evidence for any of the thrusts imagined by Dr. Hicks
nor had he seen any of the dykes. He admitted that the summit
and base of the system were not defined, but the system itself was
there. The beds below the Shineton Shales on the west side were
continuous to the base of the Cambrian.

MISS COIGNOU ON A NEW SPECIES OF CYPHASPIS. 421

22. Ona new Species of Creuaseis from the CarBontrenovs Rocks of
Yorksurre. By Miss Cotenou, Scholar of Newnham College,
Cambridge. (Read March 26, 1890.)

(Communicated by Prof. T. M‘Kenny Huauus, F.R.S., F.G.S.)

Dorrine the visit of Prof. Hughes’s geological party to the Craven
district in June last, I was fortunate enough to find in the Pendle-
side limestone* at the base of Butterhaw, near Cracoe, a fairly
perfect head of a Trilobite which appears to belong to the genus
Cyphaspis. Hitherto this genus has not been recorded above the
Devonian, and its discovery in rocks of Carboniferous age seems
worthy of notice.

Description.—Head small, semicircular, very convex, 3°5 millim.
in length and 5 millim. in width. Frontal border broad, flattened,
minutely granulate. Its margin produced into a number of equi-
distant, horizontal, cylindrical spines, ‘5 millim. long. In our
specimen they are visible on the right antero-lateral portion of the
border, and one near the left genal angle. ‘They are -4 millim.
apart from each other, and as the frontal border is 9°6 millim. in
length, there must have been 24 spines present. Genal angles
inyisible, probably prolonged into short spines. Glabella very
prominent, ovoid, narrow behind, and widening gradually for four
fifths of its length. Slghtly constricted at the two glabella-furrows
on each side, much raised above the cheeks; covered with small
granules and bearing four tubercles, a pair near the upper part of
the anterior sloping surface, a large unpaired one near the centre,
and a smaller median one behind. Of the glabella-furrows the
anterior one is short and, seen from the side, is directed backwards,
while looked at from above it appears as a pit in the axal furrow,
marking off an imperfectly defined narrow oblong lobe. Posterior
furrow deep, extending backwards to the neck-furrow and bounding
the postero-lateral lobes, which are elevated and pyriform. Neck-
furrow broad and shallow. Neck-lobe short, convex, badly
preserved. Cheeks subtriangular, elevated, sloping abruptly along
the inner and posterior sides, finely granulated, continuous in front
of the glabella. Facial suture invisible. Eyes sessile, reniform, at
the summit of the cheek, opposite the centre of the glabella.

Thorax and tail unknown.

Affinities—The specimen is provisionally referred to Cyphaspis,
but it differs from the typical species of that genus in possessing two
pairs of glabella-lobes. Barrande mentions the occurrence of two
transverse furrows on each side of the glabella in C. novella and C,
depressa t, From both of these our species is clearly distinguished

* « Explications des Excursions,” Congrés géologique International (1888),
p. 80.
+ Syst. Sil. de la Bohéme, vol. i. p. 479.

iv. G.S, No. 183. 20

422 MISS COIGNOU ON A NEW SPECIES OF CYPHASPIS,

by the frontal border being produced into spines. It closely
resembles C. Davidsoni, Barrande, and agrees with it in haying :—-.

(1) The frontal border produced into spines.
(2) Two or four tubercles on the glabella.
(3) The granulated ornamentation of the head.

In our specimen, however, the frontal spines are longer and
further apart, and the granules are finer than in C. Davidsoni.
Further, the anterior glabella-furrows appear to be absent in the
Bohemian species.

As it appears to be distinct from any species of Cyphaspzs hitherto
described, we propose to name it Cyphaspis acanthina on account of
its thorny appearance.

Barraude records nine species of Cyphaspis from Bohemia, three
only of which have the body-segments preserved, the other six
species being represented by heads only.

All those with body-segments preserved have smooth borders to
their cephalic shields, and all have the 6th axial ring prolonged into
a strong median spine (see woodcut, fig. 1, s). -It is possible that
the species with spinose borders to the head-shield may belong to
another genus or subgenus. ‘The pair of lobes (7) at the base of the
glabella are, perhaps, the best diagnostic character to rely upon in
dealing with detached head-shields.

Outlines showing the Structure of some Cephalaspides.

S rs
° 2 9

(aad rie
SS
me :
LE

G

Woodeuts are here given of a typical example of the genus Cyphaspis, and of
those species which are most nearly allied to the specimen under con-
sideration,

EXPLANATION OF FIGURES.
Fig.1. Cyphaspis megalops, M‘Coy. Wenlock Limestone; Dudley, Stafford-

shire.
ee Davidsoni, Barr. Etage F. Mnienian, Bohemia.
0. —— Cerberus, Barr. Etage F. Mnienian, Bohemia.
4, —— coronata, Barr. Etage G. Moulin de Vavrovitz, Bohemia,

5, —~ uwcanthina, sp. nov. Carboniferous series; Yorxshire.

2 ; oor

a ee ee he he Pa e
: \

, 1
Se 7 7 r

Quart.Journ.Geol. Soc. Vol. XLVI. Pl. XVI. |

nk Rutley del. F.H Michael lith Mintern Bros . imp,
COMPOSITE SPHERULITES IN OBSIDIAN
Hot Soruigs near Luile Lake, (alitorna.

, a

ON COMPOSITE SPHERULITES IN OBSIDIAN FROM CALIFORNIA, 493

23. On Compostre Spuervrtres in Osstpian, from Hor-Sprines,
near Lirrte Lake, Cartrornia. By Franx Rortey, Esq.,
F.G.8., Lecturer on Mineralogy in the Royal School of Mines.
(Read March 26, 1890.)

[Prare XVII.]

Iy a paper read before the Royal Society in 1885 *, allusion was
made to certain greyish or yellowish-white spherulites occurring 10
a specimen of black obsidian which was given me by the late
Mr. John Arthur Phillips, F.R.S.

These spherulites (portions of two occur in the specimen) are
about an inch in diameter and are seen to consist of numerous
spherulites of very much smaller dimensions. In the paper referred
to it was suggested “that the smailer spherulitic structure was set
up in the large spherule after its formation, the vestiges of a

radiating erystalline structure tending to confirm this view.” This

opinion was based merely upon what could be scen on a fractured
surface by the help of a pocket- -lens. The microscopic examination
of a section made through one of these bodies seems, however, to
show that the smaller spherulites were formed first, and that after
they had assembled together in spheroidal aggregates, a radiating
crystallization was set up within the mass, travelling stage by stage
from the centre to the periphery.

As I have not yet met with any account of precisely similar
spherulites, even in Mr. [ddings’s monograph f, it seems to me that
the following notes may prove of some interest to petrographers.

In reflected light, but better when dark-ground illumination is
employed, the entire section of the spherulite is seen to be composed
of much smaller spherical or spheroidal bodies, so closely packed
that they are usually in contact, the matter occupying the interstices
appearing darker than the spherical or spheroidal bodies themselves,
which latter, by dark-ground illumination, appear brightly lighted,
fig. 4, P]. XVII. In ordinary transmitted light these bodies are
scarcely to be recognized, except ina few parts of the section, where
they are somewhat darker than the remaining portions, although
they are more or less translucent (fig. 1, Pl. XVII.). These are the
small pellets which, by the help of a lens or even by unassisted
vision, may be seen to compose the large spherulites in the hand-
specimen, In the following description these smaller bodies wili be
termed primitive spherulites.

The general aspect of the section, when viewed in ordinary trans-

* “On the Microscopic Characters of some Specimens of Devitrified Glass,
with Notes on certain Analogous Structures in Rocks,’ by Douglas 2 wane
and Frank Rutley. Communicated by Prof. T. G. Bonney, D.Se., F.R.S.
Proce. Roy. Soe. vol. xvxix. p. 106.

+, “Obsidian Cliff, Yellowstone National Park,” Seventh Annual Report,
U.S. Geol. Sury. Washington, 1838.

24H 2

4O4 MR, F. RUTLEY ON COMPOSITE SPHERULI‘IFS

mitted light, is that of a portion of a large spherulite composed of
anastomosing flexuous rods or fibres diverging from an approximately |
common centre. The rods or fibres are traversed transversely to
their length by delicate cracks, which are very numerous but
interrupted (fig. 2, Pl. XVII.). Between the rods or fibres there is
more or less isotropic matter with minute globulites. The latter
appear to be ranged in irregular linear aggregates following the
direction of the crystalline rods. Trichites and granules and
minute crystals of magnetite are somewhat plentiful in this fibrous
mass,

When viewed between crossed nicols the fibres or rods composing
the spherulite polarize, but not vividly, and the extinction, so far as
it can be made out in the matted mass of fibres, appears frequently
to be parallel and at right angles to their length, at other times it
seems to make an angle approximating to 21° with the long axis of
the rod, which would correspond to the extinction seen on (010) in
orthoclase. It would therefore appear that the divergent rods which
constitute the main bulk of the spherulite are orthoclase, as in the
cases described by Iddings in his work on *“ Obsidian Cliff.” There
is, however, little dependence to be placed upon the measurement
of the extinction-angles, since the confused and branching character
of the rods (fig. 5, Pl. XVII.) is, I believe, due to the fact that the
entire mass is made up of a succession of divergent bundles of
rods, similar to those met with im artificially devitrified glass,
Where this structure is strongly marked the section shows a well-
defined concentric banding (fig. 3, Pl. XVII.), each band occurring
at the terminal boundary of one zone of bundles of divergent rods,
which boundary forms the floor from which the divergent crystalline
fasciculi of the next zone grew.

The most interesting point i is that these concentric bandings pass
completely through ihe primitive spherulites already alluded to, as
shown in fig, 4, Pl. XVII., which represents the same parti of the
section given in fig. 3, the different appearances being due to the
methods of illumination respectively employed. It may therefore,
I think, be safely assumed that the divergent crystalline structure
of the large spherulite was developed subsequently to the massing
together of the small (primitive) ones, which are also traversed by
the divergent structure proper to the lar ge or secondary spherulite.

The small or primitive spherulites show no fibrous or crystalline
structure of their own. What appears tv be tridymite is present
in a small cavity situated at a little distance from the margin of the
spherulite, and it is probable that some of the isotropic matter
occurring between the divergent fibres of the spherulite may also be
referred to this mineral, as in some of the cases described by
Iddings *,

Colourless microliths may be detected in the section, but they
do not appear to be numerous.

Some of the dark specks which, in reflected light, are seen to be
of a reddish or brownish colour, may be regarded as iron-oxides,

* Op. cit.

IN OBSIDIAN FROM CALIFORNIA, 425

To sum up the history of these spherulites, I think we may
assume that in the first instance small spherulitic bodies (the
primitive spherulites) were developed in the obsidian before it
assumed a condition of rigidity. Secondly, tiiat these small spheru-
lites floated towards certain points in the still viscid lava and
sevregated in more or less spherical groups, although what deter-
mined their movements, whether mutual attraction or some other
cause, there is no evidence to show. ‘Thirdly, that from a point or
points, situated at or near the centre of each group, crystallization
was set up, giving rise to a radiating fibrous or rod-like structure,
which gradually developed zone after zone of divergent tufts or
fibres, until the entire mass of primitive spherulites was permeated
by this secondary structure, a structure engendering a molecular
rearrangement of the mass such as would obliterate any trace of
structure which the primitive spherulites might have originally
possessed.

There are two or three small spherulites visible in the section,
which apparently arrived too late to be incorporated in the general
mass and which occupy conspicuous positions on the margin of the
crowd, and an independent divergent ery stalline structure has been
developed about them as shown in fig. 6, Pl. XVIT.

It was not until the foregoing aed were made that I had the
good fortune to see Mr. Iddings, whose work has already been
alluded to, and to converse with him upon the question now under
consideration.

Mr. Iddings has examined the specimen and section now laid
before the Society, and kindly given me his opinion upon them.

He considers that the bodies which I have here ventured to term
primitive spherulites are of secondary origin, and that they probably
consist to a large extent of tridymite, altnough from his cursory
examination of the section he could not speak positively as to the
presence of this mineral.

In this case he stated that he reasoned from analogy, and that he
had seen very similar phenomena in the spherulites and lithophysze
occurring in the obsidians of the Yellowstone National Park. From
an examination of a vast amount of material collected in that
district, he had been able to trace out structures of this class ranging
from some very obscure or minute to others occurring on a sufti-
ciently large scale to admit of more accurate determination,

In the present case he considered, Ist. that the spherulites or litho-
physz (he regarded them as the latter) originated in the development
of a radial crystallization, in which felspar microlites were developed
in a succession of twins which gave rise to delicate ramifying
growths; 2nd, that diminution of volume resulted from this action
of crystallization, and that vacuities were thus produced between
the twigs, if one may so term them, of this divergent crystalline
structute, so that the mass of the spherulite or lithophysa was
thoroughly cavernous or spongy in texture; 3rd, that within these
spaces tridymite was subsequently developed in small spherical bodies
consisting of aggregates of minute scales or plates of tridymite, and

426 MR. F. RUTLEY ON COMPOSITE SPHERULITES

that between these small spherical pellets of tridymite vacuities
still remained. In such empty spaces he finds that in most
cases emery or other grinding-material has collected during the
preparation of sections, In the central portion of one of the frac-
tured sphernlites in the specimen now described, he detected one or
two small crystals of altered fayalite.

Although it is not very easy to give the results of a conversation
accurately, , Without having taken notes at the time, yet I think that I
have here expressed the opinion with which Mr. Iddings favoured
me, clearly and correctly, and he kindly gave me permission to
make this statement.

That it is difficult, if not dangerous, to question the opinion of a
caretul observer who has had such unparalleled opportunities for the
study of spherulitic structures as Mr. Iddings has enjoyed, is a
fact of which Lam fully cognizant ; yet there appear in this particular
instance to be certain matters of detail which seem to support the
conclusions expressed by me in the foregoing paper.

They may be summarized in the following manner :—

Ist. That although diminution in volume is attendant upon crys-
tallization in cases such as that with which we are now dealing,
would it occur to an extent so appreciable that a cavernous or
spongy structure would be thus developed throughout the entire
mass of a spherical body an inch in diameter, or would it not rather
result in the production of one or two appreciably large fissures or
cavities such as are met with in lthophyse, assuming that those
fissures or cavities would not be developed through other causes
than contraction ?

2nd. That if such a spongy condition of the spherulitic ia were
induced, so that the entire spherulite consisted merely of divergent
and anastomosing filaments composed of felspar microliths, forming
a kind of delicate network, the interspaces of which were filled
neither with vitreous matter por with any other solid, would
tridymite deposited within such interspaces be developed in the
form of closely-packed, well-defined, spherical pellets, or would it
tend to crystallize out along the twigs of the divergent microlithic
structure of the spherulite, thus filling all the interspaces com-
pletely ?

3rd. That tridymite is in the habit of forming more or less
spherical groups is well known, but would such spherical groups be
formed in a closely matted aggregate of crystalline rods, since each
small pellet (primitive spherulite) would consist as much of felspar as
of tridymite? Furthermore, would not these minute felspathic rods
afford surfaces along which crystallization would be set up, and thus
seriously impede the crystallization of the tridymite in spherical
ageregates, if, indeed, it would not render such spherical development
impossible ?

4th. The small spherical pellets have well-defined boundaries
such as ordinary spherulites might have. Examination in polarized
light reveals the presence of comparatively little, if any, isotropic
matter, the pellets appearing to consist to a very large extent

IN OBSIDIAN FROM CALIFORNIA. 427

of doubly refracting fibres or matted microliths. From this fact
alone it is evident that it would be useless to attempt to determine
the presence of tridymite, either by solubility of the pellets in a
solution of an alkaline carbonate or by specific gravity.

5th. Where spaces occur between the small pellets or primitive
spherulites, they are filled with crypto-crystalline matter associated
with isotropic matter, which may be glass or which may be tri-
dy mite.

6th. On comparing what 1 here regard as the secondary structure
developed in this spherulite with the structures produced by the
devitrification of artificially formed glass, there appears to be a very
strong resemblance in most cases, making allowance, of course, for
differences in texture. The ramifications of the crystalline rods here
indicate the existence of divergent crystalline bundles, which are
probably bounded by radial planes of arrest, planes which in this
instance evade detection by reason of the delicate nature of the rods
composing each bundle, and the consequently confused appearance
caused by the overlap of several fasciculi within the thickness of the
section; whereas, in a more coarse phase of devitrification, a single
bundle would occupy the entire thickness of the section, so that, in
such a case, the arrest-planes would be well defined.

Now it is evident that if the initial points of divergent groups
originate very close to one another along one of the circumferential
bands of a spherulite (which band may be taken to represent a
pause in the crystalline development) those rods which diverge
most strongly from any radius of the spherulite will be quickly
arrested by the development of similar rods in the adjacent bundles,
and such rods will be excessively short, while those which approxi-
mate more closely to radii of the spherulite will be comparatively long.
Under such circumstances, the crystalline rods belonging to successive
zones will exhibit an apparent continuity. This seems to support
the view that the divergent crystalline structure in these spherulites
differs in no essential respect from the structure commonly observed
in manufactured glass which has been artificially devitritied.

Taking all these points into consideration, I am inclined to think
that the conclusions arrived at in this paper are substantially
correct; but, on the other hand, the wide experience of Mr. Iddings
in connexion with obsidians and the structures developed in them,
renders his opinion worthy of the most careful attention.

I trust that I have in no way misinterpreted his views, and I
would gladly substitute them for my own if, in this instance, I felt
that they offered a more satisfactory explanation of the phenomena
here described.

EXPLANATION OF PLATE XVII.

Fig. 1. Border of composite spherulite in black obsidian, from Hot-Springs,
near Little Lake, California, x 45. Ordinary transmitted light.

The light upper portion of the drawing represents the obsidian. The

boundary of the spherulite is here seen to be irregular, owing to the

al

partial reception of two smaller spherulites. The latter were traversed

428 ON COMPOSITE SPHERULITES IN OBSIDIAN FROM CALIFORNIA,

by the radial fibrous structure of the large spherulite with which
they are incorporated.
Fig. 2. Ditto, x 195. Ordinary transmitted light.
The radial structure is here seen to be crossed by short and delicate
circumferential shrinkage-cracks. The crystals and specks are
magnetite.

3. Part of the same spherulite, x 45. Ordinary transmitted light, showing
concentric banding.

4. The same part of the section shown in fig. 8, x 45, dark-ground
Uliwnination. By this method of illumination the composite nature
of the spherulite becomes clearly demonstrable, and it may be shown
that it is composed of a number of small, closely packed, primitive
spherulites, through which the concentric banding is seen to pass.

5. Radial fibrous structure of the same spherulite, as seen between crossed
nicols, the principal sections of the latter being situated at 45° to
the general direction of the fibration. The fibres are felspars, appar-
ently orthoclase, x 195.

Marginal portion of the same spherulite, showing smaller outlying ©
spherulites, around which an independent radial crystallization has
been set up, X 18. Oblique ordinary transmitted light.

o>

Discussion.

The Caarrman said that the sequence of the different portions
brought forward with so much care by the Author is one which
admits of much discussion.

Rey. E. Hitt said that the explanation of the divergence of these
crystallizations was extremely interesting. As to which structure
came first, it is difficult to determine. In the section exhibited
under the microscope he agreed with Mr. Rutley as to the sequence.
The question of molecular motion after consolidation in igneous
rocks is a subject of great importance.

MR. R. LYDEKKER ON ORNITHOSAURIAN REMAINS. 429

24. On Ornirnosaurtan Remarns from the Oxrorp Cray of Huntine-
DONsHIRE *, By R. Lypexxer, Ese., B.A., F.G.8. (Read April
16, 1890.)

My friend Mr. Thomas Jesson recently forwarded to me a few
small associated bones obtained from the Oxford Clay of St. Ives,
Huntingdonshire. which are of a certain amount of interest as being
the only specimens referable to a Pterodactyle hitherto described from
these deposits in England, or, indeed, so far as I am aware, in any
other part of Europe. The specimens comprise seven vertebre,
portions of the ilia and ischia of both sides; one femur and the
distal portion of the corresponding bone of the opposite side ; part
of a bone, probably from the shaft of the tibia; and two un-
determined fragments. When they came into my hands they were
partially bedded in their native clay, and their broken surfaces show
the pyritous impregnation so characteristic of Oxfordian specimens.

The Ornithosaurian nature of the specimens is at once shown by
the hollow shafts of the long bones and the structure of the vertebra,
the latter having proccelous centra, with complete obliteration of the
neuro-central suture. The two fragments of the femur (fig. 3), which
I have placed in apposition, do not exactly fit together, so that there
may be a portion missing from the middle of the shaft, and it is
quite possible that 1 have not put the proper distal half in apposition
with the proximal one. ‘The bones indicate an individual of some-
what smaller size than the examples of the Lower-Kimeridgian
Lthamphorhynchus Gemmingi figured by Professor von Zittel in the
‘ Paleeontographica,’ vol. xxix. pl. xi.

The portions of the pelvis (fig. 4) now remaining are of the
peculiar type characteristic of Rhamphorhynchus, as is so well dis-
played in the specimen represented in fig. 2 of the plate cited. The
pecuharity of this type of pelvis is that the ischium is connected with
the hinder portion of the ilium to form a large expanded plate ;
while the ilium itself is united with the sacrum by means of four broad
and flattened sacral ribs, which are anchylosed to the ilium, of which
they appear to be mere processes. On the other hand, so far as I
can gather from Meyer’s figure of P. spectabilis, the pelvis of Pte7o-
dactylus is constituted on quite a different plan; which alone
justifies our regarding the two genera as referable to separate
families. Now, although the conjoint ilia and ischia of the Oxfordian
Pterodactyle are far from perfect, yet such of the several processes
of the ilia as remain so exactly accord with those of Rhampho-
rhynchus that I think the English form may be safely referred
to that genus.

Of the vertebrae we have two, in apposition, which from their

* When the paper was read the authOr was under the impression that the
specimens came from Northampton,

430 MR. R. LYDEKKER ON ORNITHOSAURIAN REMAINS

large size are evidently cervicals. They are somewhat smaller than
those of the specimen represented in fig. 1 of Zittel’s plate. The
arches and spine are not well preserved, but the inferior aspect ot
the centra (fig. 1) is eutire. These exhibit a feature which at the

Rhamphorhynchus Jessont.—1. Left-lateral and ventral aspects of two cervical
vertebra ; 7, rib-facet. 2. Left-lateral and ventral aspects of a dorsal ver-
tebra. 3. Ventral aspect of the left femur. 4. Ventral aspect of the left
innominate; ac, acetabulum. (All the figures are twice the natural
size. ) .

time Professor Huxley wrote his ‘Anatomy of Vertebrated Animals’
had not been observed, but which has subsequently been recorded
by Dr. Baur in the genus Rhamphorhynchus. This feature is the
presence of a distinct rib-facet at the lateral border of the inferior
surface of the centrum, thus proving the emstence of cervical ribs at
least in this genus of Pterodacty les.

Another vertebra which calls for notice is an entire dorsal. The
most noticeable feature of this specimen (fig. 2) is the lowness and
length (antero-posteriorly) of the neural spine, which strikingly
recalls that of a bird. There is no rib-facet on the centrum, and
apparently none on the arch, so that the rb was probably supported
entirely on the transverse process, as in crocodiles. An imperfect
sacral vertebra shows the widely expanded sacral ribs anchylosed to
the centrum, and corresponding in size with the sacral processes of
the ium.

The femur, as I have placed the two fragments, measures about
one inch in length. The globular head is set very obliquely to the
shaft by means of a long ‘neck ;’ there is no inner trochanter,
although the posterior surface of the shaft shows a distinct linea
aspera,

The specimens under consideration are of interest, not only as the
first recorded evidence of an-Ornithosaurian in the Oxiord Clay, but

FROM THE OXFORD CLAY OF HUNTINGDONSHIRE. 431

also as showing the natural contour of the bones, which are generally
more or less flattened in the specimens from the Lithographic Lime-
stone. They do not afford characters by which the species to which
they belong can be detinitely distinguished from Rhamphorhynchus
Genvningy? ; but since they come from a lower horizon than the latter,
I venture to regard them as the type of a provisional species, tor
which I have proposed the name Lt, Jissoni. The genus Rhamphor-
hynchus, as now restricted, has been hitherto known only trom the
Lower-Kimeridgian Lithographic Limestone.

432 MR. J. C. B. HENDY ON A “ WASH-OUT”’ FOUND

25. Nores ona ** Wasu-our” found in the Preastry and TEvErsaLy
CoLiiertes, DErBysH1RE and Norts*. By J.C. B. Henpy, Esq.
(Read April 16, 1890.)

(Communicated by Dr. W. T. Buanrorp, F.R.S., F.G.S8.)

Tue Top Hard Coal-seam of the Midland Coal-field is being worked
at these collieries at a depth of 217 yards at Teversall, and 514
yards at the Pleasley pits; the average thickness of the seam is
5 feet, with a band of cannel in the middle, varying from 4 to 14
inches. The general dip of the coal-seam is 1 in 12 to the N.E.

The *“ Wash-out ” was first met with in the Teversall workings,
about half a mile east of those pits, and from this point it has been
proved to run for a distance of a mile and a quarter in a north-
easterly direction, as shown 1m the plan, fig. 1.

The coal has now been worked off on each side of the “ Wash”
for a length of over 600 yards in the Teversall mine, and for 200
yards in the Pleasley workings, the boundary of the ‘“* Wash”
being shown on the plan by strong lnes where actually proved.
Headings have been driven through the “‘ Wash” at five different
places, four of these from the Teversall and one from the Pleasley
colhery. In each case these headings were driven next the
ordinary sagar-clay floor of the mine; this under-clay is about
18 inches thick, and contains numerous nodules of ironstone.
Careful sections of these ‘‘ headings” have been taken, plans of which
are given.

Section No. 1 (fig. 2)—At a distance of about 60 yards from the
‘Wash ” the coal commenced to thicken; this continued until imme-
diately adjoining the “* Wash” the seam reached a height of 9 feet.
On nearing the ‘* Wash” a thin layer of soft sandstone is met with
in the middle of the seam; this sandstone thickens hke a wedge
until the ‘*‘ Wash” is reached, the coal running out above and
below, as shown in the section. The width of the ‘“ Wash ” is here
about 34 yards ; and after heading this distance the coal was again
met with next the floor, at first a thin band, but gradually
increasing, until at 10 yards from the sides of the ‘ Wash” it
reaches a height of 7 feet,—from this point returning to the ordinary
section of the seam. The edges of the coal next the “ Wash” in
this section are dull and smooth, it being difficult in some places to
separate the sandstone from the coal, several thin layers ot sandstone
and earth-like impurities running from the ‘“ Wash” into the
joints of the seam, and permeating the coal for a distance of from 2
to 3feet. The “ Wash ” itself consists of a hard, yellow, stratified

* In Quart. Journ. Geol. Soc. vol. xlvi., Proceedings, November 6, 1889,
pp- 1 and 2,a short notice of this paper with the Discussion was published.
Further particulars then asked for having been supplied, the present paper has
been communicated,

IN THE PLEASLEY AND TEVERSALL COLLIERLIES,

sandstone, the lines of stratifi-
cation being horizontal, but
slightly inclining at the edges
of the “* Wash” to the top of
the coal-seam, as shown by the
lines in the Section No. 1.
‘The ordinary surface of the
clay floor of the mine is smooth
and level; but in crossing the
“Wash” this floor becomes
uneven, presenting a series of
furrows and ridges, the general
line of these being at right
angles to the course of the
“Wash.” The ironstone balls
are expused and stand, in many
places, from 2 to 3 inches
above the clay, their surfaces
being rounded and apparently
worn. In many places the
floor is finely streaked or stri-
ated, the striz running gene-
rally parallel to the course of
the “Wash.” The whole pre-
sents every appearance of
having been subject to the
action of a strong current.
Section No. 2 (fig. 3).—In
this section the ‘‘ Wash” has
divided into two branches, the
width of the northern branch
being 40 yards, and that of the
southern 50 yards; the two
being separated by about 46
yards of coal, 9 feet thick.
Several layers of sandstone run
from the north ‘“ Wash” into
the sides of the coal-seam for
from 10 to 15 yards, these
layers turning soft and friable
as they leave the ‘‘ Wash.”
In this section the thick coal
is found almost entirely be-
tween the two ‘“‘ Washes,” there
being also a marked difference
in the stratification of the
sandstone in the two branches,
that of the north branch being
horizontal, as in Section 1.
whilst that of the south bears

h1327709

—

Wor
y a ol
>

ee See
<9 \ Oras
aS aa
a 2
a
~
<*

h1927}09 [P8470 rs

oe

—— eS eee,

ran

‘punowS..apuN spvod URUT FuLMoyYs soaurvT

wi 24n}]1\ hajsvaz

17
4
hasyqay hajsna

—_—

433

/
"yno-ysn 44 ayn Durnoys ‘sarvarj09 hapsnary pun 7)n8.0909,], ayn fo UDIT—'[ “SLT

(‘oprun BOF Yul | apeo~)

MR. J. C. BD. HENDY ON A “ WASH-OUT”? FOUND

434

“TROD INE
“ATIOYSpULG *T ‘urRag pany dog, fils ‘- ‘ayeyg “9
‘AUOJSMOA YIM ‘AvJo-od lyf *Z l TLOD °G ‘oucqspurg *)

“

N "GON Uorpag “Nuayi0g hopsnag Uu~—e *Biq ‘8

"N : "Pp ON wowog *hia209 YvSssanay UT —F *B1T 's

“Nl "GON woray huar209 Ynswanay, UT —'S “SUT 'S

“NI "LON woroag *huan70g 1)Vswanay, U—'G “By ‘8
(‘[eULstio Jo + poonpary “qoog Te 04 YOu T oyeos TRorIoa £490 QT
0} YOUL T ovos [eyNoZMOF{) —*saad21p 09 Napsvarg pun [[vs1anaT ay Ut yno-YysM AA AY) JO SUOrMIG—'*G “F ‘E ‘Z "SST

IN THE PLEASLEY AND TEVERSALL COLLIERIES. 435

evidence of lateral movement and pressure, being curved and con-
torted, as shown by the lines in the section. The same peculiarities
were found in the floor of this section as described in Section 1.

Section No. 3.—This section is very similar to No. 2, the only
difference noted being, that there are not so many layers of sand-
stone running into the sides of the seam, and that the coal for a
length of 23 yards under the northern ‘“* Wash” has not been
entirely denuded.

Section No. 4 (fig. 4).—Here the two branches of the “* Wash” have
again united, and in this locality the denuding force seems to have
been strongest, for not only is the coai absent but in two places the
clay floor has been entirely removed, in one instance for 7 yards, and
in the other for a width of 10 yards, laying bare the sandstone
below, there being a thin smooth parting between the sandstone of
the * Wash” and that of the floor. On examining this sandstone
floor it is found to be furrowed and, in some places, distinctly ripple-
marked, the wave-lines being more or less at right angles to the
course of the ‘Wash.’ The line of denudation is made apparent
in the coal-seam on either side of the ‘** Wash” by a layer of
sandstone, of from 3 to 6 inches thick, which divides the upper from
the lower coal (see fig. 4). The upper coal has evidently been
re-deposited, being in many places impregnated with sand and
earthy matter, whilst the lower coal retains its ordinary appearance
and quality. On the south side of this section several blocks of
isolated sandstone appear in the middle of the seam, these doubtless
being the result of cavities formed in the coal about the time of
denudation, and afterwards filled with sand, &c. ‘The width of the
* Wash” here is about 75 yards.

Section No, 5 (fig. 5)—This section is taken in the Pleasley
colliery-workings. There is here a shale 2 feet thick, imme-
diately overlying the coal, and forming the “roof” of the
mine, instead of sandstone as in the Teversall colliery. On
approaching the ‘* Wash ” this shale disappears with the coal, the
overlying sandstone and that of the ‘“‘ Wash” taking its place.
There is the same thickening of the seam on each side of the
** Wash.” On the north side the cannel gradually runs out in the
lower coal, whilst in the upper coal it increases to a thickness of
over 3 feet. The sandstone of the “ Wash” is here harder and
more compact, its stratification not being so well marked as in the
other sections ; but, as in several other instances, it penetrates the
sides of the coal-seam like a wedge, this peculiar shape no doubt
being due to the subsequent vertical pressure. The clay floor
here maintains its ordinary appearance, there being none of the
signs of denudation noticed as described in the other Sections,
figs. 2, 3, 4.

Most careful examination has been made of all these headings,
but in none of them have any fossils been found in the ‘“ Wash.”
There are, however, several “ threads ” or thin layers of coal running
throughout the ‘sandstone ” of the ‘* Wash,” varying in thickness
from | to 3 inches, and from 4 to 20 inches in length, these being

436 MR. J. C. B. HENDY ON A “* WASH-OUT” FOUND

in most cases more numerous near the edges of the “ Wash.”
Several Stigmarie have been found in the under-clay.

In every section examined, where there is cvidence of Jateral
pressure, the sides of the “ Wash ” are more or less *‘ slickensided” ;
in other cases the sandstone of the ‘‘ Wash” is found in immediate
contact with the coal, it being difficult sometimes to separate the
two, both being in a state of transition; in other places the two
surfaces are dull and smooth, as in the ordinary bedding between
two strata.

It is impossible to say how far the “ Wash ” extends upwards ;
but, as the sandstone of the ‘‘ Wash” is similar to that overlying
the shale, in all probability it does not reach beyond that bed.
Future workings in the Pleasley colliery will doubtless further
prove its course, but evidently it either disappears or takes a sharp
turn to the east, as shown by the present workings in the Pleasley

1t.

: It has frequently been suggested that these “ Wash-outs” are
due to ‘“ faulting ”; there is, however, little evidence of this here,
the only signs of ‘ faulting ” being the partly ‘‘ slickensided ” edges
and in some few places the distortions of the coal next the ‘“* Wash ”;
these, however, are evidently due to lateral pressure and movye-
ment, subsequent to the denudation of the coal and the deposition
of the “« Wash” itself. Moreover it is difficult to conceive how any
‘¢ faulting,” in the ordinary sense, could have taken place in the coal
or the measures above, without the sub-strata, or at any rate the
clay-floor, being at the same time to a certain extent dislocated or
disturbed; yet in all these sections the under-clay and the sand-
stone below are found in their normal condition, excepting as shown
in Section 4 (fig. 4), where the clay has been denuded at the same
time as the coal.

The most striking peculiarity of the “ Wash-outs ” found in this
district is doubtless the thickening of the coal at the edges.
Several ‘‘ Washes” or “ Drifts” have been found in the Durham
coal-tield. The writer remembers examining a ‘“‘ Wash” at the
Middle Beechburn colliery in the west of Durham, which was
first proved at the outcrop of the coal-seam, and followed by the
workings on each side for a distance of ? of a mile into the hill-
side. The peculiar feature of this ‘‘ Wash’’ was, that whereas that
near the outcrop consisted of sand and fine gravel, as the distance
from the outcrop and the depth of the superincumbent strata
increased, the sand gradually changed, first to a soft sandstone, and
ultimately, when a depth of 230 yards from the surface had been
reached, to a hard and compact sandstone, the change evidently
being due, to some extent, to the increased pressure, &c., of the over-
lying strata. In the Teversall “* Wash-out,” however, there is no
thickening of the coal, the measures having been simply denuded
and carried away in suspension by a powerful current. In the case
of the “* Wash” at these pits from one third to one half of the coal
has been re-deposited in different places on the sides, the remainder
having evidently been carried away. It seems probable, therefore,

IN THE PLEASLEY AND TEVERSALL COLLIERIES. 437

that these “ Wash-outs” may be due to quite different kinds
of aqueous action :—first, as in Durham and elsewhere, by a current
flowing at a high rate of speed in one direction, denuding and carrying
away the whole of the denuded material; and secondly, as in the
Derbyshire “ Wash,” by a series of inundations or overflows of water,
each in-rush denuding a certain amount, and on subsiding depositing
part of the material at a higher level, whilst the remainder was
carried away in suspension. Such action may have been the result
of the periodical overflowing of a lake, or the more regular rise and
fall of water in an arm of the sea. At the time this action took
place the surface would doubtless be a soft, pulpy mass of vegeta-
tion in a state of decomposition, which would easily be removed by
a current of water, however slight.

A “ Wash-out” similar to the one described in these notes has
been met with in the Blackwell and other collieries, and described
in a paper read by Mr. G. E. Coke before the Chesterfield and
Midland Institute of Mining Engineers. This “ Wash” has been
proved by the Blackwell coal-workings to run within 25 miles south-
west of the Teversall pits (see the plan, fig. 1), and an impression
seems to exist in the minds of several interested in the subject, that
the Teversall and Pleasley ‘‘ Wash” is a portion or continuation of
that at Blackwell, &c. The writer submits that this cannot be so;
for, whereas the Teversall ‘‘ Wash” is found in the Top Hard-Seam,
that at Blackwell has been proved in the Deep Hard Coal, some 200
yards below; and as the Deep Soft and other coal-seams lying
between the Deep Hard and Top Hard have not been influenced by
either ‘‘ Wash,” it seems certain that they must have occurred at
vastly different periods :—the Blackwell “‘ Wash ” after the deposi-
tion of the Deep Hard Coal, but before that of the Deep Soft ; and
the Teversall and Pleasley “ Wash” at a very much later period,
viz., after the formation of the Top Hard Seam.

Q.J.G.8. No. 183. 21

438 MR. D. PIDGEON ON CERTAIN PECULIARITIES OF

26. On certain Puystcat Provrtarities exhibited by the so-called
*‘RaiseD Bracnes” of Horn’s Nosr and the THarcuer Rock,
Drvon. By D. Prpexon, Esq., F.G.S., Assoc.Inst.C.E. (Read
April 30, 1890.)

(Abridged.)

‘THE so-called ‘“‘ Raised Beaches” of Hope’s Nose and the Thatcher
Rock, near Torquay, have been so often discussed by eminent geolo-
gists that no attempt will be made to add anything by way of
description in a paper proposing to deal exclusively with certain
physical peculiarities exhibited by the “‘ beaches” in question.

The word ‘‘ beach” may be defined as an accumulation of sandy,
shelly, and pebbly materials brought together, by the action of
waves, upon the shore; while ‘raised beaches” are similar accu-
mulations which since their formation have been lifted above the
present level of the sea.

These definitions being granted, the author proposes to show, in
the first place, that certain physical considerations, applicable to
both of the “raised beaches ” in question, make it impossible to
consider them as beaches at all; and, in the second place, to suggest
a possible explanation of their origin.

The considerations in question first struck the writer while
working out the Conchology of the beaches for his friend Mr. A. R.
Hunt, of Torquay, who has embodied the results thus obtained in a
speculative paper on “ The Raised Beach on the Thatcher Rock :
its Shells and their Teaching” *. He gives a list of 43 species, with
notes on their distribution in the present seas.

Referring, in the first instance, to the stony constituents of the
beach, it will be observed—

1. That all the hand-samples exhibited to the Meeting are com-
posed of fragments of rock and shells, both of which, with scarcely
an exception, exhibit sharply fractured edges and are without any
stratification. 2. That the rock-fragments consist, almost exclu-
sively, of limestone derived from the cliffs overhanging the so-called
beach; and that they are exactly such splinters as would fall, under
the influence of weather, and particularly of frost, from those cliffs.
3. That the number of pebbles, properly so-called, in the beach is
quite insignificant ; and that, of these, very few are composed of the
local limestone, chips of which constitute nearly the whole of the
stony component of the deposit. 4. That stones other than lime-
stone occur very sparingly and consist of quartz, Triassic trap,
Devonian sandstone, and flint; and that, of these, very few are
rounded, although some were once pebbles, which had been fractured
before finding their way into the “beach.” 5. Of the very few
rounded stones of any kind, one here and there is incrusted with
Annelidan tubes, acquired under water, and not since removed by

* Trans. Devon Assoc. vol. xx. pp. 225-252.

|
|

SO-CALLED “‘ RAISED BEACHES ” IN DEVON. 439

the attrition of a beach. 6. The limestone chips are entirely free
from Annelidan incrustations and borers’ holes. 7. On the other
hand, fragments of what were once small limestone pebbles, riddled
by borers, occur in some numbers; no bored limestone pebbles,
however, are found.

Turning now from the stony to the shelly components of the
deposit, these latter demonstrate—

8. That about half the mass consists of shelly matter. 9. That
the shells, with scarcely an exception, are fractured, exhibiting
peculiarly sharp and sometimes razor-like edges. 10. That the
bulk of the shelly component consists of rock-dwelling shells, such
as Litorina and Purpura, derived from the Laminarian and higher
zones; and that a large proportion of these rock-dwellers are un-
broken. 11. That, on the other hand, all the sand-dwelling Bivalves
in the deposit are broken into fragments. 12. Whether whole or
broken, however, all the shells retain their sculpture to a very re-
markable extent, some allowance being made for chemical erosion.
There is hardly a beach-rolled shell, and very few beach-rolled
fragments of shell, in the collection. 13. No Annelidan incrusta-
tions occur on the unbroken shells, and very few on the fragmental
Bivalves—another indication that both came, for the most part, into
the beach as “‘ live” shells. 14. While the facies of the forty-three
shells obtained by Mr. Hunt is generally that of the present Mol-
luscan fauna of Torbay, one decidedly Northern shell (Zrophon trun-
catus, and one less decidedly northern (Pleurotoma turricula) occur
in the list. These two shells might, perhaps, be taken to indicate
a rather colder sea in the era of the raised beach. .

Nothing could be more unlike a true sea-beach than the breccial
deposit thus characterized. As to its stony constituents, nothing
need be said; the splinters of local limestone speak for themselves ;
but, with regard to the shelly components, it may be remarked :—

1. The shells most abundant in this breccia, namely the rock-
dwellers, are usually rare on the shore, and a beach of which Pur-
pura and Litorina form an even appreciable proportion is unknown.
Further, such rock-dwellers, when found on beaches, are always
beach-rolled. 2. Bivalves, which are.generally much more nume-
rous than Gasteropods on beaches, are usually found with parted
valves, but otherwise unbroken; and a beach upon which all the
Bivalves are fragmental, while most of the Gasteropods are whole,
does not exist. 3. Such broken shells as occur on existing beaches
have their fractured edges always waterworn; but many of the
beach shells, the Purpurw especially, exhibit almost razor-like edges.

Before attempting any explanation of the origin of the Hope’s
Nose and Thatcher Beaches, it will be well to formulate certain
questions which any such explanation must answer under pain of
being inadequate.

As to the stony constituent of the beaches, it must say:—

1. Why are the limestone chips, which constitute the chief com-
ponent of the deposit, sharply angular? 2. Why, if they be por-
tions of a true beach, these fragments exhibit no signs of beach-

212

440 MR. D. PIDGEON ON CERTAIN PECULIARITIES OF

rolling, and why are none of them bored or encrusted by Annelidan
tubes? 3. Why, on the other hand, do certain fragments of lime-
stone pebbles which have been riddled by borers occur in the
deposit? 4. Why do Annelidan incrustations occur only on the
pebbly stones in the deposit, and how have such incrustations
escaped destruction from beach-rolling? 5. How, the bulk of its
stony component being local in character, were the few small foreign
stones in it brought into the deposit? 6. Why is there no indica-
tion of stratification in these raised beaches * ?

Again, as to the shelly components of these beaches :—

Fe “Why does half the deposit consist of shells, while these (except
in the case of beaches composed entirely of shells and their frag-
ments, not in question here) form such an insignificant proportion
of existing beaches? 8. Why are the shells for the most part
broken, and why do their fragments preserve sharp edges? 9.
Why are there so few beach-rolled shells or shell-fragments in the
deposit? 10. Why are none of the unbroken, and scarcely any of
the broken shells either incrusted by Annelidan tubes or perforated
by marine borers? 11. Why are all the Bivalves broken? 12.
Why has the group of shells (see Mr. Hunt’s list referred to above)
a somewhat northern aspect ?

The answers to these questions must, in the author’s opinion, be
sought in the study of certain Arctic phenomena, to which the
attention of geologists was first drawn by Feilden and De Rance.
They say tT “ there is no point of greater interest in Arctic geology
than the occurrence of water-margins at successive elevations in
“Smith Sound, rising to heights of from 200 to 300 feet, in situations
where wave-action was impossible. These ancient sea-margins are
most persistent in bays, inlets, and narrow arms of the sea; and
are still in process of formation.”

During the short Arctic summer, upon the first signs of thaw,
masses of rubbish fall from the cliffs and form immense screes,
which not only reach, and cover, the “ ice-foot,” but are often carried,
in part, by the impetus of their fall, on to the floes beyond it.
Towards the close of the thaw episode, the sun’s rays, being rapidly
absorbed by the dark surface of the ‘ screes,” melt the uppermost
layers of the ice-foot at its point of contact with the hill-side, thus
producing a deep trench, filled, as soon as it is formed, by water
which, at this season of the year, pours from the uplands.

The overflow from the trench in question, escaping over the ice-
foot, cuts deep channels within a few hours across the latter,
draining the ditch at low-tide, while at high-tide the sea pours
through these transverse gullies into the trench and, sweeping right
and left, with more or less violence, assorts and reassorts the stony
chips which it contains.

Meanwhile, the waves throw all sorts of “jetsam” both upon-the
surface of the ice-foot and into the ditch, mingling shells, weed,

* There is none seen in the lumps of beach exhibited.
+ Quart. Journ. Geol. Soc. vol. xxxviii. p. 563 (1878).

SO-CALLED ‘‘ RAISED BEACHES ”’ IN DEVON. 441

erustacea, &c. confusedly with the stony chips which have already
accumulated there.

Attempting now to apply the observations of the Naturalists who
accompanied the Nares Expedition to the phenomena of the Hope’s
Nose and Thatcher beaches, it will be presumed that the British
Channel was encumbered by floe-ice, and its bays margined by an
ice-foot, at a time when the so-called beaches were accumulated,—
and that they are composed, partly of chips of local limestone falling
into an ice-foot-formed trench, such as that already described, and
partly of such shells and fragments of shells as were thrown into
the trench in question by the sea.

If that be so, the following answers may be given to the questions
already proposed :—

1. The limestone chips which constitute almost the entire mass
of the stony deposit are sharply angular because they were
weathered out by frost from the cliffs above the so-called “ beach.’
2. These chips have not lain long enough under sea-water to
become either rolled, bored, or incrusted by Annelids. Such sea-
water as, entering the trench, rushed this way and that, with more
or less violence, at every tide, might give the contained mass arude
stratification, but could not convert the chips into pebbles or afford
time for the growth of borers and Annelids. 3. Such fragments ot
bored limestone pebbles as occur in the deposit were thrown into
the trench by the sea, after the pebbles from which they were
derived had been triturated by floe-ice. 4. The stones on which
Annelidan incrustations occur were probably thrown by the sea
into the “trench”; and there, protected from attrition by their
sheltered position, they preserved such incrustations as would have
been almost immediately lost on a beach. 5. The bulk of the
stony constituents of the deposit is local, having fallen from the
cliffs above, under the influence of frost. The few foreign stones it
contains have been thrown in by the sea. 6. There could be no
real “ stratification” of its contents in a trench, now full and now
empty of water, into which chips from the overhanging cliffs were
continually falling, and to which every tide and every storm
furnished each its quota of *“‘ jetsam.” 7. The contribution which
the sea in rough weather would make to the deposit in the “ trench ”
would consist for the most part of shells derived, in a more or less
triturated condition, from the Laminarian zone and somewhat deeper
water. 8. After being broken by the action of floe-ice on the shore,
these shells were quickly thrown into the trench; and some of the
rock-dwellers would be more, and others less damaged by the floes
before the waves took them in hand. 9. These, forming part of
the “jetsam” thrown during storms into the trench from com-
paratively deep water, were insignificant in quantity relatively to
the stony matter always falling into it, and to the rock-dwellers
which the floes were always crushing and putting at the immediate
disposition of the waves. 10. Whether broken or unbroken, nearly
all the shells were thrown into the trench “ alive,’ in which condi-
tion shells are seldom found either bored orincrusted. 11. Coming

4492 MR. D. PIDGEON ON CERTAIN PECULIARITIES OF

from deeper water than the rock-dwelling Gasteropods forming so
large a proportion of the deposit, they were sure to suffer more
trituration than the latter from floes on their way from compa-
ratively deep water to the “trench.” 12. If Trophon truncatus
proves anything, it must be that the climate was colder during the
accumulation of the deposit than it is to-day.

All the foregoing remarks, together with the speculation founded
upon them, apply solely to the “raised beaches” of Hope’s Nose
and the Thatcher Rock. About the physical peculiarities of other
raised beaches the author does not here pretend to speak; but if it
should be admitted that the two raised beaches in question are not
“‘ beaches ” at all, it is probable that other similar deposits will pro-
fitably bear re-investigation. Meanwhile, if the writer’s hypothesis
should stand the strain of criticism, it would appear probable that
the ‘‘ raised beaches” of Hope’s Nose and the Thatcher Rock are
phenomena marking the close of the Glacial Period in England.

Discussion.

The Presipent remarked that anything which might throw lght
on what took place in Glacial times in the non-glaciated regions of
Southern England would be welcomed by geologists.

Mr. Ussner asked if the Author would not expect the stones in
the beach to show some traces of glaciation if his explanation were
correct. He was glad to hear that the Author considered that colder
. conditions prevailed during the formation of the beaches, though he
himself did not think that the climate was Arctic. He instanced
the occurrence, on a pinnacle 30 yards from the main cliff, of a
fragment of raised-beach platform which was originally talus from
the high ground behind the beach.

Prof. Huexes was glad to hear that these were not exactly beaches,
but subaerial accumulations with shells and pebbles thrown up in
storms, as he had supposed from an examination of the Braunton
beach, and did not therefore necessitate any considerable changes
of level. He, however, saw no necessity for glacial action to account
for the phenomena. Trophon clathratus and Mangelia turricula
were elsewhere associated with Scandinavian shells, but he con-
sidered them to be last survivors from former colder conditions. He
did not understand how the materials were thrown over the ice-foot.
The materials were comparable with those of modern talus. Iso-
lated pebbles were thrown to a great height above sea-level.

Mr. Crement Re maintained that the shells were common British
species. The fact that Purpura was less worn than the bivalves was
paralleled on the ledges above modern beaches. He could not agree
with Prof. Hughes as to the “raised beaches” of the south of
England having been accumulated by the sea at its present level ;
for in Goodwood Park, 7 miles from the coast, they are found up to
a height of 130 feet. The fauna of these is distinctly not Arctic.

The Prestprenr had seen these beaches. It never occurred to him
at the time that they afforded evidence of glacial conditions, though

SO-CALLED ‘‘ RAISED BEACHES” IN DEVON. 445

he thought the shells showed them to be tolerably old. He thought —
the deposits might have been formed by agents now in operation
along the same coast, though they certainly differed from any other
‘‘ raised beaches ” with which he was acquainted.

The AurHor, in reply, stated that evidence of extreme glaciation
was not to beexpected. He thought the “ head” was formed during
the passing away of glacial conditions, and referred, in corroboration
of his views, to Dr. J. Geikie’s work. He had seen sand and shingle
thrown to a great height, but never fragments of broken shells such
as those exhibited. Col. Feilden and Dr. Moss distinetly stated that
materials were thrown over the ice-foot. Mr. Reid had touched the
true difficulty; for there were several Southern shells, such as
Adeorbis, present, and the general assemblage was not a northern
one; but too much might easily be made of this, while he had
himself relied chiefly upon the physical evidence to show that the
deposit was not a true beach.

444 MR. E. T. NEWLON ON NEW MAMMALS FROM

27. Gn some New Mammats from the Rep and Norwicu Crags.
By E. T. Newron, Esq., F.G.8S. (Read May 14, 1890.)

(Communicated by permission of the Director-General of the Geological Survey.)
[Puate XVIII. ]

Contents.

Introduction.
Description of Species :—

1. Lutra dubia, Blaine.
Lutra Reevei, sp. nov.
Phoca Moori, sp. nov.
. Phocanella minor, Van Bened.
. Trogontherium minus, sp., nov.
. Mesoplodon floris, sp. nov.
. Mesoplodon scaphoides, sp. nov.
. Ailurus anglicus, Dawkins.
Explanation of Plate XVITI.

OO ISD Ore oo bo

Introduction.

Norwirusranpiné the many additions which within the last few
years have been made to our knowledge of the Pliocene Mammalian
Fauna, by Mr. Lydekker, in the Quarterly Journal of this Society,
in the ‘ Geological Magazine,’ and in the British-Museum Catalogues
(1885-87), several species new to the British Crags, and others
altogether new to science, have come to light during a critical inves-
tigation of the Crag Vertebrata, which it has been my official duty
- to undertake.

As it is likely to be some time before the results of this inves-
tigation can be published, it is hoped that an account of the new
forms will be acceptable to the Fellows of this Society.

For several of the specimens here described I am indebted to the
kindness of Mr. E. C. Moor, of Great Bealings, Suffolk, who has
most courteously placed these and many other fossils at my dis-
posal. Mr. James Reeve, of the Norwich Museum, has likewise
been good enough to lend me many specimens, and among them
the unique tooth which is now to be named after him. For the
opportunity of studying the rostrum of esoplodon Flower * I am
under obligation to the genial Curator of the Ipswich Museum, Dr.
Taylor. ‘To all these friends of science I tender my best thanks for
their kindly assistance.

Description of Species.
1. Lurra pusia, Blainville. (Pl. XVIII. figs. 1 a—1 c.)

Within the last few years Mr. E. C. Moor, of Great Bealings,
has obtained from the nodule-bed of the Red Crag, near Wood-
bridge, a right ramus of a lower jaw of an otter-like animal (fig. 1),

* Since this paper was read, the author has altered this name to ©. floris, see
p. 448.

ee
OAT Nt

my
aly

—

Quart.Journ.Geol Soc Vo} XLWI. PL XVIUI.

€ oh = SH E AM (at fintern Bros inp
i Mint: t Lit SRI it 110 Jed M, N MA S)-
mtern del. et th EN N 3

THE RED AND NORWICH CRAGS. 445

which differs from Lutra vulgaris in having the carnassial tooth
longer from before backwards, and proportionately narrower, while
its inner cusp is smaller than in this recent species. The entire
alveolar border is preserved, excepting that for the incisors, and
measures from the back of the canine to the back of the hindermost
molar 40 mm. ‘The depth of jaw below the middle of the carnassial
tooth is 17 mm. The carnassial itself is 16 mm. long, 6 mm. wide,
and the crown is 5 mm. high. The number of cheek-teeth is appa-
rently the same as in Z. vulgaris (c. 1, pm. 3, m.2); but the front
premolar seems to have been smaller and placed more obliquely,
while the hinder premolar was larger than in ZL. vulgaris. The
fangs of the premolars also differ from those of ZL. vulgaris in that
each tooth has the hinder fang much larger in proportion to the
front one, and this is especially the case in the tooth immediately in
front of the carnassial, the piece of tang remaining in the hinder
alveolus of this tooth being nearly three times the size of the ante-
rior fang. ‘These differences prevent the Red-Crag specimen from
being referred to Lutra vulgaris.

LutraValetoni, as figured by M. Filhol*, shows the alveolar border
a little longer than it is in our specimen; but the carnassial tooth
is proportionately smaller: moreover 1. Valetont has four premolars,
and these approximately equal in size.

Lutra affinis, Gervais?, seems to have little to distinguish it from
L. vulgaris.

Lutra Bravardi, Pomel {, corresponds in size with the Red-Crag
specimen ; but, as the species is only represented by an upper jaw,
it cannot be compared with our example of a lower jaw.

Lutra dubia, Blainy.§, from the Miocene of Sansan, bears a very
close resemblance to our specimen; and I have been able to com-
pare it more closely, as Prof. A. Gaudry has kindly sent me a cast
of the type, which is preserved in the Muséum d@’Histoire Naturelle
at Paris. The length of the alveolar border is the same in both
specimens ; the carnassial teeth are as nearly as possible of the same
length ; the premolars have similar large posterior fangs, and
decrease in size towards the front in the same manner; also the
depth of the jaw below the carnassial is the same. The greatest
differences observable are—that the Paris specimen has the ‘ramus
deeper below the premolars, the carnassial tooth not quite so narrow
at its hinder part, and not so much curved from before backwards.
The last molar also seems to be somewhat larger than the tooth
could have been which occupied the hinder alveolus of the Red-
Crag specimen. These differences, which are to some extent due
to wearing and rolling, are not sufficient, as it seems to me, to pre-
vent this British Red-Crag lower jaw being referred to De Blain-
ville’s Lutra dubia.

* Ann. Sci. Géol. vol. x. pl. vii. (1879).

‘t Zool. Pal. Fr. edit. 2, p. 244 (1859).

{ Gervais, doc. cit. p. 243.

§ ‘ Ostéographie,’ Genus Musfe/a, p. 76, pl. xiv.

446 MR. E. T. NEWTON ON NEW MAMMALS FROM

2. Lurra Reever, sp. nov. (Pl. XVIII. figs. 2 a—2¢.)

One of the most remarkable teeth which I have seen from the -

British Crags was found by Mr. James Reeve, in the lower beds of
the Norwich Crag at Bramerton. This tooth (fig. 2), though small,
is in a most perfect state of preservation; and, being a germ-tooth,
the cusps are entirely free from facets of wearing ; it consists of the
enamel cap, with a layer of dentine supporting it within, and con-
sequently the crown may have a less altitude than it would have
had in the completed tooth. The length from before backwards is
20 mm., the width 10 mm., and the height + mm. In general
contour the tooth is nearly parallel-sided; one end is flattened and
the other bluntly pointed; the half corresponding to the pointed
end is occupied by three cusps of nearly equal size, while the other
and somewhat smaller half has a broad depressed space, with a
cusp on one side and a ridge on the other; the cusp being a little
smaller than either of those at the opposite end of the tooth.

The various species of Otters exhibit considerable differences in
the form of their teeth; some, such as the Indian clawless Otter
(Lutra cinerea), having broad and low-crowned teeth, of a type
somewhat similar to the fossil now under examination; while others
have narrower teeth, with the anterior cusps higher, and sometimes,
as in the L. hessica lately described by Mr. R. Lydekker*, the three
anterior cusps are equally developed.

Mr. Lydekker has kindly examined the Norwich-Crag specimen,
and is of opinion that it belonged to a Lutrine species of a very
brachyodont type, probably nearly allied to the Lutra sivalensis 7,
which also has broad-crowned teeth. Unfortunately, however, the
only known example of a lower jaw of this Sivalik species has a
very imperfect carnassial.

It would seem, therefore, that this Norwich-Crag tooth is a right
lower carnassial of an extremely low-crowned type, with strong
Lutrine affinities ; and, accepting Mr. Lydekker’s opinion, it is pro-
visionally placed in the genus Lutra. 1 propose to name the species
L. Reever, as an acknowledgment of the services rendered to science
by the worthy Curator of the Norwich Museum.

3. PHoca Moor, sp. nov. (Pl. XVIII. figs? 3a, 36.) »

Mr. EK. C. Moor has a small left humerus of a Seal (fig. 3), wanting
the lower articulation, from the nodule-bed of the Red Crag near
Woodbridge. It agrees in form most nearly with the corresponding
bone of Phoca vitulinoides, described by Prof. Van Beneden¢; but
differs in being much smaller and of more slender proportions, the
shaft just below the deltoid crest being especially small. Since
there is no reasonable doubt that this humerus represents a new
specific form, I propose to associate it with a name which has for

* Proce. Zool. Soc. 1890, p. 3.
tT Pal. Indica, ser. 10, vol. xi. p. 195, pl. xxvii., and pl. xlv. fig. 8 (1884).
{ Ann. Mus, Roy. Belg. vol. i. pt. 1, p. 72, pl. 15 (1887).

i

ad

THE RED AND NORWICH CRAGS. 447

many years been connected with the preservation of Crag fossils,
and to call it Phoca Moort.

4, PHocANELLA Minor, Van Beneden. (Pl. XVIII. figs. 4 a, 4 6.)

Prof. Van Beneden has given the above name to certain speci-
mens from the Belgian Pliocene*, and Mr. E. C. Moor has a
humerus from the nodule-bed of the Red Crag, near Woodbridge
(fig. 4), which agrees so closely with the corresponding bone of
P. minor that I have no doubt as to its belonging to the same
species. The upper portion of Mr. Moor’s specimen is wanting,
and it is much rolled; but the general form and remarkable
triangular section of the shaft agree precisely with the cast of this
species preserved in the British Museum; but the peculiarities of
this humerus are not so well seen in the figures given by Prof. Van

. Beneden 7.

5. TROGONTHERIUM MINUS, sp. nov. (PI. XVIII. figs. 5a, 56, 64,
6 6.)

Another interesting specimen in the possession of Mr. E. C. Moor
is a right maxilla (fig. 5) of a beaver-like Rodent, also from the
nodule-bed of the Red Crag, near Woodbridge. Three teeth are
preserved in this fossil, the enamel-folds of which so closely resemble
those of Trogontherium Cuvieri that I have no doubt as to its
belonging to this genus; but the teeth are much smaller than in
any known specimen of 7. Cuvieri, and I do not feel justified in
placing it in the same species, more especially as it comes from a
lower horizon than any at which 7. Cuvieri has yet been found.

The three teeth preserved are premolar 4 and molars 1 and 2.
The grinding-surface of each of these is more or less triangular, one
angle being directed backwards and outwards, while the rounded
base is turned forwards. The front surface of premolar 4 is
exposed, and is 18 mm. long, 8 mmm. wide, and the grinding-surface
is 8 mm. from back to front. Molar 1 is 16 mm. long, 6 mm.
wide, and the grinding-surface 6 mm. from front to back. The
length of molar 2 cannot be seen; it is 5 mm. wide and 6 mm.
from front to back. Hach tooth has had three enamel-folds on
the outer side and one on the inner, as in Castor and T'rogontherium ;
but they resemble those of the latter genus in being connected with
the exterior of the tooth for only a short distance downwards from
the summit; indeed, in each of these teeth the three outer folds
have already become isolated, and the single inner fold is nearly in
the same condition.

This specimen can hardly be a young example of 7’. Cuvieri, the
teeth of which increase in size towards their bases, for the alveolar
portion of the largest one (pm. 4) is closing in at the base to form
fangs, and its greatest width is much less than in 7’. Cuvieri.

I propose to name this species T'rogontherium minus, and in it to

* Ann. Mus. Roy. Belg. vol. i. pt. 1, p. 71 (1877).
t Loc. cit, pl. xiv.

448 MR. E. T. NEWION ON NEW MAMMALS FROM

provisionally include the incisor tooth from the Norwich Crag of
Sizewell Gap, near Southwold (fig. 6), alluded to by Sir R. Owen
as ‘“‘ Beaver” *. ‘This incisor, preserved in the Society’s Museum, |
has the front rounded and its enamel rugose, thus agreeing with
Trogonthertum and not with Castor.

6. Mxrsoritopon Fioris, sp. nov. (Pl. XVIII. figs. 7a-7c, and A,
B,C.) (=Mesoplodon Floweri, Canham, MS.)

The Rev. H. Canham, whose collection of Red-Crag fossils is now
preserved in the Ipswich Museum, gave the name of Mesoplodon
Flowert to a new form of Ziphioid rostrum which he had obtained
from the Red Crag of Trimley, Suffolk. A cast of the specimen is
in the Museum of the Royal College of Surgeons, and the name
given by Mr. Canham is there retained for it (Flower, Cat. Vert.
Mus. R. Coll. Surg., part ii. p. 562, no. 2915, 1884). This species
is also noticed by Mr. Lydekker (Quart. Journ. Geol. Soc. vol. xlii.
p- 15, 1887), but no description has hitherto been published.
Unfortunately the specific name Floweri has already been used by
Julius von Haast f for a recent species of Mesoplodon; but as the
form thus designated has been shown by Prof. Flower to belong to
a species previously described, it seemed to me very desirable to
keep the name 1. Flower: for this fossil Ziphioid. Since, however,
the present paper was read, the Referee has pointed out that it will
be far better at once to establish a new specific term; and, as by
the use of Latin instead of English, the same honoured name may
be kept in association with this Cetacean fossil, I propose to call
the species Mesoplodon floris [July 1, 1890].

By the kindness of Dr. Taylor of Ipswich, I have had the oppor-
tunity of examining the original specimen (fig. 7), and propose now
to give some details of its structure. In general appearance this
rostrum is slender and regularly tapering, something like MW. tenui-
rostris or M. medilineatus, but exhibiting important differences,
its most striking peculiarity being the flattening of the anterior
part of the upper surface, which gives to the transverse section of
this region a quadrate appearance. The length of this specimen is
about 420 mm. (164 inches). The ossified mesethmoid (fig. 7 a)
occupies about 285 mm. of the upper surface, and is about 23 mm.
wide towards its hinder part; but it becomes narrower towards
its front, the anterior third tapering away more rapidly, to end in
an acute point. In front of this is a deep median groove which
extends to the end of the rostrum. The mesethmoid narrows
somewhat posteriorly, and its outer surface seems to consist of
denser bone than the interior, probably because it is an ossification
of the epichondrium, while the more cancellous interior is an ossi-
fication of the mesethmoid cartilage itself. And further, the
ossification of the perichondrium is not complete towards the hinder
part of the upper surface; but a median groove is left similar to

* Brit. Foss. Mamm. p. 192 (1846).
+ Proc. Zool. Soc. 1876, p. 478.

THE RED AND NORWICH CRAGS. 449

that seen in MW. medilincatus. Indications of this mode of ossifica-
tion are also seen in examples of other species of this genus.

On each side of the mesethmoid there is a distinct channel,
running along the upper surface of the rostrum, for about 190 mm. ;
it then gives off a much smaller channel, which, passing inwards,
follows the tapering point of the mesethmoid, to end with its
fellow of the opposite side in the median groove already noticed.
Passing forward from the origin of the smaller channel, the outer
wall of the larger channel becomes strenger, forming a distinct
angle, which continues to the front of the rostrum, and gives it the
characteristic flattened aspect, while the channel itself gradually
dies out. Towards the hinder part of the specimen the maxillary
region on each side is produced into an obtuse lateral angle (fig. A),
which gradually subsides as it passes forwards and downwards
(fig. B). At about 150 mm. from the front a channel takes the
place of the ridge (fig. 7 ¢), and passes quite to the lower surface of
the specimen. A little above and in front of this point, a much
larger channel is seen issuing from under the bone and extending
to the front of the rostrum; and below it there is a roughened
area from which the anterior extension of the maxillary has been
broken away. In the present condition of the specimen the front
of the rostrum is formed solely by the two premaxille, which,
although in contact with each other, are distinctly separated by a
fissure clearly seen on the upper and under surfaces; moreover, the
line of division is clearly shown on the surfaces where the snout
has been broken across (figs. B, C). The boundary separating the
maxilla from the premaxilla is seen on the upper surface towards
the hinder end (fig. 7 a) as well as in front (fig. 7¢); but in the
intermediate region no such boundary can be traced.

The openings of the premaxillary canals are on the upper surface
(fig. 7a) near the posterior extremity of those bones; and in a
hinder view of the specimen the apertures of two other large
canals may be seen on each side.

Near the middle of the rounded lower surface (fig. 7) there is a
lenticular area, which is probably an exposure of the vomer, and on
each side of it is the opening of a canal; while towards its front
part may be seen the sutures separating the maxille from the
premaxille.

The end of a rostrum figured by Van Beneden and Gervais* as
Ziphiopsis servatus, Du Bus, bears some resemblance to Mr. Can-
ham’s specimen in the flattening of its upper surface; but the
narrowing of the hinder part of this region is an indication of
important structural differences. Moreover, Ziphiopsis or Chonezi-
phius, with which it is now included, has the mesethmoid more or
less unossified, and not appearing on the upper surface of the
rostrum.

None of the specimens of Mesoplodon, either recent or fossil, so
far as I can ascertain, present the same peculiar conformation of

* Ostéogr. Cétacés, pl. xxxvii. bis, fig. 8.

450 MR. E. Tf. NEWTON ON NEW MAMMALS FROM

the front of the rostrum as that which is seen in Mr. Canham’s
example, and he is no doubt right in regarding it as a new
species.

7. MusorLopon scaPHoIpDEs, sp. nov. (Pl. XVIII. figs. 8 a, 8 6.)

The Ziphioid rostrum from the nodule-bed of the Red Crag, near
Woodbridge, now to be described is preserved in the Museum of
Practical Geology, and is one of the most aberrant forms yet
known from this deposit. The rostra hitherto described from the
Red Crag are more or less elongated forms, some being very long
and attenuated; the present specimen, however, is remarkable for
being extremely short and proportionately deep. When seen from
above (fig. Sa), it has the form of a triangle, the hinder part
forming an irregular base, about three inches Bache ; and the sides
passing almost straight to the front to meet in a sharp edge.

The greatest length of this specimen is about five and a quarter.
inches. In a side view (fig. 86, 3 nat. size) the hinder part is
seen to be about one inch and three quarters deep ; but it increases
anteriorly to about two and a quarter inches; the front margin
curving upwards like the prow of a boat. The mesethmoid is
completely ossified, and in a back view its outline is clearly defined :
its hinder end having a deep fossa which may have lodged the front
of the internasal septum ; its lower margin is received into a trough
of what is doubtless the vomer. Anteriorly the vomer itself seems
to be covered in by downward processes of the maxillz ; but all the
bones of the front part of this rostrum are so completely codssified
that the divisions between them are entirely obliterated. At the
hinder part of the upper surface there are some indications of a
division between the mesethmoid and the premaxille ; also on the
right side there is a line which may indicate the junction of the
hinder part of the maxilla and premaxilla.

On the upper surface posteriorly are the apertures of two
large, covered canals, which evidently correspond with those
in Professor Huxley’s figures of Belemnoziphius compressus *,
marked with the letters a,a. On the right side the covering is
broken away, but it is retained on the left. These canals, passing
downwards and forwards, soon become open channels, running
along the sides of the premaxillary region, and turning a little
upwards they become wide and shallow at the front of the rostrum.
If one of these premaxillary canals, as they may be called, is
followed backwards under the bony covering, it will be found to
bifurcate ; one of the branches passing upwards and backwards is
the canal already noticed, which issues at the aperture, and
may be further traced as a shallow depression passing backwards
over the premaxilla; the second branch is directed downwards
and backwards, and after a short course opens, fig. 86, into
a large cavity, partly preserved on the right side (seen in
fig. 8b), but better defined on the left. From each of these

* Quart. Journ. Geol. Soc. vol. xx. pl. 19.

THE RED AND NORWICH CRAGS.. 451

cavities, which seem to be situated in the maxillary bones,
issue several canals. The most clearly defined of these is the
one alluded to above. as the premaxillary canal; a second (as
seen in fig. 8b), passing almost directly forward on the outermost
edge of what seems to be the maxilla, may be termed the
maxillary canal, and is best seen on the left side; from the
lower part of the cavity a third channel may be seen passing |
forwards; and, then curving upwards, it extends as a shallow
groove to the end of the rostrum; this may be termed the sub-
maxillary canal; and from about the middle of this latter canal a
subsidiary groove may be seen branching off below it. These three
canals, seen on the sides of the specimen, evidently correspond with
those described by Prof. Huxley in Belemnoziphius compressus, and
seem to: be present, more or less covered in by bone, in all the
rostra referable to Mesoplodon.

From the cavity on the right side of the specimen another large
canal passes upwards and backwards; but on the left side a much
smaller canal seems to occupy a similar position in the maxilla.

Each of the large cavities in all probability lodged a ganglion of
the fifth nerve, the branches of which passed out through the
various apertures and canals.

When first examining this specimen | thought it might be a much
denuded portion of the more elongated rostrum of another species;
but a closer attention has convinced me that, although much abraded
(as indeed are almost all the fossils from the same deposit), itis as
much to be relied upon for its main features as are most of the forms
hitherto described.

The complete ossification of the mesethmoid being one of the

chief characters of Mesoplodon, this specimen must de placed in
that genus; and the short rostrum, with its sharp boat-like anterior
extremity, i is so entirely different from any form yet described that
it becomes necessary to give it a specific designation by which it may
in future be known, and it is proposed to name it Mesoplodon
scaphordes.

8. Ainurus aneticus, Dawkins. (Pl. XVIII. figs. 9a, 96.)

Prof. Boyd Dawkins described before this Society in 1888* a
portion of a lower jaw with the carnassial tooth in place, from the Red
Crag of Suffolk, which he referred to the genus Adlurus, and named
A, angtious. In the discussion which followed the reading of the
paper, Dr. Blanford called attention to the restricted distribution of
this genus, and to its affinities with the American Racoons; he
thought Prof. Dawkins’s reference was possibly correct, but that one
tooth was scarcely sufficient to go upon, and on the whoie the
determination would require confirmation. Iam happy to say we
have now some additional evidence.

Mr. Percy H. Browne, of Reigate, has recently presented to the
Museum of Practical Geology a perfect upper molar tooth, from the

* Quart. Journ. vol, xliv. p. 228,

452 MR. E. T. NEWTON ON NEW MAMMALS FROM

lower part of the Red Crag (nodule-bed), near Boyton. This
tooth being unlike anything hitherto known from the Crag, was
awaiting determination, when Mr. Lydekker saw it and, recognizing -
its resemblance to the tooth of Ailuwrus fulgens, kindly lent me a
skull of this recent species for close comparison; it is to Mr.
Lydekker, therefore, that we are indebted for the first identification
of this tooth. On comparing the specimen with the left, upper,
first true molar of Adlurus fulgens (see Pl. XVIII. figs. 10 a, 10 5),
the resemblance between them in the form and position of all the
cusps and tubercles is most striking. On the outer side are two
cusps (4, B, the front one being the larger of the two), which have a
strong ridge running down their anterior and posterior surfaces; a
third cusp, c, placed within and near to the hinder one, is flattened
on the outer aspect and rounded on the inner, while ridges pass from
its summit downwards and outwards towards the outer cusp. The
inner portion of the crown is occupied by a cusp, D, larger than either
of the others, from which a ridge extends forwards and outwards to
join a large tubercle, 1, situated upon the front of the tooth. This
tubercle, in common with all those now to be mentioned, forms part
of a strong cingulum, which may be traced round the crown. On
the outer side of the tooth are three large tubercles, one (2) before,
one (4) behind, and one (3) between the two cusps; and at the back
of the tooth, between the outer and inner cusps, is another smaller
tubercle (5). The inner part of the tooth is rounded, with the cin-
gulum particularly well marked, and towards its hinder part deve-
loped into one or two small tubercles (6). In all these particulars the
fossil and recent teeth are precisely similar; with only such trifling
differences as might be due to individual variation, the greatest
being the absence, in the recent tooth, of the small tubercle marked 5
in the fossil.

It will be remembered that the lower tooth of Azlurus anglicus
was described as about one third larger than that of A. fulgens (7. e.
70 mm. and 48 mm.): and the upper tooth, now described, has the
same proportion to the first upper molar of that species; its length
from before backwards, however, is greater in proportion to its
width, as will be seen by the following measurements :—

A, fulgens. A. anglicus.
Upper m. 1, length from before .
DAG ew aR OS oii ora cee kaa 95 14°5 millim.
Upper om,, di, wadtine. 2a cies 11:5 14°5 millim.

The height of the crown and cusps in the fossil is proportionately
less than in the recent form, and in this particular corresponds with
thelower tooth described by Prof. Boyd Dawkins. Another peculiarity
of the upper tooth is that the bases of all the cusps are strongly
erooved or striated, a character which is only seen to a very slight
extent in A. fulgens.

This tooth is of itself sufficient to establish the presence in the

Red Crag of a species closely allied to Aclurus fulgens; and, as it

> a

THE RED AND NORWICH CRAGS. 453

agrees in size with Ailuius anglicus, we can scarcely do otherwise
than associate it with the latter species.

A portion of a lower jaw, which, like the type, is in the Reed
Collection, York Museum, and from the Red Crag near Woodbridge,
is also referred to A. anglicus. The high position of the articular
condyle, the deeply curved lower margin, and the high and large
coronoid process agree with A. fulgens ; while the flattened alveolus
for the hinder tang of the last molar is like what is seen in the
type specimen of A. “onglious.

EXPLANATION OF PLATE XVIIL

Fig. la. Lutra dubia, Blainv. Right ramus of lower jaw: natural size.
From the nodule-bed of the Red Crag near Woodbridge. In the
collection of Mr. KE. C. Moor, of Bealings.

16. Same, seen from above.

le. Carnassial tooth, seen from above, and enlarged.

2a. Lutra Reevei, sp. nov. Right lower, carnassial tooth, seen from
above: natural size. Fyom the Norwich Crag of Bramerton. In
the collection of Mr. James Reeve, of Norwich.

26. Same, seen from outer side.

20: Same, seen from before.

3a. Phoca Mocri, sp. nov. Left humerus, front view: natural size.
From the saine horizon and collection as fig. 1.

36. Same, side view.

4a. Phocanella minor, Van Beneden. Left humerus, front view: natural
size. Same collection and horizon as fie, A

46. Same, side view.

5a. Trogontherium minus, sp.nov. Right maxilla, outer surface: natural
size. Same horizon and collection as fig. 1.

5b. Same, grinding-surface of teeth.

6a. Trogontherium minus, sp. nov. Lower incisor: natural size. From
the Norwich Crag, Sizewell Gap, near Scuthwold; in the Museum
of the Geological Society. Provisionally referred to this species.

6 6. Same, transverse section.

7a. Mesoplodon floris, sp. nov. Rostrum, seen from above: one third of
the natural size. From the Red Crag of Trimley, Canham Collection,
Ipswich Museum.

76. Same, seen from below.

7c. Same, right side view.

A, B,C. Transverse sections at points indicated in fig. 7 a.

8a. Mesoplodon scaphoides, sp. nov. Rostrum, seen from above: one
third of the natural size. From the nodule-bed of the Red Crag
near Woodbridge. In the Museum of Practical Geology.

86. Same, right side view.

Qa. Ailurus a anglicus, Dawkins. Left upper, first true molar: natural size,
From the nodule-bed of the Red Orag near Boyton. Presented to
the Museum of Practical Geology by Mr. P. H. Browne.

9. Same, outer view.

10a. Ailurus fulgens, F. Cuv. (Recent.) Left upper, first true molar:
natural size. From specimen in possession of Mr. R. Lydekker.
For comparison with A. anglicus.

100. Same, outer view.

Q.J.G.S. No. 183. 2K

454 MK, G. R. VINE ON THE POLYZOA OF

28. A Monoerarnu of the Potyzoa (Bryozoa) of the Rep Cuarx of
Hunstanton. By Groreu Roserr Vinn, Ksq. (Read March
26, 1890.) ;
(Communicated by Prof. P. M. Duncan, F.R.S. &c.)
[Puate XIX. ]

ConrTENTs.
I. Introduction.
II. Bibliographic Notices: 1. Palseontological.
1*. Faunal References.
2. Stratification, Horizons, &e.
IIT. Known Ranges of Polyzoa in the Red Chalk.
IV. Description of Species.
§ I. Cyclostomata, Bush.
A. Parallelata, Waters.
Genus Stomatopora, Bronn.
Proboscina, Audouin.
Diastopora, Lamouroux.
Unitubigera, d@’ Ord.
Entalophora ?, Lamz.
Heteropora, Blainv.
B. Rectangulata, Waters.
Genus Ceriopora, Goldfuss.
Reptomulticava, d’ Ord.
Zonopora, d' Orb.
Multicrescis, @’ Orb.
Unicavea, @ Orb.
§ II. Cheilostomata, Bush.
Genus Membranipora, Blainville.
Hippothoa, d’ Orb.
Explanation of Plate XIX.

I. [yrropucrion.

Iris not my intention in this monograph to discuss any of the
stratigraphical questions raised by authors who have written about
the Red Chalk of Hunstanton. JI have to deal with one group of
fossils only; but, before entering on my investigations, it was
necessary to make myself familiar with the views of others, and
more especially with the paleontological evidence afforded by thestudy
of the fossils from the various zones of the Chalk. One source of
information has been, however, more helpful to me than all the
others. When compiling material for my British-Association
Reports on Fossil Polyzoa*, I was allowed to examine all the type
series in the Museum of Practical Geology, from the Cambrian to
the Upper Chalk; and recently (September 1889) I have re-examined,
for the purpose of this and another paper on the Polyzoa of the
Upper and the Lower Greensands (Bibliographic List, 21; see
page 458), all the Cretaceous forms mentioned in the Catalogue of
that Museum (Bibliogr. 12). Besides the examination of these forms
Mr. Alfred Bell has placed in my hand for study and description a
fine series of Polyzoa preserved on flints, as well as free examples,

* Brit. Assoc. Reports, 1880-1885.

.
a
i)

a

* Hay)

Dasr, .if
a

“iy fe fs
. ‘

ee i ian a‘ eres «6
eee ia ok oth i ei

ie

Quart Journ Geol Soc Vol. XLVI P] XIX. |

4

~\

a

ox

GeoWeat & Sons del lith et imp.

POLYZOA OF THE RED CHALK.

——E————

THE RED CHALK OF HUNSTANUON. 455

from the Upper Chalk at Chatham. Thanks to the kindness shown
towards me by Prof. Judd, F.R.S.,and Dr. Pergens, of Belgium, I have
been enabled to study the Polyzou of the Faxoe Limestone and
Maastricht Beds, by the gift of beautiful examples derived from
these typical horizons of Cretaceous Polyzoa.

In the ‘ Catalogue of the Cretaceous Fossils in the Museum of
Practical Geology,’ 1878, we have lists of a fair assortment of
British examples from several horizons, but there are many unavoid-
able blanks. Out of nine Cretaceous divisions given in the Catalogue,
in four important sections there is no mention of a Polyzoan fauna.
In the Neocomian (Lower Greensand) division (pp. 6, 7) much of the
material is still unworked; but at least twenty-one forms are named
specifically. These belong to the following genera: Stomatapora,
Bronn ; Proboscina, <Audouin; Diastopora and Entalophora,
Lamouroux, together with species of Ceriopora, Heteropora, and
Radiopora. The locality from which most of these Polyzoa were
derived was Faringdon, but other localities are mentioned. In the
Gault (pp. 26 et seg.) there is no record of Polyzoa; but in the
Blackdown series (p. 39) there are four entries under the head-line
“ Polyzoa.” In the Upper Greensand (Cenomanian, pp. 49-50)
there are fifteen species named, besides references to others, most of
which are from Warminster. In the Cambridge Greensand,
Chloritic Marl, and Red Chalk there is likewise no mention of
Polyzoa. In the Lower Chalk (p. 83) two references are given; and
in the Upper-Chalk division of the Catalogue (p. 95) twelve species
are named in full.

It is hard to account for this poverty of a polyzoan fauna in many of
our own Cretaceous beds otherwise than by supposing that probably it
arises from other causes than mere absence, and one of the chief may
be that of British workers on the group being so few. In foreign
localities the Cretaceous beds have been well worked, the upper
divisions especially, and the number of species described by Goldfuss,
von Hagenow, d’Orbigny, von Reuss, and others, though considerable,
are still being added to by persistent and careful research, whilst
our own strata are at present characterized as poor in Polyzoa.

Independently of the species catalogued as existing in the Museum
of Practical Geology, or referred to by Morris. in his ‘ Catalogue of
British Fossils,’ lists of Polyzoa from certain British Cretaceous
horizons below the Upper Chalk are extremely rare, and I am not
aware that any exist except those mentioned below. Mr. Ethe-

ridge, F.R.S., gives * the following summary of known Cretaceous

Polyzoa :—
Upper Chalk.... 38 genera, 50 species.

ovnrnonaic fh. 6 4 Bie les
Cligtemarl...:. 1 genus, 1 ,,
Cenomanian.... 15 genera, 24 __,,
Con oa 3 ss

‘Neocomian .... 21 sen eae

* Philips, ‘Manual of Geology and Palwxontology,’ vol. ii, 1885, p. 581.
2x2

456 MR. G. R. VINE ON THE POLYZOA OF

The four Gault forms are distributed thus :—

Genus Berenicea.... two species.
53, . (Cersocgig y.. |b. ONet, ae
55 ABCC Ore... OMB) a,

With a catalogue like this it is impossible to give satisfactory
ranges of species in British Cretaceous rocks.

The Rey. T. Wiltshire, in his paper on the Red Chalk of England
(Bibliography, 3), names only one species, Diastopora ramosa, as
found by him in the Hunstanton Chalk, and two other forms, /dimonea
dilatata, VOrb., and Ceriopora spongites, Goldf., from Speeton.
Neither Prof. Seeley (Bibliograph. 14 and 15) nor Prof, Judd (Biblio-
graph. 16), in any of their papers on the Hunstanton rocks, mention
Polyzoa in their lists of fossils; and the same remark will apply to
the two more recent papers on the lower beds of the Upper Chalk,
by Messrs A. J. Jukes-Browne and William Hill (Bibliograph. 38
and 39). My own papers on Lichenopora ? paucipora (Bibliograph.
18) and Notes on the Polyzoa of the Cambridge Greensand (Biblio-
graph. 19) called the attention of palzontologists to the probable
existence of many undescribed forms in the cabinets of collectors.
Some additions I was enabled to make through the kindness of
T. Jesson, Esq., F.G.S., who overhauled his cabinet of Gault and
Cambridge-Greensand fossils for that purpose; and the forms now
to be described and illustrated I owe to the same careful collector.
Already Mr. Jesson has placed in my hands over 1000 fossils, from the
Red Chalk of Hunstanton, on most of which encrusting forms of
Polyzoa are found; whilst others from the Gault and Chalk-mar] still
await special attention. The groups of fossils submitted to me for
examination belong to the following :—

Nautilus and Ostrea species ;

Ammonities, several species ;

Echinodermata and Belemnites ;

Inoceramus, J. concentricus and I. Crispii ;

Terebratula, 7’. biplicata, Sby., and 7’. capillata, d’Arch.

On the Inocerami and Ammonites, the best Diastopore and
Proboscine are found ; but the most abundant of all the individuals
examined are the Stomatopore, on Terebratula biplicata chiefly.
Species of Entalophora, Idmonea, and Ceriopora are very rare,
while Lichenoporide are either rare or badly preserved. Cheilosto-
matous forms, individuals or species, are also very rare.

In the present monograph, on account of the peculiarities of the
Cretaceous fauna, I have been obliged to limit or redefine the generic
terms employed. Since the publication of Mr. Busk’s British-
Museum Catalogues (1854), the Polyzoa, both recent and fossil, have
been studied much more systematically than previously, and the
names of Reuss, Manzoni, Novak, Marsson, Pergens, Waters, Wal-
ford, and many others are especially suggestive of arrangements in
grouping, more or less advantageous in a paleontological sense.
Since the publication of the Rey. T. Hincks’s ‘ British Marine

THE RED CHALK OF HUNSTANTON. 457

Polyzoa’ his family-arrangement of the Cyclostomata has been
accepted. either intact or modified in the smaller divisions, by
competent authorities working on fossil groups more especially.
Thus, Dr. Pergens, while working along the lines of Hincks,
generally adds to or modifies the family-arrangement according
to circumstances; so also Mr. Waters, working along the same
lines, suggestively leaving out the family § grouping, arranges genera
only, and formulates two convenient sections, in ener of calito
fossil and recent Cyclostomata can be appropriately placed. The
family-arrangement of the Cyclostomata, as adopted by Dr. Mars-
son *, is both novel and peculiar, but ‘cannot be dealt with so
fully as I could wish in the present memoir. The author established
two divisional types to include the Riigen species of Cretaceous
Polyzoa :—I. The Sotenoportna, Marsson, embracing six well-
known Family-groups; and Il. The Meroportna, Marsson, in
which he places, in the Family Crrpra, the genus Filicea, d’Orb.,
and in the Family Exerpra the heretofore much misunderstood
genera, Melicertites, Romer, and Nodelea, d’Orb.

I am aware of the nomenclatural difficulties which Mr. E. A.
Walford had to encounter in his Liassic paper (Bibliograph. 29), and
also in his more recent memoir on the “ Inferior-Oolite Bryozoa™
(Bibliograph. 30). It is not only difficult, but almost impossible to
arrange fossil Polyzoa occurring in and below the Chalk under the
modern family-grouping. The Tubuliporide of Hincks include Sto-
matopora, Tubulipora, Idmonea, Entalophora, and Diastopora. In
one sense certainly this grouping is convenient, but the difficulty
referred to above is in making Stomatopora a multiserial as well as
a uniserial group. By accepting the genus Proboscina, I find that 1
can arrange the biserial Stomatopore of the Red Chalk, and keep in
accord with the Liassic and Jurassic features of typical forms :
whereas by accepting recent biserial Stomatopore as typical ex-
pressions we altogether ignore facial differences that ought to be
recognized, palontologically at least. Undoubtedly in Mesozoic
rocks generally uniserial Stomatoporw gradually glide into Pro-
boscine, as Proboscina in some few cases fades into Diastopora. To
formulate mere arbitrary divisions, therefore, in the present state of
our knoweledge is useless; yet the study of fossil Polyzoa will be
greatly facilitated if, understanding these peculiarities, the student
accepts certain generic terms as expressions of growth rather
than as fixities. The uniserial Stomatoporw of the Red Chalk
are, however, a distinct group of fossils, and they very rarely, if
ever, pass into biserial forms. The Proboscinw, as a matter of course,
begin their existence as uniserial Stomatopore; but very early in
their development they pass into bi- and multi-serial varieties. The
Diastopora of the Red Chalk also have the occasional Proboscinal
features ; but the disc-like character of the genus is very constant
in all those forms which I place in that division. TI have studied
these varied and varying changes in all the forms indicated, on

* Die Bryozoen der weissen Schreibekreide der Insel Riigen, 1887, p. 8.

458

MR. G. R. VINE ON THE POLYZOA OF

account of the multiplicity of the material placed in my hands ; but
it would be impossible for students to formulate for themselves -
other than the arbitrary divisions given by Busk and Hincks.

13865.
1883.
1884.

1885.

Il. Bisirocraputc Nortczs.

1. Paleontological.

1. Goxpruss, Petrefacta Germaniz.

2. Von Hacenow, Monographie der Rugen’schen Kreide-

IQ KH oo

verst. .
Ramer, Verstein. norddeutschen Kreidegeb.

Von Reuss, Verstein. bohm. Kreideform.

. Von Reuss, Polyp. Wiener Tertiairbeckens.
. Von Hacenow, Bryozoen Maastrichter Kreidebildung.
. D’Orsiexy, Paléont. francaise; Terrains Crétacés,

Vol. v. Bryozoaires.

. BursseL, Bryozoen Aachener Kreide.
. Srmonowirscu, Beitrige zur Kenntniss der Bryozoen

des Essen Griinsands. Verhandl. naturf. Ver. Bonn,
Jahrg. 28, 3 Folge, vol. vill.

. Von Reuss, Bryozoen des Unteren Planers, in Geinitz’s

Elbthalgeb. in Sachsen, vol 1.

. Von Reuss, -Bryozoen des Sichsischen Pliners. /bid.

vol. il.

1*, More particularly for Leferences to Faune.

12.
13.
14.
15.
16.
te
18.
oe

20.
21.

Huxtery, Newton, and Ermerine®, Catalogue of Cretac.
Fossils in the Museum of Practical Geology.

Wittsuire, Rey. T., Red Chalk of England. Geologist,
vol. iil. pp. 261-278.

Sretry, H. G., Hunstanton Limestone. Ann. & Mag.
Nat. Hist. (3) vol. viii. (Lists.)

Sretey, H. G., Hunstanton Limestone. Quart. Journ.
Geol. Soc. vol. xx. (Lists.)

Jupp, J. W., Strata of the Lincolnshire Wolds. bid.
vol. xxii, (Lists.)
Vint, G. R., and H. C. Sorsy, Report on Foss. Polyzoa.

Brit. Assoc. Report, 1884.

Vine, G. R., On some Cretaceous Lichenoporide. Quart.
Journ. Geol. Soc. vol. xl. pp. 850-854.

Ving, G. R., Polyzoa of the Cambridge Greensand.
(Abstract, Proc. Geol. Soc. No. 407; Quart. Journ.
Geol. Soc. vol. xli. p. ror.) Proe. Yorksh. Geol. Soe.
vol. ix. pp. 1-16.

Ving, G. R., Notes on Classification. Proc. Yorksh.
Geol. Soc. vol. ix. pp. 346-362.

Ving, G. R., Further Notes on the Cambridge-Green-
sand Polyzoa. Ibid. vol. xi. p. 250.

THE RED CHALK OF HUNSTANTON. 459

1886. 22. Prrcens, E., and A. Meunier, Bryoz. Environs de Faxoe,
| Ann. Soc. Roy. Malacol. Belg. vol. xx.

1884. 23. Warmers, A. W., Tert. Chilostom. Bryoz. Australia.
Quart. Journ. Geol. Soc. vol. xl. p. 674. :

1887. 24. Warers, A. W., Tert. Cyclostom. Bryoz. New Zealand.
Ibid. vol. xlii. p. 40 & p. 337.

1887. 25. Waters, A. W., Cyclostom. Bryozoa. Ann. & Mag.
Nat. Hist. (5) vol. xx.

1888. 26, Warsrs, A. W., Ovicells of Cyclost. Bryoz. Linn. Soc.
Journ. vol. xx. p. 275.

1888. 27. Waters, A. W., Ovicells of Laichenoporide. Jbid.
vol, xx, p. 280.

1888. 28. Marsson, Tu., Bryoz. weiss. Schreibkreide Ins. Riigen.
Paliont. Abhandl. 1888. Do turus, G., Review of
Marsson’s ‘ Rigen. Bryoz.,’ Annuaire Géol. Universel,
1888, p. 822.

1887. 29. Watrorp, E. A., Polyzoa from the Lias. Quart. Journ.
Geol. Soc. vol. xl. p. 632.

1889. 30. Watrorp, HK. A., Bryozoa of the Inf. Oolite. Jézd.
vol. xlv. p. 561.

1875. 31. Busx, G., Cyclostomata, Part ui. Brit. Mus. Cat.

1886. 32. Busk, G., Cyclostomata. ‘Challenger’ Report, Polyzoa,
Part 11.

1880. 338. Hinexs, J., History of the British Marine Polyzoa,
2 vols.

1877. 34. Novax, O., Bryoz. der bohmischen Kreideformation.

1850. 35. Lonspate in Dixon’s ‘Geol. of Sussex.’

1885. 36. Eraprimen, R.,-in Phillips’s ‘Manual Geol.’ vol. ii.
Hd. by R. Etheridge. “Cretaceous,” part vii.
pp. 512-597.

1854. 37. Morris, J., Catalogue British Fossils.

2. Stratification, Horizons, Sc.

1887. .38. Juxres-Brownn, A. J., and Hitz, W., Lower Part of the
Upper Cret. Series in W. Suffolk and Norfolk. Quart.
Journ. Geol. Soc. vol. xii. p. 544.

1888. 39. Hitz, W., Lower Beds of the Upper Cret. Series in
Lincolnshire and Yorkshire. bd. vol. xliv. p. 320.

1878. 40. Mavre-Corz, E., On the Red Chalk. Journ. Yorksh.
Geol. Soc. vol. vii.

1874. 41. Braxsz, J. F., Note on Red Chalk in Yorkshire. Geol.
Mag. dec. 11. vol. i. pp. 362-364.

1877. 42. Garpner, J.8., Letter on the Gault &c. bid. vol. iv.
p. 377. ,

Other works have been consulted for special details, but the above
(chiefly the Palsontological) have been constantly referred to for
description of species and the ranges of particular fossils.

460

MR. G. R. VINE ON THE POLYZOA OF

IU. Kyown Raness oF Potyzoa In tar Rep Cuark.

“i
So | &S i
mS sic & os oS
Paes ta | oe] 2
Se ee eee
Edis ols t/Sala lis] a
S| os | Sa a ees
SO |jOd|joebola |ala
Order POLYZOA, Bush.
§ I. Suborder Cycnostomata, Bush.
Genus Sromatopora, Bron.
ig eracilig, MAWUndSe: 5..cc8 meencs rere basen ASHS| [poe
Devdivavieniba, WUeewmer :) is.08.. ih eeeee tees wee *
d.yoranilaiba, LOU yt eines cas omentaecnee *
4. , var. A (S. inerassata, @’ Orb. ?) kag Tgigve *
5. ramea, Blainville ...... alain ataemeemener : *
6. longiscata, d’ Orb. ........ zo le eae oe se Wee a)
davlinenbigya Oro! tiie ceceeecneeme ees *
Genus Proposcixa (Audouin), d’ Orb.
8. angustata, d’Orb. & varr. .....2...0000- x Ay Se:
OUR OSA GP) Gk OND ea epee nena * : *
10. irregularis, sp.nov. & var. A ......... ok’ ese aese
ii stiberrinianSpanov- aah toc cs ee as *
gracilis (?), Reuss.
12, s Vanessa moiyet ech cee ace 2 3
15. subelerans,'d Orb:.c)..cc.cahabatoaessenctes *
14. hunstantonensis, sp. nov. ........-...6- % | *?
15. jvaramiplrata, mov. 12050. .250.5.. é sa |
| LG. Jessomi; Sp. NOV. see des a) dea ot ali A ae ae x
| iy. pigantopora, ane i202... epee tt etches etl ee %
bohemica (?), Novdh.
18. REVAL STOVE tre corte otiactic abe Mone : 2 *
19) Dowcasiana() diOrb. oo... -ste-a ee es Pee *
20. xammosa(?), 0 Ore ee, ts. lee ae eee see *
dilatata (?), @ Orb.
21. , var. cantabrigiensis, ine ...... * . ?
Genus DrAstopora, Lan.
22. hunstantonensis, sp. NOV. ............... wba 9 9b s Dae He
23. Vii Pass MON heuk bia teademon maa tke * ?
94. foecunda, Vane +i. fceoc.sseseetevtae ne tee x *
De), SPERUIATIS SO NORD 0 sess rectineh cen cradeuecs z *
26." radians (7); Nota, ware’ vcss-cceceus ee Pty he 3
Bf papillosa(?)) ess... c.set sean eeeet *
2G. RESON, ‘SP. MOV... 2-1-0 ase eid itea pe *
Genus Unitrupicera, d Orb.
29. ‘papyracta, d Ove, i:-S2y esis cape ien tere *
Genus Enratornora (?), Lame.
BOs BPs “wasierenchsberesveccheeae seem Ce eae : * /
/
Genus Hurnrorora (?), Blaine. |
De BD. podipny ascyasnccwaseoandes cost sense empotee - | *
. }
Genus Currorora (pars), Goldf, |
32. ‘micropora'(?), Golf.” <. <iissndewewenwss * | ve] x | *

THE RED CHALK OF HUNSTANTON. A61-

TABLE (continued).

Cambridge
Gault
Cambridge
Greensand.

Chalk
Marl
Upper
Chalk
| Red Chalk.
| lili Bec
| Top Beds.

SSS eS ee

Genus Repromuuricava, d’ Orb.
somesmmex (2) 9G OFD.. oc. .cscwesetaeeven- FS MR a ee en
CNN (COTO sc scys voocecsieeeneceecnsecs) “ae5 asowe heen Pisa Wee

Genus Zonopora, d’ Orb.
aoeirecmlarig(’), OOD, vicicacccasvescessl’ 50s peerall Oca lyiead Wet «lke
poo mactabilis( 2) O70.) cc .eccecscesccecese Son eae eee ne | eed Meee ae

Genus Mutrtcrsscis, d’ Orb.
SHemaMiA DUNS), Wi OTDS) coos..s.c.catese sees ra oP cal a En ene eed OPE lc

Genus Uncicavga, d’ Oro.
SOON POV ORD soa. caves coscrese se secusse ses Be bled orealb inde Milly Wht he- 30

*

*

§ II. Suborder CuerLtostomata, Busk.
Genus Mempranrpora, Blainville.

ESTAS. MOV. sos.c0se.cgvasceseses sas coe event ee ae (es
SONS (CG OTD. Lic caccan- see -sesnare-
AN velliptiea (2), v. Hagencw ...........605-
EEDeOMG UN GOTO! loa. sie teasers eeeeaese

Genus Hirrornoa, d Orb.
doy simapless DO OPO. 5c. eens eseeeen nny n-

* OK

TV. Descrirrion or SPECIEs.
POLYZOA, Busk.
$I. Suborder CYCLOSTOMATA, Busk.

= Bryozoatres centrifuginés (in part), d’Orbigny.

SA. PARALLELATA, Waters.

Zoaria encrusting, dendroid, or anastomosing. Zoariwmn, to a
large extent, formed of the walls of the Zowcia.

Genus Sromatorora, Bronn.

1821. Alecto, Lamouroux= Aulopora (part), Goldf.

1825. Stomatopora, Bronn.

1852. Stomatopora (for uniserial species), d’Orbigny.

The uniserial Stomatopore of the British Cretaceous rocks have
been variously identified and treated of by different authors. In
‘the earlier days of palzontological investigation only a limited
number of works, dealing with the Polyzoan group of fossils, could

462 MR. G. R. VINE ON THE POLYZOA OF

be referred to with any degree of authority. Lamouroux and Gold-
fuss, however, were soon followed by Bronn, Michelin, Blainville,
and Milne Edwards; and as these writers professedly dealt with
Cretaceous Bryozoa, among others, names established by them
eradually found their way into British scientific (paleontological)
literature. The earlier names for the Stomatoporw were Alecto,
Lamx., and Awlopora (in part), Goldf., and for a long time these had
precedence over the now generally accepted term Stomatopora,
Bronn. Amongst foreign authors antecedent to d’Orbigny the
names of vy. Reuss, Reemer, and v. Hagenow are justly remembered as
specialists who have materially advanced our knowledge of Creta-
ceous Polyzoa. The publication of d’Orbigny’s ‘ Paléontologie
Francaise,’ with an atlas of 200 plates, inaugurated a new epoch in
the history of Polyzoan groupings, and any one who undertakes to
describe British Cretaceous Polyzoa should be familiar with d’Or-
bigny’ s beautiful illustrations of the French Cretaceous species,
however independently his elaborate, but almost unmanageable,
classification may be criticized or disregarded.

| As regards British Cretaceous Sue atopore, Prot. Morris (1854),
‘ Catalogue of British Fossils,’ records two species only—Alecto
gracilis, Edw., and A. ramea, Blainville. Mr. Woodward, in his
' Geology of N orfolk,’ records A. gracilis, Kdw., from the Norwich
Chalk; and Lonsdale, in Dixon’s ‘Geology of Sussex,’ A. gracilis
and A. ramea from the Upper Chalk of Kent and Sussex. Since
the publication of these names very little has been done, specifically,
to increase the number of forms, but in the ‘ Catalogue of the Mu-
seum of Pract. Geol.’ 1878, Alecto reticulata, @Orb., is adopted as
the name of a Lower-Greensand Polyzoon. In Mr. Etheridge’s
summary, however, of the Organic Remains of the Cretaceous Strata
(Bibliography, 26, p. 589), only two species of Alecto are recorded,
both in the Upper Chalk.

In working out the uniserial Stomatopore of the Red Chalk, I
have, to a large extent, followed the leading of @Orbigny. In some
few cases I have not been able to adopt his names wholly for other
eroups ; and to prevent confusion, or misconception even, as to the
value of the Red-Chalk fauna generally, I have created a few new
names, varietal or specific, for forms which merited this distinction.

D’Orbigny describes, and illustrates by a nuwber of figures, the
following species of Stomatopora as belonging to the French Creta-
ceous series. British species are marked with *.

*1. Stomatopora granulata, Bronn, p. 836, pl. 628. f. 5-8.

*2 incrassita, d’Orb., p- 837, pl. 628. f. 9-11.
3. subgracilis, d’Orb., p. 838, pl. 629. f. 1-4.
¥4, linearis, d’Orb., p. 838, pl. 629. f. 5-8.

longiscata, VOrb., p. 839, pl. 629. f. 9-11.
plicata, VOrb., p. 839, pl. 629. f. 12-15.
‘al divaricata, Roemer, p. 840, pl. 629. f. 16-18.

ae, reticulata, @Orb., p. 841, pl. 630. f. 1-4.
9 calypso, VOrb., p. 841, pl. 630. f. 5-8.
=I ramea, Blainville, p. 842, pl. 630. f. 9-12.
m4 gracilis, Edwards, p. 843, pl. 758. f. 17-18.

THE RED CHALK OF HUNSTANTON. 463

1. Sromatopora GRaciLis (Kdwards).

1838. Alecto gracilis, Edw. Ann. Se. nat. (9) p. 207, pl. 46. f. 2.

13848. Stomatopora gracilis, Bronn, Index Paleont. p. 1202.

1850. Alecto gracilis, Lonsd. in Geol. Sussex, p. 269, pl. xvii. A,
1601

1852. Stomatopora gracilis, D’Orb. Terr. Crét. v. p. 843, pl. 758.
fe Ls.

1883. Stomatopora gracilis, Vine, Brit. Assoc. Rep. Foss. Polyz.

Zoarium delicate, wholly adherent; branches dichotomizing
irregularly, and rather variable in breadth. Zowcia uniserial, origi-
nating from a disk-like base, from which two cells are generally
thrown off, and these form the nucleus of two distinct branches ;
cells slightly lateral at their points of juncture with the parent cell,
aperture circular, occasionally oval, even when not worn; turning
alternately to the right and left, but sometimes pointing ‘upwards.
Gonccvum ?

Habitat. On Terebratula biplicata, Sow., Inoceramus, &c. Fossil
No. 14. There are several other colonies and species on this
specimen. |

Horizon. Red Chalk, Hunstanton.

This is by far the most delicate and most abundant of all the
uniserial Stomatopore in the Red Chalk of Hunstanton. It is not
always possible to make out the zowcial details, or ramifications,
of this interesting species on account of the secondary incrustations,
which very often obscure the delicate branches. I have, however,
been rather successful in defining several small colonies (one
with the basal originating disc), which were adherent on a variety of
fossils. The fossil marked No. 1 has on it many other colonies ;
and the same fossil bears the type species of Deastopora hunstanton-
ensis, described further on. It may be well to keep the Red-
Chalk S. gracilis separated, as a variety, from the more robust form
found in the Upper Chalk. D’Orbigny characterizes the species as
the least in dimensions of all the uniserial Stomatopore known
to him, and he states that the diameter of the branches is + millim.
The branches of the Red-Chalk examples are, generally speaking,
of about the same dimensions, but others are more delicate.

2. STOMATOPORA DIVARICATA (Roemer).

1840. Aulopora diwaricata, Roem. Ool. 11. p. 15, pl. 17. Baiede

1841. Aulopora divaricata, Roem. Kreid. p. 18.

1847. Alecto divaricata, @Orb. Prod. 11. p. 175

1848. Stomatopora divaricaia, Bronn, Index Paleon. p. 1201.

1850. Alecto brevis, dOrb. Terr. Crétac. v. pl. 629. f. 16-18.

1852. Stomatopora dwaricata, d’Orb. Terr. Crét. p. 840, pl. 629.

1872. Stomatopora divaricata, Reuss, Pliiner*, p. 112, pl. 28.
ele 2.

Adherent to a large number of fossils, many of them species of
| Enoceramus and ToreBeaniia, is a hunt or stunted Stomatopora.

* Bibliographic List, No. 10, p. 458.

464 MR. G. R. VINE ON THE POLYZOA OF

The forms are not altogether unlike the Hippothoa inflata, Hall, a
Silurian species referable, says Dr. H. A. Nicholson, to Stomatopora,
as this genus is usually understood*. In the Jurassic rocks there
are similar stunted forms; but, as these have not been described as
yet, I cannot refer to them more minutely. The example that I
have selected for description is adherent to one of the smaller fossils ;
but some of the best examples are found on those that are larger.
Zoarium rarely bifurcating, branches linear or twisted, occasionally
anastomosing. Zoawcia short and plump, with aperture considerably
less than the diameter of the cell; length of zocecia generally about
4 millim., and rather less in breadth.

Halitat. Type, on Terebratula biplicata. Fossil No. 2.

Horizon. Red Chalk, Hunstanton.

This little Polyzoon is one of the most peculiar that I have met
with in the Red Chalk, and for a long time I was inclined to regard
it as belonging to some other group of fossil organisms. In the
type form I have been able to detect the small orifices in some of
the cells, and, in an example on one of the larger fossils, a more
perfect ecll.

3. STOMATOPORA GRANULATA (Edwards).

1838. Alecto granulata, Edw. Sur les Cris. &c. pl. xvi. f. 3, 3a.

1852. Stomatopora granulata, Bronn, 1848; d’Orb. Terr. Crét.
v. p. 836, pl. 628. f. 5-8.

1875. Alecto granulata, Busk, Brit. Mus. Cat. pt. 11. pl. 32. f. 1.

1880. Stomatopora granulata, Hincks, Brit. Marine Polyzoa.

1889. Stomatopora granulata, Waters, Quart. Journ. Geol. Soe.
vol. xlii. p. 341.

Zoarium variable in shape and in the general arrangement of its
anastomosing branches. Zoccia uniserial, nearly uniform in breadth,
oral extremity occasionally erect and free; surface of zocecia punc-
tured in the younger, granular in the older colonies. Gonaciwm (?)
a cell rather more inflated beneath the aperture than ordinary zowera.
Diameter of branch from % to 1 millim.

This species is not abundant in the Red Chalk, but I have met
with some good fragmentary examples. It is almost useless to
compare the fossil with recent examples of the species, or even with
New-Zealand Tertiary species and variety. Mr. Waters (Bibliogr.
24), however, includes in his synonymy of S. granulata a large
variety of forms that may be facially united. If I were to do
the same with the fossils before me, my labours would be less irk-
some, for it is indeed difficult to keep S. ramea and S. imerassata,
@Orb., apart if we study the illustrations only. In dealing with
the fossils the case is different, and in all my descriptions it must
be understood that I describe and illustrate the Red-Chalk fossils

* See Ann. & Mag. Nat. Hist. ser. 4, vol. xv. Feb. 1875, pl. xi. f. 1-3; and
‘Manual of Paleontology,’ edit. 1890, vol. i. p. 637.

+ Mr. Waters’s variety, before me while I write, has been lent to me by
Miss EK. C. Jelly.

THE RED CHALK OF HUNSTANTON. 465

only, using the illustrations and descriptions of other authors as

key-notes to a proper interpretation of the species indicated.
Habitat. On Terebratula biplicata, Fossil No. 3, and Inoceramus.
Horizon. Red Chalk, Hunstanton.

4, Sromatopora eRaAnuLATA (Edwards). Var.* A.

1852. Stomatopora incrassata (?), @Orb. Terr. Crét. v. p. 837,
pl. 628. f. 9-11.

Zoarium much more stunted, compressed, and broader than the
normal form; branches short, generally from two to three cells
(more frequently the first) before each bifurcation; the length of
the branch in this interval about 1 millim. Zowcra stunted, occupy-
ing the whole width of the branch, punctured in horizontal lines ;
length of each 4 millim.

Habitat. On Terebratula biplicata, Fossil No, 4.

Horizon. Red Chalk, Hunstanton.

©), STOMATOPORA RAMEA (Blainyville; non d’Orb.).

1834. Alecto ramea, Blainv. Man. d’Actinol. p. 464, pl. 78. f. 6.

1850. Alecto ramea, Lonsdale, Dixon’s Geol. Sussex, p. 268,
pl. xvii. f. 35-40.

Good examples of this species are rare in the Red Chalk, though
fairish examples are found in the Upper White Chalk.

Zoarvum uniserial, branches irregular and of nearly uniform
breadth, but bordered in this case by a very narrow band, probably
-a slight development of a basal lamina similar in some respects to
the basal lamina of Diastopora obelia, Johnst.t. Zowcra nearly uni-
form in width throughout; peristome inclined upwards ; aperture

.cireular (normal), slightly oval when worn.

Habitat. On Terebratula biplicata. Fossil No. 5.
Horizon. Red Chalk, Hunstanton ; White Chalk, Sussex.

‘6. SroMATOPORA LoneIscata, d’Orb.

1852. Stomatopora longiscata, d’Orb. Terr. Crét. v. p. 839, pl. 629,
f. 9-11.

There are several examples of Stomatopora, adherent to Tere-
bratula biuplicata especially, that I cannot place with either
S. granulata or S. ramea on account of the peculiarities of the
zocecia. ‘These may be placed, I think, under the above name.
Generally the cells are of one width throughout; but there are
several fragments in which the proximal extremities are thinner
than the distal; this, however, cannot be accepted as arule. On

“Fossil No. 8” are apparently two colonies, differing slightly

from each other, yet I cannot separate them so as to make two

* This variety is not common, for I have met with only two examples, the
finest of which I have taken as the type. Whenever I can, I preter working
along the lines of Mr. Waters and Dr. Pergens, so as to reduce the nomen

clature of species, rather than increase the difficulties of the palzeontologist by

the introduction of new names unnecessarily.
t+ Busk, Brit. Mus. Cat. pt. iii. p. 28, pl. xxvi.

466 MR. G. R. VINE ON THE POLYZOA OF

species. In one colony some of the cells are long and pointed at
the proximal extremity, while others are thick at both extremities
of the cell. In one colony many of the cells are less robust, but
of a character similar to those in the other. On another fossil a
small delicate colony (only a few cells) is preserved, which comes
very near to d’Orbigny’s type species. The dimensions of the cells
(length and breadth in all these examples), in some parts of the
colony at least, are similar to the dimensions given by d’Orbigny
(op. crt. p. 839). |

Habitat. On Terebratula biplicata and Torynocrinus manon, Seeley.
Fossils: No. 6, two colonies; and No. 8, two colonies, much better
preserved.

Horizon. Red Chalk, Hunstanton.

7. STOMATOPORA LINEARIS, d’Orb.

1852. Stomatopora linearis, d’Orb. Terr. Crét. v. p. 838, pls. 629-—
658.

The species described and figured by d’Orbigny represents a free-
growing Polyzoon, with peculiarly irregular branches. The prin-
cipal branch is long and flexuous and contains eleven cells; after-
wards the branching is thrown off at right angles rather freely, and
not dichotomously, as in other species of Stomatopora.

I have met with only one unbranched example of this species in
the Red Chalk, and the differences between the Cenomanian form
(V’Orbigny) and this are slight indeed. The zoccia of the British
form are rather less oval than the French, and there are indications
that these were delicately punctate.

Habitat. On Terebratula biplicata. Fossil No. 7.

Horizon. Red Chalk, Hunstanton. French example—Havre
(@’Orb.). ,

Genus Prosposcrna, Audouin.

1838. Criserpia, Edw.; 1847. Idmonea, dOrb.; 1852. Probo-
scina, d’Orb. Terr. Crét. v. p. 844.

The genus Proboscina 1s a convenient, rather than a natural
division of the Stomatopora group. Partially accepted and defined
by @’Orbigny, the genus loses much of its individuality, for many
of his species have been variously located by other authors. Mr.
Hincks says (Bibliogr. 33, p. 482), ““I do not venture to identify
Stomatopora eapansa with dOrbigny’s Proboscina ramosa (=1d-
monea cenomana, d’Orb.), though it bears a strong general resem-
blance to it;” while Tubulipora fimbria, Lamk. (p. 448)= 7. flabel-
laris, Busk (Bibliogr. 31, p. 25), is identified, though doubtfully, by
both authors as Proboscina latifolia, d’Orb. Both Mr. Busk * and
Mr. Hincks disallow the genus for recent species ; the latter author
bracketing the Stomatopore whose zoaria are partially erect and
free as the subgenus Proboscina, Smitt. Stomatopora imerassata,
Hincks, thus absorbs Vubulipora (Proboscina) incrassata, Sm.,
Alecto retiformis, Hincks, and ? Filisparsa incrassata, @Orb. From

* «Challenger’ Report, pt. ii.

THE RED CHALK OF HUNSTANTON. 467

this it is evident that, unless the genus is more rigidly defined than
it has been previously, it would be impossible to accept it for the
purposes of this memoir. By Reuss (Bibliogr. 10,11) and Novak
(Bibliogr. 34), and recently by Mr. Walford (Bibliogr. 30), the genus
has been accepted as a kind of passage-form between Stomatopora
and Diastopora. There is, however, one peculiar species, Proboscina
spatiosa, in examples of which Mr. Walford traces varietal characters
so abnormal that, if disconnected fragments were found, andif growth
only was a consideration in the definition of a species, it could be
placed as a Tubulipora, as a Dirastopora, and even as an erect
Entalophora. Such instances, however, are rare, but I had already
noticed some of these abnormal features in material given to me by
Mr. Walford derived from the same locality (Inferior Oolite,
Shipton). In my new Cambridge-Greensand material I have seen
a similar Proboscina (Kntalophorian growth), but I have not noticed
examples similarly constituted in the Red Chalk, except in one case
that will be referred to again further on.

Jules Haime, in his admirable memoir on “ Jurassic Bryozoa,”
accepts Proboscinu as a passage-group, and suggests that probably
Cellepora echinata, Goldf. (=Tubulipora echinata, Hag.), and
Siphoniotyphlus plumatus, Londs., are really Proboscinal species ;
and Diastopora ramosa, Mich. (Londs. Bibliogr. 35) is undoubtedly
another.

Mr. E. O. Ulrich, examining some of Prof. Nicholson’s species *,
places two of them in the Proboscina group. Thus Alecto confusa,
Nich., and dAulopora frondosa, James, become Proboscona respec-
tively; and Mr. Ulrich remarks that the Silurian forms are like
Stomatopora, but with cells in two or more series 7. As yet I have
not found the multiserial Proboscina in our own Silurian rocks, but
the antiquity of the genus is sufficiently established by the citation
given above.

In determining new species and varieties for Red-Chalk forms,
J have been desirous of not increasing the difficulties of the Paleeon-
tologist ; and in every case where I have called a species by a new
name, I have previously examined all the attainable iilustrations
and descriptions by other authors before committing myself; but
in the interests of truth I have preferred this course to promul-
eating false identities, which, to me, would be far more obnoxious.

8. Proposcina aneustata, d’Orb. Varieties. (Plate XIX. figs. la—
Id:)

1852. Proboscina angustata, @Orb. Terr. Crét. v. p. 852, pl. 632.
fies. 7-9.
"1872. Proboscina angustata, Reuss, “ Bryoz. Unteren Planers,”
p. 1138, pl. 28. figs. 3, 4.
1885. Stomatopora gracilis (?), Vine, Proc. Yorksh. Geol.
Polytech. Soc. vol. ix. p. 4, pl. 2. fig. 7.

* Ann. Mag. Nat. Hist. ser. 4, vol. xv. 1875.
t Journ. Cincinnati Soc. Nat. Hist. 1882, p. 149.

468 MR. G. R. VINE ON THE POLYZOA OF

1889. Proboscina angustata, Vine, Proc. Yorksh. Geol. Soe. vol. xi.
p. 265. :

Small colonies belonging to this species are found on several of the
fossils in the Red Chalk, and generally associated with other forms.
In the Cambridge Greensand a rather ill-preserved example was
found (the only one—adherent to a small phosphate nodule), which
I placed originally as Stomatopora gracilis. I believe, after a re-
examination of the fossil, the proper location ought to be here.
D’Orbigny, in his description of the species, refers to it as being
composed of two lines of longitudinal alternating cells, and this,
generally, is the character of the Red-Chalk fragments. Reuss
figures his species as partly uni- and partly bi-serial, and the
Cambridge-Greensand form more closely resembles that of the
‘“« Pliner ” than d’Orbigny’s form from Le Mans.

Habitat. On Terebratula biplicata. Fossil No. 1%. Also on
Inoceramus and Ammonites.

Horizon. Cambridge Greensand; and Red Chalk, Hunstanton.

9. PRozoscina RuUGOSsA (?), d’Orb.

1852. Proboscina rugosa, @Orb. Terr. Crét. v. p. 853, pl. 633.
Hon U0,

Amongst the rarer Polyzoa of the Red Chalk there are a few
examples similar to the beautiful species figured by d’Orbigny
quoted above. In only one small specimen are the cells in the
branch arranged in three rows; and in this only some of the cells
are rugose, as in the form from Le Mans. There are, however, a
few examples of a branching Polyzoon encrusting Terebratule in
the Red Chalk that may be regarded, if not identical with d’Or-
bigny’s species, at least as belonging to a variety of the same. The
arrangement and character of the cells are similar, and the rugose
markings on one cell (many of the others are broken or abraded)
are very perfect. The diameter of the branches in the British form
is fully 1 millim. against the ‘“‘ 1 demi-milliméetre” of the Le Mans
form.

Habitat. On Terebratula biplicata. Fossils No. 9 4 and No. 118.
Also on Jnoceramus and Ammonites,

Horizon. Cambridge Greensand ; Red Chalk, Hunstanton.

10. Proposcrins IRREGULARIS, sp. nov. (Plate XIX. figs. 2a, 2b;
Variety A, figs. 2 c, 2 d.)

Zoarium repent; very irregular in its mode of growth and
general habit. The zoarilum is unbranched, but made up of many
divergent cells, which, springing from a central or semi-central
nucleus, diverge in a variety of ways from that point. The zowcia
are slightly ventricose in the originating cells and in the more
fully developed zoarium ; but the zocecia here also are very irregular.
Gonecium double-celled ; having the bust-like aspect of a pouter-
pigeon in the type species, but generally speaking the gonccium
is a largely inflated cell.

THE RED CHALK OF HUNSTANTON. 469

Habitat. Type on Terebratula biplicata; var. A, on a Belemnite.
Fossils No. 10 and 10*.

Horizon. Red Chalk, Hunstanton.

This species is only known to me by a few rather imperfect
examples beside the type form, and some of these may easily be
mistaken for other species. In the type (on Fossil No. 10, figs. 2 a,
2 b) the originating point of the colony is situated in the midst of a
clustered mass at the base of the zoarium. From out this mass
another colony (or branch ?) passes off to the right, and towards the
upper right-hand side is apparently the nucleus of another. Alto-
gether, the general habit of the Polyzoon, the peculiar mode of deve-
lopment, and arrangement of cells in the colony, justify my charac-
terizing this form by a new name. A very simple form of the
species is found on one of the larger fossils. In this example the
largely-clustered zoarium, as found in the type form, has apparently
not been reached.

11. ProposcinaA UBERRIMA, sp. nov. (Plate XIX. figs. 3a, 30.)

The zoarium of this beautiful species is similar in many respects
to that of P. wrregularis, except that the zowcra, which are feebly
punctate, could not be consistently described as “irregular” in the
same sense as with that species. The distinctive features of this,
however, are the well-developed ovicells (three in number) right
across the middle of the zoarium. Each gonecium (ovicell) is
separated from its near neighbour by the proximal extremity of
an intervening cell. The aperture of each ovicell is small, and in
one, in the area below the aperture, there is a circular dotted (punc-
tured?) patch which occupies the greater portion of the facial
surface of the ovicell. This is the only example of the species that I
have met with in the Red Chalk.

Habitat. On Inoceramus ? sulcatus. Fossil No. 11 a.

Horizon. Red Chalk, Hunstanton.

12. Proposcina eRactiis, Reuss, var. Ruussiz, nov. (Plate XIX.
figs. 4 a, 40.)

Zoarium adherent, simple or branching; branches originating
from a single cell, and gradually widening towards the distal extre-
mity. Zoewcia smooth (?), arranged alternately in the older part of
the branch, clustered and contiguous in the upper; peristome
circular, slightly raised.

Habitat. On Terebratula biplicata. Fossils No. 124, type;
branching form No. 12.

[Since this paper was read, a separate copy of Dr. E. Pergens’s
‘¢ Revision des Bryozoaires du Crétacé figurés par d’Orbigny,”
premiere partie : Cyclostomata +, has come tohand. Without enter-

+ [Bull. Soe. Belge Géol. Paléont. Hydrol. vol. iii. for 1889), 190, pp. 305-
400. |
Q.J.G.8. No, 183. oe

470 MR. G. R. VINE ON THE POLYZOA OF

ing on other particulars, I may mention that one of the species
which Dr. Pergens has redrawn and redescribed should be referred
to here: thus, instead of my proposed Proboscina claviformis, D.sp.,
the following is substituted :—

13. Proposcrna sUBELEGANS (d’Orb.).

Stomatopora subelegans, dOrb. Terr. Crét. v. p. 853, pl. 759.
figs. 8-13.

Stomatopora subelegans, Pergens, Rev. Bryoz. Crét. p. 332, pl. xi.
fig. 3. |

Zoarium wholly adnate, branches rounded and slightly elevated in
the centre: clavate. Zowcia decumbent or partially depressed ;
in the older part of the zoarium the surfaces of the tubular cells
are delicately punctured while in the younger, or growing portion,
the prominent peristomes only are noticeable.

Habitat. On Inoceramus. Fossil 18.4.

Horizon. Red Chalk, Hunstanton.

At first sight this species may be easily mistaken for a British
example of Novak’s Proboscina Suessi (Bibliogr. 34), which, in
its clavate character, it closely resembles ; but the number of zocecia,
and their pecuhar character, entirely exclude the possibility of
confounding what I believe to be two distinctly characteristic
forms.

14, ProzposcIna HUNSTANTONENSIS, sp. nov. (Plate XIX. figs. 5a,
5 b.)

Zoartum raultiform or irregular; branches originating from a
small discoid body, and then spreading in various directions.
Zoccaa: originating cells simple, and generally unlike the zocecia in
the more fully developed colony. Here the zowcia are flask-like,
rugose, and very variable in their general outline ; orifice contracted
and of less diameter than the cell. Gonaciwm a peculiarly flask-
shaped cell, contracted towards the aperture.

Flabitat. On Inoceramus : Terebratula biplicata. Fossils No, 17 at
(type); No. 164; a’, slightly varying in the character of the
cells.

Horizon. Red Chalk, Hunstanton,

This peculiar species is rather common in the Red Chalk ;
but the colonies are often found in such out-of-the-way places, and
on the larger fossils, that it is by no means easy to get a form
suitable for drawing, either of the species or of its variety mentioned
below ; and it is impossible to get a whole colony under the micro-
scope at once.

15, PRoBOSCINA HUNSTANTONENSIS, Vine; var. AMPLIATA, noy. (Plate
XIX. figs. 6 a—6 d.)

This well-marked variety is similar in many respects to the foregoing

species ; but, as there is a difference in the character of the ‘‘ ovicell ”

THE RED CHALK OF HUNSTANTON, AGL

and the cells surrounding the “ ovicell,” I have decided to keep the
forms separated.

Habitat. Ou Inoceramus. Fossil No. 168.

Horizon. Red Chalk, Hunstanton.

16. Progposcina JESSONI, sp. nov. (Plate XIX. figs. 7a, 7 6.)

Zoariwm fan-like. Colony simple, originating from a disc-like
cell, and between this and the base of the zoarium there is a simple
intermediate branch about 1 millim.in length. Out of the upper
part of this connecting “ link,” which may be, really, only a portion
of the “egg-cell” (d’Orb.), the true zoarium is developed. The
first formed zocecia are in pairs, alternately placed, and then, after a
small interval, the colony widens out, fan-lke. Zowcia tubular,
depressed towards the proximal, raised slightly near the distal
extremities; walls contiguous, and towards the outer margin of the
goarium only the upper portion of the cells is visible. Several of
the middle cells of the colony have their orifices closed, and the
“¢losure” is delicately perforated. These probably are the
goneecia or * ovicells ” of the colony (?).

Habitat. On Terebratula biplicata; unique. Fossil No. 15.

Horizon. Red Chalk, Hunstanton.

After [ had received from Mr. Jesson by far the larger portion
of the one thousand fossils previously referred to, he sent me a small
parcel of selected examples, especially drawing my attention to them.
‘¢On some of the fossils,” he wrote, ‘‘unless lam greatly mistaken,
you will find some new forms.” Proboscina Jessont was one of the
forms in this batch; and, as species bearing ‘closure-cells”’ are
very rare in the Red Chalk, I feel a pleasure in dedicating this
species as above.

Reuss (Foss. Polyp. Wiener Tertiirbeck. pl. vil. fig. 9) figures
and describes a species with a zoarium similar to that of P. Jessont
as Diastopora flabellum, from the marine limestone of Hiseustadt
in Hungary. I do not think that the two forms, though apparently
similar in habit, could be easily confounded; for Reuss shows in his
figure, and refers to it in the text, that the cells are well separated
in the zoarium, whereas in P. Jessont the walls of the tubular cells
are contiguous, not separated, though at first sight they may

appear to be so.

17. Progoscrna cicantopora, Vine. (Plate XIX. figs. 8a, 80.)

Reference: Entalophora gigantopora (Proboscidian stage), Vine,
Camb. Greensand Polyzoa, Proceed. Yorksh. Geol. Polyt. Soc. vol. ix.
1885, p. 8, pl. 1. fig. 3, and vol. xi. 1889, p. 262, footnote.

Zoarium wholly repent, unbranched. Zoweva very large, tubular,
but Escharoidal; depressed, with large circular apertures, rarely
raised above the surface of the zoartum ; surface punctate; closures
occasionally.

Habitat. On Terebratula biplicata. Fossil No, 204.
PN Oe

472
i< MR. G. R. VINE ON THE POLYZOA OF

Horizon. Red Chalk, Hunstanton ; and Cambridge Greensand.

I have only one example of this very interesting species, and this _
being slightly abraded, has the apertures of several of the cells
broken ; but sufficient perfect cells remain to enable me to give the
diagnosis as above.

I have already (1885, Bibliogr. 19) described from the Cambridge
yreensand a peculiarly flattened Hntalophora with large cells, which
I named £. gigantopora. Later still (1889, Bibliograph. 21), I
referred an example, similar in many respects to the present one,
to the Proboscina gigantopora group. I have no evidence that the
Red-Chalk form ever assumed a bi-diastoporan or Entalophorian
stage, consequently I cannot write so fully of this habit in the
present as in the Greensand form; but, as this species ought to find
a resting-place in the Proboscina group, I prefer to give it the same
specific name as the Hntalophora already referred to, and to figure
it as perfectiy as possible.

18. Pronoscrna poHEmica (?), Novak. Variety. (Plate XIX. figs.
9 a—9 d.)

1877. P. bohemica, Novak, Bryoz. bohm. Kreidef. p. 101, pl. v.
figs. 24, 25.

1852? Idmonea radiolitiorum, @Orb. Terr. Crét. v. pl. 633.
figs. 8-10.

This beautiful little Polyzoon more closely resembles P. bohemica
of Novak than P. radiolitiorum, d@Orb., which probably is an ally
of Novak’s species; but ours differs from both in the general habit
of the zoarium, but less so in the arrangement and disposition of the
zocecia.

In the British form the branching is very irregular, but is unlike
the Jdmonea-character shown in the figure of d’Orbigny’s species.
In the early stage of the form the branch is thin, and from this
nucleus two, or even more, diverging, rounded branches are deve-
loped. The general character of the zoarial habit is unlike any
other species described from these strata. The zocecia, though tubular,
are rarely wholly exposed, and only the apertures with rather thick
peristomes are seen. From an abraded fragment (figs. 9 a, 9 6) it
seems that the tubular zooecia are short; but this feature is what
one would naturally expect from a delicate Proboscina like this.

Habitat. On Terebratula biplicata. Sossil No. 21.

Horizon. Red Chalk, Hunstanton,

19, Prososcrva Tovcastana (?), d’Orb.

1847. Idmonea Toucasiana, d’Orb. Prodr. i. p. 265.

1847. Idmonea elegans, d’Orb. Prodr. 11. p. 265.

1852. Proboscina Toucasiana, d’Orb. Terr. Crét. vy. p. 856, pl.
634. figs. 1-6.

[1890. Stomatopora Toucasiana, Pergens, Revis. Pryoz, Crét.
Pp. del; pl xi es; ||

The species described by d’Orbigny under the names cited above

THE RED CHALK OF HUNSTANTON. ATS

form a peculiar group of Proboscine. The habits of the whole may
be characterized as follows:—Zoarium creeping, dendroid, with
narrow depressed branches, which nearly anastomose at the tips.
These branches are narrow at the base, enlarging towards the tops,
and bearing from two to six or seven rows of alternately disposed
cells. In his fig. 1, pl. 634, @Orbigny figures a form of the natural
size, and enlarged in fig. 2. Taking this form, Proboscina ({dmonea)
elegans, cited by d’Orbigny as P. Z'oucasiana, as above, the British
form which I place here resembles the habit of the more robust part
of the colony, where the branches anastomose. The zowcia, how-
ever, differ slightly. Ina portion of the zoarium the cells are
arranged similarly to fig. 4, pl. 634; but the surface is rather
rugose; in other portions of the zoarium the cells are depressed,
rugose, and stunted like the cells on the branches of P. fasciculata,
d@Orb., fig. 11, pl. 634. On the whole, rather than make a new
name for the British form, I think it will be wise to leave this
unique example under d’Orbigny’s name, without any additional
varietal term.
Habitat. On Terebratula biplicata. Fossils Nos. 28 B and 19.
Horizon. Red Chalk, Hunstanton; Senonian Stage, d’Orbigny.

20. PRoBoscina RAMoSA (?), d’Orb.

1845. Diastopora ramosa, Michelin, Icon. Zoophyt. pl. 52. fig. 13.

1847. Idmonea ramosa, a’ Orb. Prodr. i. p. 175.

1852. Proboseina ramosa, d’Orb. Terr. Crét. v. p. 851, pl. 632.
figs. 1-3, pl. 638. figs. 1-3.

Mr. Hincks (Brit. Mar. Polyz. p. 432) says “I do not venture to
identify Stomatopora expansa with d’Orbigny’s Proboscina ramosa,
though it bears a strong resemblance to it.” There is certainly no
affinity between the present form, which I believe to be identical
with dOrbigny’s P. ramosa, and the recent Stomatopora expansa,
Hincks. Indeed the more closely that I study these Cretaceous
fossils, the less inclined I am to identify any of the species found
in the Red Chalk especially with recent forms.

In the list of references given above I have followed d’Orbigny,.
but the Red Chalk ne now being described is more closely
allied to Jdmonea cenomana of that author than to either Michelin’s
D. ramosa or Idmonea ramosa, d Orb. ; but I believe that the whole
of the forms indicated are inseparable, the slight variation in the
habit being of little consequence.

Habitat. On Inoceramus. Fossil No, 14a.

Horizon. Red Chalk, Hunstanton ; French horizon, Cenomanian,
Le Mans.

21. Prozoscina pinatata (?), dOrb., var, CANTABRIGIENSIS (?), Vine.

In my second paper on the Cambridge Greensand Polyzoa
(Bibliogr. 21)-in describing the above variety (p. 261) I refer to an
impression of a species similar to, even if not identical with, the
Greensand form, on an Jnoceramus. No zoarium nor zocecia bein2

474 MR. G. R. VINE ON THE POLYZOA OF

preserved on the fossil referred to, I cannot give further details, and
J only place the species or variety as doubtfully present in the Red
Chalk. J have mislaid the fossil, but probably it will be found, ©
marked “ cast,” in Mr. Jesson’s Collection.

Specialists working both on recent and fossil encrusting Polyzoa
have noticed that certain of the repent species apparently leave
behind them an impression on shell or stone, when all trace of
cell or cell-arrangement was destroyed. On fossil No. 23 is the
basal outline of a fine colony of Proboscina, but of what species
I cannot say. The P. dilatata variety referred to was one of these,
and on the fossil referred to is another.

Habitat. On Terebratula biplicata. Fossil No. 23.

Horizon. Red Chalk (one ‘‘ colony ’’).

Genus Driasropora, Lamouroux.

The genus Diastopora, as now accepted by authors, has had a
peculiar history. By Lamouroux, d’Orbigny, Haime, and others,
and even by M‘Coy, the term Berenicea was used for adherent
discoid forms, and the term Diastopora was reserved for foliaceous
forms. When, however, it was found that adherent Berenicece
occasionally put on the habit of foliaceous species, the former term
was, to some extent at least, abandoned; while d’Orbigny in the
interval between lithographing the plates of the ‘ Paléontologie
Francaise’ and writing the description of his figures, was eyi-
dently undecided which term to use; for some of the figures in the
plates are named Diustopora, and in the text the same figures are
described as Berenicea. Since the publication of Busk’s ‘ British
Museum Catalogue,’ pt. 111., and Hincks’s ‘ British Marine Peclyzoa,’
the one term Dastopora has been more frequently used; but this
practice is by no means general ; even so lately as the new edition
of Phillips’s ‘ Manual of Geology’ in 1885, Mr. Etheridge still
clings to the old term. In the present paper, and in my writings
generally, I make no distinction between the adherent and the
foliaceous forms. In the Red Chalk, however, there are none of
the latter; but in the Jurassic rocks, both British and foreign,
the two groups are pretty evenly balanced. Mr. Hincks gives the
following as his definition of the genus :—

“ Zoartum adnate and crustaceous, or foliaceous, usually discoid
or flabellate, less commonly irregular in form. Zowcia tubular,
with an elliptical or subcireular orifice, crowded, longitudinally
arranged, in great part immersed ” (‘ Brit. Mar. Polyzoa,’ p. 457).

The Diastopore now to be described are peculiar. Most of them
are altogether unlike any known British Cretaceous forms; but
some of them are evidently allied to species, described by d’ Orbigny
and others, derived from foreign Cenomanian or Senonian horizons ;
while others, such as D. hunstantonensis and its allies, are quite
distinct and new to science.

THE RED CHALK OF HUNSTANTON, 475

22. DIAsTOPORA HUNSTANTONENSIS, Sp. nov. (Plate XIX. figs. 10a,
10 0b.)

Zoarium wholly adnate, forming a thin irregular discoid crust
on a variety of fossils, without marginal lamina or stunted marginal
cells. Zowcia irregular both in breadth and length, but disposed in
series, and generally radiating from a central point; robust and
strongly wrinkled or punctate on the surface. Central or nuclear
cells, short or stunted, consisting ordinarily of an “ egg-cell” from
which other cells branch off in opposite directions; these are swollen
in the middle, slightly compressed towards the orifice ; orifice cir-
cular, raised; peristome rather thick. Gonecium either a double
or triple combination of cells or a single large cell. Breadth of
ordinary colony from 12 to 16 mm.

Habitat. On Terebratula, Inoceramus, iAitomlbbis and almost on
every class of fossils previously referred to. ype on Terebratula
biplicata. Fossils No. 1 (type) and 17 Bt.

Horizon. Red Chalk, Hunstanton.

This is by far the most abundant and most prevailing form of all
the Red-Chalk Polyzoa. The larger fossils, especially the Ammo-
nites, have adherent to their exterior surfaces a number of colonial
growths; while many of the smaller fossils, Znocerami especially,
have occasionally from one to three. The type form, however,
on Yerebratula biplicata is one of the most beautiful examples of
the species. The double character on the surface of the zocecia,
wrinkled and punctate, is more noticeable on this than on the
other forms; some of the cells being marked in regular transverse
dotted lines, while others are most irregular; and on one edge of
the zoarium is an overlap of another colony, very strongly wrinkled,
bearing the peculiar gonecium, with its triple combination of cells,
referred to in the diagnosis.

23. Diastovora HUNSTANTONENSIS, Vine; var. A. (Plate XIX. figs.
ipa, (11 &.)

There are a few examples of this species, which, bearing most of
the characters of the typical form, differ sufficiently from them in
the disposal and markings on the surface of the cells to merit
varietal distinction. These varieties are not abundant on the Red-
Chalk fossils, but they have, nevertheless, well-marked characters.
‘Zoarium irregular, rarely discoid. Zowcia less wrinkled than in the
type, and more regular in their disposition or arrangement. Cen-
tral cells similar to those of the type-form.

I have met with several forms of D. hunstantonensis which, under
ordinary circumstances, would be justly regarded as varieties and,
im one case, as a new species; but, being able to trace in most of
these particular features which seem to ally them to the type form,
or to var. A, I think it useless to load the text unnecessarily.

Habitat. On Inoceramus and Verebratula. Fossils No. 17 ct,
ordinary variety, and No. 22, var. A.

Horizon. Red Chalk, Hunstanton.

476 MR. G. R. VINE ON THE POLYZOA OF

24, Diasr poraA FmcunDA, Vine.

1885. Diastopora feecunda, Vine, Proc. Yorks. Geol. Polytech.
soc. vol, 1x. p. 9,

1889. Diastopora facunda, ibid. vol. xi. p. 266.

In the last of these two papers I have given a bibliography of
species alhed to the above; and at ene time I was inclined to place
the present species under d’Orbigny’s name Reptomultisparsa glo-
merata, Terr, Crét. v. p. 877; but, as Reuss includes this form
in his list of synonyms of Berenicea confluens (Romer), 1 cannot
identify this with any of the forms indicated by him, Tertiary or
Cretaceous.

The Red-Chalk form is rather larger than the one previously
described from the Cambridge Greensand ; but its general charac-
teristics are similar. Zoariwm discoid, and more or less proliferous
in habit, The present form is rare in the Red Chalk and very
badly preserved.

Habitat. In a water-worn piece of Red Chalk. Fossil No. 24.

Horizon. Cambridge Greensand (== Phosphate-beds) ; Red Chalk,

Hunstanton.

25. DIAsTOPORA REGULARIS, d’Orb.

1850. Diastopora regularis, dOrb. Terr. Crét. v. pl. 636. fig. 10
(only).

1851. Diastopora densata, dOrb. ibid. pl. 637. figs. 1, 2.

1851. Diastopora orbicula, @Orb. ibid. pl. 637. figs. 3, 4.

1852. Berenicea regularis, VOrb. ibid. p. 865, pl. 636. figs. 9, 10;
pl. 637. figs. 3, 4.

The species included in the synonymy by d’Orbigny,. as above,
differ materially in their mode of growth. The D. regularis,
pl. 636. fig. 10, has the flabellate character of a Proboscina,
rather than that of a Dvastopora, the discoid form of the species
not having been reached; but in D. densata, pl. 637. fig. 2, we
have a completed discoid form with the originating cells slightly
excentric. D. orbicula, pl. 637. f. 4, has an entirely. different
form of cell and cell-arrangements. The Red-Chalk form is more
hike D. resularis (pl. 636. fig. 10), and I restrict my ideuntifi-
cation to this figure only. The zoarium, though in an advanced
Proboscinal stage only, is a true Diastopora; but it is not wholly
discoid. The zowcia originate from a primary ‘“egg-cell” at the
base of the zoarium, which, unlhke that of d’Orbigny’s species, is
soon enclosed by the eurly zocecial growth, after which the growth
is upwards and outward, to the right and left, until a disc-like form
is reached. The oritices of the originating zocecia, which are short
and stunted, are circular; but on two of them these are covered by
perforated opercula (‘ closures”), and some of the cells in other
parts of the zoarium bear “closures” as well. The zomcia are
broad towards the orifices, narrow towards the base, contiguous,
depressed for nearly the whole length; surface faintly punctate.

Habitat. On Terebratula biplicata. Fossil No. 28 4.

a

THE RED CHALK OF HUNSTANTON. ATT

- Horizon. Red Chalk, Hunstanton. Cenomanian Stage of Le Mans
(d’Orb.).

This is the only example of the species that I have found in the
Red Chalk.

26. Drastopora rapians? (Novak). Variety ?

1877. Berenicea radians, Novak, Bryoz. bohm. Kreidef. p. 98,
pl. iv. figs. 15-18.

The example which I place under Novak’s name, as a variety
of his species, is the only one that I have found among the Red-
Chalk fossils. The identification of unique forms is always difficult ;
-and this is especially so, because some of the characters in the
British species seem to ally it more closely with D. pilosa of the
same author than with D. radians. The Red-Chalk form, however,
is similar to fig. 16, both in the general outline of the zoarium and
in the arrangement of the cells; but the partly formed marginal
cells of the British example are more abundant. Zowcia not con-
tiguous, interspaces and cells finely punctate, disposed in linear
series radiating from excentric originating cells. About the middle
of the zoariwm there is a raised gonocyst, which embraces several
cells, similar in character to the one depicted by Novak as the
“ ovicell” of D. (Berenicea) foltum, Novak (p. 96, pl. iv. fig. 14,
op. cit.).

Habitat. On Terebratula biplicata. Fossil No. 26.

Horizon. Red Uhalk, Hunstanton ; Chalk-marl, Bohemia (Novdk).

27. Drastopora PAPILiosa (?), Reuss.

1846. Diastopora papillosa, Reuss, Verst. bohm. Kr. p. 65, pl. 15,
figs. 44, 45.

1847. Diastopora papillosa, d’ Orb. Prodr. ii. p. 266.

1847. Diastopora oceanica, d’Orb. ibid.

1851. Diastopora disciformis, Hag. Bryoz. Maastr. Kreid. p. 16,
pe. ts., 7.

1852. Berenicea papillosa, d@Orb. Terr. Crét. v. p. 866, pl. 639.
figs. 6, 7.

D’Orbigny describes and illustrates a series of Diastopore having
very diverse habits, but the whole of them are very closely related,
if we consider the cell and cell-arrangement of the forms. Thus
the zocecia of Diastopora tuberosa, D. grandis, D. oceanica, and
even D. congesta and D. littoralis (pls. 639 and 640) are strikingly
similar, but the habits of nearly all are different. The example
that I place here resembles D. disciformis, Hag., D. tuberosa, and
D, oceanica, @Orb.; but the proliferous habit of D. tuberosa is so
very peculiar that I think it would be unwise to place it under that
name. As D. papillosa is accepted by d’Orbigny, under which he
places his own D. oceanica, Reuss’s name has a prior claim to our
notice. ‘The Red-Chalk form is disciform, one colony overlapping
another ; originating cells central.

The wonderfully wide range of this species as given by d’Orbigny

478 MR. G. R. VINE ON THE POLYZOA OF

(Terr. Crét. p. 867) shows how very common the Diastepore with
simple non-characteristic zocecia are. It is, indeed, as Dr. Pergens -
very wisely suggested in a recent letter, a most unsatisfactory group
to deal with and distinguish. I have been, however, so far very suc-
cessful with the Red-Chalk species; but duplicates of all the forms
indicated in the text are by no means easy to get, even out of the
abundant series submitted to me.

Habitat. On Terebratula biplicata. Fossil No. 27.

Horizon. Red Chalk, Hunstanton.

28. Drastopora JEssoni, sp. nov. (Plate XIX. figs. 12 a, 12 6.)

Zoarium adnate, without marginal lamina or partially formed
cells on the edge, orbicular. Zowcta: originating cells central, very
short and compressed ; radial cells either linear or slightly oblique
where the lines reach the edge from the centre; these linear series
widen out towards the margin, so as to admit an intermediary
series between the radii, by which the zoarium is enlarged ; zocecia,
either elongated tubes, of about the same diameter throughout, or
flask-lke, narrow towards the proximal and bulging at the middle
or at the distal extremities; orifice circular or oval (?), raised,
with very thin peristomes; surface of cells punctate in fine and
closely transverse series, which give a rugose appearance to the
zocecia 1f only examined under a low power of the microscope, or by
the hand-lens. Closure-cells occasional, with very finely perfo-
rated ‘ opercula,” which form a slightly rounded covering over the
orifice of the cells. These closure-cells are probably equal to the
ovicells in other species; anyhow they are very characteristic in
certain species of Diastopora in the Red Chalk.

Habitat. On Terebratula biplicata, Fossil No. 25; and on Nautilus
albensis, d’Orb., in Mr. C. D. Sherborn’s collection.

Hlorizon. Ked Chalk, Hunstanton.

The general outline of Diastopora Jessont is similar to that of
D. gracilis (WOrb. pl. 635. fig. 9), and it is about the same, size
(natural) of fig. 8 on the same plate. In d’Orbigny’s text (Terr.
Crét. p. 864) I find that the author includes under Berenicea gracilis,
d’Orb., both D. intermedia and D. vassiacensis, d’Orb., of the same
plate; in any case it would be impossible to place the Red-Chalk
form under any of these specific names, whether we regard them
as synonyms of Milne Edwards’s D. gracilis cr not. The next
species, somewhat similar as regards the flask-like cells, is the
Berenicea pilosa, Novak (Bibliogr. 34, pl. iv. fig. 10, only); besides
these, I know of no other species with which I can compare
D. Jessoni.

I have already dedicated a Proboscina to Mr. Jesson, so as to
connect his name with these Red-Chalk fossils, and, m my remarks
on Proboscina Jessoni, I made reference to the small special col-
lection which came after the larger mass of fossils had been placed
in my hands; and the fossils to which P. Jessont and D. Jessoni
were adherent were in this parcel. Mr. Jesson has, therefore, a
double claim to remembrance in the distribution of specific names.

THE RED CHALK OF HUNSTANTON.. 479

Genus Unirunicrra, d’Orbigny.

1852. Unitubiera, @Orb. Terr. Crét. v. p. 759.

D’Orbigny founded this genus to include a very peculiar group of
fossil Polyzoa. The zoariwm was fixed (parasitic ?) on a large num-
ber of fossils; the zowcia were disposed in primary rays, radia-
ting from the centre, with intermediate rays between the primaries
in the wider parts of the zoarlum. On the border, or outer edge,
of the zoarium were a number of ‘“‘ germes de cellules,” probably
remains of former colonial (?) growths. D’Orbigny gives a list of
eight species of Lichenopora and Defrancia, from other authors,
that may be placed under this generic head, and one of these is the
peculiar Ceriopora disciformis of Goldfuss. In the Paléont. Frang.
Terr. Cret., d’Orbigny describes and illustrates two species only,
Unitubigera discus, d’Orb., p. 760, pl. 763. figs. 4-6, and Uni-
tubigera papyracea, d’Orb.; and to this latter species a single Red-
Chalk Polyzoon seems to be related. In Mr. Etheridge’s list
(Biblograph. 36, p. 590) he uses d’Orbigny’s generic name for a
Lower-Greensand species.

29. UNITUBIGERA PAPYRACEA, d’Orb.

1850. Actinopora papyracea, Orb.

1852. Unitubigera papyracea, dOrb. Terr. Crét. v. pl. 64:3. figs.
12-14.

The example which I place under the above name is almost
unique. The zoarzum is disciform, slightly raised above the surface
of the fossil to which it is attached, and is wholly adherent. Zowcia
disposed in linear rays, radiating from the centre of the zoarium,
with intermediary rays when the zoarium begins to widen out
towards the margin; short, punctate, contiguous. The raised and
slightly slanting border is composed of what d’Orbigny calls
“‘ vermes de cellules,” already referred to.

Habitat. On Terebratulu biplicata. Fossil No. 29.

Horizon. Red Chalk, Hunstanton; Meudon, in 22 stage Seno-
nian (d’Orb.).

The following two species (?), which I do not attempt to classify,
are placed here temporarily :—

30. Enratopnora (?), Lamouroux, sp.

This and the following species (?) I cannot attempt to identify
with any known Polyzoa; but, because of their rarity, they ought
to be recognized here, in the hope that better examples may be
sought for and found.

Habitat. On Spondylus. Fossil No. 301.

Horizon. Red Chalk. Hunstanton.

Re-examining some of Mr. Jesson’s fossils, I find another obscure
specimen rather better preserved.

480 MR. G. R. VINE ON THE POLYZOA OF

31. Hererorora (?), Blainville, sp.

In fragments of Red Chalk two different species (?) of Polyzoa are
embedded, and I should hesitate to place them anywhere except that
I have met with Heteropora tencra, in the Faringdon rock, having
characters as obscured as these until fragments were sectioned,
when their true character was revealed.

Habitat. In pieces of Red Chalk. Fossils No. 30 11. and No. 31.

Horizon. Red Chalk, Hunstanton.

§B. Recraneurata, Waters.

Genus Crrtopora, Goldfuss.

1826. Ceriopora (pars), Goldfuss; 1834. Blainville; 1847. D’Or-
bigny ; 1852. Certopora, Goldfuss, d’Orb. Terr. Creét. v. p. 1029.

In establishing the genus Ceriopora, Goldfuss took for his type
Alveolites, Lamarck; altogether Goldfuss described and admitted
in the group about 37 species. The group has since been very much
broken in upon by Blainville and others, and at the present time it
is impossible to accept the genus for any considerable number of
Polyzoa. D’Orbigny admits (Terr. Crét. p. 1030) the following
Cretaceous species as Certopore :—

1845. Ceriopora truncata, Mich. Icon. pl. 51. fig. 7.

1830. Ceropora tubtporacea, Goldf. Petrefact. pl. 10. fig. 15.

1830. Ceriopora milleporacea, Goldf. Petrefact. pl. 10. fig. 10.

1830. Ceriopora micropora, Goldf. Petrefact. pl. 10. fig. 4.

He also describes a new species from the Senonian stage as
Ceriopora digitalis, Orb. I have only two examples of Ceriwpora
from the Red Chalk, which I prefer to place in this genus rather
than in the Ceriocava, d’Orb.

32. CERIOPORA MIcRoPoRa (?), Goldf.

1830. Ceriopora micropora, Goldf. Petrefact. p. 33, pl. 10. fig. 4.

1852. Ceriopora micropora, d’Orb. Terr. Crét. v. p. 1030.

1872. Ceriopora micropora, Simonowitsch, Bryoz. des Essen
Griinsands. :

The two examples, which I place here doubtfully, are difficult
to separate, except by slight variation in their form. Ceriopore
are rare in the Red Chalk, and the present specimens differ in the
characters of the cell-orifices, so much so that Dr. Pergens, who has
examined most of the Red-Chalk Polyzoa, made the following note
respecting them :—

“ Ceriopora (Heteropora?), n. sp.; the orifices are 0:14—0°16
millim.” The forms seem to me, however, closely related to C. mi-
cropora, Goldf.

Habitat. Embedded in fragments of Red Chalk. Jossils Nos, 34
and 35 (variety ?).

Horizon. Red Chalk (middle bed *), Hunstanton ; Essen (G'old-
fuss).

* 'The ranges in the several zones are shown in the Table at p. 460.

THE RED CHALK OF HUNSTANTON. 481

| Genus Rrepromuttrcava, d Orb.

1826. Ceriopora (pars), Goldfuss ; Blainville.

1852. Reptomulticava, dOrbigny, Terr. Crét. p. 1032.

Under the above generic name d’Orbigny places a considerable
number of fossil forms. The colony is fixed by the whole of the
inferior surface, and the general character of the superior face
would be sufficient in itself to characterize species as Ceriopora,
Goldfuss, previous to the rigid separation of that group by Blain-
ville and d’Orbigny. Many of the flattened discoid Monticulipore
of the older rocks are to some extent similar to these Cretaceous
forms,

30. REPTOMULTICAVA SIMPLEX (?), d’Orb.

1852. Reptomulticava simplex, VOrb. Terr. Crét. v. p. 1041,
pl. 793. fig. 5.

The &. simplex, dOrb., resembles, by its flattened figure, the
Red-Chalk fossil placed here. The zoarium is simple, or disc-like,
without any elaborate detail other than the small openings in the
surface, which are very fine and characteristic, as in figs. 5 and 8
of plate 793, Terr. Crét.

Habitat. On Terebratula biplicata. Fossil No. 32.

Horizon. Red Chalk, Hunstanton.

34, REPTOMULTICAVA COLLIS (?), d’Orb.

1852. Reptomulticava collis, @Orb. Terr. Crét. v. p. 1036, pl. 792.
figs. 1-3.

1854. Reptomulticava collis (?), VOrb.; Morris, Cat. Brit. Fossils,
p. 128. |

On several fossils of the Red Chalk are small colonies of a species
similar to the forms described and figured by d’Orbigny as fepto-
mmulticava collis. ‘The general character and markings of the sur-
face of the little dome-like zoarium are more like the species which
d@Orbigny calls R. cupula, d’Orb., pl. 792. fig. 10; but this form is
only partially attached at the base (figs. 8, 9), whereas the Red-
Chalk examples are wholly attached. I have met with several
examples of these little forms, but I am unable to follow d’Orbigny
in establishing, even suggestively, other than these two species.
Even those indicated vary slightly in their colonial growths.

Habitat. On Terebratula, Inoceramus, Belemnites. Fossils Nos.
33 and 36,

Horizon. Red Chalk, Hunstanton. Neocomian, Fontenvoy
(a Ord.)

Genus Zonopora, d’Orb.

1847. Zonopora, @Orb.; 1851. Plethopora (pars), Hagenow ;
1852. Zonopora (Fam. Caveide, d’Orb.), Terr. Crét. vy. p. 928.

D’Orbigny, in his 5th family Caveide (Terr. Crét. p. 922), has
brought together no fewer than twenty-seven genera, all of which,
to say the least, are peculiar and characteristic. The author includes

482 MR. G. R. VINE ON THE POLYZOA OF

in this family, among others, Zonopora, Ditawia, Lichenopora,
Domopora, and Radiopora.

The Zonopora group may be regarded, judging from one of its
species (4. vartabilis, d@Orb.), as a Heteropora, but not so with the
other forms. As I have met with two or three examples in the
Red Chalk that may be placed here, rather than elsewhere, I pro-
visionally refer them to this genus, hoping that other and better
examples may be brought to light.

30. ZONOPORA IRREGULARIS (?), d’Orb.

1849. Zouopora irregularis, @Orb, Prod. il. p. 87.

1852. Zonopora trregularis, VOrb. Terr. Crét. v. p. 390, pl. 771.
figs. 4-6.

Two small fragments of a species either allied to, or identical
with, the above have been found in the top beds of the Red Chalk
of Hunstanton. D’Orbigny shows in his fig. 4 two sorts of orifices :
Ist, in raised cells, with thick peristomes, distributed in zones, but
irregular; 2nd, very fine intermediary openings, similar to those
found in Heteropora. Small sections, worked up to view as semi-
transparent, show Heteropora-like intermediary ‘ cells” in the
centre, while the produced thick orifices of the larger ceils, or true
zocecia, of the species appear like those found in sections of Hetero-
pora also. My material is far too limited to warrant further re-
search at present.

Habitat. This is possibly a derived Polyzoon embedded in Red
Chalk. Fossil No. 45.

Horizon. Top beds of the Red Chalk, Hunstanton. D’Orbigny’s
species was found in the Neocomian, 17th stage.

36. ZonopoRA ? VARIABILIS, d’Orb.

1852. Zonopora variabilis, dOrb. Terr. Crét. v. p. 931, pl. 771.
figs. 9-13.

There are only minute fragments, which I place here doubtfully.

Fossil No. 46.

Horizon. Top Beds, Red Chalk, Hunstanton. D’Orbigny’s species
was found in Senonian strata, 22nd stage.

Genus Muuticrescrs, d’Orb.

37. Moutricrescis vARIABILIs (?), d’Orb.

1852. Multicrescis variabilis, VOrb. Terr. Crét. v. p. 1077, pl. 800.
figs. 3-7.

In some respects the zoarium of the present species is similar to
the example that I have placed under the Ceriopora micropora (°),
Goldfuss; but careful examination of the orifices of the two forms
shows that the two are specifically distinct.

Fossil No. 47.

Horizon. Top Beds, Red Chalk, Hunstanton. D’Orbigny’s species
is found in the 20th Cenomanian stage at Le Mans.

In Mr, Etheridge’s list of Cretaceous Polyzoa (Bibliograph. 36,

THE RED CHALK OF HUNSTANTON. 483

pp. 589, 590) he cites Zonopora (probably Z. wndata) as occurring
in Cenomanian strata; and five species of Multicrescis, three from
the Neocomian, but the other two are not located; and also one
species of Ceriocuva from the Gault.

Genus Unicaves, d’Orb.

1826, Melobesia, Aud. (non Lamouroux); 1839. Tubulipora
(pars), d’Orb.; 1848. Defrancia, Reuss (non Bronn); 1852. Uini-
cavea, d’Orb. Terr. Crét. v. p. 970.

The genus Unicavea, as founded by d’Orbigny, embraces a most
peculiar group of fossils (Lichenoporide, Hincks). The colony is a
very simple, discoid, dome-like zoarium, fixed by the whole of its
under surface to some foreign body, sometimes surrounded by a
basal lamina, which is not always apparent in some of the species
of the genus. The zowcia are disposed in primary and intermediary
rays, each of which bears the orifices of depressed tubular cells.
Between the rays are cancellated interspaces, with a depressed,
cancellated, non-zocecial space in the centre of the zoarium. Uni-
caved radiata (Audouin), one of d’Orbigny’s species, is cited by Busk
as Discoporella (Catal. Mar. Polyz., Cyclostom. Polyz. 1875, p. 32),
and by Hincks as a Lichenopora (Brit. Mar. Polyz. p. 476); but
as none of the figures compare favourably with the Red-Chalk forms,
which I shall place in the genus Unicavea, 1 make no apology for
passing over the recent species, ignoring at the same time some
citations by d Orbigny and others,

38. UNICAVEA CoLLtis, d’Orb.

1850. Actinopora collis, dOrb. Terr. Crét. v. pl. 643. figs. 1-4.

eZ. Onicavea cols, d Orb. ibid. p. 973, pl. 778. figs. 1, 2.

There are a few forms in the Red Chalk that may be regarded
as allies of the French Senonian species, even if they be not iden-
tical. The zoaria are dome-like and fully attached by the under
side to foreign bodies. The zowcia are disposed in primary and
intermediary rings, which begin to form a little beyond the central
cancellated centre. The examples are too badly preserved to allow
me to discuss the Lichenoporidal features, ovicells or cancelle,
entered into by Mr. Waters *; but the characters, so far as I can
make out, are more in accord with the Cretaceous (Senonian) forms
than with any recent example of Lichenopora radiata, Aud., known
to me.

Unicavea collis, d’Orb., must not be confounded with Reptomule-
cava collis, d’Orb., already described. The species are quite
distinct.

Habitat. On Terebratula, Inoceramus, and Bourqueticrinus. Fossils
Nos. 37, var. A, on Terebratula ; 38, var. B, on Bourgueticrinus.

* A. W. Waters, 1884, pp. 694-5, Quart. Journ. Geol. Soc. vol. xl.; 1887,

pp. 345-347, vol. xlin.; “On the Ovicells of some Lichenoporidz,” ‘Journ.
Linn. Soc., Zoology, vol. “xX, pp. 280-285 (1888).

484 MR. G. R. VINE ON THE POLYZOA OF

§ IL. Suborder CHEILOSTOMATA, Busk.

Celloporina, Ehrenberg.
Genus Mempranipora, Blainy. See Hincks’s Brit. Mar. Polyz.

Eschara (pars), Pallas; Flustra (pars), Linné, Lamarck, Flem-
ing, Lamouroux, Audouin; Membranipora, Blainville, Johnston,
Busk, Smitt, Hincks; Cedlepora (pars), Marginaria, Dermatopora,
v. Hagenow ; Cellepora, d’Orb. T

“ Generic Characters.—Zoarium encrusting. Zowcia quincuncial,
or irregularly disposed, occasionally in linear series ; margins raised ;
front depressed, wholly or in part membranaceous ” (p. 128, op.
cit. ).

The few species that I place in this group are very characteristic,
and likewise very rare in the Red Chalk.

39, MEMBRANIPORA GAULTINA, sp. nov. (Plate XIX. figs. 13 a—
13 d.)

Zoarium very simple and uniserial. Zowcia elongate, sub-ovate,
produced or attenuated below; area oval, occupying nearly the
whole front, area-walls smooth (?), occasionally crenulated; the
produced portion of the wall just below the area folded or puckered.
Zocecia linked together in linear series ; branches lateral, sometimes
from every cell, at other times three cells apart, and occasionally
from both sides of the same cell; tiree of the longest zocecia
together measure one quarter of an inch.

Habitat. On Inoceramus, Terebratula brplicata, Terebratula ca-
pillata. Fossils Nos, 38 and 39*.

Horizon. Gault, Cambridge ; and Red Chalk, Hunstanton.

This very peculiar Membranipora I have been obliged to describe
as new, but not until after an examination of the illustrations of
all apparently similar forms known to me; even then I should
have hesitated to do so, had not a fine series from the Gault of
Cambridge been sent to me for examination by Mr. Jesson.

At first I thought that the species described above may be placed
as an ally of either Hippothoa elegans or H, lawata, @Orbigny
(Terr. Orét. pl. 711. figs. 1-4 and 12-15); but a reference to the
figures is sufficient to show that no identity can be established
between these forms. Novak (Bibliogr. 34} described two species
of Hippothoa, H. desiderata and H, labiata, both of which, certainly
in some of their characters, closely resemble M. gaultina; but
among at least one hundred zocecia examined, not a single attenu-
ation of the cell-wall exhibits the wavy outline indicated in Novak's
figures. Then, again, the Membranipora-like area shown by Novak
is an accidental breakage of the once covered portion, judging
from some of the perfect cells depicted, whereas.in the present

+ In reproducing these names, Mr. Hincks says in a note (p. 128), “I have
not thought it necessary to swell this list of synonyms by referring to all d’Or-
bigny’s genera which include species of Membranipora as now defined. The
groups to which they belong are given in the Family synonymy ” (p. 126,
op. cit.).

—_—- —%,

THE RED CHALK OF HUNSTANTON, 485

species the area-opening appears to me to be perfectly normal. The
folding-in of the wall below the area also precludes the placing of
the form here described even as a variety of Membranipora catenu-
laria, Jameson (Hincks, Brit. Mar. Polyz. pl. xvii.).

I have figured the Red-Chalk form of MW. gaultina, but I have
had the better-preserved Gault examples before me when drawing
up the characters. It is in the Gault form that the puckering of
the wall below the area is found.

40. MeMBRANIPORA FRAGILIS (d’Orb.).

1852. Flustrellaria fragilis ?, d’Orb. Terr. Crét. v. p. 545, pl. 723.
figs. 5—9.

I have met with two or three examples of a form closely resem-
bling the #. fragilis of @Orbigny. Very rarely more than from
3 to 6 cells are preserved; and the fossil cited below contains the
best-preserved colony that I have found. As the Red Chalk, so far
as my experience goes, is very poor in Cheilostomatous forms, I have
done my best to preserve every record of their existence, hoping
that other workers will be able to add to the meagre list.

Habitat. On Terebratula biplicata. Fossil No. 41.

Horizon. Red Chalk, Hunstanton.

4], Mempranrpora ELLrprica (?) (Hagenow).

1839. Cellepora elliptica, Hag. Neues Jahrbuch &e., p. 268;
Marginaria elliptica, Romer ; Membranipora ellipteca, d’Orb.

1877. Membranipora elliptica, Hag; Novak, Bryoz. bohm. Kreid.
Deco. plegs fe, 16.

Hesitating to identify this species with von Hagenow’s C. ellip-
tica, I refer the student to the long list of synonyms given by
Novak, and to his reasons for adopting that course. I have only
one example; and as Novik’s fig. 16, pl. ii., closely resembles its
general features, his identification is adopted. I should have been
more inclined to place this unique example under M. tuberosa,
Novak, but the cells of that species are not elliptical, like the British
Red-Chalk form. The avicularian cells in the intermediary space
between the ordinary zocecia are very conspicuous and abundant on
the Fossil No. 42.

Habitat. On Pentacrinus Fittont. Fossil No. 42.

Horizon. Red Chalk, Hunstanton.

42, Me=MBRANIPORA OBLIQUA (?) (d’Orb.).

1852. Piliflustrellaria obliqua, WVOrb. Terr. Crét. v. i 513,
pl. 723. figs. 1-4.

If we are to regard d’Orbigny’s species mentioned above as a
Membrantpora, then the present form is allied to, if not identical
with, it. The British example, the only one that I have met with,
is adherent to a fragment of a Belemnite, and is apparently much
larger than the fragment figured by d’Orbigny. The zoariwm

Q.J.G.8. No. 183. 2M

486 ON THE POLYZOA OF THE RED CHALK OF HUNSIANTON.

branches dichotomously. The zowcia are oval, but attached; area
oval; walls thick. This is a poor and unique example of the
species ; I cannot follow d’Orbigny in the other characters drawn —
up by him.
Habitat. On Belemnites. Fossil * No. 44.
Horizon. Red Chalk, Hunstanton.

Genus Hiprornoa, d’Orb.
43. Hiprornoa simpiex (d’Orb.).

1851. Hippothoa simplex, dOrb. Terr. Crét. v. p. 385, pl. 711.

figs. 5-8.

The forms that I have been able to identify are certainly not
members of the Hippothoa group as now understood; but, as a
set of four cells appear to belong to H. simplex, d’Orb., or a close
ally, I place them here provisionally. They are all that I have met

with adherent to Red-Chalk fossils, and are too characteristic to be
overlooked.

Habitat. On Inoceramus. Fossil No. 40.
Horizon. Red Chalk, Hunstanton.

EXPLANATION OF PLATE XIX.
Polyzoa from the Red Chalk of Hunstanton, Norfolk.

(The objects enlarged are magnified about 15 or 20 diameters.)

Fig. 1. Proboscina angustata, VOrb. Variety: 1a, natural size; 1 0, eniarged.
Var.: le, nat. size; 1d, enlarged.
. P. irregularis, sp. nov.: 2a, nat. size; 26, enlarged. Var.: 2c, nat.
size; 2d, enlarged.
P. uberrima, sp. nov.: 3a, nat. size; 3, enlarged.
P. gracilis, Reuss, var. Reussii, nov.: 4a, nat. size; 46, enlarged.
P. hunstantonensis, sp. nov. : 5a, nat. size; 5, enlarged.
, var. ampliata, noy.: 6a, nat. size; 66, portion enlarged ;
6c, nat. size; 6d, portion enlarged.
7. P. Jessoni, sp. nov.: 7a, nat. size; 7 6, enlarged.
8. P. gigantopora, Vine, var.: 84, nat. size; 8 4, portion enlarged.
9. P. bohemica, Novak, var.: 9a, nat. size; 9b, enlarged ; 9c, nat. size;
9d, portion enlarged.
10, Diastopora hunstantonensis, sp. nov.: 10a, nat. size; 10, portion en-
larged.
11, —— ,var.: lla, nat. size; 11, portion enlarged.
12. D. Jessoni, sp. nov.: 124, nat. size; 126, portion enlarged.
13. Membranipora gaultina, Vine, var.: 13a, nat. size; 13, enlarged; e¢, d,
portions enlarged.

iw)

Sons G9

Discussion.

Dr. Hriypze commented on the imperfect preservation of the
specimens exhibited, and the difficulty of satisfactorily determining
species from such specimens.

* The fossil No. 43 (Zercbratula biplicata) has attached to it several examples
of Webbina (?), which seem to simulate the characters of M. obliqua; but a
careful examination of the two forms will be sufficient to disprove any supposed
relationship between the polyzoon and the protozoon.

We

ON LHE DEVONIAN ROCKS OF SOUTH DEVON. 487

29. The Duvontan Rocks of Sovra Devon. By W. A. KE. Ussaer,
Esq., F.G.S., of the Geological Survey of England and Wales.
(Read April 30, 1890.)

By permission of the Director-General of the Geological Survey
of the United Kingdom.

Contents.

§ [. Inrropucrion.
§ IL. Guneran Descriprion.
S$ IIL. Rerations or tan Cutm any Deyonian,

S$ IV. Lowrr Devonian.
|. Torquay Area.
2. Paignton Area.
$V. Mippie Duvontay.
1. Eifelian.
2. Middle Devonian.
3. Middle- and Upper-Devonian Limestones.
$ VI. The Asurrineron Votcanic Series.
§ VIT. Urerr Devonian.
1. Massive Limestones.

2. Goniatite-beds.
3. Cypridinen-Schieter (Hntomis-slates).

§$ VIII. Concrustons.

$ [. Iyrropvcrion.

*‘In South Devonshire the rocks are greatly disturbed, broken by
faults, standing at various angles, folded, and distorted; eruptive
rocks frequently cut through them, and beds of volcanic ash are
interstratified with them. Henee has arisen great dispute and
uncertainty as to the true order of succession of deposits, although
their fossils were referred to the Devonian age nearly fifty years
ago. It will be seen without comment that the South Devonshire
sections, from which most of the Middle- and Lower- Devonian fossils
have been obtained, are valueless for determining the order of
sequence of the faunas. There are many places (I saw such near
Newton-Abbot) where limestones, appearing very similar in colour
and structure, and within a stone’s throw of each other, hold distinct
faunas. In fact, the interpretation of the order of the beds is a
matter of the greatest difficulty, even when occasional fossils appear.”

Here is the geology of South Devon as epitomized by Professor
H. 8. Williams, of Ithaca, N.Y., in a paper read before the American
Association for the Advancement of Science as lately as Aug. 30,
1889. Explorations .in the rocks of Devonshire gave rise to the
Devonian System; explorations in France, Belgium, Germany, Russia,

and North America have made us acquainted with the succession of
; 2m 2

4838 MR. W. A. E. USSHER ON THE DEVONIAN

the Devonian faunas, and the extraordinary persistence of homo-
taxeous horizons, such as those characterized by Stringocephalus,
Rhynchonella cuboides, and Goniatites, at the same time presenting
us with the varied evidences of straticraphical succession.

The disturbances to which Prof. Williams refers, the distortion of
fossils in consequence, and the paucity of localities rich in charac- _
teristic fossils, renders South Devon a most unprofitable field to the
casual investigator, whilst depriving the stratigraphist of the only
means of piecing the scattered details into a connected whole.

The late Mr. J. E. Lee’s * discoveries of the Biidesheim and Adorfer-
Kalk faunas at Saltern Cove and Chudleigh proved that the Gonia-
tite fauna had extended to Devonshire; but the faulted occurrence
of the beds containing it precluded the observation of their true
position in the formation.

The South-Devon limestones were, with two or three exceptions,
regarded as Middle Devonian, and the presence of Lower Devonian
was only proved in the Torquay Promontory.

The old l-inch Ordnance Map on which De la Beche, Godwin-
Austen, and subsequently Dr. Harvey Holl and Champernowne,
were compelled to record their observations on the stratigraphy of
South Devon is much too small to note minutie which have the
most important bearing on the question.

Dr. Holl+, in 1868, placed both the Plymouth and Paignton
sections in the wrong sequence, through the acceptation of inverted
dips as natural evidences of superposition ; yet his sections account
for the position of many of the types which he correlated by
inverted plication. The succession he advocated in descending
order is:—Staddon and Cockington grits, slates, limestones. He
likewise endorsed Godwin-Austen’s view that the limestones of
Ashburton were a lower series than those of Newton and Ipplepen.

During a re-survey of portions of the country around Newton-
Abbot and Torquay in 1874-75, my colleague, H. B. Woodward f,
arrived at the conclusion that the Devonian rocks occurred in
descending order as follows :—

Limestones.
Slates.
Red Sandstone (of Cockington).

When this general succession was published in 1876, it was
adopted by Mr. Champernowne as affording “the clue to unravel
the country.”

Mr. Champernowne §, in “ Notes on the Devonian and Old Red
Sandstone of North and South Devon,” gave the true succession in
sections of the Mudstone-Bay coast. ce This,” he says, ‘* brings the
Red Sandstone into direct and natural relation with those of
Cockington, the Warberry, Lincombe, &c. at Torquay, which are

* Geol. Mag. 1877, p. 100, and 1880, p. 145.
+ Quart. Journ. Geol. Soc. vol. xxiv. p- 400.
t Geol. Mag. 1876, p. 576.

g Ibid. 1878, p. 193.

ROCKS OF SOUTH DEVON. 489.

beneath the limestones.” Unfortunately, subsequent investigations
near Cockington, Marldon, and Paignton induced Mr. Champer-
nowne to abandon his previous views and to endorse, on strati-
eraphical grounds, the erroneous succession given by Dr. Holl. The
independent observation of the Plymouth section led me to adopt
the same views. We were both under the impression that the
Cockington beds were unfossiliferous, and in ignorance of the dis-
covery, by the Rev. G. F. Whidborne, of Lower-Devonian fossils in
them, no detailed account of which had been published beyond
incidental reference to it in Dr. Davidson’s Supplement to Devonian
Brachiopoda, Pal. Soc. Mon., note by G. F. W. at p. 4.

Thus, through a mere accident, the geologist whose painstaking
devotion has furnished the first detailed map of the Devonian rocks
of South Devon, and vastly increased our knowledge of that forma-
tion, was deprived of reaping the results of his exhaustive labours.

For the publication of the erroneous succession given in Proc.
Geologists’ Assoc. vol. vill. pp. 442 &c., I am alone responsible,
Mr. Champernowne’s views having, at my request, been promptly
reduced by him to their simplest form in spite of the uncertainty he
entertained respecting them.

The existence of contemporaneous volcanic action,—the definition
of the Ashprington series and of sporadic evidences of local vuica-
nicity outside its borders,—the correlation of the Ashburton lime-
stone with that of Newton and Ipplepen,—and paleontological
contributions, adding to our knowledge of the Middle and Lower
Devonian, stand prominently forth amongst the labours of my
deceased friend. Had he lived, the task I briefly and inadequately
undertake would have fallen into better hands.

During our friendship I became so thoroughly conversant with
the special difficulties he encountered, and with the doubts he
entertained, that, when it devolved upon me to carry on his work
on the six-inch Map, I started already equipped with the results of
his experience, and was stimulated to researches in quest of fossils
in beds before regarded as unfossiliferous in character and anomalous
in position. So the present communication must be taken as the
outcome of my friend’s Jife-work in Devonian geology, and will, I
trust, form a not unfitting tribute to his memory.

After the London Meeting of the Geological Congress in 1888 I had
the advantage of conducting MM. Gosselet, Kayser, Tschernyschew,
Holst, and Frech over the North-Devon section and over those parts
of South Devon near Newton-Abbot, Chudleigh, and Torquay, which
would in a short time best show the different varieties of rock and
evidence of their fossil contents.

Dr. Kayser embodied the results in a pamphlet entitled ‘“‘ Ueber
das Devon in Devonshire und im Boulonnais,”’ Neues Jahrbuch fiir
Mineral. &c. Bd. i. (1889). The identification of the Cypridinen-
Schiefer, by the Lewell-Path road and at Whiteway Farm, was of
immense service to me. The identification of the Hope’s Nose thin
limestone with the Calceolen-Kalk, and the correction of Rh. cuboides
to procuboides, were also important.

490 MR. W. A. E. USSUER ON THE DEVONIAN

M. Frech kindly furnished me with the names of fossils found
ui the different localities visited.

I have great pleasure in acknowledging my indebtedness to MM.
Gosselet and Barrois, and subsequently to Dr. Kayser, for their
kind and prompt assistance in identifying fossils sent to them from
time to time in 1889.

I am indebted to M. Tschernyschew for the assistance afforded
me, by the presentation of his admirable contributions to the
Devonian geology of Russia; and to MM. Gosselet, Kayser, and
Barrois for similar favours.

My friend Prof. Gosselet devoted a week last September to con-
ducting me over the typical sections of the Ardennes rendered
classic by his investigations. His kindness supplied me with more
information and encouragement than I can hope to repay.

$ IL. Gryerat Description.

The area to which this paper more particularly refers lies north of
the River Dart and East of Dartmoor, and comprises the most
complex and lithologically varied tract in South Devon.

We naturally turn to the limestone districts to obtain evidence
of structure. Owing, however, to crushing, it is impossible to
obtain persistent and reliable dips beyond the actual exposures ;
and the acceptance of apparent superposition of limestone on slate.
or vice versd, in any one place must lead to endless confusion 1n its
general application, as inversion is rather the rule than the
exception.

Evidences of stratigraphical relations are often so dubious as to
suggest alternative explanations, such as anticlinal or synelinal
inversion or consecutive sequence. Moreover the sharp plications
often displayed in a single quarry, in beds otherwise exhibiting low
dips, inspire caution.

When, however, we regard the district as a whole, the local
development of limestones in the Kingsteignton, Ipplepen, King’s-
Kerswell, Torquay, Yalberton, and Brixham districts,—the preva-
lence of slates in the Berry-Park and Staverton districts,—and of
voleanic materials north-east of Bickington, south of Totnes, and
east of Yalberton, compel us to ascribe the anomalous distribution
of the limestones to very irregular accumulation dependent on
locally favourable conditions. Thus, in the area south of Totnes
the formation of limestone has been restricted, owing to a long-
continued period of volcanic activity ; whilst near Rickington,
Dartington, and Yalberton its accumulation has been partially
arrested from a similar cause. Again, in the Broadhempston
district the limestones are clearly impersistent ; and the Plymouth
and Yealmpton masses, although equivalent to the Ipplepen and
Denbury limestone, and to that of Ashburton, are, in the intervening
district, represented by slates with very occasional, insignificant
patches of limestone.

Without such a broad interpretation as the above it is found that

| Lo face p. 490.

Map of the Distribution of the Devonian Rocks in the District between

the River Teign and the Ialdon Hills ;

cession and the new KMossil Minds.

‘ig. 2.

Kingsteignton Suc-

showing the

0 e

>

Bo

g >
>
Q!

?

Q.J.G.8, vol. xlvi.|

{ Lo face y, 490.

Fig. 2.— Map of the Distribution of the Devonian Rocks in the District between
: rh sabe dee : : <a = , ; the River Teign and the Haldon Hills :
Fig. 1.—Map of the Distribution of the Devonian Rocks in the District West of Torquay ; showing the Relation of the Volcanic Series cession and the new Fossil Finds.

and the Kossil Finds, proving Upper and Lower Devonian.

showing the Kingsteignton Suc-

——

SS =.

TPS SS SS [ey
—— ——- =

TORBAY

Lhd

EXPLANATION OF KEIGS. 1 & 2.

\)
NS Culm-measures.
mI Post-Cretaceous. ZF U.D. Upper-Devonian Slates.

Aphanite, hard Diahase.

M.D.L. Middle Devonian
Limestone.

Gq au.
Cg AVI
9 BON a

ad
a

Cretaceous. U.D.L. Upper-Devonian Limestone. H, Hifelian Slates,
PSs T. Lower-Trias Breccia and be V. Voleanie Tuffs, Schalsteins, and Diabases. THD ener Deventamn
eyo Sandstone, eu (Harder Diabase masses, b/ac/.) Gasca OTE US

g. Goniatite-beds. G. Goniatite-beds: Goniatites found, P, Pleurodictyum-beds.

‘ fone
P Li 1 : r " (ain a at ee ¥ c aL? | i
on kan
u by lee” mad Al ry My? ba ls Ls enuatl nae ~ aa iy bad 4
seetathen ay." SEBEL. Via, Aatte gi ih os Sa
’ ad i
a ae ed, Al PS |
oe Pgs Nee x
yar "|"? i \ { ' ’
cy ee pines

ee 0s:

ROCKS OF SOUTH DEVON, 491

local successions are not capable of general application. Thrust-faults
on the axes of inversions are frequently present on a small scale ;
but to ascertain their existence on a large scale demands paleon-
tological data of a most definite character, which from the com-
parative rarity of characteristic fossils does not appear to be
obtainable. We have therefore to fall back upon such information
as can be procured of the general types of Upper-, Middle-, and
Lower-Devonian faunas; for without these an appeal to stratigraphy
can only lead the enquirer to a mass of apparently contradictory
details.

From this it must not be inferred that the occurrence of indi-
vidual characteristic forms is anywhere of weight unless supported
by sufficient positive, negative, or comparative evidence, or that its
admission in any way violates definite stratigraphical position.

Although the lithological constituents of the Upper-, Middle-, and
Lower-Devonian beds are broadly distinguishable, yet there is no
definite lithological boundary between the groups. The Lower
Devonian is mainly distinguished by the occurrence of sandstone
and grit; but the upper beds are slates or shales passing, where
unfaulted, indistinguishably upward into the Middle Devonian
slates. In no part of the Lower-Devonian area have igneous rocks
been found.

The Middle Devonian consists of limestones upon shaly limestones
upon slates.

The slaty and shaly basement-limestone and underlying slates
represent the Calceolen-Kalk and Calceclen-Schiefer. The Calceolen-
Schiefer is somewhat variable in character, the irregular grey slates
with fossiliferous lenticles, developed in Berry Park, and the even
grey and bluish-grey slates of Mudstone Bay, being different types.
These slates and the overlying thin limestones are characterized by
_ the occurrence of Spirifer specrosus.

The Middle-Devonian limestones are well bedded in the lower
part of the mass, where they “are usually dark-grey, and contain
Helholites porosus, Cystiphyllum vesiculosum, Oyathophyllum helian-
thoides, and C. damnoniense. Stringocephalus is found here and
there throughout the district in the bedded limestones. The upper
part of the Middle Devonian generally consists of pale bluish-grey
and grey limestone, often massive, as in the Lummaton and Barton
quarries, where it is composed of corals, amongst which Smitha
Henna and S. Pengellyi are noticeable. ‘These massive limestones
denote the passage from the Middle Devonian, in which the Lum-
maton fauna occurs, to the Cubordes-beds of the Upper Devonian ;
and, as it is not possible to draw any definite boundary in them,
they must also be regarded as partly of Upper-Devonian age.

The Upper Devonian first becomes distinctly recognizable by thin-
bedded limestones and limestone lenticles intercalated with chocolate-: .
red, lilac-weathered slates and mudstones. ‘These limestones are,
as a rule, red or liver-coloured and of very compact texture; they
are often knubbly or concretionary, as at Lower Dunscombe, at Old-
chard, near Whiteway Farm (where they contain Gonzatites), and

492 MR. W. A. E. USSHER ON THE DEVONIAN

by the River Teign opposite Combe Cellars. This concretionary
character, distinguishing the Knollen-Kalk, is locally developed in the -
form of calcareous nodules in irregular dark-grey slates, as near
Lewell (Chudleigh), near Bishopsteignton, by the Teign west of
Combe Cellars, and west of Abbotskerswell.

Above the Knollen-Kalk we encounter chocolate-red slates and
mudstones, containing Posidonomya venusta and Entomis, locally
greenish and grey. In addition to the localities mentioned by
Kayser, these beds, correlated by him with the Cypridinen-Schiefer,
occur in Kingsteignton Railway-cutting at Newton-Abbot, Anstey’s
Small Cove, and Goodrington. In the district west of Newton-
Abbot the Upper-Devonian beds consist mainly of red and greenish
slates, the latter furnishing badly preserved G'onzatites at Wrigwell
House.

Sporadic evidences of vulcanicity frequently render the relations
of the Upper and Middle Devonian extremely obscure, and outside
the limestone areas, where the normal slate type everywhere
prevails, the localization of these groups (as may be seen from a
recent communication to the Devon Association on the geology of
Tavistock) is extremely indefinite.

The main distinctions between the lithological characters of the
three Devonian groups in the area under description are as fol-
lows :—Lower Devonian: presence of grits and sandstones, often in
mass.

Middle Devonian : slates, of grey and bluish tints; fossils in
lenticles and much distorted, but not infrequent.

Upper Devonian: slates, very unfossiliferous, red and pale
ereen tints prevalent.

The common characteristics of the groups are :-—

Middle and Lower Devonian: slates in which the boundary can
only be ascertained by paleeontological evidence.

Upper and Middle Devonian: massive limestones, in which no
hard-and-fast boundary-line can at ‘present be traced by the dis-
covery of fossils ; local prevalence of volcanic schalsteins and tuffs,
breaking up the limestones and obscuring general indications of
boundary.

$ ILL. Rerarions or tar Curtm anp DrEvontan.

No paper on the Devonian rocks of South Devon would be com-
plete without a reference to the relations of that formation to the
Culm-measures. Here it must be confessed that the details supplied
by this district are wholly inadequate to furnish even general con-
clusions of a trustworthy nature, the boundaries being in most
cases fault-lines. There are, however, certain known facts outside
- the district available to supplement the meagre evidence within it.
Holl * advocated the existence of a considerable unconformity be-
tween the Culm and the Devonian rocks of South Devon, on the

* Quart. Journ. Geol. Soc. vol. xxiv.

ROCKS OF SOUTH DEVON. 493

ground that, whilst the lower beds of the Culm-measures were
equally well developed in North and South Devon, the upper beds
of the Devonian did not correspond; and even in South Devon and
East Cornwall the Culm-rocks appeared to rest upon Devonian
strata of different ages.

I have elsewhere given reasons * for regarding the Petherwin
beds and those of Druid, near Ashburton, as probably contempora-
neous with the Lhynchonella-letiensis-zone of the “ Fammenien” of
the Ardennes, but beyond this I have been unable to extend the
comparison to that region; the Cypridinen-Schiefer mainly consti-
tuting the upper part of the Devonian in the district under descrip-
tion proves, as Dr. Kayser has shown, a correlation rather with the
German than the Franco-Belgian Upper-Devonian type.

In 1887 I discovered Upper-Devonian slates in the Culm-measure
area between Bickington and Bovey Tracey; these consist of grey
slates and grey and brown mudstones, somewhat recalling the
Druid beds, and of red aud greenish slates of the normal type of
the Cypridinen-Schiefer. In the only places where untaulted
junction-relations with the Culm-measures are visible, no uncon-
formity is apparent. Coddon-hill beds (identified as phthanites by
Professor Gosselet) seem to overlie the Knollen-Kalk and Cypridinen-
Schiefer by the path-road to Lewell, near Chudleigh. This junction
appeared to Prof. Kayser to be a natural one; whilst M. Gosselet
regarded it as a proof of unconformity. ‘The subsequent experience
I have acquired does not enable me to decide authoritatively
between these views ; but the acceptance of a natural junction in
this spot is not in accordance with the development of the Upper-
Devonian slates in the South-Devon area.

We may conclude generally that the Upper-Devonian slate
and psammite type of North Devon gave place southward to a
purely slate type; and that the latter, probably from unequal rate
of deposition in deeper water, attenuated as the distance from
the shoal-areas increased; but, as the conditions which produced
similar sedimentation in the earliest Culm-rocks of North and
South Devon would probably be the same, it is not unlikely
that their production in South Devon precluded the equivalent
representation of the upper part of the Devonian series, and even
occasioned an overlap of the Culm-measures.

I purpose to lay before the Society the evidence for the grouping
of the Devonian rocks of South Devon under the following heads :—

{ Cypridinen-Schiefer (Entomis-slates).
Upper Devonian ...... , Goniatite-limestones and slates.
| Massive limestones.

( Middle Devonian Limestones.
Middle Devonian ...... { Ashprington volcanic series.
| Hifelian slates and shaly limestones.

Lower Devonian ...... Torquay area, Paignton area.

* Trans. Devon. Assoc. for 1889.

494 MR. W. A. E. USSHER ON THE DEVONIAN

S IV. Lowrr Devonian.

1. Torquay Area.—Up to the year 1889 the record of the
occurrence of Lower Devonian in South Devon is confined to the
Torquay promontory. (See Map, Fig. 1, opposite p. 490.)

In that promontory two divisions of the Lower Devonian had
been recognized, the Upper (Lincombe and Warberry beds) con-
sisting of red sandstones and grits with shales, the Lower (Mead-
foot beds) of irregular bluish-grey slates with hard grits.

Mr. Champernowne discovered Homalonotus on the east side of
Lincombe Hill by the New Cut, ‘in some red finely-sandy or silty
beds, interstratified with grits. The beds are traversed by a coarse
cleavage dipping south, which usually ignores the hard grit-bands.

“We may call them... . the Lincombe, Warberry, and Smug-
gler’s-Cove grits .... Within a hundred yards west of the spot
where the specimen occurred, this subgroup becomes mottled with
light colours, brown grits appearing, and passes down into the
Meadfoot series... . The grits of the Meadfoot series are less
distinctly quartzose, and are more tenacious, requiring heavier
hammers. Jf we imagine this lower group coloured red, it is
difficult to say whether, on purely paleontological grounds, they
would be separated from the upper; but it is probable they might
be. ‘The buff and brown weathering of the Meadfoot beds disappears
with depth, as the heaps shot out from the Torquay drainage-works
show, grits and shales alike being of a blue-black tint; whereas red
or purple beds, as a rule, are so both at the surface and in depth.
In the passage-beds described above, | hold that we have a horizon
corresponding in general terms with that between the Hangman
and Lynton groups of North Devon. ... If now we look abroad,
we seem to gain some insight into the occurrence of red sandstones
of marine origin on the same horizon in the Devonian rocks. In
the Kifel district the ‘ Homalonotus Red Flagstones,’ so named by
Murchison, “ occupy a horizon high in the Lower-Devonian beds,
scarcely removed from the base of the Calceolen-Schiefer, and the
bulk of the Coblentzian or Ahrian, the chief home of Plewrodic-
tyum problematicum (though this mud-loving Favositid ranges
higher in the series) lies below them ” *.,

The Lincombe and Warberry beds occupy the highest land in
the Torquay promontory; in their extension to the coast at Smuggler’s
Cove they are faulted on the north and south, but on the hill
above Kilmorey they occur in an isolated patch.

These grits do not appear on the coast in unfaulted relation ;
and, as red Kifelian shales and shaly limestones with Calceola
directly underlie the limestone of [addy-Hole-Knoll, their absence
between this and the Eifelian slates and limestones of Hope’s Nose
is only to be accounted for by an extensive fault cutting them out,
unless we are prepared to admit that they underlie the Meadfoot
beds, or occur impersistently in the upper part of that series.

* Geol. Mag. 1881, pp. 487, 488.

ROCKS OF SOUTH DEVON. 495

The following is a list of Fossils obtained in the Lincombe and
Warberry beds :—

At Warberry Hill fossils are very rare. ‘Tentaculites have been
identified ; also Beyrichia Wilckenstana*.

From the Lincombe-Hill grits fossils have been obtained in the
following places :—
Oxlea hill:

Homalonotus. Pentamerus.
Spirifer. \ Orthis.
New Cut :
Orthoceras. | ©, Chonetes sordida, often crowded
c. Myalina (small). in certain layers.
Tentaculites. c. Homalonotus Champernownel.
c. Cypricardites. Pleurodictyum problematicum.

Avicula anisota.

[c.c.c.c. from Mr. Champernowne’s list. |

On the hill behind Kilmorey :

Atrypa. Spirifer cultrijugatus.
Chonetes. Homalonotus Champernownei.

From Smuggler’s Cove :

Hdmondia. ¢ Leptana laticosta.
Macrocheilus. Pleurodictyum.
¢. Orthis. N , te
¢. Spirifer. \ umerous casts.

From the Meadfoot beds the following fossils were obtained :—

In beach-reefs near Kilmorey, described by Kayser as dark slates and
grauwacké, here and there enclosing masses of fossils :

KK. Chonetes sarcinulata. K, Strophomena, allied to Murchisoni.
K. Pterinza costata. U. Cucullea.

U. P. spinosa, U. Trimerocephalus.

kK. Rhynchonella daleidensis. ‘| U, Pleurodictyum problematicum

K. Spirifer hystericus. (two specimens).

K. Sp. paradoxus. U. Fenestella.

F, Sp. macropterus. F. Zaphrentis oolithica.

| K. denotes Kayser’s list ; /. identification by Frech on the spot ;
U. found by Ussher. |

The following were obtained by me in the Meadfoot Beds : —

Near St. Raphael’s Home :

Spirifer. | Streptorhynchus.
Jn quarry east of Kilmorey :
Chonetes. Homalonotus.

Spirifer. Pleurodictyum.

* |The Beyrichia (or rather Kledenia) Wilckensiana from Warberry Hill is
matched by what Richter has figured and described as Beyrichia aurita in the
Zeitschrift deutsch. geol. Gesell. vol. xx. (1869), p. 775, pl. xxi. fig. 15 (not
fig. 16), from the Upper or Middle Devonian, which is, indeed, the same as
Kledenia Wilckensiana.— April 29, 1890, 'T. R. Jonzs. |

496 MR. W. A. E. USSHER ON THE DEVONIAN

Grit-bed on beach in cove west of the raised beach at Hope’s Nose:
Loxonema. | Pleurodictyum problematicum.

On surface above Hope’s Cove:

Orthis. Homalonotus (? Champernownei).
Spirifer (? undiferus).

At small cove, 30 chains from Kilmorey :
Natica. Petraia.
Spirifer. Fucoids.

At 50 chains from Hope’s Nose Quarry-well :
Spirifer (? speciosus).

In slates faulted against the limestone of Hope’s Nose* Quarry :
Strophomena rhomboidalis. | Pleurodictyum problematicum.

By wood north-east of Kilmorey :

Pleurodictyum.

Before proceeding to the consideration of the Lower-Devonian
area of Paignton, it must be remarked that slates identical in
character with those of the Hifelian of Torquay occur in the area
occupied by the Meadfoot beds.

Furthermore, between Kingsteignton and Bishopsteignton a strip
of dark-grey fossiliferous clay-slates, faulted on the south against
the Entomis-slates, but overlying, with inverted dip, volcanic beds,
which separate them from the Middle-Devonian limestones, show
Middle- and Lower-Devonian affinities, containing :—

Pleurotomaria. Aulopora.
Phacops. Pleurodictyum (numerous).

[It seems possible that the traces of ** Plewrodictya,” so numerous
in the quarry near Bishopsteignton, might be casts of portions of
Spheronites tesselatus. I do not in any case think that they belong
to the species Pl. problematicum.—June 1890. |

2. Paignton Avca.—The Triassic area of Paignton is bounded by
red and brown sandstones and grits and red slates. The grits, con-
stituting the heights of Beacon Hill and Windmill Hill on the north
of Stoke-Gabriel, are faulted against Middle-Devonian limestones
and volcanic materials on the south, and against Berry-Park (Kife-
lian) slates on the west. These sandstones give place on their
borders to red slates, partly intercalated with hard grit bands, as
near Westerland and at the south end of Goodrington beach. They
are very irregularly associated with red slates, which appear to
underlie the sandstones, with a low dip, south of Cockington, but to
pass up into the Kifelian near Marldon. (See Map, Fig. 1.)

The red slates with hard grit beds south of Goodrington beach

* Petraia bina and P. celtica, doubtfully identified by Messrs. Sharman and
Newton, were found both here and in the quarry west of Bishopsteignton.
Goniatites spiralis was also found in the latter, and furnishes an inexplicable
anomaly.

ROCKS OF SOUTH DEVON. 497

support a Triassic outlier, and are faulted against the red slates and
mudstones in which Mr. Lee discovered the Upper-Devonian Gonia-
tite-fauna of Biidesheim. The fault is entirely concealed by slips

-and undergrowth, and at the bridge spanning the adjacent railway-

cutting it is by no means clear.

As before mentioned, Mr. Champernowne placed the Cockington
erits in their true position at the base of the series in 1878*; but
the stratigraphy of the districts he subsequently investigated was
so contrary to this view that he abandoned it, placing them at the
top of the series, a conclusion I also came to from the independent
observation of the Plymouth section’.

Mr. Champernowne’s later views appeared in the succession
given in the Ashprington paper lately communicated to this
Society {, in which the Lower-Devonian slates or shales, correlated
by him with the Cockington beds, were placed above the Goniatite-
beds. ‘his opinion was evidently entertained in ignorance of the
discovery of Lower-Devonian fossils by the Rev. G. F. Whidborne
in these beds in the adjacent railway-cutting. Incidental reference
to this discovery is given by Davidson in the ‘Supplement to the
British Devonian Brachiopoda,’ p. 4, in the following passage :—
‘«¢ At Saltern railway-cutting (behind Saltern Cove, within four or
five miles of Torquay), Mr. J.G. Greenfall and Mr. G. F. Whidborne
came upon a light brownish-red shale, in which several species of
Brachiopoda occurred in considerable numbers, accompanied by
Pleurodictyum problematicum and Petrara, sp. The fossils occur in
the condition of impressions and casts, much distorted and compressed,
so that it is not possible in most cases to arrive at a satisfactory
identification. I thought I could, however, recognize among them
Spirifera levicosta, Rhynchonella Pengellyana, Lepteena Looiensis,
Orthis hipparionyx, a small circular species of the same genus
somewhat similar in shape to O. arcuata, and Chonetes Hardrensis.”

At p. 8, further on, ‘“ Goodrington Sands (south of Paignton) ” is
bracketed with ‘‘ Pleurodictyum-problematicum beds,” under the
heading of Lower-Devonian localities.

On accidentally hearing of this discovery from Mr. Hunt, early in
1888, I visited the cutting with him and Mr. Whidborne, when we
obtained Pleurodictyum problematicum, Chonetes sordida, &c.

As I considered a single find of Lower-Devonian fossils insuf-
ficient to disprove my friend’s stratigraphical conclusions, I pro-
ceeded to ascertain whether the fossiliferous beds were really a part
of the Cockington series, and whether that series was wholly untos-
siliferous.

The success | met with in these quests is more than neutralized
by regret that my friend cannot share in it.

Fossils are exceedingly scarce in the Lower-Devonian slates,
shales, and sandstones of the Paignton area ; but a diligent search,
in spite of repeated disappointments, has enabled me to place the

* Geol. Mag. 1878, p. 198.

+ Proc. Geologists’ Assoc. vol. vill. pp. 442, &e.
+ Quart. Journ. Geol. Soc. vol. xlv. p. 369, &e.

498 MR. W. A. E. USSHER ON THE DEVONIAN

Cockington Beds in the Lower Devonian on paleontological evidence
quite as strong as any furnished by the Torquay promontory, as may
be seen from the following discoveries :—

In the red slates with grit-bands at the south end of Goodrington

Sands:
Orthoceras. Spirifer.
Tentaculites. Pleurodictyum.

In the adjacent railway-cuttings (the site of Mr. Whidborne’s
find) :
Orthis. Pleurodictyum problematicum.
Spirifer speciosus.
Near Westerland House, south of Marldon, in red slates passing
into the Middle Devonian (Hifelian) :

Orthis. Pleurodictyum problematicum.

Petraia.

In red slates (resembling those at the south of Goodrington Beach)
south of the Ship Inn, Churscombe, by the highroad east of
Lower Westerland :
Orthis. | Streptorhynchus.
Spirifer speciosus. Pleurodictyum problematicum.

The above finds prove the position of the red slates of the Saltern-
Cove cutting to be at the top of the Lower Devonian.

The following lists further prove their connection with the Cock-
ington grits. For the identifications I am indebted to Messrs.
Gosselet and Barrois, whose remarks accompanying the identifi-
cations are quoted :— |

In sandstones on the margin of Staddon plantation, near Cockington :
Pterinzea. | Spirifer hystericus.

In shaly sandstones near Shortdown, north of Paignton:
Spirophyton.

In red shales and sandstones between Churscombe and Ramshill
Cross:
Pleurodictyum.

On Beacon Hill, south of Westerland House, in red and brownish
sandstones :
Nucula, “ voisine de NV. Aahlebergensis, Bausch, peut-étre Palzeoneilo du
Coblenzien ” (M. Gosselet’s label).
Homalonotus.

In a little quarry on Windmill Hill, north of Stoke-Gabriel, in slaty
grits resembling those of the New Cut:

Chonetes sarcinulata,

semiraciata.

Rhynchonella hexatoma, ‘‘ voisine de daleidensis.”
daleidensis (identified by Prof. Kayser).
Homalonotus gigas (‘* Coblenzien inférieure”),
Pleurodictyum problematicum.

In a surface stone in the same district:

Leptena, “ probablement l’espéce que j’appelle Leptenu spathulata”
(M. Gosselet’s label).

ROCKS OF SOUTH DEVON. 499

My first discovery in the Cockington Beds was a fragment of
Homalonotus in red slaty beds in Seaway Lane, Cockington.

The subdivision of the Lower-Devonian Beds of the Torquay and
Paignton area into Upper aud Lower Coblenzian is not justifiable,
the districts being too much disturbed to furnish a certain succes-
sion; very detailed investigation in the Torquay district would,
however, probably settle this question; all that can be said so far
is that the Middle-Devonian slates pass downwards into Lower-
Devonian slates, and these, through intercalation with grit, into
the Lincombe, Warberry, and Cockington Sandstones ; but whether
the main mass of the Meadfoot beds are below these grits or not,
depends on the existence of a dislocation of sufficient magnitude to
cut out the latter on the coast near Hesketh Crescent, and this I
consider to be probable.

V. Mippir Devontran.

1. Hifelian.—The Warberry beds near Ellacombe, and the Cock-
ington beds near Westerland and in Berry Park, are bounded by
grey slates, generally irregular, which contain distorted fossils in
lenticles. Streptorhynchus is common in these beds, and Spirifer
speciosus is by no means rare: the Zaphrentide in a crushed con-
dition are also frequent, as well as Phacops latifrons. The more
usual type of these slates is exhibited in the cliffs of Mudstone Bay,
near Hope’s Nose, and in Daddyhole Cove. In their upper part
they contain limestone lenticles, and frequently pass up into the
limestone through thin-bedded limestones, calcareous slates, and
slaty limestone, representing the Calceolen-Kalk.

Speaking of the relation of the Cockington beds to these slates,
we find amongst the unpublished notes of Mr. Champernowne the
following passages :—

“The same beds form Staddon Heights and Mount Edgecombe
in Plymouth Sound, and, as Dr. Holl has shown, they also support
the Paignton Trias, rising on opposite sides into the high ground of
Windmill Hill and Westerland Beacon ; and they must be many
hundred feet thick around Cockington, but are too disturbed to form
any estimate from.”—‘t Wherever the sequence is anything like
complete the last beds appear to pass down by an easy transition
into bluish slaty shales, which are well exposed in road-cuttings and
small quarries in Berry Park. Nevertheless good sections at the
junction are exceedingly rare, and certain local appearances would
lead to a belief in more or less unconformity between the two, or
even a complete covering-up of the bluish slates . . . Fossils, almost
entirely in the state of casts, are fairly common. Streptorhynchus
umbraculum, much distorted, is common near Berry Castle; and in
the same beds at Dartington, at the former locality, I found a cast
of Khynchonella cuboides.”

The above: passages represent the evidence of stratigraphy. At
Lower Westerland Berry-Park slates occur, apparently underneath
red Lower-Devonian slates, the anomaly being probably due to

500 MR. W. A. E. USSHER ON THE DEVONIAN

thrusts ; and east of Wildwood the bluish slates seem to dip under the
Cockington beds. The Rhynchonella cuboides above mentioned is pro-
bably procuboides, noticed by Kayser as occurring in the Eifelian
limestone of Hope’s Nose.

The Eifelian slates occur on Meadfoot Road, ‘Torquay, south of
Marychurch, from Broadhempston southward to Totnes, and thence
to Marldon, bounding the limestones of Dartington, Berry-Pomeroy,
Little Hempston, and Marldon, which, with natural, inverted, or fault
dips, overlie them; and they also bound the Ashprington voleanic series,
under which they pass, generally with inverted dips. The shaly
Calceolen-Kalk, or Eifelian limestone, is frequently brought up in
the limestone masses of Torquay and elsewhere by contortion. At
Hope’s Nose slaty Calceolen-Kalk is apparently completely inverted
upon massive bedded limestone, containing /eliolites porosus, and is
also affected by thrust-faults. Patches of limestone occur at the
base of the Ashprington series at and near Totnes, which belong to
this group; the lower parts of the Berry-Park, Dartington, Little-
Hempston, and Marldon limestones belong to the same horizon, also
apparently the base of the Torbryan limestones, the Broadhempston
limestone, and part of the limestones in Ellacombe, and perhaps
Babbacombe and Torre, and the thin beds in Torquay cemetery.
The Calceola-beds and their relations to the limestones of Daddyhole
were described by Mr. Champernowne in a paper published in the
‘Transactions’ of the Devon Assoc. for 1874.

The following fossils are common in the Eifelian slates :—Atrypa
reticularis, Streptorhynchus cremstria, Spirifer speciosus, Phacops
latifrons, Fenestella, Aulopora, and less frequently Leptena inter-
strialis and Strophomena rhomboidalis, found in a quarry in Berry-
Park slates west of Westerland House; Phacops batrachius east of
Little Hempston wood; Reteporu repisterva near Bulleigh Cross ;
and Orthis striatula north of Follaton House, west of Totnes, iden-
tified by Professor Gosselet, as also Orthis, near to O. cifelensis,
near Port Bridge, north-east of Stoke Gabriel.

Helianthaster filrciformis, Woodw., was found by Mr. Champer-
nowne™* in the upper port of the Eifelian slates near Harbertonford.

The following lists of fossils from the thin limestones of Hope’s
Nose and their representatives elsewhere will show the connection of
the beds, in a paleontological aspect, with the slates they overlie
and the limestones above : — |

Krom Hope’s Nose thin limestones. Dr. Kayser’s list :—

Atrypa reticularis. Spirifer curvatus (in typical

Kayseria lens. shapes).

Leptena interstrialis. speciosus.

Pentamerus galeatus. | Streptorhynchus wnbraculum.
|

Rhynchonella procuboides. Cyathophyllum heterophyllum.

Identified by M. Frech on the spot:
Cystiphyllum yesiculosum. | Phacops latifrons.

* Geol. Mag. 1874, p. 1.

ROCKS OF SOUTH DEVON. 501

. Identified by Messrs. Sharman and Newton:

Atrypa aspera. Scoliostoma (Turbo) texatum.
—-— desquamata. Heliolites porosus.
Productus subaculeatus.

From Daddyhole Cove. Identified by M. Frech on the spot:

Cyrtina Whidbornei. | Calceola sandalina.
Pentamerus galeatus. | Monticulipora, allied to M. fibrosa,

In red shaly limestones and shale under Daddyhole Knoll*, at
south end of Meadfoot sands, I obtained Atrypa, Leptena resem-
bling laticosta, Spirifer like speciosus, Phacops, Calceola sandalina,
and Lenestella.

In Torquay Cemetery irregular limestone beds, associated with
slate, furnished Atrypa reticularis and Spirifer speciosus, identified
by Prof. Gosselet.

In shaly limestones turned out of wells at Higher and Lower
Weston Farms, identified by Dr. Kayser: Atrypa reticularis, Spirifer
allied to speczosus, not apparently the speciosus with broader folds.

Weston Wells. Identified by Messrs. Sharman and Newton:

' Arca. | Alveolites.
Chonetes. Favosites Goldfussi.
Orthis. | Cyathophyllum damnoniense.

Limestone north of Bridgetown, Totnes:
Cystiphyllum vesiculosum.

Limestone at Highlands, Totnes:

Alveolites. Cyathophyllum helianthoides.
Stromatopora concentrica.

Reddish-weathered shaly limestones, at base of Brixham limestones, at Chursten
Station :

Favosites Goldfussi. | Heliolites porosus,

As there is absolutely no line of demarcation between the upper
horizon of the Hifelian (the Calceolen-Kalk) and the bedded lime-
stones aboye, this separate treatment of Eifelian limestones and
limestones of the Stringocephalus horizon is purely arbitrary.

2. Middle-Devoman Limestone (Stringocephalus-horizon).—The
Middle-Devonian Limestones of Dartington, Littlehempston, Berry-
Pomeroy, Gatcombe Park, Marldon, Daddyhole, London Bridge
(Torquay), of Anstey’s Cove in part, and of Babbacombe-Down
cliffs belong to the same series; they are usually bluish grey or dark
grey and distinctly bedded. The lower part, at least, of the Torbryan,
Denbury, and West-Ogwell limestone, and probably the limestones of
Whilborough and Abbots-Kerswell, and those between Bulley-Barton
and Wrigwell, south of Dainton, may be bracketed with the above.
But the limestones of Barton, Lummaton, and Yeadown, and those

* Kyamodes, a new genus of Ostracod, was obtained by the Rey. G. F. Whid-
borne in the lower part of the Daddyhole limestone (Hifelian).

Q.J.G.8. No. 183. 2N

502 MR. W. A. E. USSHER ON THE DEVONIAN

between Carey Arms, Babbacombe, and Ilsham, for the most part,
the Kingskerswell and Kerswell-Down limestone mass, the lime-
stones of Woolborough, Langs Copse, Bradley Manor, East Ogwell,
Conniter, and Dornafield, north of Ipplepen, belong to a higher
horizon, in which we may also include the Clennon-hill limestones
and most of the limestones south of Goodrington. Parts of the East-
Ogwell, Woolborough, Kingskerwell, Barton, and Ilsham limestones
may be included in the Upper Devonian. The commonest corals
are Alveolites, Favosites potymorpha, and Stromatopora, whilst in
the lower beds Cystyphyllum vesiculosum, Cyathophyllum hetian-
thoides, and OC. damnoniense are locally common, as also Heliolites
porosus, and Favosites Goldfussi.

The Marldon limestones contain in the lower beds Ampleaus
tortuosus, Cyathophyllum helianthoides, and Cystiphyllum vesi-
culosum.

The age of the West-Ogwell limestone is sufficiently proved by
the occurrence in it, near Chircombe. Bridge, of Stringocephalus.
Receptaculites Neptunt was found in the same locality by Professor
Gosselet; yet three species of Phillipsia, identified by Salter, viz.
P. anticipator, P. Brongniarti, and P. Pengellyi, are recorded by
Mr. Pengelly (in “‘ Notes on Recent Notices,” &c., pt. i. Trans. Dev.
Assoc. for 1874) as having been obtained at Chircombe Bridge*. Cri-
noidal iimestones occur at Denbury and Torbryan ; but crinoidal
limestones are not restricted to particular horizons.

Stringocephalus has been obtained at Clennons-Linhay, near
Ipplepen, and in the Kingsteignton limestone mass, which also con-
tains Heliolites porosus. I can trace no persistent Gasteropod-
horizon in the Middle-Devonian limestone; numerous small Gas-
teropods occur locally in it, as near Stantor, north-east of Marldon.
‘ The limestones betray a tendency to pass into slate near Little
Hempston ; and, as the Marldon, Berry-Park, and Dartington lime-
stones form only the lower part of the larger masses of Ipplepen,
Kingsteignton, Kingskerswell, and Torquay, it seems asif the centre
of the Dartington trough was occupied by slates representing the
middle or upper parts of the Middle-Devonian limestone. As the
Ashburton limestones also die out southward, there is an apparent
replacement of limestone by slate to the south of Torbryan, the
upper part of the limestones being the least persistent.

At Dartington, north of Little. Hempston, and at Dainton, blue-
black slates, ‘similar to those at the base of the Babbacombe cliff,
occur; but the suggestion that these are a type of slates replacing
the medial portions of the Middle-Devonian limestone is not at
present susceptible of proof. Those in the Babbacombe cliff were
compared by Dr. Kayser to ‘the upper part of the Wissenbach and
Goslar slates of the Upper Harz, which belong to the Stringo-
cephalus-horizon.” Mr, Champernowne’s version of the Dartington
structure would entirely confirm Dr. Kayser’s comparison, which is
also in general accord with the facts; but these are of so complex

* These would now be doubtless referred to the Devonian genus Dechenella,

ROCKS OF SOUTH DEVON. 503

a nature, and involve so close a study of local relations, that J must
here merely confine’ my remarks to general conclusions as to the
formation and occurrence of the limestones of South Devon, without
presenting the innumerable local observations on which those con-
clusions are based. |

3. Middle- and Upper-Devonian Limestones.—The massive lime-
stones of Woolborough and Lummaton are so well known through
Mr. Whidborne’s researches that it will be unnecessary to give fossil-
lists; Dr. Kayser correlates the Lummaton shelly limestone with
the upper part of the Middle Devonian. From its massive nature
the structure of the Lummaton limestone, as also that of Barton,
which I correlate with it, is not apparent. ‘The Brachiopod fauna
occurs in a very restricted space, and the rock is there very similar
to parts of the Ugbrooke-Park and other limestone masses on the
border-land between the Middle and Upper Devonian.

The upper part of the Kingsteignton mass, &c., the massive lime-
stones of Chudleigh, Ugbrooke Park, Oldchard, and Ideford belong
to the same general group, as also a considerable part of the
Kingskerswell mass.

The limestones of Barton and Lummaton-are coralline masses,
Alveolites, Stromatopora, and other common forms being associated
with Smithia. In the Barton quarries, Chonophyllum perfoliatuwm
is common, and this form occurs in the Ramsleigh limestone ™*,
associated with Acervularia pentagona.

A part of the Barton limestone is a coral-breccia recemented ; and
in one nearly vertical fissure or fault the fragments also appear
rolled. Whether this phenomenon is due to surf-talus banked on a
mass of coral-growth or not, I leave to the judgment of those better
qualified to form an opinion.

North of the Woolborough quarry, in Langs Copse, I obtained the
following :—

Athyris. | Rhynchonella pugnus.
Atrypa desquamata. | Strophomena rhomboidalis.

Duboisi. | Alveolites.
Rhynchonella cuboides. Heliolites porosus.

Mr. Champernowne, in unpublished notes, mentioned his discovery
of “a fine example of Rhynchonella cuboides at Ramsleigh ” ; and
further, ‘‘ Rhynchonelia cubordes, in Devonshire, is most abundant
at Woolborough quarry and Lummaton hill, near Torquay, both of
which contain occasional Stringocephali” ..... ‘ Kither the first
shell lived earlier in Britain than on the Continent, or. the Stringo-

* With reference to this we find the following query in Mr. Champervowne’s
unpublished notes :—“ Is not the so-called Chonophyllum perfoliatum, E. & H.,
of Ramsleigh, more allied to the genus Ptychophyllum? Milne Edwards and
J. Haime state that it has neither columella nor walls. The latter I admit; but
the central area, either in horizontal or vertical sections, consists of densely
twisted plates (very like what occurs in Ptychophyllwm). |The outer part of
the expansions of which the coral is made up is rounded, plicated, and slightly
granulated on the surface, which expansions, as they near the true central
depression (calice), are crested by a septal ridge.”

2n 2

504 MR. W. A. E. USSHER ON THE DEVONIAN

cephali survived later.” In the same manuscript we find :—* In
cutting the Torquay line at Kingskerswell Station many specimens —
of Acervularia, corresponding to those of Ramsleigh, were found.”
In a quarry near Kingskerswell Station I obtained Leptana inter-
strialis, Orthonota (Oypri wcardia) semisulcata, and fragments of Tri-
lobites.

In the same limestone mass, east of Bulleigh Copse, the limestone
is pale grey and pink, and contains Orthoceras plentifully ; with
this I would compare the limestone on the north of Oddicombe
beach, which is in part red and rich in Orthoceras and lithologically
similar to the rock just mentioned; both probably belong to the
Cubordes-beds.

From what has been said it will be seen that the bedded lime-
stones which succeeded the shelly and coralline bauds representing the
Eifelian limestone became in places the bases for more uninterrupted
-coralline growth, and that that growth was locally continuous to
the earlier stages of the Upper-Devonian period ; but that from pli-
cation and fracture it is impossible to trace the marks of change in
fauna, which during the prevalence of uniform conditions might be
very gradual and local.

§ VI. Tur Asuprineton Vorcanic SERIES.

It is unnecessary to describe the tuffs, schalsteins, and harder dia-
base masses which constitute this series; that has already been ably
performed. We are here concerned simply with the chronology of
this long period of volcanic activity. In the first place, we find that
the volcanic beds are bounded on the north and south by slates,
which are the upper part of the Eifelian slates, as in the vicinity of
Totnes and elsewhere. Eifelian limestones occur here and there at
the base of the volcanic series, as at Highlands, Weston Farms, &c.

Slates are occasionally visible in the volcanic area, as at Parker’s
Barn, where they contain calcareous lenticles, and near Gerston
Cross, where they are dark grey and either partly calcareous or
accompanied by small masses of limestone.

In unpublished notes by Mr. Champernowne we find the fol-
lowing :—‘‘ Tuckenhay Creek, on the west side of the Dart, is along
the line of an anticlinal, with inversion on the north. A strip of
limestones and shale extends about half a mile on the south side,
where one quarry is still worked, very rich in corals.” These beds
are on the same horizon with those near Galmpton Mill mentioned
in the Ashprington paper as rich in Cyathophyllum damnoniense,
Cystiphyllum vesiculosum, &c.*

At Endsleigh, Totnes, limestone is visible in almost undistinguish-
able association with the volcanic rocks. With this may be com-
pared the following note by Mr. C “ At Hazard
quarry, near Sandwell (on south border of the volcanic beds), where
the trap overlies limestone dipping N. at about 10°, the top beds of

* Quart. Journ. Geol. Soe. vol. xlv. p. 337.

ROCKS OF SOUTH DEVON, 505

the limestone, which abounds in Alveolites vermicularis, EK. & H.,
appear to be intimately mixed with volcanic matter, so as to be,
in Sandberger’s words, either a ‘ Kalk-Schalstein’ or Schalstein-
Kalk. A similar intimate blending of material appears to take
place at Factory-hill quarry, near Harbertonford.”

In a note on the site of a Starfish (named by Dr. H. Woodward,
Helianthaster filiciformis), Mr. Champernowne mentioned the low
northerly dip of the Harbertonford limestone, the occurrence, at
Roster Bridge, of numerous “ large Spirifers and other fossils,” and
the predominent cleavage of the limestone *.

At the Lion Brewery, Totnes, a boring was made to a depth of
139 feet in blue slate rock, under blue limestone only 2 ft. 6 in.
thick.

From the above observations it is evident that an extraordinary
uniformity in conditions is manifested by the deposits immediately
preceding the volcanic outbursts, and that the volcanic materials
were poured out upon a muddy bottom whereon masses of shells and
corals were here and there accumulating.

But, as by fossil and stratigraphical evidence, the position of the
limestone patches is proved to coincide with the Eifelian limestone,
we are at once supplied with a reliable date for the commencement
of this phase of volcanic activity, namely the later stages of the
Kifelian deposition. ‘This is borne out by the absence of volcanic
materials in the Lower-Devonian and Eifelian-slate areas.

The Ashprington series may represent continuous or intermittent
vuleanicity up to the middle of the Frasnian ; but, as there are no
newer sedimentary beds above it, no measure of its duration is
furnished in the Ashprington area.

The numerous evidences of volcanic activity outside the Ash-
prington area are so distributed as to suggest local centres of erup-
tion; thus the aphanites and tuffs of Saltern Cove and Goodrington
obscure the relations of the Middle and Upper Devonian, vulca-
nicity having there begun during a late stage in the accumulation
of the Middle-Devonian Limestone. Again a volcanic area north of
Waddeton complicates the relations of the Middle-Devonian lime-
stones of Yalberton and Crabb’s Park and Upper-Devonian slates,
even suggesting partial voleanic activity near Waddeton as early as
the commencement of the Ashprington series. |

It is instructive to find a great development of Middle-Devonian
limestone on the immediate borders of the volcanic materials, north
of Stoke-Gabriel, as it is thereby demonstratively proved that the
accumulation of the limestone took place contemporaneously with
the Ashprington volcanic outbursts. This is further proved by the
occurrence of detached masses of the Berry-Pomeroy limestones in
direct contact with the volcanic series near True Street, east of
Totnes.

Near Yalberton volcanic materials appear to rest on the lime-
stone; but when we consider that these impersistently associated

* Geol. Mag. 1874, p. 5.

506 MR. W. A. E. USSHER ON THE DEVONIAN

materials have since been inverted, plicated, faulted, and chemically
altered to a very great extent, it 1s not extraordinary that we are_
unable to trace the different incursions of the tufts and ashes of the
successive eruptions of this ancient Krakatoa, or to distinguish the
necks from which they emanated.

The Middle-Devonian limestones are frequently dolomitic, and
where this is the case their surface is susceptible of irregular disso-
lution into hollows, wherein overlying tuffs would gradually sub-
side. This state of things no doubt to some extent accounts for the
irregular indentations of the volcanic and limestone boundaries near
Aish and Yalberton; but near Goodrington and Kast-Ogwell the
accumulation of limestone has been distinctly interrupted by local
influxes of volcanic materials. Felspathic tuffs occur in the Upper-
Devonian slates south of Goodrington. North of Little Hempston
the Middle-Devonian slates (replacing limestones above the Eifelian)
contain tuffs and occasionally schalsteins. The limestone of
Dartington is partially replaced by diabase; this is also the case
with the Bickington limestone. At both Bickington and Ashburton
the limestone is overlain by tuffs and schalsteins. The Kingsteignton
limestones are bounded by tuffs, schalsteins, and aphanites, which
appear to be inverted upon them.

North of Broadhempston numerous patches of diabase occur in
Middle-Devonian slates. Between Newton-Abbot and Woodland
there are also an infinite number of diabase and melaphyr patches in
the Upper-Devonian slates. The Babbacombe limestone, which is of
the same age as that of Dartington and Marldon, is plicated with a
mass of diabase, occasionally associated with purple igneous rocks
identical with peroxidated materials in the Ashprington series ; in
the Babbacombe cliff and beach-reefs masses of diahase, in some
places coarsely porphyritic, occur.

Spilosite is frequently noticeable in the Upper-Devonian slates at
contact with the diabase, particularly north-west of Chircombe
Bridge. This type of contact-metamorphism has been recognized in
the Middle-Devonian slates of Babbacombe by Dr. Kayser.

§ VIL. Upper Devonian.

Prior to 1887, Mr. Lee’s find of the Biidesheim fauna at Saltern
Cove, and of the Goniatite-limestones at Lower Dunscombe, and the
Acervularia-limestone of Ramsleigh, were the only proved occur-
rences of Upper-Devonian rocks in this district. In 1887 I dis-
covered inliers of Upper-Devonian slate at and near Livaton in the
Culm-measure area south of Bovey-Tracey, and also near Lewell in the
Chudleigh area. The discovery of Clymenia levigata, in irregular
grey and greenish slates, near Lewell by M. T’schernyschew, and the
identification by Kayser of the red slates beneath them, with Posido-
nomya venusta and Entomis serratostriata, as the Cypridinen-Schiefer
of Nassau and the Harz, supplied a clue to past and future work, as
I hadidentified exactly similar slates in Kingsteignton Railway-cutting
and in Anstey’s Small Cove, Torquay, and had discovered both these

ROCKS OF SOUTH DEVON. 507

forms in them. Several new fossil finds in 1889 have enabled me
to extend the Upper-Devonian districts very much further.

1. Massive Limestones *.

The limestones of Petitor, part of the Kingsteignton mass, the
Chudleigh limestone, the Ugbrooke-Park limestone in part, the
Oldchard limestone in part, the Ideford limestones, and the upper-
most part of the Kingsteignton mass, may be regarded as Upper
Devonian ; as also certain rather thin-bedded limestones on Elbury
Warren and perhaps portions of the limestones south of Goodrington.

The Cuboides-beds form a lower Frasnian horizon than the

Goniatite-beds; and the massive limestones of Chudleigh, Oldchard,
and Kingsteignton are directly overlain by the red, compact, con-
eretionary Goniatite-limestones; whilst the red slates of Petitor
combe, at their junction with the Petitor limestones, contain red
shaly limestone with Goniatites, and also furnished imperfect Gonza-
tites. Again the Ramsleigh limestone is irregularly bounded near
Kast-Ogwell Mill by slates resembling those of Saltern Cove, and
in Hast Ogwell by dark slates containing Hntomis. The Wool-
borough limestone is partly bounded by slates of Upper-Devonian
types.
The Bradley-Manor limestone, near Newton-Abbot, is also
bounded on the north by Upper-Devonian slates. The Barton
limestone, near Marychurch, is nearly surrounded by slates of the
Saltern-Cove type. The junctions of these limestones with the
Upper-Devonian slates are so often abrupt and irregular that they
suggest coralline growths at a much more rapid rate than muddy
sedimentation on their immediate borders, so that Upper-Devonian
slates might be banked against Middle-Devonian limestone in places.

Dr. Kayser’s list from Lower-Dunscombe quarry below the
Goniatite-beds, in light crystalline limestone, is :—

Rhynchonella cuboides. Spirifer bifidus.
— acuminata. Productus subaculeatus.

Atrypa reticularis. Conocardium.
Athyris concentrica. Harpes.

In a small quarry in the Ideford limestone, near Coalmansford,
I obtained Rhynchonella ; comp. Camarophoria formosa, Schnur, and
Rh. near to parallelopipeda, identified by Dr. Kayser, who remarks
“¢ Wohl Oberdevon=Cuboides-Kalk.”’

The Goniatite-beds near Whiteway Farm rest upon a limestone
exactly similar to that of Chudleigh, in which I found a small
Spirifer (bifidus?), Goldius granulatus, Cyathophyllum hevagonum,
and Fenestella.

* Partly Middle Devonian, under which head the same limestones haye also
been alluded to. I do not think it is possible to draw an arbitrary boundary be-
tween Middle and Upper Devonian, below the shaly Goniatite-limestones, in
South Devon; nor is it possible in dealing with the massive limestones to con-
fine the description of such limestones to particular headings. Any apparent
confusion in arrangement is strictly in accordance with the state of the case.

508 MR. W. A. E. USSHER ON THE DEVONIAN

Buckley-Wood quarry, on the opposite side of the valley, yielded
Stromatopora Htipschii, Barg., and <Actinostroma clathratum (?), -
Nich., kindly identified by Professor Nicholson.

The Ramsleigh limestone contains small Brachiopods at a short
distance north of the quarries, amongst them the Rev. G. F.
Whidborne identified Spirifer lineatus, Martin, and Waldhemia
Whidbornei, Dav.

A similar Brachiopod-horizon occurs in a patch of limestone at
Daggers-Mellons Copse between the Broadridge-Wood and Bradley-
Manor limestone masses. Amongst these small Brachiopods may
be, as Dr. Kayser kindly informs me, Nucleospira lens, Schnur,
perhaps Spirifer Urei, Fleming. Mr. Whidborne identified Merista
plebeva.

The fibro-crystalline calcite veins termed ‘“ Stromatactis” by
Dupont abound in the limestones of Petitor and Ramsleigh (or
Ransley), and have also been detected by Prof. H. A. Nicholson in
specimens from Bickley Wood, near Whiteway Farm, and from Upper
Bradley, near Newton-Abbot.

2. The Goniatite-beds.

Some months ago I visited Elbury Cove to test the boundary of
the Brixham limestones and the slates which there apparently
underle them.

These slates exhibit Upper-Devonian characteristics. After a
fruitless search for fossils in them, I proceeded along the coast to
Silver Cove, where more or less massive limestones are apparently
underlain by tolerably thin, plicated limestone, passing down into
red slates and mudstones, through red slates intercalated with thin
bands and plaques of limestones. The whole was so suggestive of
the Saltern-Cove Goniatite-mudstones that I searched diligently,
and was rewarded by the discovery of the Saltern-Cove fauna.
The Goniatites are much crushed; but well-preserved examples of
Cardiola vetrostriata and numerous Bactrites were obtained.
Further investigation proved the junction to be inverted, the thin
beds of limestone occurring in their natural position in the low
cliffs of Galmpton Point.

The Galmpton-Point limestones are full of Alvcolites, and they
resemble the Ramsleigh limestone in colour and texture. ‘The
Silver-Cove and Elbury slates extend as far west as the borders of the
Yalberton volcanic series; and they also occur in Fishcombe Cove,
near Brixham. |

The Upper-Devonian slates of Saltern and Silver Coves are
chocolate-red, weathering to a lilac-red hue, which is distinct from
the colour of the red Lower-Devonian slates, against which they are
faulted at Saltern Cove.

The Silver-Cove and Galmpton-Point limestones seem to be repre-
sented by the limestone bands and coralline masses which occur
in Saltern-Cove railway-cutting, on the beach, and at the point on
the south of the large Cove, in which places, as Mr. Champernowne

ROCKS OF SOUTH DEVON. 509

pointed out, they irregularly overlie aphanites and tuffs. Beds of
concretionary limestone-nodules occur in the Saltern-Cove slates
and mudstones; these are the indications of the knubbly Gonia-
tite-limestones or Kramenzel-Stein and of the Knollen- Kalk.
Wherever we find the Cypridinen-Schiefer in the vicinity of fine,
crystalline, grey limestone, we should expect to meet with a repre-
sentation of the Goniatite-beds; accordingly we find the Isham
limestone most irregularly bounded by red limestone, much crushed,
with calc-spar veins and filaments, distributed so as to suggest
Goniatites or Orthcceras distorted beyond recognition ; and further
from the grey hmestone concretionary limestone beds occur.
The Upper-Devonian slates of Anstey’s Small Cove and [sham are
probably faulted against the massive limestone of Anstey’s Large Cove.
The red slates of Petitor combe contain thin bands and lenticles
of limestone at their junction with the limestone on the south and
north. In one spot on the north side I have obtained Goniatites
sagittarius and several specimens of Goniatites on the south side *.
The red slates of Barton have as yet yielded no fossils; in one or
two places, where their junction with the massive limestone of
Barton can be seen, they are associated with red limestone beds.
Due north of Combe-Cellars, on the north side of the River
Teign, greenish-grey argillaceous slates, with buff, powdery nodules
and lenticles of decomposed limestone, pass down into similar
slates with lenticles and nodules of limestones, very compact and
distributed in beds, as in the Saltern-Cove Upper-Devonian slates.
Near a small patch of Trias, by the river, red slates crop out con-
taining similar nodules of brown powder; in their vicinity I discovered
two Cephalopods on the beach, which had been evidently washed out
of rock, they were sent to Dr. Kayser, who says:—‘‘The smaller
Goniatite (or Clymenia) is unidentifiable. The larger specimen is
probably a Goniatite, but of a species unknown to me.” In some
of the powdery nodules in the slates I detected bivalve impressions,
resembling Cardiola retrostriata. I sent these to Prof. Gosselet,
who returned them with the following identifications, at the same
time recommending me to submit them to Dr. Kayser :—

Gasteropod fragment. Encrinite fragment.
Sanguimolaria ellyptica ?

Cardiola (very near to retrostriata; ornaments effaced).
Chonetes.

Goniatite or Clymenia.

In these fragments Dr. Kayser identified :—

Cardiola retrostriata.
A small Orthis or Chonetes.

These beds are the Knollen-Kalk. The concretionary limestone-
beds are similar to those on the margin of the Ilsham limestone

* The Goniatites were discovered after this paper had been sent in.

510 MR. W. A. E. USSHER ON THE DEVONIAN

near Anstey’s Small Cove, and also to the Goniatite-limestones of the
Chudleigh district and of Oldchard,

The Knollen-Kalk passes under the red slates of the Cy pridinen-
Schiefer, so well exposed in the Kingsteignton railway-cutting, and
in lane-cuttings west of Bishopsteignton. On the south bank of
the Teign west of Combe-Cellars the Knollen-Kalk, consisting of
dark slates with hard concretionary nodules in which no fossils
were found, passes under the Entomis-slates.

In the autumn of 1889, I reinvestigated the boundaries of the
Kingsteignton limestone on the 6-inch scale map; and, in following
its faulted junction with the Culm-rocks from Lindridge Hill
toward Whiteway Farm, discovered a strip of red, compact, con-
cretionary limestone, associated with red and grey slates resting
directly on the massive limestone. Although these beds are cut
out by the fault at Torhill Cottages, they reappear in the form of
the Chudleigh Goniatite-limestone above an abandoned quarry in
grey finely crystalline limestone at 15 chains from Whiteway Farm.
Here we have a-replica of the junction in Lower-Dunscombe quarry,
and I found many very imperfect traces of Goniatites, which on
slicing revealed the septa. Just after this discovery I noticed a
large red limestone block used to cover a drain in Whiteway Farm-
yard, containing a large example of Gonvutites intwmescens, and
traces of other Goniatites, including G. sagittarius, Thinking the
block might have been brought from Lower Dunscombe, which is
two and a quarter miles due north of Whiteway Farm, I questioned
Mr. Soper, the farmer, who assured me that the block had been
quarried on his farm, and had, to the best of his recollection, been
obtained from the neighbouring quarry, viz. that in which I had
shortly before proved the presence of the Goniatite-beds. This dis-
covery, In enabling us to trace the connection of the Goniatite-
limestones with a continuous limestone formation extending from
the Eifelian upward, is of the utmost importance.

Another link in the chain of evidence was obtained at Old-
chard, about halfway between Whiteway and Lower-Dunscombe
Farms. Here the Devonian rocks are faulted against Culm-
measures on the south and west, and concealed on the north by
débris from the Trias and Cretaceous formations.

In Oldchard-Well Farmyard pale grey, finely crystalline, massive
limestones are exposed in a quarry behind the house, where they
are faulted against red shales with plaques of limestone, exactly
similar to those of Silver Cove. Beneath these are thin-bedded,
compact, nodular limestones, which in the adjacent orchard are seen
to rest upon the massive grey limestone. No fossils were obtained
in the farmyard, but between 10 and 15 chains west of it grey and
greenish clay-slates, with nodular pieces of compact limestone, but
more often of pale buff powdery matter resulting from its dissolu-
tion, recall the Knollen-Kalk by the River Teign. These beds rest
on red shales or slates containing red nodular limestone, which is
ploughed up in an adjacent field, and proved to be rich in Clymenia,
associated with very imperfect Goniatetes.

ROCKS OF SOUTH DEVON. 511

Dr. Kayser identified the Clymeniaw as C. levigata and C. annu-
lata.

The Goniatite-limestone of Lower Dunscombe, with overlying red
slates or shales, forms a very small patch, faulted against Culm-
measures on the east and west and overlying the massive limestones
on the north and south, in the form of similar compact, con-
cretionary, red limestones; it also occurs in a triangular patch
bounded by faults at the westernmost termination of Ugbrooke Park,
near the pathroad to Lewell. The Chudleigh limestone is probably
folded or thrust over the greenish slates, which bound it on the
west, the latter being of Upper-Devonian aspect. In the middle
or lower part of the limestone Mr. Clement Reid * found Heliohtes
porosus; the same coral in association with Rhynchonella cubordes
was found by me in the Woolborough limestone in Lang’s Copse ;
hence it becomes a question as to the relative importance of the
Coral or the Brachiopod in determining the Middle- or Upper-
Devonian age of the rocks. There is, however, no reason to object
to the Middle-Devonian age of the lower part of the Chudleigh
limestone.

Dr. Kayser’s list of fossils from the Goniatite-limestones in Lower-
Dunscombe Quarry consists of :—

Goniatites intumescens. Cardiola retrostriata.
acutus. Myalina.
simplex.

Herr Frech identified in these beds, in addition to the above :—

Goniatites complanatus (a variety of intumescens).
Cyrtoceras and Harpes.

Add to these Goniatites multilobatus (G. sagittarius) found by
Mr. Lee *.

In the disturbed districts between Ipplepen and Newton-Abbot,
Upper-Devonian beds have not been detected by their fossils, except
in the case of the Ramsleigh t+ limestone, and the presence of
voleanic materials appears to have irregularly interfered with the
accumulation of the limestones; but it is probable that the red
slates between Woolborough and Abbotskerswell, and those
bounding the Lang’s-Copse limestone, may be Upper Devonian, as
also the slates and tuffs south of Hast Ogwell. Even in this ex-
cessively faulted and complicated district, however, a patch of
Upper Devonian is proved to occur on the south of the faulted
termination of a mass of Culm-measures near Rydonball Cross, be-~
tween Rydon Farm and Abbotskerswell Cross. Here a band of
grey and red, compact, nodular, concretionary limestone, with
irregular yellowish-brown kernels of decomposed limestone, occurs
in red, greenish, and grey slates resembling those of Livaton, Lewell
pathroad, and the Teign Bank opposite Combe-Cellars. These

* Geol. Mag. 1877, p. 454.
t Ibid. 1880, p. 145.
t Ransley on the 6-inch Map.

612 MR. W. A. E. USSHER ON THE DEVONIAN

slates are blackish by the highroad west of Abbotskerswell, and
they contain lenticular limestone (resembling that in the little
quarry at Livaton) at 25 chains south of Rydonball Cross. I have
no hesitation in regarding these beds as Upper Devonian, prebably
representing the Knollen-Kalk and Entomis-slates.

As the Cypridinen-Schiefer has been traced by its characteristic
lithological character and by the presence of Entomis and Posido-
nomya at Newton-Abbot, Highweek, and Houghton, the repre-
sentation of the Goniatite-beds between it and the limestones and
diabases of Bickington on the one side, and the limestones of
Bradley Woods and West Ogwell on the other, is almost demon-
strated.

As the occurrence of Upper-Devonian beds between these lime-
stones is established by the discovery of the Cypridinen-Schiefer
(Entomis-slates), Mr. Champernowne’s correlation of the Ashburton
and Ogwell limestones is demonstratively proved, by synclinal, not
anticlinal structure, as was supposed. This synclinal is occupied by
red, pale greenish, and grey slates, in which fossils are extremely
rare. Py lithological character no line can be drawn in this slate-
area.

Red slates resembling those of Saltern Cove bound the Bradley-
Manor limestone on the north, and can be traced, with varying
characters, to the Lemon Valley opposite East-Ogwell Mill. Near
Kast-Ogwell Mill they contain limestone plaques and are very
similar to the slates of Silver Cove; from the Mull these slates,
varying to greenish and dark-grey tints, may be traced southward
through East Ogwell, where they contain Hntomis, and round the
southern termination of the Ramsleigh limestone.

Following round the limestone border from Bradley Farm to
Denbury, we find a gradually broadening area of grey slates
separating the red and green Upper Devonian, which are continuous
through Woodland, from the limestone. These slates, traced south-
ward, are found to represent the Middle-Devonian limestones of the
Ipplepen and Plymouth districts; they contain shaly limestones
here and there near Staverton.

Here, then, we have the Middle- and Upper-Devonian types de-
scribed in my paper* on the Tavistock district, and an analogy is
presented to the Morthoe and Ilfracombe slates of North Devon,
and the red slates of the Pickwell-Down series.

In the area between Newton-Abbot and Bickington, at Wrigwell
House, 2? miles west of Newton, in pale greenish slates I dis-
covered traces of Goniatites, one though indistinct being perfect,
although, alas, quite unidentifiable. In the same slates I obtained
small Orthocerata or Bactrites. All Dr. Kayser says about these
fossils is ‘scarcely recognizable, but by the matrix probably
Goniatite-slates (= Biidesheim),”

Near Metley, at about half a mile south of Wrigwell House, and
near Killinch, about half a mile west of Metley, I detected traces of

* Trans. Devon. Assoc. 1889.

ROCKS OF SOUTH DEVON. ales

small fossils in similar slates, which appeared to me to resemble
the Saltern-Cove fauna very badly preserved.

These green and lilac slates are not similar to the types of
the Goniatite-beds we have been considering ; but they occur where
we should expect to find Frasnian beds represented ; and therefore,
if the fossils in them in any way resemble the Goniatite-fauna,
they are more likely to belong to it than to other horizons, as we
do not find the Posidonomya venusta and Hntomis in their vicinity.

To the north of the Entomis-slates, which are continuous by
fossils from Newton to Houghton, and by lithological character
from thence to Woodland, [ feel convinced that these practically
unfossiliferous slates would reveal to a patient searcher traces of the
Goniatite-fauna, my find at Wrigwell House being quite accidental,
and the time at my disposal much too limited for protracted search
for fossils.

The relations of the Upper-Devonian slates to the Middle-
Devonian slates and limestones of Chircombe Bridge and Bradley
Manor, as also to the limestone of East Ogwell, are such as
I can in no way account for by ordinary fanlts or plications, but
such as would be explained by thrust-faults, or by the abrupt termi-
nation of the limestones, and the slower rate of accumulation of
muddy sediments on their borders ; for the limestones which these
slates bound at Hast Ogwell and Ramsleigh seem to be higher in
the series than those which they bound at Bradley Manor; and
this difficulty is not to be explained by assuming that the slates in
the former case represent higher Upper-Devonian beds than those
in the latter.

3. Cypridinen-Schiefer (Entomis-slates).

The description of these beds has been almost completed by the
references to them in the previous notes.

They occur in the area between Kingsteignton and Bishop-
steignton, on each bank of the Teign, where the characteristic
Posidonomya and Hntomis, with an occasional imperfect Trilobite
(perhaps Phacops), have been found in them. On the other side of
the Teign alluvium from Knowles Hill, Newton-Abbot (where
contact alteration with diabase has converted them into spilosite in
places), to Highweek and Houghton their occurrence is similarly
proved by fossil evidence. They are recognizable by similar cha-
racteristics near Isham and Anstey’s Smail Cove.

In Whiteway farmyard greenish-grey clay-slates were identified
as Cypridinen-Schiefer by Kayser, who mentions the occurrence of
numerous examples of Posidonomya venusta as well as Trimero-
cephalus cf. cryptophthalmus in them. At Goodrington red clay-
slates contain Posidonomya venusta and Entomis serratostriata.

The faulted inliers of Upper-Devonian slate in the Culm-measure
area between Bickington and Bovey-Tracey contain beds of dit-
ferent lithological type, all of which have their analogues in the
Chudleigh district and in the Upper-Devonian tract between Rydon

514 MR. W. A. E. USSHER ON THE DEVONIAN

Farm and Abbotskerswell, south of Newton-Abbot. ‘Though they
probably represent the Cypridinen-Schiefer for the most part, there
are beds at and near Livaton and Woodhouse which may belong to
a higher horizon. As these beds were mapped on the old 1-inch
sheet in the commencement of 1888, and the fossils obtained,
including numerous Clymenice, Spirifer, and Orthis, have yet to be
specifically determined, I shall not refer more particularly to them.

The discoveries of the extension of the Waddon-Barton horizon,
of the representation of the West-Leigh limestone horizon, and of
the occurrence of Culm conglomerates and of interbedded tuffs or
schalsteins, and other points in connection with the Culm-measures
of this area, are of sufficient interest to constitute a separate com-
munication.

Addendum.—Since this paper was written, Professor Rupert
Jones has had the opportunity of examining many specimens col-
lected in the Entomis-slates (Cypridinen-Schiefer), and his kind offices
enable me to append the following identifications with localities :—

Whiteway Farm, some small oblong Ostracoda (? Primitee).

About a quarter of a mile north-north-west of Whiteway
Farm: Entomis serratostriata (Sandberger), good and abun-
dant; and Entomis Sandberg: (Richter), rare.

South bank of the Teign, west of Combe-Cellars : Hntomzs, very
obscure.

Kingsteignton Railway-cutting, near Hackney: Hntomis serrato-
striata, numerous.

Knowles Quarry, Newton-Abbot: Hntonus serratostriata and
E. gyrata (Richter).

East side of Knowles hill, Newton-Abbot: Entomis serrato-
striata and EH. gyrata.

North of Greenaway Place, near Newton-Abbot: Hntomis
serratostriata ?

Castle-Dyke Quarry, near Highweek: Hntomis gyrata, abun-
dant; H. serratostriata, rare.

West of Western House, near Highweek: Entomis serrato-
striata.

By road west of Western House: Hntomes gyrata.

East Ogwell: Hntomis serratostriata.

West of Livaton: Hntomis serratostriata, rare.

Lane near Lenda Mill, near Livaton: Entomis serratostriata,
obscure.

Anstey’s Small Cove Cliff: Hntomis serratostriata, numerous.

West end of Goodrington village: Hntomis serratostriata,
squeezed and obscure.

I also gladly embrace the opportunity of here expressing my
thanks to Professor Dr. H. A. Nicholson for his kindness in identi-
fying a series of specimens of Devonshire limestones containing
Stromatoporoids.

ROCKS OF SOUTH DEVON. 515

The following may be mentioned :—

Stromatopora Hiipschit, Barg., from Langs Copse, Compton
near Marldon, Buckley Wood.

Dania, sp., South of Colway Cross, west of Bishopsteignton.

Actinostroma hebbornense, Nich., Coombes End Quarry, south of
Whiteway Farm, Daddyhole Knoll, Yarneford Copse
Quarry.

Actinostroma clathratum, Nich., Broadridge Wood.

Actinostroma verrucosum, Goldf., Old Quarry, Coombes End.

Stromatopora buchahensis, Barg., Stantor.

Clathrodictywm, Highlands, Totnes.

$ VIII. Concrusions.

From the above observations it will be seen that by detailed
investigations, aided by the discovery of characteristic fossils, the
Devonian rocks of this part of South Devon fall naturally into
Upper, Middle, and Lower groups, each possessing distinctive litho-
logical and paleontological characteristics, yet also exhibiting in
both respects points of similarity which prevent the definition of
sharp boundary-lines.

The structure of the country, owing to faulting and plication, and
to a still greater degree owing to the impersistence of the limestones,
either from the abrupt termination of organic growth, from gradual
or irregular replacement by slate, or from episodes of vulcanicity
during their accumulation, is only to be interpreted by piecing the
evidence and amalgamating disconnected data to form a connected
sequence.

Although there is no evidence of atolls, and barrier and fringing
reets are out of the question, in a district where volcanic materials
--were being spread beneath the sea during a period in which coral-
line growth was taking place, and the débris of organic existence
actually strewed the sea-bottom upon which the earliest volcanic
ejectamenta were outpoured, it cannot be denied that we have con-
ditions manifested somewhat similar to those which are known to
be favourable to coralline growth in the present day in the Java
seas.

The discovery of Goniatites near Whiteway Farm in beds which
directly overlie massive limestones of the Chudleigh type, them-
selves succeeded by bedded limestones containing Strinyocephalus
and Heliolites porosus, which are separated by inverted aphanites
and schalsteins from slates with both Middle--and Lower-Devonian
affinities, affords, notwithstanding inverted dips, at once, the most.
important and the most connected succession to be met with in
the district.

It will be seen that the irregular unfaulted junctions between
the Upper-Devonian slates and the limestones in some places give
colour to the supposition that the limestones were partly accumu-
lated as coral-banks, and that the muddy sedimentation on their
margin may have taken place at a much slower rate.

516 MR. W. A. E. USSHER ON THE DEVONIAN

From what Professor Gosselet has shown me in the Ardennes,
and on a brief visit to the Kifel, I was greatly struck with the
comparatively recent appearance of the Upper-Devonian shales, —
which reminded me more of weathered Lias- and Oolite-shale, and
of Rheetic shales, in places, than of any Upper-Devonian slates in
Devonshire, where the rocks are much more indurated, compressed,
and cleaved. The same phenomenon is exhibited by the Eifelian
slates of Couvin and of Gerolstein on comparison with the slates of
Berry Park and Mudstone Bay.

In the Lower-Devonian of the Gerolsteiner-Wald, I recognized
similarities to Lower-Devonian rocks in North and South Devon:
and in the Lower-Devonian slate types of St.-Hubert, Oignies, and
Mondrepuits, in the Ardennes, near Fumai, I detected a great
resemblance to the Dartmouth slates. In fact, in the districts where
the rocks had undergone the greatest disturbance the similarity to
those of Devon seemed to be the most pronounced.

As regards South Devon, the facts established in this paper have
a much wider application than to the district described; for De la
Beche’s Map and the Report (pp. 76-79), referring to the geology
of the district from the Dart southward to Plymouth, will show the
existence of extensive areas of Lower Devonian (Cockington beds)
from Morleigh Down and Black Down to the coast at Erme Mouth,
and at Staddon heights and Modbury.

I conclude with the following quotations from Mr. Champer-
nowne’s Notes on the Ashprington series, when referring to the
relations of the volcanic materials to the limestones :—‘‘ all these
anomalous appearances are at the same time quite capable of being
accounted for, if we consider what might take place in a reef
district which was at the same time the arena of volcanic dis-
turbance.”

Referring to the difficulty in distinguishing the slates below from
those above the limestone, he says:—“But why should there not
also be slates neither exactly above nor below the limestone, but
replacing it? So that De la Beche’s words would also be true, viz.
that ‘the geological continuation of certain limestones appears to
consist of slate’”*. ©

Discussion.

The Prestpen referred to the late Mr. Champernowne’s paper on
the Ashprington Series, and to the maps presented by that geologist
to the Geological Survey. The task of dovetailing the Survey-maps
with those of Mr. Champernowne was entrusted to Mr. Ussher,
who had now for the first time made a careful comparison between
the rocks of South Devon and those of the Continent. Dip and
strike went for little in such plicated and dislocated countries as
that which the Author had surveyed, but he had with great patience
and success pieced together the fossil evidence, and had thus brought

* Quart. Journ. Geol. Soc. vol. xlv. p. 377.

ROCKS OF SOUTH DEVON. 517

the different members of the Devonian series in relation to one
another and to those of other countries.

Prof. T. Rurrerr Joves called attention to the distortion of the Os-
tracods. He adopted the term Hntomis-shales, or Entomiden-Schiefer,
for the old and incorrect Cypridinen-Schiefer. Having had some of
the Author’s specimens figured, he exhibited the figures. The genus
passed up into the Carboniferous. Kledenia Wilckensiana, found in
the Warberry Grits, also occurs in the Devonian near Saalfeld.

Prof. HueHes maintained that two horizons occurred at Lumma-
ton, the Stringocephalus occurring at the base of the quarry. The
limestones often thickened, owing to folding, but he believed the
Lummaton succession was a true one. He was quite prepared to
follow the Author’s explanation of the Saltern-Cove district.

The AvrHor, in reply, defended the term slate for the L. serrato-
striata beds. If it were definitely proved that Stringocephalus came
below the very fossiliferous horizon in the Lummaton quarry, he
would be very glad; but fossils were frequently brought from a
distance by the quarrymen.

Q.J.G.8. No. 183. ae

518 MR. S. S. BUCKMAN ON THE SO-CALLED

30. On the so-called ‘* Upprr-Lias Cray” of Down Crrrrs *,
By 8. 8S. Buckman, F.G.S. (Read May 14, 1890.)

In a former paper t I gave a section of part of Down Cliffs, near
Seatown, Dorset ; but I had obtained no evidence of the paleonto-
logical contents of the Bed 19.

Partly, no doubt, on account of its position (only a little above
the Marlstone), and partly on account of its blue colour, this bed has
been called by Day { and by H. B. Woodward § “ Upper-Lias Clay ;”
and I think that I am correct in saying that this term has, in this
country, usually signified those argillaceous deposits which, occupying
avery similar position above the Marlstone, contain the fauna of the
Faleferum- and Commune-zones.

Last summer I had an opportunity of further examining Down
Cliffs, and, after some search, was enabled to procure sufficient
evidence to show what is really the correct horizon of the clay- or
marl-bed in question. The evidence consisted of Ammonites of the
genus Dumortieria; but their condition was unsatisfactory for pre-
servation, since they were little else than impressions or casts in
the marl, and were often crushed. I was, however, able to preserve
a few specimens; and, haying frequently met with similar Ammo-
nites in the Cotteswolds, I was able to determine even those
specimens which I could not preserve. One species I could make
out with certainty, namely Dumortieria radians ||. Accompanying
this, was a wider-ribbed form of the same genus—a genus so easily
recognized by the peculiar straightness of the ribbing. The wider-
ribbed species was most probably Dumortieria Levesquei.

Now, species of the genus Dumortieria are practically confined to
a limited horizon, namely, to strata to which I applied the terms
Moorei- and Dumortieria-beds J, in other words, the base of the
Opalinum- and the top of the Jwrense-zone; and D. radians may be
regarded as a species distinctive of the top of the latter zone. In
that case, this blue marl is really only a part of the Yeovil Sands,
seeing that this species occurs also in them; and this blue marl is
of distinctly later date than the blue clay of the White-Lackington
Section **. Here, then, is a further instance of the later prevalence
of clayey conditions the further we go South.

* This paper consists of notes supplementary to a paper on the Cotteswold,
Midford, and Yeovil Sands, &c., Quart. Journ. Geol. Soc. xlv. 1889, pp. 440—
473. t Ibid. p. 452.

t Day, ‘On the Middle and Upper Lias of the Dorsetshire Coast,” op. cit.
vol. xix. 1863, p. 285.

§ Geology of England and Wales, 2nd ed. p. 276. “The Upper Lias in
Dorsetshire is represented by a clay-deposit,..... which rests upon the re-
markable junction-bed” .....

|| In my former paper (p. 443) this species was alluded to as D. rhodanica.
I must refer the reader to the forthcoming Part V. of my Monograph on
Ammonites (Pal. Soc. vol. for 1890) for the explanation of this matter.

€ Q. J.G.S. vol. xlv. p. 443.

** Tbid. p. 450, bed “ 2,” &e.

‘6 VPPER-LIAS CLAY” OF DOWN CLIFFS, 519

This blue clay or marl lying below the Yeovil Sands contains
Dumortieria radians; but the position of the same species in the
Cotteswolds is in the limestone above the Cotteswold Sands*. In
other words, the blue clay of Down Cliffs is contemporaneous with
the limestone above the Cotteswold Sands of Gloucestershire ; yet the
former is called ‘“‘ Upper Lias,” while the latter has been placed in
the ‘“ Inferior-Oolite Series.”

The names themselves are of no importance. The cause of com-
plaint is that the same paleontological horizon should receive two
names, causing it to appear of earlier date in one place than in the
other.

It is possible to obtain a fairly complete section, from the Middle
Lias to the top beds of the Inferior Oolite, by superposing upon
Down Cliffs the Chideock Hill, which lies just inland to the north ;
and the following is the result :—

Section at Chideock Hill and Down Cliffs.

Parkinsoni- 1. Paleand somewhat shelly limestone, with Parkin- ft. ine

zone. sonia Parkinsom, Terebratula spheroidalis, Wald-
OUR IMCRTANO” Oi icc. cdatwented-nctiawsserreees about 9 O
2. Brown limestone, with small grains .................. by 99
Concavun- 3. Yellow limestone, with very coarse, almost pisolitic,
zone. brown grains; in places much disintegrated ... 1 3
Murchisone- 4, Yellowish limestone, with small dark grains ;
zone. Ludwigia Murchisone, LInoceras bradfordense,

TEGCOCERASIW TIGHT. 35 ics ssciedeecsceadeceees visible for 3 6
5. Small part unseen.
Opalinum- 6. Yellow sands and calcareous sandstone, with Lio-
zone. ceras opalinum, capping the
‘ 7. Yellow sands.

ee }8. Yellow sands with Dwmortieria eee =aaeneny LODO

*/ 9, Blue micaceous (?) shale, altogether more com-

pact. D. radians,and a coarser-ribbed species

of the genus, possibly D. Levesquet............ about 70 0
Commune- 10. Mottled, pink and cream-coloured limestone
and Falci- in two layers; as may be seen from fallen blocks,
Serwm-zones. Hildoceras bifrons is dominant in the upper layer,
and Harpoceras falciferwm in the lower ............ 10
Spinatume- 211. Ironshot limestone, much stained in places ;
zone. WU MOMON CUO URCILOLD ce ccsccecceeddsntsesestsecons 7

Note,—Bed 9 is more clayey below ; and, as it passes upwards, becomes more
of a marl. The Ammonites were found some distance down (12 feet and more).
Nothing was discovered in the lower part of the bed; but, of course, it is
possible that the lower part may contain different species of Ammonites.
When compared with the Cotteswolds, it is seen that the horizons: called Dis-
pansum-, Striatulwm-, and Variabilis-beds—the latter being equal to the Cottes-
wold Sands—should come between the Comiune-zone and the Dumortieria-
beds, that is to say, somewhere in the lower part of Bed 9, or, it may be, partly
in Bed 10.

The section of Chideock Hill differs in one noticeable particular

* The limestone-capping of the Cotteswold Sands, usually called the
Cotteswold Cephalopoda-bed, contains four Ammonitiferous horizons, namely
(in descending order) Moorei-, Dumortieria-, Dispansum-, Striatulum-beds. It
is in the second of these that D. radians occurs.

520 MR. S. S. BUCKMAN ON THE SO-CALLED

from the section at Burton-Bradstock *; and, although somewhat
outside the scope of this paper, it may be interesting to call atten-
tion to it. This is in regard to the bed with Ludwigia Murchisone, ©
from which I collected several fine specimens; but at Burton-Brad-
stock I neither detected this species, nor a bed of similar matrix.

At the neighbouring Symondsbury Hill I found Ludwigia Mur-
chisone and Lioceras opalinum in the same bed; and this bed was
probably on the horizon of “5,” “ part unseen,” at Chideock Hill.
The occurrence of these two species together is a most interesting
fact, rendering it rather difficult to draw any line of demarcation
between the Lias and the Volite at the top of the Opalinum-zone.

Not only do the lowest beds of the so-called ‘‘ Inferior-Oolite
Limestone” belong to the Opalinum-zone, but the upper portion of
the Yeovil Sands as well, a fact which the Burton-Bradstock section
showed very noticeably. (In this case also we have parts of the
same horizon receiving two distinct names.) Further down in the
Sands there is good evidence, at Burton-Bradstock, of the Moorei-
beds (lower part of the Opalinum-zone) with Grammoceras aalense,
&c. Where the JMoorei-beds begin and the Dumortieria-beds
(upper part of Jurense-zone) end cannot, as in the Cotteswolds, be
stated with certainty; but at the base of the Sands of Down Cliffs,
and also in the yellow Sands of Ham Hill, we have species of Du-
morteeria, Showing clearly that the lower part of the Yeovil Sands
belongs to that horizon. This, again, is borne out by the section at
White Lackington, where the argillaceous deposits immediately
below the Sands show the fauna of the Dispunswm-beds, that is, of
the beds next in descending order in the Cotteswolds.

The Blue Clay of Down Cliffs, however, does not contain, so far
as I could discover, any trace of the Dispansum-beds. It yielded
only Ammonites of the Dumorticria-horizon. It is, therefore, of
rather later date than the Clay of the White-Lackington section ;
and still more, therefore, is it of much later date than what is
generally known as Upper-Lias Clay,—namely, the Commumne- and
Falaferum-zones. At Down Cliffs the only representative of the
Commune- and Falciferum-zones i$ to be found in the Pink Lime-
stone, which lies at the base of the blue shaley. It is 10 inches
thick, and really contains two layers. Extended search, judging
from other localities which have been carefully and minutely
worked, would reveal a distinct fauna for each of the beds.

The foregoing remarks furnish additional evidence of the unre-
liability of a grouping which depends on lithological appearances.
This was one of the points of my former paper; and it was because
no satisfactory line could be drawn between the Lias and the Oolite,
as is usually proposed, that I supported the Continental plan of a
grouping upon paleontological grounds, which would combine the
Upper Lias and the lower part of the Inferior Oolite under the term
“'Toarcian.” The following statements in support of this view may

* Op. cit. p. 451.
t -Op. cit. p. 458.

‘‘ UPPER-LIAS CLAY” OF DOWN CLIFFS. .o21

be here noticed. In 1865* and subsequently + Brauns ends the
Lias with the Amaltheus-zonet; he unites as ‘“‘Toarcian”’ ‘* Der
obere Lias und unterste braune Jura” §; he also speaks of this
as the ‘ Falciferenschicht ” ||; and he commences the ‘‘ Unteroo-
lith ” with the “ Coronatenschicht ” 4]. Branco** states that in
Alsace-Lorraine the Lias ends most naturally with the zone of
Amaltheus costatus ++, and he finds no sharp line of division from
the Posidonomya-beds until the zone of Harpoceras Sowerbyt tt

Haug $§ says that the zones of Opalinum and Jurense are so
closely united by what are practically the same species that one
cannot draw the line separating Lias and Oolite as the Germans
wish ; further, that the zones of Murchisone and Opalinum are quite
as closely connected ||||, and he is of opinion that, from a palonto-
logical point of view, the division at the base of the Sowerbyi-zone
is the most practicable 74.

These opinions are worthy of attentive consideration. When the
views of d’Orbigny, Deslongschamps, Vacek ***, and Lepsius Tf are
added to the above, and also the facts which Hudleston ttt so
constantly impresses upon us concerning the difference between the
Upper and Lower divisions of the Inferior Oolite, it will be seen
that there is a very strong case in favour of a division like the
Toarcian.

Discussion.

Mr. H. B. Woopwarp observed that Mr. Day had, in 1863, first
described in the Down Cliffs a band of limestone forming the junction
of Middle and Upper Lias. The lower portion, an ironshot-limestone
(Marlstone), yielded Ammonites spinatus and A. crassus, and the.
upper portion, a pale limestone, A. befrons; while, common to both
portions, Mr. Day found A. communis, A. Holandrei, A. serpentinus,
and A. radians. He had himself found A. striatulus in the base of
the Upper Lias at Down Cliffs and at Allington near Bridport. The
same lithological characters and stratigraphical succession, and the
same assemblages of fossils, characterize the Marlstone and the base-
ment-beds of the Upper Lias from Dorsetshire to Lincolnshire. He

oF “ Die Stratigraphie und Palaontologie des siidéstlichen Theiles der Hils-
mulde,” Palseontographica, xiii.

+ Untere Jura in Nordwestlichen Deutschland, 1871.

+ Die Stratigraphie, p. 85. SU Us tevle Wes ess jp. 90.

** “ Untere Dogger,” Abhand. zur geol. Spez.-Karte Pibeeathicaen! Bad. ii.
Heft i. 1879.

ih py lal. t p. 140.

s, * Polymorph,” Neues Jahrbuch fir Tabane &e., Bd. i. 1887,

‘i | aetie my remarks, p. 520.

“(4 Haug would extend the Lias to this point, as Vacek wishes; but I prefer
the division Toarcian for the period dominated by the Hi/doceratide or the
Falciferi.

**¥* Quart. Tourn. Geol. Soc. vol. xlv. p. 466.

i Tt} Beitrage Jurass. Unter-EHlsass, 1875.

tit Inf. -Oolite Gasteropoda, Pal. Soe, vol. xl. p. 26 et seg.

Q. JaGs:, Noy des: 2°?

522 ON THE SO-CALLED ‘‘ UPPER-LIAS CLAY” OF DOWN CLIFFS.

read lists in support of this view, showing that forms identified as
A. radians and A. striatulus occur with the ordinary characteristic
species in the basement-beds of the Upper Lias, as far as Lincoln-
shire. Hence, while accepting the Author’s facts, he could not
accept his conclusions, as by so doing we should abolish the Upper
Lias throughout the country.

The occurrence of A. opalinus with A. Murchisone was interesting.
Such an association of two zonal forms was common in the Lias, in
the case of A. margaritatus and A. spinatus, &e. He pointed out
that the Author appeared to settle his zone in defiance of strati-
graphical evidence, by range of species rather than by the assem-
blages of forms, upon which he (the speaker) would himself prefer
to lay stress.

Mr. Huptxston pointed out that we had here a test case as to the
relative value of lithological and paleontological characters in deter-.
mining horizons. At Down Cliffs he thought the Author was practi-
cally correct in his contention that the clays were a continuation of
the Yeovil Sands with Ammonites of the upper part of the Jurense-
zone. He had very little doubt that, in the main, the Author’s
Ammonite-horizons were accurate; and that, when a predominance
of any particular Ammonite occurred, it indicated a definite horizon,
whatsoever might be the lithological characters of the horizon. He
was surprised at Mr. Woodward’s remarks concerning the comming-
ling of forms in the Marlstone, including species usually characteristic
of the Jurense-zone. He could not understand this, and laid great
stress on the desirability of collecting fossils inch by inch, as other-
wise zones might easily be missed. He felt that the statement that
such forms as Amm. margaritatus, spinatus, bifrons, communis, and
radians occurred together should be challenged ; for if they did, the
whole question of the identification of strata by organic remains was
attended with extreme difficulty. He, however, objected to the
introduction of the term “ Toarcian” in the sense used by the Author ;
for English geologists were the best judges of what were the proper
divisions of their own Jurassic rocks, and M. de Lapparent was
on the side of the British geologists so far as to include the
“ Miliere” of Normandy (zone of Amm. Murchisone and opalinus)
in the Bajocian. On purely paleontological grounds he thought
the best line between Upper Lias and Inferior Oolite was the base
of the Opalinus-zone.

Mr. H. B. Woopwarp did not wish to assert that the forms
identified as Amm. radians and A. striatulus were common in the
Marlstone or Upper Lias.

The Presrpenr thought that there was a tendency to aim ata
too artificial precision of paleontological zones, and to regard these
as everywhere applicable. He believed that in Nature there were
no hard-and-fast lines, either lithological or paleontological. As
regards tracing lines for cartographical purposes, he did not know
how this could be done without some lithological characters upon
which to depend, and he would be very sorry to see the line which
Mr. Woodward had drawn done away with.

ORIGIN OF THE BASINS OF THE GREAT LAKES OF AMERICA. 523

fittihes NAV 11890

31. Ortein of the Basrys of the Great Laxss of America. By J. W
Spencer, M.A., Ph.D., F.G.S. (Read April 16, 1890.)

ConTENTS.

. Introduction.
. Features of the Ontario Basin.
Erie Basin.
A » Huron Basin.
Features of Lake Michigan.
. Buried Valleys revealed by Borings.
. Glaciation of the Region.
Former High Continental Elevation of North America.
. Deformation of Raised Shores and Beaches.
Conclusions from the Observations.

9 39

S69 WO AVS? Ore OO DO

—

1. Lntroduction.

Even as recent as a decade ago very little was known as to the
origin of the Great Lakes of North America. Whilst we find such
generalized statements as ‘“‘most lakes are due to terrestrial crust-
movements,” yet such crust-movements had not been tested in the
American lake-region. Again, from the time of early geological
investigations in America, statements are found that the basins were
the result of erosion; but the methods of erosion were not explained,
and this was the more necessary as most of the basins have rock-
bound outlets. Later, in some geological literature, the method of
excavation was hypothetically attributed to glaciers. Such was the
unsatisfactory condition of our knowledge of the problem when the
writer first commenced the study, in attempting to solve the origin
of the Dundas Valley, at the western end of Lake Ontario, more than
a dozen years ago. ‘This investigation has developed results bearing
not only upon the origin of the lake-basins, but also upon the phy-
sical history of the lakes, and broader questions of the building and
sculpturing of the continent.

The methods of investigation have been the studying—(1) of the
hydrography of the modern lake-basins and submerged channels upon
the coast of America; (2) of the deep wells bored into, or through,
the Drift deposits, by which buried channels, and their relation to
or contrast with the modern valleys, have been discovered ; (3) of the
elevation of the continent ; (4) of the direction of the glaciation in the
lake-region ; and (5) of the now high-level beaches, in which are
recorded continental uplifts, together with the deformation of the
old surfaces, owing to unequal terrestrial movements or warpings of
the earth’s crust*. The lakes which have been the basis of the more
careful investigation are Ontario, Erie, Huron, and Michigan, with
the respective altitudes of 247, 573, and, of the last two, 582 feet
above the sea (see the Map, p. 524). }

* Tn the ficld-work I here acknowledge the assistance of Professors D. F. H.
Wilkins, W. W. Clendenin, and W. J. Spillman.

Q.J.G.8. No. 184. roa /-p 890 2a

DR. J. W. SPENCER ON THE ORIGIN OF THE

524

SS

S3IIW OO OS O09 Ob ozo
s1v9s

ANA
BY hen

Gm

Sonim ——
Neep ints i
————— et <x

‘x ZB:
OfSHULTT

RY
‘vos ON
OY} PAOGV Joog ZZ), VOIUIIG “Jooy
ZSG ULSTIYOIPY puw uoangT ‘yooy
CLE MM “02S LFS OlLVJUQ ov]
‘OLIVJUGQ oyey Ut
quoudavosy passourqnd *y ‘9
‘MOAN TT oye] Ut
quewuduvossp posaouqng *y ‘p

‘MOTPLIOVPL) JO WOLOAI(T a

"sayvT way 242 burmsof pun paron

Vee Mu Bt
ws AS Aly
“SS

7)

anvijzaaano |e

LOTS

30S C Drwmbuif il
—a gos < Y,

4sqo

mou

‘Layo yj wnrywa

p °w2107

bP 2OLINGT

Ava

SSUSAVYL

unyT quawup ayn fo abur

una ayp fo

copy

.

-

On
bo
O1

BASINS OF THE GREAT LAKES OF AMERICA.

2. Features of the Ontario Basin.

Lake Ontario, as was shown in an earlier publication *, is a basin
bounded on its southern side by escarpments, often precipitous, of
which some of the steps are now submerged. At the foot of the
submerged escarpments a valley like that of an ancient river may
be recognized from the western part of the lake to near the eastern
end, but there it disappears, for reasons to be noted later. The
deepest part of this valley is 733 feet beneath the surface of the
lake. From this trough the floor of the lake rises gradually, or with
occasional low steps, to the northern shore. In short, the basin was
once an old land-valley traversed by a river. At the western end
of the lake borings have revealed an old channel, having a lateral
depth of 292 feet. This is the continuation of the canon of the
Dundas Valley, which is about two and a half miles wide, bounded
by rocky walls nearly 500 feet high, capped with Niagara Lime-
stone. Down this valley the waters of the ancient Erie basin once
flowed rf.

If the waters of Lake Ontario were withdrawn, its present basin
would be a broad valley, continuous with that of the St.-Lawrence
valley, having a breadth of thirty or forty miles. Into this plain, at
a point about twenty miles east of Toronto, there is a channel, ap-
proaching the shore, whose bed is 474 feet below the surface of the
lake +, but with boundaries submerged to only 200 feet. This de-
pression trends southward and joins that at the foot of the sub-
merged escarpment before mentioned §.

3. Features of the Erie Basin.

The floor of Lake Erie is a broad flat plain, now rarely submerged
to a depth of more than 84 feet, and usually less. Only a small
area, situated directly south of the western end of Lake Ontario, is
of greater depth, and there the greatest sounding is 210 feet'||.
But from this region the Erie Valley was drained by the Grand
River and Dundas Valleys into the western end of Lake Ontario, as
was shown in 1881; for the Niagara river did not then exist.
Numerous tributaries of the modern shallow lake flow over deeply
buried channels, the deepest of those discovered being 228 feet
below the lake-surface, as described by Dr. Newberry 4, although
the floor of that portion of the lake is nowhere over 84 feet below
the surface of the water.

Similar channels, buried to depths below the floor of the eastern
end of Lake Erie, near Buffalo, have been described by Dr. Julius
Pohlmann**, The borings into many others in the region of the

* “Discovery of the Preglacial Outlet of the Basin of Lake Erie into that of
Lake Ontario,” by J. W. Spencer; Proc. Am. Phil. Soc., Philad. 1881.

t See “ Discovery of the Preglacial Outlet of Lake Erie,” &c.

+ See British Admiralty Chart of Lake Ontario.

§ See U.S. Lake-Survey Charts of Lake Ontario.

| See U.S. Lake-Survey Chart of Lake Hrie. 4 Geology of Ohio.

** Paper read before the Amer. Assoc, Advance. Science, 1883. -

2@2

526 DR. J. W. SPENCER ON THE ORIGIN OF THE

western end of the lake have been recorded by Prof. T. Sterry Hunt*,
and prove the existence of similar buried channels.

The original recognition tT of the valley-like character of the
basins of Ontario and Erie was based upon the above-mentioned
characters, and upon others now supplemented by a more perfect
collection of facts; but the greatest difficulty was in the occurrence
of the rock-bound outlet of Lake Ontario, a difficulty which obser-
vations have at last dispelled, as will be seen later on.

4, Features of the Huron Basin.

The southern half of Lake Huron is a plain traversed by valleys
and submerged to form only a shallow lake. Northward of this
shallow basin, and extending obliquely across the lake for ninety
miles, there is a submerged escarpment rising to a height of from
300 to 450 feet, facing north-eastward. The deeper part of the
lake then trends northward in the direction of Georgian Bay. At
one point the extreme depth of the submerged valley reaches 750
feet. The absolute depth of the rock in the deepest channel between
Lake Huron proper and Georgian Bay is not known, but soundings
show 306 feet; and as there 1s a deep channel upon the western side
of Georgian Bay it becomes highly probable that a deeper and con-
necting channel is filled with Drift, like those known to occur else-
where, beneath the lakes. From the straits, between the islands,
the narrow channel in Georgian Bay, just referred to, extends
south-eastward and is submerged to a depth of 510 feet. This is at
the foot of the Niagara escarpment, which extends, as a strong to-
pographic feature, from the head of Lake Ontario, and, rising in places
to 1700 feet above the sea, into the peninsula between Georgian
Bay and Lake Huron proper. The channels at the foot of escarp-
ments, submerged or otherwise, in Lake Huron and Georgian Bay
are fragmentary records of the history of the lake-valleys ¢.

5. Features of Lake Michigan.

This lake is divided into two basins. The more northern and
larger basin has a maximum depth of 864 feet. It is, in part,
bounded by vertical submerged escarpments, one of which, upon the
eastern side, has a height of 500 feet. Whilst the deepest sounding
at the modern outlet of the lake is only 252 feet, there are adjacent
channels buried to unknown depths. But these have been imper-
fectly explored. Into this shallower portion of the lake, however,
the fjord of Grand Traverse Bay has a northernly trend; it is
612 feet deep. This and the lesser fjords indicate the existence
somewhere of a deep channel connecting with the Huron basin, as
much as the river-valleys buried beneath the Drift materials of the
modern floor of Lake Erie prove deep channels throughout that

* See Reports Geol. Canada, 1863-66.

t See “Discovery of the Preglacial Outlet of Lake Erie,” &e.

t See U.S, Lake-Survey Chart of Lake Huron, and the Canadian Chart of
Georgian Bay,

BASINS OF THE GREAT LAKES OF AMERICA. 527

basin, although not shown by the soundings ; for the Lake-Michigan
valley is carved out of undisturbed and almost horizontal Palaeozoic
rocks, the newest of which are Coal-Measures.

The southern basin of Lake Michigan is separated from the:
northern by a plateau submerged to a depth of from 300 to 342 feet ;
whilst the southern basin itself is now 576 feet deep. The area
of this portion of the basin is now much smaller than that of the
Prepleistocene valley, as its margins have been filled with Drift,
and now form broad plains bounding the lake. Beneath these de-
posits is a deeply buried channel, leading to the valley of Lake
Huron, and to be noted further on.

6. Buried Valleys revealed by Borings.

The deep wells revealed the existence of the buried channel down
which the waters of the Erie Valley originally drained, and thus
established the relationship of the Erie with the Ontario Basin.
But the most important series of borings were those between Geor-
gian Bay and Lake Ontario, for here we have the connecting-link
between the valleys of the upper lakes and that of Lake Ontario,
and indeed the key to the origin of the valleys of the lakes.

Between Georgian Bay and Lake Ontario, a distance of about
95 miles, a portion of the country is comparatively flat or com-
posed of a series of rising plains; but there are also high trans-
verse ridges of Drift, having a general trend of east and west. It
is upon the northern side of the Drift ridges that Lake Simcoe, with
a diameter of about twenty miles, is situated. But upon the
northern side of Lake Simcoe there is another series of Drift ridges
trending towards the north-east. Both of these series of ridges rise
to between 200 and 550 feet above Lake Huron, these measurements
being the extreme variation in their height.

From Georgian Bay to near Lake Simcoe, for a distance of thirty
miles, the country is low and flat, with a known absence of rock to
far below the level of the bay. Lake Simcoe is 140 feet above
Georgian Bay, but upon its northern side, at Barrie, a well has been
sunk in the Drift, without penetrating it, to a depth of 280 feet
below its surface. Thirty miles further inland, south of Lake
Simcoe, at Newmarket, a well was in the process of being bored.
It had reached a level below Georgian Bay and was yet in Drift
deposits when visited. In another well, several miles to the west-
ward, near the side of the ancient buried valley at Beeton, rock was
reached at 50 feet below the surface of Georgian Bay.

Between Newmarket and Richmond Hill there are several deep
wells on the heavy Drift ridges which cross the country. But at
Richmond Hill, at a height of 217 feet above Georgian Bay, there
is a well 400 feet deep without penetrating the Drift. This proves
the thickness of the Drift of the higher ridges crossing the old
Valley north of the well to be not less than 700 feet in the old
channel. Southward of Richmond Hill the country falls away in a
series of more or less rolling steppes to Lake Ontario, but these

528 DR. J. W. SPENCER ON THE ORIGIN OF THE

plains show the absence of rock along deeply-cut valleys to far below
the level of the upper lakes. Upon the western side of this chain
of borings, but a few miles distant, there is the Niagara escarpment.
Upon the eastern side of Lake Simcoe the country is covered with
flat limestones, rising to 150 feet above thatlake. From the known
absence of rocks along the line of borings and stream excavations,
between a high mountainous escarpment upon one side and a rocky
floor upon the other, and from these borings reaching to 200 feet or
more below the upper lakes, without penetrating the Drift but stop-
ping in quicksand, there has been discovered the existence of the only
channel of antiquity which could now draw off the waters of the upper
lakes, if the Drift were removed. Although none of the borings have
reached the original rocky floor, yet the depth of the buried valley
is suggested by the channel close upon the northern side of Lake
Ontario, now submerged to 474 feet, which is deep enough to drain
the last drop of water out of Lake Huron.

We have now found one continuous channel from Lake Michigan
through Lake Huron and Georgian Bay, and thence buried beneath
Drift deposits until it is again recognizable throughout nearly the
whole length of Lake Ontario, being joined at the western portion
by an ancient outlet of the Erie Valley (the ancient Hrigan River).
But the relative maximum depression of the channels, as far as ex-
plored, is disturbed by terrestrial warpings to be described hereafter.

Across the southern part of the peninsula of Michigan, between
hills rising upon either side to heights of sometimes 800 or 1000 feet
above Lake Huron or Lake Michigan, there is a valley whose western
portion is occupied by the Grand River, and the eastern by a small
river emptying into Saginaw Bay. At the divide between these
rivers the land does not exceed 100 feet above the lakes. The topo-
graphic features of the valley show its original opening as having
been into the Huron Valley by Saginaw Bay; but a considerable
proportion of the modern drainage is in a direction opposite to that
of the valley, or flowing towards Lake Michigan—that is, the drain-
age has been reversed. The maximum depthof the western portion
of this buried valley is not: known, but there is an absence of rock,
as shown in several borings, to between 100 and 200 feet below the
lake-level. But farther east in this trough there are several deep
wells, in one of which the Drift is 500 feet below the floor of the side
of the valley, or 350 feet below the surface of Lake Huron*. Hence
we have established the great depth of the buried valley between
the southern part of Lake Michigan and Lake Huron, whose ancient
river I name the Huronian.

Other buried valleys and channels submerged could be given, but
they all indicate the origin of the basins of the lakes as the valleys
of a great riverand its tributaries—a river of such high antiquity that
the rains and rills had already ground off the surrounding hills to
broaden the valleys. But for all this evidence, there are now rocky
barriers forming an apparent obstacle in the way of a complete
solution of the problem.

* This is at the Sanitarian Well at Alma, Mich., the record being furnished by
Prof. Charles A. Davis,

BASINS OF THE GREAT LAKES OF AMERICA. 529

7. The Glaciation of the Region.

At the present stage in the investigation this subject can be quickly
dismissed. The question whether glaciers can erode great lake-
basins is hardly pertinent, for nowhere about the lakes is the glaci-
ation parallel to the shores or vertical escarpments which are asso-
ciated with the lakes. Indeed, the direction of the striz is often
at high angles, even to 90°, to the trend of the vertical walls of rock
bounding or crossing the lakes. Nor are the faces of these great
walls of limestone polished by an agent moving along their faces.
That there are no striz parallel to some local inlet or valley would
be perhaps rash to assert ; but, if so, it is a mere coincidence, with no
bearing upon the origin or moulding of the Great Lake-valleys.
Hence we are forced back upon a conclusion that the lakes were
subaérial valleys in spite of the barriers, and the fact that the floors
of most of the basins are below sea-level—that of Ontario being
nearly 500 feet.

8. The former High Continental Elevation of North America.

If the lakes and valleys originated from atmospheric and river
erosion, then the continent stood at much greater elevation than at
present, as shown by the depths of the lakes themselves. But there
is much collateral evidence that in the later Tertiary days, probably
during the Pliocene, the continent was very high. This is shown by
the submerged valleys of the St.-Lawrence Gulf, of the Gulf of Maine,
off New York, at the Mouth of the Mississippi River, upon the Pacific
coast, and in Hudson Strait. These indicate that eastern America
stood for long ages at between 1200 and 1800 feet above its present
altitude ; and the whole continent in more recent times, but for a
briefer period, at upwards of 3000 feet *. Hence the former con-
tinental elevation was sufficient to satisfy all demands for the erosions
of the lake-valleys ; but the rocky barriers still demand explanation,
both on account of the present obstructions not having impeded the
erosion of the valleys, and on account of their subsequent closing
the valleys, in part, into lake-basins—the necessary observations for
the explanation having long eluded investigation.

9. Deformation of Raised Shores and Beaches.

At the close of the episode of the newest Till, the region of the
Great Lakes was submerged to a depth of at least 1700 feet, as is re-
corded in the beaches which overlie the Till. These high beaches
only remain as fragments about ancient islands ; butif we descend
to beaches of lower levels we find them well developed and contain-
ing all the necessary evidence for explaining the rock-barriers at the
outlets of the lakes. Gen. G. K. Warren, Corps of Engineers,
U.S. A., was the first to suggest the closing of the lakes by warp-
ings of the Earth’s crust’. Portions of the high-level beaches
_* “High Continental Elevation preceding the Pleistocene Period,” by J, W-

Spencer, Bull. Geol. Soc. Am. vol. i. 1889 ; and Geol. Mag., May 1890.
+ Appendix 13, Report of Chief of Engineers, U.S. A., 1875.

e

530 DR. J. W. SPENCER ON THE ORIGIN OF THE

about the lakes have long been noted. But it was Mr. G. K. Gilbert
who first connected the beaches upon the southern and eastern sides
of Lake Ontario, and measured their great rise towards the north-
east; but, as he did not apply his discovery to the explanations of
the lake-basins, it was first applied by the present writer*. The
results of Mr. Gilbert’s investigations of beaches in New York and
Ohio, and of the writer’s researches in Canada, Michigan, New York,
and elsewhere, are sufficient to form a chapter by themselves, and are
still mostly unpublished, but I will draw upon them only to the
extent of explaining the barriers across the outlets of the old valleys.

The most important raised beach of the Ontario basin is the
Iroquois t. At the western end of the lake it now rests at 363 feet
above the sea, but rises slightly to the east and still more towards
the north, until at four miles east of Watertown it is 730 feet above
the sea. Still further north-eastward, near Fine, on the borders of
the Adirondack Wilderness, it reaches an elevation of 972 feet above
the sea, beyond which I have made no instrumental measurements.
At the western end of the lake the uplift is scarcely two feet in a
mile in the direction of N. 28° EK. At and beyond the north-
eastern end of the lake the uplift 1s found to have increased to five
feet in a mile, and in the region of farthest observation to somewhat
more, in a north-eastward direction. Thus in the deformed water-
level I have already measured a barrier of about 609 feet raised up
at the outlet of the lake. Of this, about 530 feet is confined to the
region of and beyond the eastern end of the lake, where the later
Pleistocene barrier across the ancient Laurentian Valley has ap-
peared. Whilst we know what are the maximum soundings in the
river, yet the old channels are so filled with Drift that their depths
are not revealed. Still, we know that in one portion of the channel
cut out of limestone and more or less filled with Drift, the sounding
is 120 feet. A short distance beyond, the channel across the Lau-
rentian gneisses shows soundings of 240 feet. The maximum depth
of the lake-basin is 738 feet. The deformation recorded in the
beaches is more recent than the episode of the Upper Till. Conse-
quently, if the continent were at a high level, with the warping,
known to have occurred since the Drift was deposited, removed, as
shown by the above figures, there would be not only no barrier, but
a sufficient slope in the Laurentian Valley for the drainage of what
is now the Ontario Basin.

Furthermore, the presence of the rocky barriers of the Rapids of
the St. Lawrence, further east, are wholly accounted for by the
terrestrial warpings of the region. Hence I have demonstrated, after
a decade of study, that no barrier existed across the Ontario Valley
when it was being carved out by the ancient St. Lawrence, and that
this barrier is of quite modern origin.

South-east of Georgian Bay the average measured warping is four

* See “Notes on the Warping of the Earth’s Crust in its Relations to the
Origin of the Basins of the Great Lakes,” Amer. Nat., Feb. 1887, pp. 168-71.

t “Troquois Beach ; a Chapter in the Geological History of Lake Ontario,”
Proc. Roy. Soc. Canada, 1889.

BASINS OF THE GREAT LAKES OF AMERICA. 531

feet per mile, in mean direction of N. 20° E. This will account for
a portion of the barrier closing the Georgian outlet of Lake Huron.
The more elevated beaches in the region of Lake Huron record a
still greater change of level.

At the outlet of Lake Erie, Mr. Gilbert and myself find a differ-
ential uplift of about two feet per mile, and this is sufficient to ac-
count for the recently formed basin of Lake Erie.

The warping affecting the Michigan Basin has been that towards
the north and east; and even in the buried channels south of
Lake Michigan there is no evidence of an ancient drainage to the
south, as their beds were too high compared with those of the
northern, although the latter have been elevated recently by warping.

10. Conclusions from the Observations.

The valleys of the great lakes here studied are the result of the
erosion of the land-surfaces by the ancient St. Lawrence (named
Laurentian) River and its tributaries, during a long period of con-
tinental elevation, until the streams had reached their base-lines
of erosion, and the meteoric agents had broadened the valleys. This
condition was at the maximum just before the Pleistocene period.

The closing of portions of the old Laurentian Valley into water-
basins occurred during and particularly at the close of the Pleis-
tocene period, owing, in part, to Drift filling some portions of the
original valley, but more especially to terrestrial warpings of the
Earth’s crust, which, to a sufficient degree, is measurable.

DIscuUssION.

The Cuarrman noted that there were one or two Fellows who had
a local knowledge of the area, but the question of the origin of lake-
basins in general was raised in the paper.

Dr. Hiyp# did not think that Dr. Spencer’s explanation of the
origin of the American lake-basins was the true one. The sub-
merged deep channels of the alleged ancient rivers, to which the
lake-erosion was said to be due, were traced towards the east end of
Lake Ontario, where they ceased; and their discontinuity through
the barrier formed by the hard gneissoid region of the Thousand
Isles was attributed to differential elevation, or so-called earth-
warping. This assumed warping where barriers existed could
always be brought in to account for them. He (the speaker) asked
where the beaches existed near Kingston, at the east end of Lake
Ontario, on the difference of level of which. the supposed warping was
based. From his own observations on the region, he doubted the
existence of the alleged buried channel between Lakes Huron and
Cntario, and he did not think that the acknowledged great thickness
of Drift now covering the elevated area between these lakes should
be regarded as proof of the presence of a former channel directly
connecting them. With reference to the supposed old channel
between Lake Erie and Lake Ontario, by way of the Grand River
and the Dundas valley, the water of Lake Erie was supposed to

5a2 DR. J. W. SPENCER ON THE ORIGIN OF THE

have run w» the valley by which the Grand River now came down
to the lake. All these lakes and the elevated regions between -
them had been covered by glaciers, and their movement had been
in a contrary direction to that of the present water-drainage ; aud
judging by the amount of drift-material transported by the ice from
the lake-basins over the adjoining land-surface, he believed that the
glaciers had been important factors in their excavation. If, on the
Author’s views, there had been a recent submergence to the extent
of 1700 feet, where were there traces of marine remains over the
lake-region west of the meridian of Kingston, though such were
not uncommon in the clays of the St. Lawrence and Ottawa rivers ?
Also, on the Author’s hypothesis of a former great lake whose
surface would be at a considerable elevation above the sea, what
barrier was there at the south end of Lake Michigan, near Chicago,
to keep such a lake from draining into the Mississippi valley ?

Prot. Bonney thought that Dr. Hinde’s criticism was not a valid one,
as he had not understood that the Author denied the occupation of the
lakes by ice, though he did not uphold their glacial origin. He could
not understand the formation of Georgian Bay by ice and the pre-
servation of Manatoulin Island. He was struck with the similarity
of the Author’s sections and those of the Lake of Como, published by
the late Mr. J. Ball, which he had previously shown to be adverse to
the glacial theory of the origin of lake-basins. It was not safe to
argue from the absence of remains of marine organisms ; for else-
where they were commonly wanting in deposits formed under cir-
cumstances similar to these, yet undoubtedly marine. He, again,
could not follow Dr. Hinde in his objections to differential movements
of the earth’s surface, and insisted on the great movements of recent
times, as evidenced along the Frazer River and in Norway. Only
last autumn he had seen distinct evidence of comparatively modern
depression along the Dalmatian coast. He suspected some changes
even in historic times. The buried river-channels described by the
Author were paralleled in Switzerland. He did not deny the
efficiency of ice to produce some effect, but it did not bring about
what had been attributed to it by some geologists.

Dr. Irvine congratulated the Author on the results he had placed
before the Society. He thought Dr. Hinde had not followed
Dr. Spencer’s arguments throughout, as, for instance, in the case of
the connexion between Huron and Ontario. He was glad to find the
main points of his own theoretical conclusions as to the inability of
ice to excavate confirmed by the Author’s observations in Norway and
America. He saw nothing startling in the “ warping” hypothesis.

Mr. Cremrent Reip had no objection to Dr. Spencer’s views on
“warping.” He thought all turned on accuracy of observation
in tracing the terraces, and he wished to know whether it was
absolutely certain that the same terrace was traceable throughout
the whole distance.

Rev. E. Hitt called attention to the fact that tracts of Lake
Superior were now below sea-level, and yet no marine deposits
are forming there. He called attention to the advantage of the

BASINS OF THE GREAT LAKES OF AMERICA. 533

Hydrographic Survey, which the Author had utilized, and which we
had in yain asked forin England. The depth of the Saguenay valley
would be also accounted for by the Author’s explanations.

Prof. SreLry was prepared to accept the ancient drainage of the
Laurentian river as nowset forth. But he did not think it followed
that the ancient valleys had been excavated by the river any more
than that they were the work of ice. The general course of the
Laurentian lakes followed the outcrop of the strata sufficiently to
suggest that the lakes were originated by earth-movements. The
main work of excavation seemed to him attributable to marine
denudation in times when the level of the land was lower. And
as tidal waters retired from the valley which they had cut out, the
river-drainage necessarily occupied these inlets after the land was
elevated.

Mr. Wuitaxser asked why objection was raised by Dr. Hinde
to deductions from borings in America when in England they
were accepted. No other evidence of buried channels was to be
had, sometimes. He would like to have some idea of the number of
borings on which the Author relied.

The Avurnor, in reply, answered Dr. Hinde and Mr. Whitaker
that he had only written a condensed account of the origin of the
basins, not of the lakes themselves. There were no escarpments in
the place where Dr. Hinde had asserted their existence. There
were scores of deep wells sunk in the Drift between Lake Simcoe
and Georgian Bay, where deep Drift was shown. Similar sections
were shown at the south-east end of the lake. He gave fuller details
of the extension of these borings to the 8.E. He cited instances of
modern buried channels of a similar nature to those which he had
described, and which evidenced a high continental elevation. To
Prof. Seeley he replied that he had no objection to the assistance
of sea-waves, in part, enlarging the valleys in some Pre-Pleistocene
times. ‘The old Erie-Ontario channel has been warped two feet per
mile, which would account for the obstruction of the ancient valleys.
Mr. Gilbert and he had traced one particular beach continuously
round Lake Ontario. The elevations he had deduced from obser-
vations were founded on accurate instrumental measurements along
this line, and similar observations had been made by him in other
areas. ‘There was no other evidence of barriers in the Erie-Ontario
valley other than such as were due to differential elevation or
partial filling with Drift. The Pre-Pleistocene drainage of the Lake-
Michigan Basin was not to the south; hence no barrier greater
than at present was needed, as explained in the paper.

There were no beaches about Kingston on account of the low
altitude, but he had traced beaches in other parts of the region.

If we were to follow the differential elevation we should find that
there were no Canadian Highlands at the close of the episode of
the Upper Till, but he could not now enter into the ice-hypothesis.
He gave instances of the absence of marine organisms in undoubted
marine beaches, and instanced the discovery of a whale in beach-
deposits upon which the evidence of warping was partly founded.

534 PROF. T. R. JONES ON SOME DEVONIAN AND

32. On some Dervontan and Stuvr1an Osrracopa from Norra
America, Francs, and the Bospuorvs. By Prof. T. Ruperg
Jongs, F.R.S., F.G.S. (Read May 21, 1890.)

[Puares* XX. & XXI.]

ConrENTs.

§ I. Devonian Species, from North America and the Bosphorus.

§ 1. From Clarke Co., Indiana.

§u. From Thedford, Ontario, Canada; and Eighteen-mile Creek,
Lake Erie, New-York State.

§ 11. From the Bosphorus.

§ II. Silurian Species.

§ 1. From Anticosti, Canada.

§ 1. Silurian Species from Dundas, Ontario, Canada.

§ur. Silurian Species from Canada, Coll. Geological Survey of
Canada.

§ iv. A Lower-Silurian Beyrichia (from Brittany), named and dis-
cussed by M. G. de Tromelin some years ago, but not hitherto
figured.

§ I. Drvontan SPECIES.

§1. As stated at page 14 of the Quart. Journ. Geol. Soc. for
February last, Mr. J. M. Clarke, of Albany, N. Y., sent me some
Devonian Ostracoda, collected by him in Ontario Co., N. Y., and
some from Clarke Co., Indiana. These are now illustrated and
described herewith.

1. The first-mentioned occur in the buff-coloured, earthy portion
of a decomposing siliceous rock, known as “ the Chert of the Corni-
ferous Limestone,” and cavernous with casts (internal and external)
of Polyzoa, Ostracoda, remains of Trilobites, and other organisms,
comprising some interesting specimens of Beyrichia and allied
genera. ‘There are six species, and these are illustrated in Pl. XX.
figs. 4, 9-13, and Pl. XXI. fig. 1.

2. Two species, collected also by Mr. J. M. Clarke, from the
Hamilton Group, Clarke Co., Indiana, U.S., Pl. XX. figs. 6 & 7.

§1r. Among the additional Ostracoda, collected by Dr. Hinde,
F.G.S., as mentioned at page 28, Feb. No., Q. J. G.8., are some Devo-
nian Ostracoda from the Hamilton Group at Thedford, Ontario,
Canada, and from the same formation at Highteen-mile Creek, Lake
Erie, N.Y. Four of these, being new species, are here described
and figured (Pl. XX. figs. 5 & 8; and woodcuts, figs. 1 & 2).

Note.—The genera Bollia, Moorea, Octonaria, Eurychilina, and
Ulrichia are hereby added to the list of ‘‘ Hamilton ” fossils.

* These Plates have been drawn with the aid of a Grant from the Royal
Society.

106

10q@

West, Newman, imp.

PALA OZOIC OSTRACODA.

Quart. Journ. Geol. Soc. Vol. XLVI.PI. XA.

i

116

iV)
alr

West, Newman.,imp.

OSTRACODA.

PAL AOZOIC

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. 539

§ 1. The Devonian Beyrichia collected some years ago by M.
Dumont at the Bosphorus, and noticed by Dr. Ferd. Rémer in the
‘Neues Jahrbuch, &c. for 1863, having been kindly lent by M.
Dewalque for examination, is here figured and described in detail
CE) 2ek. fe. 1).

Devonian Species.
T. Primitia, Jones § Hall.
1. Primitia Clarket, sp.nov. Pl. XX. fig. 11. Ontario Co., New York.

“IL Bayrrcnra, M‘Coy.

2. Beyrichia devonica, Jones. Pl. XX. figs: 1a, b, 2a, 6,3. Bosphorus and
Devon. 2a5,and 3 are from Devon.

3. subquadrata, sp.nov. Pl. XX. fig. 4. Ontario Co., N.Y.
4, —— Kledeni, M‘Coy, variety. Pl. XXT. figs.1a,b. Ontario Co., N.Y.
5. —— Kolmodini, sp.nov. Pl. XX. fig.6. Clarke Co., Indiana.

III. Hurycsruna, Ulrich.
6. Hurychilina reticulata, Ulrich. Pl. XX. figs. 13a, bd. Ontario Co., N.Y.

IV. Bours, Jones § Holl.

7. Bollia bilobata, sp. nov. Pl. XX. fig. 12. Ontario Co., N.Y.

8. Hindei, sp.nov. Pl. XX. fig. 5. Eighteen-mile Creek, N.Y.

8*. Bollia? An undetermined form, not figured. Highteen-mile Creek,
Lake Erie, N.Y.

Y. Srrepuna, Jones & Holl.

9. Strepula plantaris, sp.nov. Pl. XX. figs. 8a,b. Highteen-mile Creek,
Lake Hrie, N.Y.

VI. Ocronarta, Jones.

10. Octonaria Linnarssoni, sp. nov. Pl. XX. figs. 7a, 6b. Clarke Co.,
Indiana.

VII. Moorza, Jones & Kirkby.
ll. Moorea Kirkbyi, sp.nov. Pl. XX. figs. 9a, b, 10a, 6. Ontario Co.,
N.Y. .

Also, figured in woodcuts :
12. Primitia(?) Walcotti,sp. nov. Thedford, Ontario, Canada, Woodcut,
fig. J

g. 1.
13. Ulrichia Conradi, gen. et sp. nov. Thedford, Ontario, Canada.
Woodcut, fig. 2.

I. Priurrra, Jones and Holl.
J. Primrrm Crarker, sp. nov. (Pl. XX. fig. 11.)

Length 1°66 mm.

Obliquely-subovate, narrow (low) and semicircular in front, boldly
and obliquely rounded behind, where the height is to that in front
as 16 to 13, measured at the ends of the hinge-line, which is
about half of the greatest length of the valve. Surface almost
uniformly convex, but fullest along the ventral and_ posterior
regions; and marked with a relatively large oval pit between the
centre and the back.

The nearest to this is Primitia humilis, J. & H., referred to in the
February No. of the Q. J. G.S., p. 5; but it is much less oblong,

536 PROF. T. R. JONES ON SOME DEVONIAN AND

having a diagonal obliquity; it is more convex than P. humilis:
and its normal pit or umbilicus is large and without a furrow.

From the decomposed Chert of the Corniferous Limestone (Devo-
nian), Ontario Co., New-York State. Collected by Mr. J. M.
Clarke, of Aibany, N.Y.

There are also in this rock some other more or less oblong, very
small casts of Primitie (?); and a few minute, almost oval casts,
indeterminable.

Dr. Hinde, F.G.S8., has favoured me with the following note
(March 27, 1890) :—* The siliceous rock seems to have been com-
posed of calcareous organisms and then infiltrated with silica.
Subsequently the shells, &c., composed of carbonate of lime, have
been dissolved out, whilst the silica has been changed into ‘ rotten-
stone.’

“IT do notsee any traces of siliceous organisms in the decayed rock ;
and, if these had been originally present, they have been dissolved.
I am very familiar with this kind of rock, which prevails in the
Corniferous Formation of Canada. Wherever it occurs, the corals
and other organisms are replaced by silica. I have often searched
for spicules in this chert before it has been decayed, but not with
much success, but I have some Indian arrow-heads made from it
in which spicules are plainly seen.

‘* Dana, in ‘ Manual of Geol.’ edit. 1875, p. 257, figures a variety of
microscopic forms* from this Corniferous chert or hornstone of
Central and Western New York, some Xanthidia, some perhaps
spicules, but the forms are not very characteristic.”

II. Bryricura, M‘Coy.

2. BryricH1a Devonicat, Jones. (PI. XX. figs. la, 16, 2a, 26, 3.)

Beyrichia, sp., Ferd. Romer, N. Jahrb. f. Min. &c. 1863, p. 521,
pl. 5. figs, 9a, 9b.

Beyrichia devonica, Jones, Geol. Mag. 1889, pp. 386-388, pl. 11.
figs. 3, 4, 5.

Beyrichia (Bollia) obliqua, Fr. von Sandberger, Jahrb. Nassauisch.
Ver. Heft 42, 1889, p. 33.

Length 3°8 mm., probably longer than at first ; height 1-9 mm.,
probably rather less than at first; thickness about ‘9 mm., pro-
bably less than at first.

In the ‘ Neues Jahrbuch fiir Mineralogie, &c.’ Jahrgang 1863,
Heft 5, pp. 513-524, Prof. Dr. Ferdinand Romer gave a geological
account of a journey to Constantinople, &c., and included a notice

* See also Dr. M. C. White, ‘ American Journ. Sci. & Arts,’ ser. 2, vol. xxiii.
1862, p. 386; and ‘Geologist,’ 1862, vol. v. pp. 289-240.

+ In the ‘ Neues Jahrb. f. Min.’ &c. Jahrg. 1890, vol.i. p. 184, Dr. Frid. von
Sandberger mentions that B. devonica is identical with his MS. species Beyrichia
obliqua, given in the list of fossils from the Lower-Devonian strata near
Offdillen, between Dill and Sieg, in the northern part of the Dillenburg
district, Nassau, as B. (Bollia) obliqua, Jahrb. Nassauisch. Vereins f. Naturk.,
Heft 42 (August 1889), p. 83; and he withdraws this latter name.

7

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. 537

of some fossils previously collected by M. Dumont from the fossi-
liferous, Devonian, schistose rocks at Arnaut Kj0i, on the Bosphorus,
and preserved in the Museum of the University of Liége. M. De-
walque, the Director of that Museum, has very kindly allowed me
to examine and describe the Beyrichia noticed by Dr. Ferd. Romer
in the memoir referred to above, the two little figures given in 1863
not being sufficient for the determination of the species.

It is a somewhat worn, ferruginous cast of a left valve in a
schistose sandy mudstone, containing also casts of the remains of
Brachiopods and Encrinites. The valve has been squeezed, length-
ened, and considerably distorted, as is especially shown by its pro-
file, fig.16. Apparently it possessed three lobes ; two of them joined
together ventrally, thus making one curved lobe; the other being
separate and close to one end of the valve. In the cast, however,
the horseshoe lobe (consisting of the large pyriform posterior or
cigot lobe, and the middle lobe, united) has been pushed far on over
the middle of the valve, closely approaching the separate (anterior)
lobe, and leaving a wide, sloping, blank area behind.

For comparison, fig. 2, B. devonica, from Devonshire (left valve ;
Geol. Mag. loc. cit. fig. 3, of the same natural size, but x6 diam.
instead of x 12), is here introduced ; also fig. 3, which is a squeezed
modification of the same species (right valve; ibid. fig. 5, nat. size
3mm. and x6 diam.), in which the curved junction of the big and
middle lobes is broken, and the anterior lobe somewhat lessened in
size. Taking fig. 2a, which was chosen from among numerous
more or less modified individuals in the same rock, to represent a
valve (from Devonshire) in its natural condition, we may readily
take fig. 1 (from the Bosphorus) as a distorted example of a similar
form ; and I venture to suggest that it may belong to the same
species.

At page 517 of his Memoir mentioned above, Dr. Ferd. Romer
refers these fossiliferous rocks of the Bosphorus to the Middle and
Upper Devonian; but M. de Verneuil (Bullet. Soc. Géol. France,
ser. 2, vol. xxi. (1864), pp. 147-155) regarded them as of Lower-
Devonian age. In his memoir on the Geological Conditions of the
Eastern part of European Turkey (Jahrb. der k.-k. geol. Reichs-
anstalt, vol. xx. 1870), Dr. Ferd. von Hochstetter referred them on
paleontological grounds to the horizon of the Lower-Devonian beds
of Western Europe, noting also that they contain some few Upper-
Silurian fossils. Mr. W. R. Swan, also, in the Quart. Journ. Geol.
Soc. vol. xx. 1864, p. 115, treats of them as being on a level with
the Lower Devonian of the Rhine and probably of Plymouth and
Ogwell in Devonshire.

3. BEYRICHIA SUBQUADRATA, sp. nov. (PI. XX. fig. 4.)

Length 1°3 mm.; height -93 mm. ;

A hollow cast of the outside of a Beyrichian valve gives, in re-
verse, the shape and contour shown in fig. 4. This approximates in
some degree to B. devonica (figs. 1, 2,3), having an isolated anterior
lobe and two thick lobes united by a ventral curve. Its relative

538 PROF, T. R. JONES ON SOME DEVONIAN AND

squareness of form, however, being only one third longer than high,
whereas B. devonica is twice as long as it is high, is a character- -
istic distinction. Therefore I propose to give it a separate name—
B. suBQUADRATA.

In the decomposed Chert of the Corniferous Limestone, Ontario
Co, N.Y. Coll Mr, J: M. Clarke.

4, Beyricura Kieprni, M‘Coy, variety. (Pl. XXI. figs. 1a, 16.)

Length 5-7 mm. ; height 3 mm. ; breadth (through the middle lobe)
3 mm.

This is evidently a smooth B. Alaxdeni, of the var. clausa type,
with a pimpled hypertrophied anterior lobe. The correctness of
this determination may be seen by reference to the April No. of the
‘Ann. & Mag. Nat. Hist.’ 1836, pp. 354-356, pl. xi. figs. 9 & 18,
where specimens having one or the other of the characters here
present are treated of; and the perfectly smooth variety is men-
tioned, op. cit. p. 351, as var. nuda.

So true a varietal form of B. Kladent in the Devonian Forma-
tion is of great interest, as an instance of persistency of species.

The specimen figured is from the Corniferous Chert of Ontario |
Co., New York. Coll. Mr. J. M. Clarke.

5. Beyricara Kortmoprini, sp. nov. (Pl. XX. fig. 6.)

Length 1-7 mm.; height 1 mm.

This has evidently a structure analogous to that of the Scandina-
vian Beyrichia clavata, Kolmodin, especially of that variety figured
in the ‘Ann. & Mag. Nat. Hist.’ ser. 6, vol. i. p. 399, pl. xxi. fig. 8,
in which the upper part of the anterior lobe is crossed by a sulcus.
In the specimen before us the front of the valve is more acute
(narrower) than in B. clavata, and the hinder portion rounder and
fuller, with a bold curvature. Thethree lobes run together at their
base, but more equally than in the fig. 8 referred to, the front and
hind lobes making one nearly uniform, curved, sausage-like, pinpled
swelling, from the inner curve of which the small, smooth, pyri-
form, middle lobe divides off with a narrow neck. ‘The separated
portion of the anterior lobe is bold and round, and much larger
than in the variety of B. clavata above-mentioned. The free margin,
though very distinct, is not radiated.

It is from the Hamilton Group, of Clarke Co., Indiana, U.S.A.
Collected by Mr. J. M. Clarke, of Albany, N. Y.

The species is worth naming after the Swedish paleontologist
Dr. Lars Kolmodin, of Wisby, who has given good drawings and
descriptions of Scandinavian Ostracoda.

III. Evrycuitra, Ulrich, 1889.

Geol. and Nat.-Hist. Survey of Canada: Contributions to the Micro-
paleontology of the Cambro-Silurian Rocks of Canada, Part II.,
by E. O. Ulrich, 8vo, 1889, p. 52.

This is a proposed genus, characterized by a thickened marginal

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. 539

lip along the free border of the valve, bearing a thin, flange-like,
projecting border, either narrow or broad, and either plain or marked
with radiate strie. In other respects the valves are Primitian in

shape and ornament*.

6. EvrycHitina RETICULATA, Ulrich. (Pl. XX. figs. 13a, 136.)
Eurychilina reticulata, Ulrich, Contributions, &c., Part II., 1889,
feel. Ooties, 9 & 9a.

mm.
Length, including the fringe........ 35
a GMO We. RINGO vcs eras. 2:5
IbleienG, With tie TTIMGE cies. ew, ales 2
SSeS) yO ILS UNAIDS A 1i

An inner (fig. 13 a) and an outer cast (fig. 13 6) of one fine indi-
vidual belonging to this handsome species, in the decomposed Chert
of the Corniferous (Devonian) Limestone of Ontario Co., New-York
State, supply material for the recognition of the same form as is
figured and described by Mr. E. O. Ulrich, as quoted above, from
“the Trenton Shales at Minneapolis, St. Paul, Fountain, and other
localities in Minnesota.” The recurrence of this beautiful species
in the Devonian Formation is of great interest.

Another fringed Ostracode, having the Primitian features of um-
bilical pit and furrow, and a reticulate sculpture, is the Sardinian
““ Beyrichia reticulata,” of J. G. Bornemannt. Though imperfect,
the specimen has evidently been carefully figured; and it is
reproduced here for comparison (PI. XX. figs. 14a, 146), because
the work is rare. There is not, however, sufficient evidence in
the drawings that the ventral border had the inner thickened
marginal lip or rim that Hwrychilina requires. Should, however,
Dr. Bornemann’s prove ultimately to belong to this genus, the spe-
cific name of Mr, Ulrich’s species will have to be changed.

* For some Beyrichian forms, with thickened and frilled edge, and regarded
as Beyrichiopsis by Jones & Kirkby, see ‘Geol. Mag.’ 1886, p. 433, &e. pls. 11
& 12; and others still retained in Beyrichia are noticed in ‘Ann. & Mag. Nat.
Hist.’ ser. 5, vol. xiii. 1886, p. 257, pl. vii. figs. 1 & 2. Dr. Aurel Krause has
described some flanged and fringed Primitie, and a fringed Hntomis, in his
Memoir on the Beyrichig and related Ostracoda from the Lower-Silurian Drift-
gravel of North Germany, ‘ Zeitsch. d. D. geol. Ges.’ 1889, pp. 1-26, pls. 1 & 2.
Without sections of the ventral border, to show the proportions of the thick-
ened marginal rim and flange, it is impossible to determine how far any of
these may agree with Mr. Ulrich’s diagnosis of Hurychilina. Fig. 3b in Dr.
Krause’s plate, referred to, does not exhibit the required thickness of lip, being
only the surface-outline of one valve of Primitia distans, Kr., which is curiously
like Bornemann’s “ Beyrichia reticulata,” allowing for the effect of pressure on
the latter (Pl. XX. figs. 14a, 140).

t ‘Paléontologie de Tile de Sardaigne,’ par le Prof. Chev. Joseph. Mene-
ghini, Turin, 1860; Supplément (p. 8). ‘ Voyage en Sardaigne,’ &c. par Lieut.-
Général Conte Albert De la Marmora, 3eme Partie, Géoiogie, vol. 1i. Lettre
de M. ie Docteur J. G. Bornemann (p. 7), relating to fossils found in schis-
tose Silurian rocks at a spot called Perdas de Fogu, near the village of Flumi-
nimaggiore, Province of Cagliari, in the Island of Sardinia; collected and de-
scribed by Dr. J. G. Bornemann.

Q.J.G.S. No. 184. on

540 PROF. T. R. JONES ON SOME DEVONIAN AND

TV. Borris, Jones and Holl, 1886.
Bollia, J. & H. ‘Ann. & Mag. Nat. Hist.’ ser. 5, vol. xvii. p. 360. -

7. Bottia BILoBATA, sp. nov. (Pl. XX. fig. 12.)

Length 1°38 mm.; height 1 mm.

This is a broken and worn cast from the decomposed Corniferous
Chert of Ontario Co., N. Y. It is probably an oblong Bollia, the
two lobes of which have been very prominent, but have been modified
by accidental rubbing, and their curved connecting ventral ridge
almost worn away. It is much like B. bicollina, J. & H. (¢ Ann. &
Mag. Nat Hist.,’ April 1886, p. 361, pl. xii. figs. 14-16), but the
valve is longer, being more oblong, and the lobes are much lower
down, away from the dorsal margin. There is also an appearance
of similarity to such a form as fig. 2a, Pl. XXI., but the two re-
stricted lobes are too far away from the dorsal margin; and the
marginal lobe is at the contrary end of the valve, and herein agrees
with the thick posterior marginal ridge in fig. 5 (Bollia Hindet).

Coll. Mr. J. M. Clarke, of Albany, N.Y.

8. Borris Hinpet, sp. nov. (PI. XX. fig. 5.)

Length 1°7 mm.; height 1 mm.

This differs from the typical Upper-Silurian Bollia bicollina, J. &
H., op. cit., in being relatively longer, in having a much thicker
marginal rim, a shorter and less open curve of its thick horse-shoe
lobe, and in having not only the anterior part of that lobe pinched
at its neck, but the hinder portion impressed with a strong oblique
furrow. JB. interrupta, Jones, op. cit. vol. xix. p. 408, pl. xii. fig. 14,
presents an analogy in having its hinder lobe divided into two un-
equal parts, but the rest of the valve differs from our specimen.
The latter is from the Hamilton Group (Devonian), at Eighteen-
mile Creek, Lake Erie, New-York State (attached to a small Coral),
where also some of the Devonian Ostracoda described in the
February No. of the ‘ Quart. Journ. Geol. Soc.’ vol. xlvi., were ob-
tained. Coll. Dr. G. J. Hinde, F.G.S., after whom it is named.

S*. Borris ?, sp. (Not figured.)

Length °64 mm.; height -48 mm.

A very small semicircular valve, rather rounder at one end than
at the other, somewhat undulate on the surface, with a faint curve
visible at the middle, as if it had been worn down from the curved

lobe of a Bollia.
From the Devonian strata at Eighteen-mile Creek, Lake Erie,

NeY.) Coll! DroG.d;, Hinde; F.G:s;

V. Srreputa, Jones and Holl, 1886.

9. STREPULA PLANTARIS, sp. nov. (Pl. XX. figs. 8a, 86.)

Length :88 mm.; height -44 mm.
This is one of the Strepule with tortuous, and not merely loop-

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. 541

like, ridges; and therefore it comes nearer to S. sigmoidal, J.
(* Quart. Journ. Geol. Soc.’ February 1890, p. 11, pl. ii. fig. 4) than
to those figured in the ‘Ann. & Mag. Nat. Hist.? May 1886,
pp. 403-406, pl. xiii. figs. 1-9 & 15. Indeed it came from the
same locality as S. sigmoidalis, namely from the Hamilton Group at
Eighteen-mile Creek, Lake Erie, N.Y. Coll. Dr. G. J. Hinde,
F.G.S.

The valve has unequal ends, being semicircular in front and ob-
liquely rounded behind. In outline it is somewhat like the sole of
the human foot. Hence it may be called prantaris. The broad or
hinder end has a thin, flat, lip-like margin, obscurely marked with
about ten shallow pits. The narrow or front end has six strong,
outstanding, marginal denticles. There is a thick curved ridge
within the posterior margin. The surface bears a thin, sigmoidal,
tortuous ridge, passing along the dorsal and along the middle and
ventral regions, curving in front and behind. It is double for a
short distance in the antero-dorsal region, and is slightly interrupted
at the anterior third of the valve. It gives off two short branches
in the posterior third of the valve; the higher one touches the in-
side curve of the thick ridge, and the lower branch falls into the
ventral end of that ridge.

VI. Octonaria, Jones, 1887.
Octonaria, Jones, ‘Ann. & Mag. Nat. Hist.’ June 1887, p. 404.

10. Octonarra Linnarssoni, sp. nov. (Pl. XX. figs. 7 a, 7 6.)

Length 1:4 mm.; height -7 mm.

In this specimen we have the two very convex and thick-ridged
carapace-valves of Octonaria, but with a surface-pattern different
from any of those described and figured in the ‘Annals & Mag. N.
Hist.’ ser. 5, vol. xix. pp. 404-407, pl. xu. figs. 1-8. In shape it
approaches O. flexuosa, loc. cit. fig. 1 (if its position on the plate be
reversed), but not at all in the ornament. ‘This is a compressed
spiral ridge, beginning with a thick portion at one end, becoming
thinner as it passes along the ventral region, and much thinner
after curving up into the dorsal region, then throwing off a short
connection with the first portion, and turning down into the middle
of the valve with a confused loop, little lumps, and central pit.
The last feature can be traced obscurely in figs. 2, 5, & 7 of the
illustrations referred to. Although, perhaps, some doubt attaches
to the determination, I think that both naturally and conveniently
it may be referred to Octonaria as O. Linnarssoni—after the
lamented Swedish paleontologist who has done good work among
these and other fossil Crustacea.

From the Hamilton Group, Clarke Co., Indiana. Coll. Mr. J. M.
Clarke, of Albany, N.Y.

542 PROF, T. R. JONES ON SOME DEVONIAN AND

VII. Moorra, Jones and Kirkby, 1867 & 1869.

Moorea, Jones & Kirkby, ‘Ann. & Mag. Nat. Hist.’ ser. 4, vol. ili.

p. 225, and ser. 5, vol. xvill. p. 261.

11. Moorea Kirxsyi, sp. nov. (PI. XX. figs. 9a, b, & 104, b.)
Length. Height. Thickness.

mm. mm. mm.
1M aR aa 1:33 73 66
ADO RNR aioe 1:2 6 48

The species of Moorea that have been described in the papers re-
ferred to above have more or less of marginal ridges, as well on the
dorsal and ventral, as at or near the ends. The specimens which
we have from the Corniferous Chert of Ontario Co., New-York
State (Coll. Mr. J. M. Clarke), have ridges only at the ends of the
valve. Another form (Silurian), M. Smithii, Jones, op. cit. vol. xix.
p. 499, pl. xi. fig. 11, has a median ridge forking at the posterior
region.

Neatly suboblong with rounded ends, straight back, and nearly
straight ventral margin, these specimens, both an inner and an
outer cast, show that two nearly equal curved ridges, each parallel
with its neighbouring margin, starting abruptly on the dorsal, and
dying away on the ventral edge, existed on each valve.

This distinct, though simple, form deserves a specific name, and I
associate it with that of my valued friend and fellow-worker, Mr. J.
W. Kirkby.

Devonian Species from the Hamilton Formation at Thedford,
Ontario, Canada.

The occurrence of numerous specimens of Primitiopsis punctuli-
fera (Hall) in various stages of development as to size, reticulation,
tubercles, and smoothness of ends (nothing of the last in the very
young state; length -9, height *5 mm.), is mentioned at page 28 of
the February No. of the ‘ Quart. Journ. Geol. Soc.’ 1890.

Some interiors of small valves of Primitiopsis punctulifera are
shown on one of the pieces of grey limestone (composed of small
Brachiopods, &c.) from the Hamilton Group at Thedfcrd, Ontario,
Canada. They are 1:25 mm. long, and ‘75 mm. high, and not full-
grown, but rather larger than fig. 7. pl. 11., Q. J. G.8., February
1890. hey show distinctly that the front border is bevelled in-
wards, the ventral edge of the right valve somewhat inturned at
its hinder moiety, the posterior edge thin, and the dorsal edge
straight, with a simple groove along its length, slightly overlapped
by the outside edge of the valve brought over at the middle.

Also collected by Dr. Hinde, in the same locality, are two other
interesting small Ostracoda associated with them. These occur with

—————————— ee llr Oe eee CU

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. 543

P. punctulifera in a thin limestone composed of the usual frag-
ments and small organisms, and are—

(1) Primitia Walcott, sp. nov.; and (2) Ulrichia Conradi, gen.
et sp. nov.

12. Prrurria (?) WALcorrt, sp. nov.

Length -95 mm. ; height -47 mm.

An oblong Primitia? (woodcut, fig. 1), imperfect at one end,
with a central pit, and elegantly ornamented with narrow curved
ridges and furrows (of about equal width). These are nearly
straight, and somewhat inosculating on the dorsal, tortuous and

Fig. 1.—Primitia Walcotti, sp. nov. (Magn. 40 diam.)
From Thedford, Canada. Coll. Dr. Hinde, F.G.S.

interrupted on the ventral region. Small pits occur here and there
along the furrows, as if marking obsolete meshes.

This I name P. Watxcorrt, in honour of C. D. Walcott, F.G.S., of
Washington, U.S., who has discovered and described several very
interesting forms of North-American Ostracoda.

VIII. Genus Unricuta, nov.

Among the Primtie which have the normal medio-dorsal sulcus,
there are many having the edges of the sulcus more or less swollen,
sometimes on one, and sometimes on both sides. ‘The varieties of
Primitia mundula often show this modification in some degree.
This varietal feature, however, becomes so much exaggerated as to
obliterate the sulcus by the presence of two large tubercles, mostly
without a definite pit or furrow between them. This is seen in
P, breornis, J.. ‘Ann. & Mag. Nat. Hist.’ ser. 2, vol. xvi. (1855),
p. 173, pl. vi. fig. 23, and op. ct. ser. 3, vol. xvi. (1865), p. 420 ; in
P. equalis*, J. & H., op. cit. ser. 5, vol. xvii. (1886), p. 412, pl. xiv.
fiend Morgan, J:, Q.J.G.S. February 1890, p.d, pl. iv.
fig. 6; and in a species now described, and dedicated to T. A.
Conrad. Mr. E. O. Ulrich, of the Illinois Geological Survey, has
shown me sketches of somewhat similar forms from the Lower
Silurian at Corryville and Fairmount, near Cincinnati. As all

* P. diversa and P. cornuta, J. & H. (op. cit. figs. 10& 12), are also regarded
as having tubercles which, although far apart, represent “essentially the
elevated sides of the modified dorsal furrow” (op. cit. p. 412).

544 PROF. T. R. JONES ON SOME DEVONIAN AND

these forms, in their two medio-dorsal knobs, usurping the place of

the sulcus on each valve, show a departure from the simple Primitia, -

and bear evidence of the persistency of their peculiar bitubercular
feature, it is allowable to give them a generic standing ; and I name
the genus Unricura, after Mr. E. O. Ulrich, who has largely col-
lected the Palxozoic Ostracoda of North America, and has figured
and described several important species.

[In his Memoir on the Fauna of the Graptolite-rock &c., ‘ Neue
Lausitzische Magazin,’ Gorlitz, vol. liv. 1878, pp. 85 & 109, pl. v.
fig. 11, K. Haupt gives a small figure of a valve (about 1:5 mm. long),
apparently belonging to this genus. He refers to it as “ Beyrichia,
sp.”

A somewhat similar form of bituberculate valve occurs in the
Lower-Coalmeasure shales of Nova Scotia (‘Geol. Mag.’ 1884,
p-. 358. pl. xi. fig. 7); but this is the young form of Beyrichia
nova-scotica, J. & K., as intimated at p. 3858, and proved by its free
association with mature forms in a series collected by Dr. Hinde. |

13. Urricnia Conrani, gen. et sp. nov. (Woodcut, fig. 2.)

Length -8 mm.; height -46 mm.

A small, left valve, suboblong, straight on the back, obliquely
curved below, rounded at the ends, the posterior higher and fuller
than the anterior. Two largish prominent knobs, oval in section
and obliquely peaked (much too neatly oval in the figure), divide
the dorsal region in three nearly equal portions ; the front tubercle
is smaller than the other. The surface of the valve is faintly
reticulated, and has along the free borders a neat marginal ridge.

Fig. 2.—Ulrichia Conradi, gen. et sp. nov. (Magn. 40 diam.)
From Thedford, Canada. Coll. Dr. Hinde, F.G.S.

This small bituberculate and punctate valve is near P. Morgani,
J. (Quart. Journ. Geol. Soc., February), p. 5, pl. iv. fig. 6; but it
is more oblong, margined with a distinct raised rim, and has the
two tubercles (which take the place of the sulcus of Primitia)
obliquely peaked, and nearly equal in size. This species I propose
to name Conrapi, in memory of T. A. Conrad, who was one of
the first to describe the fossil Ostracoda of North America.

’ . e
_ a

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC.

§ IT. Srrurran Osrracopa.

§1. From Anticosti. Arranged geologically.

Peon: (08.08 ae te
aed from gilunian ge
NS Be peiricts diff PIMA ULDidcions
: . Beyrichia diffissa, sp. nov. ... 3 . fig. 7. Division 3.
15. 2. le tend vin pe ines nov. 45 i 8. FP | ae
16. 3, Primitia Billingsti, sp. nov. Merete ik, oh as
V7: 4. Bollia semilunata, sp. nov. . i 9. » 1.) Middle or
18. 5. Bythocypris (?) Lindstremit, ; Lower
SMMIOW.| Hinecd a tacdaeeeiecedes i Vale a 1.) Silurian.
19. 6. Bairdia anticostiensis, sp. n. sf 3. Lowest. }
20. 7. Macrocypris(?) subcylindrica,
SMRMOVA! cha cis sevee scene cenine - os i Lower
21. 8. Bythocypris(?) obtusa, sp. n. 3 4, rs f Silurian.
22. 9. Polycope sublenticularis, sp. |
RON ee ciay dc \eeavesied «wo vade i 6. i y)
ce ee Genera from Anticoste.
for L.-VIITI.)
MEMEPBINMUMTA dai cccescevcetess in Division 1.
MIO MIGEMRIOHTA oo. .6.00.caenes ss bs 3 By
MEO TWA 62 cots voacne hence on a - 1.
TX. Leperpirta...............6.. ¥ y 3.
X. ByrHocypris? ............ . » 1and Lowest Div.
BRGIOSMES AISI SS, Gus occ ecenc~ once L
XIT. Macrocypris? ............ set
PEW POUYCOPE, | jocecnscrccsencses Dinas
$i. From Dundas, Ontario, Canada.
Nos. conti- Nos. of
nued from Si the
p. 550. ooo
Species.
23. 10. Primitia mundula, J.
24. ll. Beyrichia Kledeni, M‘Coy.
§ 11. From the Dominion of Canada, Coll. Geological Survey
of Canada.
25. 12. Primitia mundula, J. \
a a3 3 ovata (?), J. & H. |
: . eyrichia tuberculata, Boll. aT
, var. pustulosa (Hall). ; Boia ighs Pena
== , var. Bronni (Reuter).
28. 15. equilatera, Hall. )
29! 16. Primitia mundula, J., and varieties. — )
30. 17. Ulrichi, J.
3l. 18. ——, spp. |
32. 19. Isochilina ottawa, J., var. + Lower Silurian.
33. 20. Leperditia, spp.
34. 21. Beyrichia, spp.
30. 22. Polycope, sp. y

545

Norn.—The foregoing list supplies us with one genus (Polycope) as an addition
to the Lower-Silurian forms (already known in the Devonian and Carboni-
ferous strata); and enables us to place Macrocypris, Bairdia, and Bytho-
cypris more certainly than heretofore in the Lower-Silurian column of the

Table at page 2 of the February No. of the Quart. Journ. Geol. Soc.

546 PROF. T. R. JONES ON SOME DEVONIAN AND

§ iv. From France (Brittany).
oe Sil. s

23. ” Beyrichia Guillieri, Tromelin, Pl. XXI. fig. 2. Lower
Silurian.

§1. Of the Silurian Ostracoda, from North America, additional
to those described and figured in the February Number of the
‘Quart. Journ. Geol. Soc.,’ we have nine species collected by Dr.
G. J. Hinde in Anticosti. Of these, five belong to the Divisions
3, 2, & 1 of Billings’s four Divisions of his ** Anticosti Group,” * and
four to the lowest Division there, which he termed the ‘“‘ Hudson-
river Group.” This last Division is equivalent to Groups A and B
of the Geological Survey of Canada (Reports 1853-56, and 1863),
and is now regarded, Dr. Hinde informs me, as equivalent to the
‘* Cincinnati Group i #

Group C is equal to Tilines's Division 1 of the “* Anticosti Group,”
and was placed by him doubtfully at the base of the Middle Silurian
there, but is now regarded by Dr. Hinde as being more probably
Lower Silurian. Cioapaas = Div. 2, Group E= Div. 3, and Group F
= Div. 4 of the Anticosti Group, were Ghamapkaninee by what Mr.
Billings regarded as Middle-Silurian fossils, but the term ‘‘ Middle
Silurian ” appears to be almost obsolete with American geologists.
Mr. Billings included the “ Medina, Clinton, Niagara, and Guelph”
Formations of New-York State and Western Canada in the “ Middle-
Silurian” series.

The genera to which these nine species belong are already in-
cluded in the Table at p. 2 of the previous memoir (February 1890);
but all the species are new.

§ I. From Anticostr, Canada.
IJ. Bryricuta, M‘Coy. (See also pages 236-238.)

14, BryricH1a DIFFIssa, sp. nov. (Pl. XXI. fig. 7.)

Length 1°5 mm.; height 1 mm.

A rather narrow-lobed Beyrichia, not far removed from some
varieties of B. Kladeni, but having its anterior lobe long, narrow,
oblique, furrowed, and, as it were, split longitudinally for the
greater part of its length. Hence the proposed name pirrissa. The
middle and hinder lobes unite below; and the latter is broad and
faintly punctate. The upper ends of the split lobe are broken in
the specimen.

From the Division 3 of the Anticosti Group, Janitor River,
Anticosti. Attached to an Atrypa. Coll. Dr. G. J. Hinde, F.G.S.

* « Geol. Surv. Canada: Catalogues of the Silurian Fossils of the Island of
Anticosti,’ 1866.

+ In the February No. of the Q. J. G. S., at p. 28, 8th line from the bottom,
Div. G should be Div. A. At p. 27, 3rd ling from the bottom, for fig. 17 read
fig. 12.

SILURIAN OSTRACODA FROM NORTH AMERICA, ELC. 547

IX. Leperpiria, Rouault, 1851.
‘Ann. Mag. Nat. Hist.’ November 1881, p. 334.

15. LeperpIriA FRONTALIS, sp. nov. (Pl. XXI. figs. 8a, 36.)

Length 6-2 mm.; height 4°7 mm.; thickness 3 mm.

This is a small, subquadrate, or rather subrhomboidal, valve, with
the general aspect and the ocular tubercle of Leperditra ; its muscle-
spot is not visible; but its ventral margin is thickened, hence pro-
bably it is a Leperditia and not an Jsochilina.

In outline and contour it would be like figs. 5 & 11, pl. i. ‘ Quart.
Journ. Geol. Soc.’ February 1890, were it not so oblique from above
downwards and backwards, and less convex. Our specimen has
the antero-dorsal angle well forward, the antero-ventral margin
sloping inwards, and the postero-ventral margin boldly curved out-
wards. It is somewhat like fig. 12a (loc. cit.), but the front dorsal
angle is more pronounced, and there is no fold or sinus on the ven-
tral margin. So also it approaches F. Schmidt’s figure of a variety
of L. Hisingeri, ‘ Mém. Acad. Imp. Sci. St.-Pétersb.’ ser. vil. vol. xxi.
No. 2, 1873, pp. 9, 16, & 25, figs. 22, 23; but its front dorsal
angle is too prominent. An unnamed Lower-Silurian Leperditia
trom the East of the Cordillera of San Juan, in the Argentine Re-
public (EK. Kayser, ‘ Palecontographieca,’ Suppl. IIT. 1876, p. 10, pl. i.
fiz. 19), matches F. Schmidt’s variety of L. HMisingert. L. cana-
densis, var. anticostiana* (L. antecostiensis), Jones, ‘Ann. Mag. Nat.
Hist.’ Nov. 1881, p. 344, pl. xix. fig. 8, 1s also near our specimen,
but differs in the outline of its anterior moiety. On account of the
antero-dorsal angle being so strongly pronounced, the Leperditia
under notice may, I think, be called Fronrazis. It occurs in a
grey limestone made up of fragments of Encrinites, Polyzoans, Tri-
lobites, Brachiopods, &c., in the Division 3 of the Anticosti Group,
near the Jumpers, Anticosti. Coll. Dr. G. J. Hinde, F.G.S8.

I. Primitia, J. & H. (See also page 235.)
16. Priiria Brutrest, sp. nov. (Pl. XXTI. fig. 10.)

Length, with fringe, 2-4 mm.; without fringe 1:9 mm.
Height, 99 99 1-4 99 39 99 Nez 39

This is a fine oval-oblong, or semioval (longwise), convex, smooth,
Primitian valve, with the umbilical pit large, round, shallow, and
low down (below the middle line). A nearly uniform, wide, flat,
thin, and delicately radiate lip is attached to the free margin, and
is rather narrower in front than behind.

There is no evidence of a definitely thickened condition of the
margin behind the flange; if there were, it might be grouped as
Eurychilina (see p. 239).

This form is closely allied to both Primitia plana, Krause, and
P. cincta, Kr., ‘ Zeitschr. d. D. g. Ges.’ 1889, pl. i. fig. 1 & fig. 4; but

* This should be anticostiensis according to rule.

548 PROF, T. R. JONES ON SOME DEVONIAN AND

it differs from both; and, well deserving a specific name, I dedicate

it to the memory of the ardent and industrious paleontologist of —

the Geological Survey of Canada, who devoted much time to the
fossils of Anticosti.

It is from the Clinton or Niagara Formation, Division 2 of the
Anticosti Group, west of Jupiter River, Anticosti. Coll. Dr. G. J.
Hinde, F.G.S. In a compact, thin, grey limestone, composed of
small organisms, and showing P. Billingsic and some obscure forms
on one of the bed-planes.

IV. Borris, J. and H. (See also page 540.)

17. Borris semitunata, sp. nov. (Pl. XXI. figs. 9a, 90.)

Length ‘68 mm.; height ‘54 mm. ; thickness °32 mm.

In this little species the horse-shoe lobe is neat, nearly symme-
trical, and relatively strong, being thick and high, not reaching
below the middle of the valve, but touching each end of the hinge-
line. The outline of the valve is more than half a circle,—that is,
it is nearly two-thirds of an irregular disc, the hinge-line being its
cut edge. The marginal ridge along the free border is strong, but
fincier at one end when at the other; and the clear crescent-shaped
space between it and the curved lobe is very distinct.

From the Cincinnati Formation; Division 1 of the Anticosti
Group (Billings), South of Junction Cliff, Anticosti, attached to a
small Brachiopod. Coll. Dr. G. J. Hinde, F.G.S.

X. Byrnocyrris, G. 8. Brady, 1880.
(See ‘Ann. & Mag. Nat. Hist.’ March 1887, p. 184.)

18. Byrnocyrris? Liypstremi, sp. nov. (Pl. XXI. figs. lla,
Job, d-¢:)

Length 1:2 mm.; height ‘6 mm.; thickness :-48 mm.

In outline and contour this Cypridoid Ostracode (from Billings’s
Division 1 of the Anticosti Group; south of Junction Cliff,
Anticosti. Coll. Dr. G. J. Hinde, F.G.S.) nearly resembles the
smooth oblong-ovate Bythocypris symmetrica, Jones, ‘Ann. & Mag.
Nat. Hist.’ ser. 5, vol. xix. p. 186, pl. vii. figs. 3, 4, & 7; but it is
larger, and tapers more suddenly at the anterior third. Being
so far different, it may have a distinct name—Linpsrremit, after
my friend the eminent Swedish Paleontologist, Professor Gustav
Lindstrom, F.C.G.S., of the State Museum, Stockholm, who has
taken great interest in this branch of Carcinology.

Several specimens, somewhat variable in outline, occur attached
to small Corals and Brachiopods.

XI. Barrpra, M‘Coy, 1844.

19. Barrp1a ANTICOSTIENSIS, sp. nov. (Pl. XXI. figs. 3a, 36.)

Length 2:0 mm.; height ‘8 mm.; thickness ‘9 mm.
An elongate, subrhomboidal, very convex, smooth form; slightly
arched on both ventral and dorsal border, but the latter suddenly

_

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. 549

slopes, with a hollow curve, down to the postero-ventral angle;
rounded in front and terminating in a sharp triangular process
of the ventral border behind. Thus it approaches Bairdiza, espe-
cially such forms as were ascribed to that genus in 1879 (‘ Quart.
Journ. Geol. Soc.’ vol. xxxv. pp. 572 et seq. pl. xxix. figs. 11-16,
and pl. xxxi. figs. 1-7). None of these Carboniferous valves, how-
ever, quite match our figured specimen. Bairdia Griffithiana,
Jones & Holl, ‘ Ann. & Mag. Nat. Hist.’ July 1868, p. 58, pl. vii.
fig. 10, from the Lower Silurian of Ireland, is not far removed, but
is much shorter, higher, and blunter.

From the lowest Division of the Anticosti Group (Cincinnati
Formation, Dr. Hinde), at English Head, Anticosti. Several speci-
mens of single valves, together with numerous other Ostracoda, lie
on the bed-plane of a compact grey limestone, probably composed
of similar organisms. Coll. Dr. G. J. Hinde, F.G.S.

The edges of the valves are in general so much concealed by the
matrix that it is difficult to define many of the individuals. There
is an undetermined Leperditia among them.

XII. Macrocyrris, G. 8. Brady, 1867.
20. Macrocypris? supcyLinpRIca, sp.nov. (Pl. XXI. figs. 5a, 56.)

Length 1°6 mm.; height ‘5 mm.; thickness *6 mm.

Fig. 5 is a long, convex, smooth, right valve of a subcylindrical
carapace, nearly straight above and below, but higher behind, and
with oblique ends, one more so than the other. Nearly straight
above for four-fifths of the dorsal edge, and then sloping down with
a very gentle curve to the obtuse postero-ventral angle. Straight
below. Ends oblique; subangular behind ; the front end narrow,
with a short oblique curve bending downwards and backwards.

It is somewhat like Macrocypris siliquoides, Jones, ‘ Ann. & Mag.
Nat. Hist.’ 1887, ser. 5, vol. xix. p. 194, pl. v. fig. 9, which is
arched on the back and rather sharper at one end than the other;
and also somewhat near M. symmetrica, op. cit. p. 181, pl. vu. fig. 8,
which is blunt at the ends and with nearly equal edges: the speci-
mens under notice are very much narrower than either. As the
two Macrocyprides referred to above offer the nearest analogies,
I place this species also in Macrocypris.

This species occurs in some numbers with Buirdia anticostrensis,
&e., at English Head, Anticosti.

X. Bytnocypris. (See page 548.)
21. Byrnocypris? oprusa, sp. nov. (Pl. XXI. figs. 4a, 45.)

Length 1:8 mm.; height 1:0 mm.; thickness ‘9 mm.

This suboblong form is very near to Bythocypris symmetrica, Jones,
op. cit. 1887, p. 181; but, being much blunter in front, has almost
equal ends. —

With Bairdia anticostiensis, &c., in limestone of the Cincinnati
Group, at English Head, Anticosti. Coll. Dr. G. J. Hinde, F.G.S.

550 PROF. fT. R. JONES ON SOME DEVONIAN AND

XIII. Potycorr, Sars, 1865.

22. PoLycoPE sUBLENTICULARIS, sp. nov. (Pl. XXI. figs. 6a, 66.)

Length 1:1 mm.; height -86 mm.; thickness -53 mm.

This suborbicular form reminds us of Polycope, bemg round and
only slightly angular on its dorsal border. Whether one side or
the other of the low dorsal angle corresponds to a hinge-line, or if
the hinge were limited to the umbo-like angle itself, is uncertain.
Among the Devonian forms, however, of this genus, Polycope
Hughsie, Whidborne, and P. devonica, Jones, var. concinna, Whid-
borne, show a decided tendency to have a subangular dorsal border.
See ‘ Monogr. Devonian Fauna,’ Pal. Soc. 1889, pp. 49, 50, pl. iv.
figs. lla & 17a.

Among Silurian Ostracoda, Macrocypris? crassula, Jones, ‘ Ann.
& Mag. Nat. Hist.’ March 1887, p. 181, pl. vii. fig. 10, is one of
the nearest, but it is too nearly reniform, and has not such a uni-
form convexity. Primitia (Aparchites) Maccoyit, junior, Salter, sp.
(J. & H., ‘Ann. & Mag. Nat. Hist.’ ser. 4, vol. i1. p. 55, pl. vii. fig. 3),
is still nearer in shape, but is too uniformly oval in outline.

Several of these round valves, usually black in colour, accompany
Bairdia anticostiensis, Bythocypris obtusa, &c., on the bed-planes of
the thin grey limestone at English Head, Anticosti. Coll. Dr. G. J.
Hinde, F.G.S.

§ IL. From Dundas, Ontario, Canada. (Species, nos, 23, 24; p. 545.)

Among the Upper-Silurian Ostracoda collected by Dr. Hinde in
North America, and noted in the February No. of the *‘ Quart. Journ.
Geol. Soc.’ p. 28, are numerous small and rather obscure forms in a
thin, brownish, earthy shale (with impressions of Orthis, &c.) from
the Niagara Formation at Dundas, Ontario, Canada. Most of these
little Entomostraca are Primitie (1 mm. long, and less), neatly
suboblong in outline, with a mid-dorsal sulcus and a marginal rim.
The sulcus has its edges partially thickened in some specimens.
These features belong to P. mundula. In a few individuals a very
small, but distinct, tubercle appears in the sulcus or on one of its
edges, giving the appearance of a minute (or young) Beyrichia
notata, or a B. Kledeni, var. acadica (compare some of the figs. in
pls. xvi. & xvii., ‘Ann. & Mag. Nat. Hist.” May 1889). There is
also at least one small B. Alaedeni (more than 1 mm. long), with its
three well-developed lobes. These are not figured here.

S IIL. Stlurian Ostracoda from the Dominion of Canada, Coll. Geol.
Survey of Canada. (Species, nos. 25-35; p. 545.)
A. From Mr. H. M. Ami, F.G.S. Lower Silurian; Canada.

$1. Utica Shales.
1. Primitia mundula, Jones.
2, Ulrichi, Jones.

§ u. Chazy Limestone.
1. Lsochilina ottawa, Jones, variety.

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. dol

B. From Mr. J. F. Whiteaves, F.G.S.

B.a. § I. Upper Silurian ; Arisaig, Noya Scotia.
. Primitia mundula, J., variety.
ovata(?), J. & H.
. Beyrichia tuberculata, Boll. Young.
, var. pustulosa (Hall).

, var. Bronni (Reuter).
4. Beyrichia equilatera, Hall.

B. b. § II. Lower Silurian.

§ 1. Trenton Limestone.

. Prinitia, sp.

. Primitia mundula, J.
, varlety.

. Leperditia, sp. nov. ?
. Beyrichia, s\. nov.

. Polycope, sp.

os bo,

So Or 09 bO

§ 2. Trenton Limestone.

1. Leperditia, sp. nov. ?
§ 5. Birdseye Limestone.

1. Leperditia, sp. nov. ?

§ 4. ena Limestone.
Su. 1. Primitia, sp.

ay
Sopa Hodis ottawa, J., variety.
Sut. 1. Leperditia, sp. nov. ?
Sur. 3. Polycope, sp.
§ 5, Chazy Shales.
1. Primitia mundula (?), J
2. Leperditia?
3. Beyrichia, sp. nov.

A. Some Paleozoic specimens from Canada, sent by Mr. Henry M.
Ami, F.G.S., Assistant-Palaontologist of the Geological Survey
of Canada, to me for examination, consist of :—

§1. Some pieces of hard, black, somewhat bituminous shale from
the Utica Formation at Rideau Street, New Edinburgh, Ottawa,
containing smali obscure casts, very numerous on the bed-planes
and much squeezed. Primitia mundula, J., 1855; and P. Ulricha,
J., 1890, are barely distinguishable, and perhaps Leperditia (?) cy-
lindrica, Hall. ‘The following fossils are also present, as named by
Mr. Ami :—Tvrocholites ammonmus, Emmons, Lingula Progne, Billings,
Leptobolus insignis, Hall, Zygospira modesta, Say. Also remains of
Trilobites and Encrinites.

§ 11. Isochilina ottawa, Jones (‘ Ann. & Mag. Nat. Hist.’ April
1858, p. 248, pl. x. fig. 1), Variety : occurring—(1) abundantly on
the ped-planes of a piece of thin-bedded limestone, from a loose
block in Sussex Street, Ottowa, and probably belonging to the
Chazy Formation (upper portion). (2) Constituting, with a few
bivalve Molluscs, the greater part of an easily-broken grey lime-
stone from Nepean, Ontario, Canada, belonging to the Chazy
Formation.

552 PROF. T. R. JONES ON SOME DEVONIAN AND

B. A larger collection, submitted by Mr. J. F. Whiteaves, F.G.S.,
Palxontologist to the Geological Survey of Canada, of Canadian .
Paleozoic Ostracoda, comprises :— .

B.a. § I. Upper Silurian (Upper Ludlow) Formation. Dr.
Honeyman’s “ Arisaig Group*, Division D.” Nova Scotia.

§ 1. In dark-grey limestone, with heematitic stains, and made up
of small organisms, such as the Ostracoda, together with 14 species?
of Mollusca, Brachiopoda, and Trilobites, and some Encrinital re-
mains. Stonehouse Brook, Arisaig, Nova Scotia. Division D.

1. Primitia mundula, J.. a small variety.—This 1s probably the
Primitia mentioned at p. 492, lines 38-41, ‘ Quart. Journ. Geol. Soc.’
vol. xxvi., but not the species referred to in lines 36-37.

2. Primitia ovata(?), J. & H.—An obscure oval cast, probably
the same form as referred to in ‘ Geol. Mag.’ 1881, p. 344.

3. Beyrichia tuberculata, Boll, young; B. tuberculata, var. pustu-
losa { (Hall), and var. Bronni (Reuter).—Of six more or less perfect
casts of this Ostracode, five are very near to Reuter’s variety tuber-
culata-gibbosa ; but the middle lobe is sometimes constricted, and
the marginal rim is smooth in some, and tubercled in others. Oneis
equivalent to B. Bronni, Reuter (‘ Zeitsch. d. D. g. Ges.’ 1885, p. 638,
pl. xxv. fig. 6. Another is a variety of B. tuberculata, with its
hinder lobe almost entire, and its anterior lobe hypertrophied.

4, Beyrichia cequilatera, Hall. February No. Q.J.G.S. page 18.
—Two specimens, like that figured in pl. 11. fig. 6, op. cit., differing
slightly from it in the proportions of the lobes. I have not yet met
with a specimen having*a lobe quite divided into two parts, as in
the woodcut, fig. 20, published in 1860.

§ 2. In a brown ferruginous cavernous band or bed-plane in a
dark-grey micaceous sandstone, with casts of Polyzoa, Encrinital
joints, Brachiopods, Trilobites, &. M*Adams Brook §, below the
falls and fort, Arisaig, Nova Scotia. Division D.

1. Beyrichia tuberculata, var. pustulosa (Hall), equivalent to
tuberculata-gibbosa, Reuter.—Three or four casts, badly preserved.

B. 6. § IL. Lower Silurian ; Canada.

§ 1. Trenton Limestone.—Dark-grey hard limestone, with Ostra-
coda, Encrinital joints, and small Brachiopods. Lorette, Falls of
the River St. Charles, Province of Quebec.

1. Primitia, sp.—Large, black, subconvex, boldly curved below,
obliquely and nearly equally rounded at the ends ;*faint mid-dorsal
sulcus.

* See Quart. Journ. Geol. Soe. vol. xx. 1864, pp. 333-345, and vol. xxvi. 1870,
pp. 490-492 ; also ‘Acadian Geology,’ 3rd. edit. 1878, pp. 565-570.

+ Determined by Mr. H. M. Ami, namely :—Murchisonia arisaigensis, Hall,
M. nova-scotica, H., Nuculiteserectus, H., N. cuneatus, H., N. subovatus, H.,
Megambonia cancellata, H., Pterinea, sp., Pholidops squamiformis, H., Lingula,
sp., Rhynchonella, sp., Chonetes tenuistriata, H., Spirifera subuculata, var. per-
lata, H., Crania acadiensis, H., Calymene, sp., Dalmania Logani, H., Beyrichia
pustulosa, H., Cornulites flecuosus, H., var. gracilis, H.

+ February No., page 18.

§ See ‘ Quart. Journ. Geol. Soc.’ vol. xx. p. 342.

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. 553

2. Primitia mundula, J., with a little tubercle on each side of the
sulcus. |

3. Primtia mundula, var.—Longer and narrower than the type ;
in some cases the sulcus is mid-dorsal ; in others it is much nearer:
one end. ,

4. Leperditia, sp. nov.?—Small, subconvex, oblong, with equally
rounded ends. Also another, similar, but not showing the overlap
so clearly ; small and black.

5. Beyrichia, sp. nov.— Narrow-lobed ; the two lobes in front are
nearly equal in length, parallel, slightly curved upwards and for-
wards, joined below, and passing into the base of the hinder lobe,
which is variably compound. Rather frequent.

6. Polycope, sp.—Sublenticular, with a short, straight hinge-line.

§ 2. Trenton Limestone.—Dark-grey limestone, which contains
Lntuites undatus. Falls of Lorette, Province of Quebec.

1. Leperditia, sp. nov. ?—Like § IT. $1, 4.

§ 3. Birdseye Formation.—Free specimens from the Birdseye
Limestone. Associated with Tetradium fibratum, Orthoceras multi-
cameratum, Bathyurus extans, &c. Lot 3, Concession 3, River
Front 1, Gloucester Township, Co. Carleton, Ontario, Canada.

1. Leperditia, sp. nov. ?—Subglobose, being relatively high and
thick; ends not quite equal, the posterior curve being fuller and
bolder ; greatest height and greatest thickness a little behind the
middle. ‘The overlap seems to extend all round the free margin.

§ 4. Chazy Formation. Chazy Limestone.

§1. Pointe-aux-Pins, Aylmer, Province of Quebec, Canada.

1. Isochihina ottawa, Jones. Variety. Abundant in a dark-
grey limestone.

§ 11. South of St. John’s Market, Quebec City.— Dark fine-grained
limestone.

1. Primitia, sp.—Suboblong, neatly curved on the free margin,
which bears a nearly uniform flattened rim; sulcus represented by
a distinct relatively large round pit. This may be related to P. re-
nulina, J. & H.

2. Primitia, sp.—Suboblong, ends rounded, but narrower (lower)
in front than behind ; sulcus mid-dorsal, distinct, but not deep.

§ 1. Chazy Limestone. Broad-street Asylum, Quebec City.

1. Leperditia, sp. nov.? Small, dark-coloured, with the greatest
ventral curve in the middle; front end subangular. Abundant in
a black limestone, especially on the bed-planes.

§1v. Chazy Shales. Broad-street Asylum, Quebec City.—Dark-
coloured, micaceous, shaly mudstone, somewhat ferruginous.

1. Primitia mundula (?), J.—Rather large, with a deep sulcus,
which has one of its edges strongly tuberculate.

2. Leperditia ?—Very neat cast of the interior of a left valve, but
the eye-spot, muscle-mark, and ventral flange are not shown. ‘The
greatest ventral curve is in the postero-ventral region.

3. Beyrichia, sp. nov.—Ovate-oblong, broad-lobed ; the two main

504 PROF. T. R. JONES ON SOME DEVONIAN AND

lobes are of nearly equal bulk, and unite with a broad curved junc-

tion below; the middle lobe is of an irregular and reversed club- -

shape, constricted at its upper third ; there is also a curved, low,
subsidiary ridge at one end, just within the margin. Abundant.

SIV. From Brittany, France.
Bryricata, M‘Coy. (See also pages 236-238, 246.)
36. Breyricuta Gurtireri, Tromelin. (Pl. XXI. figs. 2a, 26, 2¢.)
Beyrichia Guillieri, Tromelin, Association Francaise pour l’avance-
ment des Sciences; Compte rendu de la 4me Session, Nantes, 1875
(8vo, Paris 1876), p. 623, footnote (not figured).

Length 2 mm.; height 1 mm.; thickness 5 mm.

This is a three-lobed Beyrichia, as shown by the cast of left valve
in light-coloured mudstone, apparently not distorted by pressure.
In outline it is subovate, but straight on one edge (dorsal). The
two smaller lobes are club-shaped, high and rather narrow, forming
a fork, which opens upwards and forwards; the front lobe is low
down, near the antero-ventral margin, and gently curved; the
middle lobe is straight, oblique, and prominent, reaching the dorsal
margin. The junction of these two lobes below is continued to
the curved base of the large and rounded posterior or gigot lobe.

In some respects, as for instance in the proportions of the lobes,
one variety of Kiesow’s Beyrichia Lindstremt, from the Upper
Silurian of Gothland, namely fig. 4. pl. 1. p. 5, ‘ Zeitsch. d. D. geol.
Ges.’ 1888, bears a resemblance to B. Guzllieri, but in other respects
it differs.

The figured specimen is from the Lower Silurian (Ordovician)
strata at Domfront (Dep. Orne), and was kindly given by M. P.
Lebesconte, of Rennes. There were several individuals together.

In the same collection (M. Lebesconte’s) are numerous specimens
of the same species, but variously squeezed, and in some instances
much distorted, in the ‘“‘Schiste ardoisier inférieur ” (Ordovician),
below the “Grés de May,” at Laillé (Dep. Ille-et-Vilaine). One
specimen, somewhat shortened diagonally, from the postero-ventral
to the antero-dorsal region, has the two smaller lobes more vertical,
and all the lobes more equally separated, than in the figured
(normal) form ; but its thick, rounded posterior lobe is still character-
istic. In another case, pressure, transverse and nearly perpendi-
cular to the long diameter of the valve, has elongated the valve,
making its height scarcely a fourth of its length, and disturbing the
positions and proportions of the lobes.

This was compared with some Bohemian and other species by M.
Gaston le Goarant de Tromelin in a footnote to a memoir by him-
self and M. Paul Lebesconte on the Silurian Fossils of the Depart-
ments of Maine-et-Loire, Loire-Inférieure, and Morbihan (Anjou
and South Brittany), in the Report of the French Association for
1875, referred to above. It is mentioned also in that paper at
p. 620, as having been first found at Domfront (Orne), and as one

ee

SILURIAN OSTRACODA FROM NORTH AMERICA, ETC. SY5y9)

of the characteristic fossils (with B. bussacensis, J., and Primitia
simplex, J. [P. mundula?]) of the Upper Zone of the “ Schistes
ardoisiers,” belonging to Barrande’s “ Faune Seconde Silurienne” ;
also in Table B, opposite p. 636, as from Le Creux and Andouillé *.
In the ‘ Bulletin Soc. Géol. France,’ sér. 3, vol. iv. 1876, in the
memoir by MM. Gaston de Tromelin and P. Lebesconte on the
Primary Strata of the Department of Ille-et-Vilaine and other
parts of Brittany, B. Guillerc is referred to at p. 601.

It may be a cast of a variety of Beyrichia ciliata, Emmons (Q.J.G.S8.
February No., p. 19), with a sketch of which Mr. E. O. Ulrich has
kindly favoured me, and for which in a letter he has proposed the
new generic name of Ctenobolbina.

It may be here noticed that in M. Lebesconte’s collection there
are casts of another species of Beyrichia from the “ Schiste ardoisier
inférieur ” of Andouillé (Dep. Mayenne), which approaches more
nearly to B. Kledeni, M‘Coy ; the lobes, however, are thin, the an-
terior and middle lobes nearly symmetrically curved, with an oval
sulcus between them, and the posterior lobe much smaller than that
of B. Guilliert. One of these specimens was referred by M. de
Tromelin, in the ‘ Bullet. Soc. Géol. France,’ sér. 3, vol. iv. 1876,
p. 088, to B. reticulata, Bornemann, but they have no direct relation-
ship at all (see Pl. XX. fig. 14, and page 539).

From the same strata at Andouillé there occur (in M. Lebesconte’s
collection) Beyrichia bussacensis, J., ‘ Quart. Journ. Geol. Soc.’ vol. ix.
petoUepe vi. figs. 5 & 6, and ‘Ann. & Mag. Nat. Hist.’ ser. 2,
vol. xvi. p. 169, pl. vi. fig. 14; also Primitia. mundula, J., op. cit.
p. 174, pl. vi. figs. 28-31; a non-sulcate Primitia or Aparchites ; a
small Leperditia, related perhaps to L. nana, J., op. cit. ser. 3, vol. i.
p. 244 (“ L. canadensis, var.”), pl.ix. fig. 12; and a Cytheroid form,
possibly a Bythocypris, near B. symmetrica, J., op. cit. ser. 5, vol.
Xie, Pe eLSG; pl: vil. ties. 3, 4, 7.

EXPLANATION OF PLATE XX.
Devonian Ostracoda, with one (fig. 14) Silurian.

Fig. 1. Beyrichia devonica, Jones. A cast of the inside of a crushed valve;
one lobe partly worn away. a, left valve; 0, edge profile. Bos-
phorus. X12 diam.

————. 4, left valve; 6, edge profile. Devonshire. 6 diam.

Right valve, obliquely squeezed. Devonshire. x6 diam.

. Beyrichia subquadrata, sp. nov. Left valve (reversed drawing of a

hollow cast). Ontario Co., New York. x15 diam.

. Bola Hinde, sp. nov. Left valve. Highteen-mile Creek, Lake

Erie, N.Y. X15 diam.

. Beyrichia Kolmodini, sp. nov. Left valve. Clarke Co., Indiana.

x15 diam.

. Octonaria Linnarssoni, sp. nov. Carapace. a, left valve seen; 0, ven-

tral view. Clarke Co., Indiana. 15 diam.

Im oO Boob

* The Entomostraca mentioned as occurring in the same strata with B. Guil-
liert I have not been able to recognize in the collection kindly submitted by
M. Lebesconte last year, excepting Bolbozoe anomala, B., and Beyrichia bussa-
censis, J.

Q.J.G.S. No. 184. On

556 DEVONIAN AND SILURIAN OSTRACODA FROM NORTH AMERICA, ETC.

Fig. 8.
9.

Strepula plantaris, sp.nov. a, left valve, outside; 6, inside. Highteen-
mile Creek, Lake Erie, N.Y.
Moorea Kirkbyi, sp. nov. a, left valve; cast (here the furrow is ~
stronger than the ridge); 0, edge profile. Ontario Co., N.Y. x15
diam.
——. 4, left valve; cast (here the ridge is stronger than the
furrow inside it); 0, edge profile. Ontario Co., N.Y. 15diam.

. Primitia Clarkei, sp.nov. Right valve, cast. Ontario Co., N.Y.

15 diam.

. Bollia bilobata, sp. nov. Left valve ; cast, with one lobe and the junc-

tion much worn. Ontario Co., N.Y. X15 diam.

. Eurychilina reticulata, Ulrich. a, convex cast of the inside of a left

valve; 0, hollow cast of the outside of the same individual valve.
Ontario Co., N.Y. X10 diam.

. Beyrichia reticulata, Bornemann. a, convex cast of the inside of a

right valve (taken with gutta-percha); 0, hollow cast of the outside
of another valve. Sardinia. %7 diam. Reproduced trom careful
tracings of the four original figures; for these I am indebted to the
kindness of Chev. W. P. Jervis, F.G.S., of Turin. (Fig. 14a is
“fig. 3,” and fig. 140 is ‘‘ fig. 2b” of the originals.)

EXPLANATION OF PLATE XXTI.

Silurian Ostracoda, with one (fig. 1) Devonian.

Fig. 1. Beyrichia Kledeni, M‘Coy. Variety. a. right valve, with hypertrophy

2
3
4.
+)
6

“J

10.
Ti.

of the antero-ventral lobe; 0, ventralview. Ontario Co., New-York
State. 7 diam.

. Beyrichia Guilliert, Tromelin. a, left valve, cast; 6, ventral view ; ¢,

front view. Domfront, Brittany. X20 diam.

. Bardia anticostiensis, sp. nov. 4a, right valve; 0, ventral profile.

English Head, Anticosti. 15 diam.
Bythocypris? obtusa, sp. nov. a, right valve; 6, ventral profile.
English Head, Anticosti. X15 diam.

. Macrocypris? subcylindrica, sp. nov. a, right valve; 6, ventral profile.

English Head, Anticosti. 15 diam.

. Polycope sublenticularis, sp. nov. a, right valve; b, ventral profile.

English Head, Anticosti. 15 diam.

. Beyrichia diffissa, sp. nov. Left valve. Jupiter River, Anticosti,

«15 diam.

. Leperditia frontalis, sp. nov. a, right valve; 6, ventral profile. Near

the Jumpers, Anticosti. <4 diam.

. Bollia semilunata, sp.nov. a, left valve; 0, ventral view. South of

Junction Cliff, Anticosti. x25 diam.
Primitia Billingsii, sp. nov.. Right valve. West of Jupiter Road,
Anticosti. 15 diam.
Bythocypris? Lindstremii, sp. nov. a, right valve; 0, edge view;
e (Ge on the Plate), end view. S. of Junction Cliff, Anticosti.
x 25 diam. j
Discussion.

Dr. HiypE wished to express the obligations of geologists to
Prof. Jones for the excellent work which he had done amongst the
Entomostraca ; and particularly on the present occasion, for the
clear manner in which he had explained the wide distribution of
some of the species.

The PresipEnv alluded to the long years of arduous labour which
Prof, Jones had bestowed on these minute fossils, and to the inter-
esting results he had obtained from them.

PLATEAU-GRAVELS OF EAST BERKS AND WEST SURREY. 557

33. Norse on the PratEAv-eRAVELs of East Berxs and West SURREY ;
‘ their Aan, Composrrion, and SrructuRE. By the Rev. A. Irvine,
D.Sc. (Lond.), B.A., F.G.S. (Read May 21, 1890.)

(Abridged.)

In the year 1883 my first paper on Tertiary geology * was published
by the Geologists’ Association. In dealing with the gravels of the
Bagshot district I pointed out that my observations up to that date
had led me to regard the Plateau-gravels as Pre-glacial and con-
temporaneous with the Crag. This view has been worked out in
fuller detail by Prof. Prestwich in Part III. of his recent paper
“On the Mundesley and Westleton Beds and their extension in-
land.” + It was a gratification to find myself in accord with him |
as to their pre-glacial age. For several years past it has been in
my mind to give the results of further studies in this subject to the
Society ; he has happily forestalled me, and brought to the con-
sideration of the subject a much wider range of data than I could
command. Still it seems that the argument by which he arrives at
the conclusion that these Plateau-gravels are of later Pliocene age is
not a very strong one; for, when the Diestian age of the Lenham
deposits is admitted (and Mr. Clement Reid’s conclusion £ that they
both are of older Pliocene age is also admitted), the assumption (which
forms the cardinal point of the whole argument) that certain outlying
sands high wp on the slope of the North Downs are contempo-
raneous with the Lenham deposits has no other support than
their being at approximately the same height; while the litho-
logical evidence points to their Eocene age§. This might very
well be, if—as seems probable from various considerations—the
north-western portions of the Weald partook in Jater Eocene time
of the movement which is recorded in the upheaval of the axis of
Kingsclere and Inkpen ||. Again, there is the absence of all marine
deposits of Miocene age in the South of England, indicating (in
addition to many other collateral considerations) a high degree of
probability that the Miocene was the period of maximum elevation
of this part of Europe, rather than one of depression beneath the
sea. ‘lo this long period of Miocene (and Pliocene) elevation of the
Weald we must look, I think, mainly for the supply of the vast
amount of flinty subangular detritus under notice. From long
exposure on the surface of the Chalk, as chemical erosion proceeded,

* See Proc, Geol. Assoc. vol. viii., “On the Bagshot Beds of the London Basin,
and their associated Gravels.”

tT Quart. Journ. Geol. Soe. vol. xlvi. pp. 155 et seq.

{ See Nature (1886), vol. xxxiv. pp. 341, 342. I have discussed this matter
with Mr. Reid, and have examined the Lenham fossils in the Museum of
Practical Geology.

§ See some remarks by the author in the Geol. Mag. 1888, pp. 128, 124; and
1890, p. 406. —

|| In Topley’s memoir “ On the Geology of the Weald” there are many facts
which point to this conclusion.

282

558 REY. A. IRVING ON THE PLATEAU-GRAVELS

it suffered that amount and kind of lithological change * which,
with subsequent fluviatile transport for distances of 10 to 15 miles,
would give such materials the character and the subangular form >
which they for the most part are found to present in the Plateau-
gravels. ‘The flint pebbles, with which they are now intermingled,
were probably preserved from the action of those atmospheric agencies
which induced the lithological changes in the subangular flints, by
having been sealed up in the Eocene strata, after having been formed
by shore-actiony. These two chief constituents of the Plateau-
gravels, together with the subangular fragments of Neocomian chert,
were intermingled, no doubt, in the rivers which flowed from the
Wealden Hill-range, as the denudation of the Eocene beds in their
formerly southerly extension proceeded, with the increased accentu-
ation of the anticline, pari passu with the transport of the angular-
flint material by rivers from the Weald across the northward-
sloping plateau of Eocene land.

These Plateau-gravels seem to have no necessary connexion in
time or otherwise with the ‘‘ Mundcsley and Westleton shingle” of
Prestwich, since the flinty materials found in that might very well
have been derived from an elevated Chalk region of Mercia and
Kast Anglia.

Even the high-level gravels of the country north of the Thames may
have had to a large extent a subaérial origin; for the fact that so many
of them are covered up by boulder-clay (and so protected from the
solvent action of carbonated atmospheric waters) renders it extremely
difficult to account for their non-fossiliferous character by the
hypothesis of “decalcification” t. The above explanation of the
intermingling of such different forms of the flinty material was put
forward in 1883; and was, as then pointed out, suggested to me
by my previous observations of the vast accumulations of angular
flint material (mere insoluble residue) found to-day on the top of
Saint-Boniface Downs in the Isle of Wight §. The quartz-pebbles
mentioned by Prof. Prestwich in his recent paper, and by Prof.
Rupert Jones ||, are in my experience rare in the Plateau-gravels ;
nor do I believe, after sifting the evidence, that Mr. Monckton’s
large rolled block of vein-quartz came out of them 4.

Observation in the field tells us that as we work south the
presumably older gravels become, as we should expect, more angular,
' and acquire a more massive development, most fully seen in the vast

* See Appendix i. Note e, in my “Chemical and Physical Studies in the
Metamorphism of Rocks,” p. 103 (1889).

+ See Proc. Geol. Assoc. vol. viii. 1888, pp. 167, 168; also the Quart. Journ.
Geol. Soc. vol. xliv. p. 184.

{ Prestwich, op. cit. p. 146. The predominance of land and freshwater
remains in the list of organic remains given in Quart. Journ. Geol. Soe. vol.
xlvi, pp. 115, 116, seems to point to an estuarine origin for the beds at_ Westleton
and Mundesley, suggesting a terrestrial origin for the higher beds inland.

§ See also the new edition of the Geol. Survey’s ‘Memoir on the Geology of
the Isle of Wight,’ 1890, p. 210.

|| See Proce. Geol. Assoc. vol. vi. p. 439.

“] See Quart. Journ. Geol. Soc. vol. xlvi. p. 154.

OF EAST BERKS AND WEST SURBEY. 559

accumulations of coarse flint detritus which cap the highest ground
remaining of the Bagshot ¢errain, on Cesar’s Camp (600', ordn.
datum) and Hungry Hills (550', 0. d.) above Aldershot *. These
vast accumulations (in places cemented into a conglomerate) of
almost unworn flints, with scarcely a trace of even the rudest
stratification, impress the mind more than anything I have seen in
this part of England with a vivid idea of the enormous extent of the
destroyed Upper-Chalk strata, which once arched over the region
lying directly to the south. They may be the remains of the
insoluble débris which accumulated under subaérial conditions
along the base of the northern slope of the old Miocene Wealden
mountain-range ; materials, which, by their assortment and trans-
port in part across the sloping plateau of the old Tertiary district
immediately to the north, furnished the chief constituent, in a more
rolled and worn condition, of the Plateau-gravels of the ‘Southern
Drift.”” I know of. nothing with which they compare so well as the
old (pre-glacial) ‘ Schotter ” (unstratified débris often conglomeratic)
of the lower Alpine valleys, which Von Hauer f and other authors
have described under the name “ Terrassen-Diluvium.”

Such materials, however, as were carried away northwards and
deposited in the lines of river-drainage or spread out on flats, where
the declivity of the plateau diminished {, assumed a more or less
stratified arrangement. ‘This structural character is of great impor-
tance in recognizing the ancient Plateau-gravels in the sections
furnished by the numerous gravel-pits opened of late years on the
hill-tops, as the demand for road-material has increased with the
opening-up of this ancient forest-country. The structural facies they
most commonly present is that of interstratified masses of sand §
(often loamy) and shingle, the sand-layers being generally coarse and
ferruginous, with pronounced oblique lamination or current-bedding.
Even where there are not distinct layers of sand in the sections,
the stratification is generally manifest from the horizontal position
of the longer axis of the pebbles and of the flint and chert fragments,
allowance being made for the occasional local disturbance of these
by the roots of pine-trees, by “soil-cap” movements on a small
scale, and by the formation of talus at the expense of the plateau-
gravels, owing to the removal of the sandy materials of the subjacent
hill-flanks by ordinary agencies of erosion ||.

Further field-work since 1883 has shown me that the plateau-
gravels must be recognized down to levels (as we work northwards)
as low as 300 ft. (o.d.) and even lower. These are, of course, the

* T cannot recollect ever meeting with rolled flint pebbles in these gravels.

t See ‘Die Geologie,’ 1878, p. 704.

+ Somewhat, as I conceive, after the fashion in which the broad expanses of
gravelly detritus are formed by the Alpine rivers as they debouch upon the
Plain of Bavaria.

§ These are sometimes cemented by ferric oxide into the hard ‘“ pan” occa-
sionally used for building, and which defies the action of the atmosphere, as
in the Roman Wall of Silchester. ‘

|| Often resulting from the high-level springs which frequently issue from the
base of the gravels; Rupert Jones, Proc. Geol. Assoc. vol. vi. p. 434,

560 REY. A. IRVING ON THE PLATEAU-GRAVELS

youngest deposits of the series ; for I conceive that the series as a
whole covers a very large interval of geologic time, perhaps the.
whole of the Pliocene Period, the oldest of them (on Cesar’s Camp
and Hungry Hill, Aldershot) being possibly of very early Pliocene
age. On the other hand, the patches of unstratified and angular
gravel found on the higher slopes and minor bluffs of the present
valleys are probably mere “‘ run-of-the-hill ” of the later denudation
of the country, and do not necessitate the idea of glacial action.

Localities furnishing Sections of the Plateau-gravels.

Locality. County. Above o.d.
feet.
Cesar's Camp and Hungry Hill (Aldershot) ............ Hants. 500 to 600
Hook Wood (north of Netley Heath)* .................. Surrey. 500 to 600
Macc ol [rel (een tains MI, US Aes bat be ol ae lea El x 390 to 400
Bemiley Iuideest rh ou ers intense cere ee 3 400
Bagshot Orphan=Asy lunmif yas ot huateis betes p eek) eaapeebtion = 400
Obelisks Halle( Camberley) js. te ca-sshaerckitees cameo ieee ee 370
Crawley (all. (Camberley). « xin.se<nsenemmarep nee beac eameace by 350
Lone Down (Sanghwrst)) \..c0s-c0ss0- done -eeeace enero Berks. 350
Hdgeburrow (Sandliwrst))! 122 7Va Ae kek cee aceeoonee 5 370
roddimoaoi: i): io Leas poats Ms) ceed pen eee eee be 400
Cesar’s Camp { (Hasthampstead).............606 ceseeeees a8 400
Wagbullock Hill (Easthampstead) { .............eeeeeeee ss 400
Grane Hal (Sn ey) tend. seece ee <a een mere aeehen tata. 5 400
Finchammstead Fides Soi020- 2. cccveecesdhaescomseenc cena rae Mi 330
Power El (Swimley) 5... jan! 2205 e eee Oka nek a ook oe . 350
Rvee-Course Ell) (Ascot) cher ssictinmteaden Manne nenree aes s 300+
(amo cETGilt GARGOB) So.) c-5 ncaa ees saee Manske ities meee cians 3 300+
Chevy Wow (CASCOG) ices vesinewclicxa ls nied Ace. -» coakoewee seine * 300+
Goatinmnest trill (ASCO) saterccns cheer ntaekeenste ae dceene eee 5 320
Buckhurst) all |e a Wee band deehed caavesasaeateneae sh 300+
Parley Halls (Sotceadine!) .25...)23-e.boasdieesnteaecep Pens 34 280
PB GAOL ae. A hs oe te i eee ok eee oe 280

The whole of Easthampstead Plain and Chobham Ridges is probably
capped with the same sort of gravels as are exposed at the localities
mentioned.

In nearly all the sections the stratification is clear, and in most
cases as pronounced as it is in the Low-level Gravels of the present
Valley of the Thames, at Reading, at Ealing, and at Kensington ; a
fact which seems to point clearly to their river-origin. They are
totally destitute of organic remains, except such as have been
brought in the flints from the Chalk (impressions of fragments,
spines, and occasionally complete casts, of Micraster, Galerites,
Ananchytes, Pecten, Inoceramus, &e.), or as Sponge-spicules from the

* Flint pebbles and coarse unworn flint débris, interstratified with a stiff
loam.

+ Nine feet of gravel proved in the well-section (see ‘Mem. of the Geol.
Survey,’ vol. iv. p. 587).

+ Three great spurs at the north end of Easthampstead Plain. Open gravel-
pits may be seen on each of these hills.

§ Three extensive pits worked for gravel.

|| This gravel extends some distance to the north in the direction of Binfield.

“| See Geol. Mag. dee. 111. vol. iv. pp. 112, 115.

OF EAST BERKS AND WEST SURREY. 561

Neocomian. On comparing their altitudes some allowance has to be
made for slight Post-Pliocene movements producing some changes
of the relative levels. They remain as indexes of the ancient
Pliocene lines of drainage northwards, having preserved the present
hills from degradation ; while the originally higher ground has been
scored with the present valley-system.

Evidence of Glaciation.

With one apparent exception * I know of no distinct evidence of
glaciation in the part of England referred to in this paper, nor in
the Thames Valley above 240 ft. (0.d.), though many examples of it
have been described at lower altitudes. If we assume, therefore,
that these mark the period of the maximum glaciation of. the old
Thames Straits, we have to allow for a very considerable amount
of excavation of the present valley-system of this cae of England
prior to the Glacial Period.

§ 1. Ina new pit fT at the Brickyards of Messrs. T. Lawrence and
Sons, close to the Nine-mile Ride, between the Wokingham and
Binfield roads, a fine section has been recently opened, exposing the
laminated basal clays of the Middle Bagshot, with the underlying
Lower Sands. The clays here are splendidly contorted, and overfolded
by great masses of gravel, in some cases weighing several tons aplece,
having been driven, probably in a solid (frozen) condition, into them.
The lamination of the clays is distinctly traceable in the contortions,
and leaves no doubt as to the nature of the agency which has here
been at work. Altitude, 230 to 240 ft. (0.d.).

The gravel is one of the secondary or terrace-gravels of the
country, derived from the older Plateau-gravels, with an increased
proportion of flint pebbles, furnished by the destruction (prior to
the glacial action) of the pebble-beds of the Bagshot terrain to the
south.

§ 2. In the Tangley cutting of the South-Western Railway near
Wokingham, on the other side of the valley. very distinct glaciation
of the same laminated clays is seen at the top of the cutting above
the Lower Sands at about 220 ft. (0.d.).

§ 3. At Sunninghill the same succession is seen in the railway-
cutting, with similar folding, puckering, and included pockets of
gravel, at about 220 ft. (0.d.).

* The case here referred to is that of a completely unstratified gravel, with
scarcely any pebbles in it, which occurs on Lodge Hill, Broadmoor, at 400 ft.
(o.d.). The angular fragments stand in all positions in it. May it not, from
its exceptional character and altitude, be a glacial deposit of the cold Plio-
cene age (Htheridge, ‘Manual of Geology,’ p. 652; and Lyell’s ‘Student’s
Elemevts,’ p. 181). The pit has been recently re-opened. It reminds me of
nothing so exactly as of the moist masses of loose, incoherent, subangular stuff,
which every observer of higher Alpine phenomena is familiar with in the trail of
the minor snowfields as they retreat up the smaller valleys during the summer. A
repetition of such deposits of trail for a number of seasons “would give just
what we see in the pit on Lodge Hill.

+ This pit has been considerably extended since the note referring to it at the
foot of p. 164 of vol. xliv. of the Society’s ‘ Journal’ was written.

562 REV. A. IRVING ON THE PLATEAU-GRAVELS

§ 4. Other evidences of glaciation may be seen (a) in an unstra-
tified clay with pebbles standing erect in it, upon an older angular |
and sandy gravel, which les upon an eroded surface of London
Clay in the Brick-and-Tile Company’s Brickyard north of Bracknell ;
(6) in what appears to be a lacustrine deposit, as if in an extra-
morainic lake, above the Bagshot beds in the brick-pits at Warfield *,
wrongly described (as I venture to think) as a part of the Bagshot
formation ; (¢) in the California clay-pits at Finchampstead +, where
a similar lacustrine deposit probably occurs above the Middle Bagshot
Clay, at about 230 ft. (0.d.).

The phenomena described in §§ 1, 2,3, I take to be due to the
mechanical work of floating ice, as pack-ice was formed from time
to time in the old Thames Straits under the influence of high
winds f.

Conclusions.

(1) Looking at the distribution of the Plateau-gravels of the
district under consideration, their roughly-stratified structure, their
constituent materials, the entire absence in them of contemporaneous
organic remains, the frequent occurrence in them (especially near
their base) of blocks of concretionary sandstone § (in many cases
unworn, in others smoothed on the upper surface by the scouring
action of sand and water), the frequent reconstruction and rough
stratification of the immediately subjacent Upper Bagshot Sands (on
which for the most part these gravels rest), and the marked erosion
of these sands in many places beneath the gravels,—it is difficult to
resist the conclusion that they had a fluviatile origin, the materials
having been derived from the south.

(2) The only conception I can form which harmonizes with all
the evidence available, is that of an elevated district of the older
Tertiaries, subjected to subaérial waste, and having a general slope
to the north towards what may have been an estuarine arm of the
ancient Anglo-Germanic Sea, on the western margin of which the
Crag was being deposited at levels not very different from those at
which it is found to-day ; the present gravels marking the drainage-
courses of the later Tertiary valleys, while the present valley-system
of the district occupies those portions which then formed higher
ground, and has been initiated owing to the absence of the gravel-
capping to which the present hills owe their preservation.

x Compare Section F, p. 386, vol. xliii. Quart. Journ. Geol. Soc. 1887.

t Ibid. vol. xliv. p. 172, Section Q.

+ In all such cases the piling up of the ice takes place too quickly for defor- .
mation of the ice-masses to proceed pari passu with the increase of pressure.
We thus get a mechanical agency brought into play quite different from anything
which we can rationally postulate from the slow movement of a glacier. See
my paper on the “ Mechanics of Glaciers,” Quart. Journ. Geol. Soc. vol. xxxix.;
also the published work of Prof. Spencer, Geol. Mag. April 1887, and ‘ American
Naturalist,’ vol. xxii. 1888.

§ In the Proc. Geol. Assoc. 1883, I gave reasons for rejecting the Sarsens as
evidence of a glacial origin of the gravels, in and near the base of which they
usually occur.

OF EAST BERKS AND WEST SURREY. 563

(3) The more ancient arterial line of drainage of southern
Eocene England * having been obliterated by the silting up of the
Kocene estuary + by the Bagshot Beds, and subsequent regional
movements of the Mesozoic strata to the south, the modern Thames
Basin began to be outlined, although probably its main line of
drainage did not coincide exactly with the modern valley of the
Thames.

(4) Distinct evidence of glaciation at much lower levels than the
plateau-gravels (210 to 240 ft., o.d.) being now to hand in the district,
and this being presumably the work of floating ice in the old Thames
Straits, we may (in the absence of distinct traces of glaciation at
higher levels) assign something like 200 feet (vertical t) of the
excavation of the present valley-system of this part of England to
a period intervening between the deposition of the plateau-gravels
of the Southern Drift and the Glacial Epoch at its maximum.

(5) The deposition of these Plateau-gravels appears to have
occupied a considerable portion (perhaps the whole) of the Pliocene
Period ; the only data available for fixing the time of the initiatory
stage of their deposition being the inconclusive evidence furnished
by the well-known Lenham deposits. The results of my own work
and of the independent researches of Prof. Prestwich are thus seen
to confirm the suggestions of Sir A. C. Ramsay §, made years ago,
as to the pre-glacial age of these Plateau-gravels, and of the present
valley-system of Southern England.

Discussion.

Mr. Moncxron had no doubt that the block of quartz referred to
in the paper came from the Plateau-gravel. Everybody was agreed
as to the materials of the Plateau-gravels having come from the
south-east. Such contortions as described were generally accepted
as evidence of snow or ice. The age of the Plateau-gravels was
admittedly doubtful; and, if possible, the Author had rendered
their age more unsettled than ever. He (the speaker) inquired
as to whether the Author used the term Boulder-clay with chrono-
logical significance, and what evidence was brought forward as proof
of the marine or fluviatile origin of the Plateau-gravels.

Prof. Ruprrr Jonus said that Mr. Godwin-Austen referred the
Plateau-gravel to an early Tertiary age. He had lately seen, at
Cuckmere, conditions of the shingle analogous to those which
Dr. Irving had suggested for the Plateau-gravel. He believed
that this, as well as the lower gravel, exhibited the effects of ice-
action.

* See “ The Stratigraphy of the Bagshot Beds, &c.” Quart. Journ. Geol. Soe.
vol. xliv. pp. 181, 182.

t This question has been discussed in my papers on the Bagshot Beds in the
Quart. Journ. Geol. Soc. vols. xiii. & xliy,

{ To this it would be easy to attach an exaggerated importance, if we over-
looked the easily-destructible nature of the Bagshot strata.

§ ‘Physical Geography and Geology of Great Britain’ (5th ed.), p. 533.

564 PLATEAU-GRAVELS OF EAST BERKS AND WEST SURREY.

The AvrHor, in reply, stated, with reference to the contortions,
that the cases cited by Mr. Monckton hardly bore on the question, as
they occurred much lower down the Thames valley, and at lower
altitudes. The main point on which he differed from Prof. Prestwich
was that he could not accept his later Pliocene date as fixing the
minimum time. The term “ Boulder-clay” was used only in a
descriptive sense. He thought that one of the speakers had not
given attention to all the facts brought forward.

ile

Quart.Journ. Geol. Soe . Vol. XLVI. PI.

SETHE INERTIAL SIGUNIE A“ GYOUOUON OOO)

a 2
= ees JE . g
a re a
<< PE 5
— :
<< E
/ s ig
Sy , 2
toe He Se <
22S WV BI =< \

‘amor g ubvyt ~ z ae A |

W.i Crowther del. et hth.

:
}

MR. J. W. DAVIS ON A NEW SPECIES OF COCCODUS. 565

34, On a New Srrcies of Coccopus (C. Linpstrami, Davis). By
James W. Davis, Esq., F.L.S., F.G.S. (Read May 21, 1890.)

{PLATE XXIT.]

Wuitst on a visit to Stockholm last year my attention was drawn
by Professor G. Lindstrém to a small fossil fish from the Hard
Chalk of Hakel in Mount Lebanon, which had been presented to the
Museum of the Academy by the Duke of Leuchtenberg. It is
nearly related to Coccodus armatus, Pictet *, and exhibits for the
first time an almost complete outline of the body of a member of this
genus. It is smaller than the species described by Prof. Pictet, and
presents several features which dissociate it specifically from
Coccodus armatus.

The fish is 0°065 m. in length from the tip of the snout to the
base of the tail; its height in front of the dorsal spine is 0:022 m.,
and rapidly diminishes to the peduncle of the tail; anteriorly the head,
triangular in outline, terminates in a pointed snout. Nearly two-
thirds of the anterior part of the body is covered with strong osseous
plates, the remaining portion being devoid of protection. The
impressions of about twenty vertebre remain; they were probably
cartilaginous, for neither in this specimen, nor in those found
previously, is there evidence of bony centra. Strong osseous neural
spines with branching neurapophyses extend from the vertebral
column, and midway along the dorsal surface support nine inter-
neural spines ; the latter are thick towards the distal extremity and
afford a broad base of attachment for the rays ef the dorsal fin.
The dorsal fin extends 0°006 m.; its anterior ray is 0-006 m.
behind the spine, and its posterior ray is separated by a distance of
0-010 m. from the base of the caudal. The hemal spines are similar
in structure to the neural, and have attached to them strong inter-
hemals, apparently broader f than the interneurals, and which
support the rays of the anal fin. The latter has its origin immediately
behind the bony armature of the head and abdomen, and extends
thence half the distance to the tail. The caudal fin is supported by
articulated rays, of which ten can be counted supporting the lower
half, and probably an equal number constituted the upper half.
The rays are 0:01 m. in length. The termination of the vertebral
column is dilated to a radiating flattened piece, with which the
caudal fin-rays are connected. The median rays of the tail are
longer than those above and below, presenting a uniformly convex
posterior margin. ‘The pectoral and ventral fins,if such existed, are
not preserved.

* FB. J. Pictet.—“‘ Description de quelques Poissons fossiles du Mont Liban,”
1850, p. 51, pl. ix. fig. 9.
_ James W. Davis.—“ The Fossil Fishes of the Chalk of Mount Lebanon, in
Syria,” Trans. Roy. Dublin Soe. ser. 2, vol iii. 1887, p. 546, pl. xxx. fig. 1.
tT Rather too weak in the illustration.

566 MR. J. W. DAVIS ON A NEW SPECIES OF COCCODUS.

The head and anterior part of the body are protected by osseous
plates of considerable thickness and strength, surmounted at the
occiput by a large and massive spine. The spine is situated near
the middle of the back at a distance of 0-04 m. from the tip of the
snout. It rises to a height of 0°015 m. from the dorsal surface,
and is inclined at a very slight angle backwards. The anterior part
of the base of the spine is connected witn the osseous plates of the
cranium by a broad expansion of its surface, which is overlapped by
the cranial bones. The surface of the spine is ornamented by
longitudinal striations, parallel with its anterior margin; the striz
on the posterior portion disappearing along that surface. The
posterior margin of the spine is armed with a series of nine or ten
denticles—long, pointed, and robust, equal in length to the diameter
of the spine in its upper part. The denticles are all inclined up-
wards, at an angle with the spine of about 45 degrees.

The orbit (Or.) is medium-sized, situated very high, and at a
distance of 0:023 m. from the extremity of the snout. The inter-
orbital space is occupied by one or more osseous plates, extending
from the base of the spine to a distance in advance of the orbit.
Connected with this is a long plate terminating in a sharp-pointed
snout, and probably overlapping the maxillary bone (Mw.). The
surface of this bone, and also of those occupying the interorbital
area, is covered with minute tubercles, arranged more or less in lines
parallel with the longer axis of the plates. The under surface of
the head is covered with a series of plates: the most anterior is
- probably the mandible (Mn.). It does not extend so far forward as
the maxillary bone, and its posterior portion assumes a V-shaped
form: the upper branch, extending parallel with the maxille, may
be the dentary, whilst the lower and longer branch probably
constitutes the articular bone. Between the orbit ( Or.) and the oper-
culum (Op.) is a series of bones, which in this specimen are some-
what indeterminate. The space between these and the lower jaw
is not very well-preserved ;’ but there are indications of a large, more
or less triangular plate, whose under surface was covered by a series
of lines radiating from above downwards, and covering the region
occupied by the mandibular suspensorium. ‘The gill-cover is large,
and consists of preoperculum (Pop.), operculum (Op.), and probably
suboperculum (Sop.). The anterior margin of the preoperculum
(Pop.) is almost straight, and extends in an oblique line from the
anterior base of the spine to the posterior extremity of the mandible.
It is a long and narrow bone; attached to its posterior margin is
the operculum (Op.), larger in size, and with a circular posterior
margin extending forwards beneath the preoperculum. ‘The
surface of both is covered with minute tubercles arranged in lines,
The space beneath the operculum may have been occupied by the
suboperculum. Behind the operculum and extending to the
abdominal aspect of the body is a large bony plate representing the
clavicular portion of the scapular arch (Sc.). The posterior extremity
of the bone forms a process extending considerably backwards; its
upper portion is enveloped by the operculum ; its surface is orna-

MR. J. W. DAVIS ON A NEW SPECIES OF COCCODUS. 567

mented in a manner similar to that of the external bones already
described. )

Coccodus armatus, Pictet.—The specimen described by Prof. Pictet
(op. cit. pl. ix. fig. 9) exhibited the under surface of the upper jaw,
with the arrangement of the teeth ; and the under surface of the
shoulder-girdle, to which is attached a pectoral spine. ‘The skeleton
is regarded as being of a more fibrous than osseous structure; the
vertebral column is deformed by fossilization ; the osseous spines are
large and solid, and probably held the fins. The pectoral arch recalled
to the mind of the learned author the organization of the Rays. The
upper jaw is armed with four ranges of flat teeth, which cover the
entire surface of the palate; they are preceded by a number of
small teeth at the extremity of the jaw. The teeth of the lower
jaw are represented by a single row ; they are smaller than those
of the upper, and Pictet found on examination that they were
attached to the jaw without roots, in a similar manner to those of
Pycnodont fishes. The spines attached to the pectoral arch recall
those of the Pimelodus Clarias, Geoff., a Siluroid fish found in the
Nile, as does also the bone to which it is attached, extending along
the side of the body. It also approaches the Sclerodermic Ostracion
in the bony covering of the anterior portion of the body. In
conclusion, Pictet considers that the fish most nearly approaches the
Siluroids, with some Sclerodermic resemblances, but differs from both
in the character of the teeth.

The second example of C. armatus, described in the Transactions
of the Royal Dublin Society, is also imperfect, but exhibits a lateral
presentment of the bones of the head, a part of the vertebral column,
and the position of the dorsal fin. The fin referred to as the
¢¢ ventral,” which should be “anal,” is shown by the specimen now
described to be the base of the caudal. The anal fin is opposite to
the dorsal, but is absent in that specimen. The arrangement of the
teeth is exhibited, and is similar to that in the specimen figured hy
Pictet. The arrangement and character of the bones covering the
posterior part of the head are shown. ‘There is an expansion of the
pectoral arch into three prominent, pointed, spinous processes. The
first has its origin behind the median portion of the operculum, and
from a broad base extends downwards, with a curvature ending in a
more or less pointed apex. A second and smaller process extends
in an outwardly diagonal direction from the body. The third
extends backwards parallel with the abdominal surface of the body,
becomes attenuated, and ends in a point. The surface of each is
striated and their margins are denticulated.

Coccodus Lindsticemt, sp. nov.—The example now described, whilst
possessing a sufficiently clear generic resemblance to Coccodus, as
defined and described by Pictet, presents several peculiar features,
which differ from the detailed characters of C. armatus, and renders
necessary the institution of a separate species. The size of the body
and the character and arrangement of the teeth are similar in all
the specimens previously described ; and the pectoral spine exhibited
in Pictet’s figure is probably represented by the lower one

568 MR. J. W. DAVIS ON A NEW SPECIES OF COCUODUS.

figured in the Transactions of the Royal Dublin Society (1887,
pl. xxx. fig. 1). In the species now described an equivalent of this
spinous process does not appear, unless the posterior extension of
the scapular arch could beso construed. The posterior basal exten-
sion of the dorsal spine is also very different in the two forms. The
dentition of this specimen is not exposed, and the size of the body is
only about one-third that of Coccodus armatus, Pictet. The dorsal
fin in C. armatus is separated from the occipital region by a distance
equal to the length of the head; but in this smaller specimen it is
comparatively near, and was, compared with the size of the fish, a
larger fin.

The imperfection of the specimen at the disposal of Professor
Pictet led him to the conclusion that the fish presented the most
marked analogy with some of the Siluroids, indicating more parti-
cularly Synodontis, locally termed “Schal,” which is found in the
Nile, and Pimelodus, also found in the Nile, but more abundantly in
the rivers of South America. These fishes are protected by dermal
coverings on the head, and possess pectoral and dorsal spines; but
in Synodontis the mouth is small, and is armed only with weak,
though long, pointed teeth ; and the jaws of Pimelodus are edentu-
lous. The arrangement of the fins, as shown in the specimen now
described, is quite different. from that of the Siluroids named above ;
in the latter the dorsal fin is attached to the spine ; in Coccodus it is
widely separated from it; and the anal isshorter and not of the form
of that in Coccodus. The great resemblance of the teeth of Coccodus
to those of the Pycnodonts, and the cartilaginous character of the
vertebre, indicate a relationship with the Ganoids; but its exact
location in that group must still remain problematical.

I have pleasure in appending the name of my friend Professor G.
Lindstrom, to whom I have been in many ways indebted, to
designate specifically the fish now described.

EXPLANATION OF PLATE XXII.

Fig. 1. Coccodus Lindstremi, Davis. Outline; natural size,
2. The same ; enlarged two diameters.
Or., orbit; Mz., maxilla; Pmz., premaxilla; Mn., mandible; Pop.,
preoperculum ; Op., operculum ; Sop., suboperculum ; Sce., seapu-
lar arch; /’7., frontal.

Cove?
.

Hey:

re Wy

ays

Wars

Quart. Journ.Geol. Soe. Vol. XIVI. PL. XXII,

———
Ms DES

Ke aim ares
UN elif), <P Gs

ZB

Yi —S aa

} i 3 , si insane a SoS
fit Liph i BiH) i ; / ey Bae I ois
Ye fy i GE s HE Be ee aa
W) IN < % inl ey f 53 p a NC
| Jona Vas Pee Ep a

: Mintern Bros. imp
MA.Gidel. M.P Parker lith ROCKS NEAR YEW GALLOWAY.

ON CONTACT-ALTERATION NEAR NEW GALLOWAY. 569

35. ConTact-ALTERATION near New Gaxttoway. By Miss M. I.
GarDINER, Science-Mistress, St. Leonard’s School, St. Andrews.
(Read May 14th, 1890.)

(Communicated by J. J. H. Teaut, Hsq., M.A., F.G-S.)
[Prare XXTIT.]

ConTENTs.

. Introduction.
The Knocknairling-Burn Section.
. Shales traced along their Strike to their Junction with the Granite.
. Flags and Grits traced along their Strike to the Junction.
. Chiastolite-mica Schists.
. Aplite Veins.
. Age of the Metamorphosed Rocks.
. Remarks.

Explanation of Plate.

GO NTS? Or G9 bo

§ 1. Lyrropvctroy.

Tn eastern end of the northern edge of the Cairnsmore-of-Fleet
granite-mass follows the crest of the Knocknairling Hill to the west
of New Galloway for about half a mile. The metamorphism of
the rocks of this hill has been briefly alluded to in the “ Memoir Ex-
planatory of Sheet 9 of the Geological Survey of Scotland,” p. 22,
but is so extreme as to deserve a fuller description.

There are many exposures on the hill-side ; and the Knocknairling
Burn gives a good section across the series at a distance of about
half a mile from the granite. It is a pity that the beds cannot be
traced farther from the granite, especially as there is some doubt as
to the series to which they belong. The Cairnsmore-of-Fleet
granite is some twelve miles by six in extent, with its greatest
elongation in the direction of the prevalent strike of the Silurians.
The Survey has given the name of ‘‘ Queensberry Grits” to the
series into which it has been intruded, but suggests that the altered
rocks of Knocknairling Hill consist of the underlying Moffat shales
and Upper Ardwells, brought up here during the folding of the
district. The Upper Ardwells, where unaltered, to the east of the
granite, consist of rapidly alternating flags, shales, and greywackés.
The flags and shales are often sandy and micaceous. The grey-
wackés do not seem to differ from those of the overlying Queensberry
Grits.

§ 2. Tun Kyocxnarritine-Burw SEcrTIon.

In working up the Knocknairling Burn from Wauk Mill (see
Map, fig. 1) one crosses first beds of grits altered to a varying
extent. Parts are grey and very like unaltered grits farther east ;
but the greater part has the tint described as “‘ purplish brown ” by

570 MISS M. I. GARDINER ON CONTACT-ALTERATION

Prof. Bonney and Mr. Alport in describing the similar altered grits
from the Bennan Hill to the south of New Galloway*. This tint
is due to the presence of brown mica in continuous planes or
in thick-set, rounded patches. Amongst the grits are bands of
pyritous shale, and one band, 6 or 8 feet thick, of spotted shale.
Above the rickety little wooden bridge is a thicker band of shale,
which I take to be that seen farther up the hill, and which, at its
contact with the granite, is entirely recrystallized. Above the shale
he grits, like those below, and then follow more shales with highly
altered schistose bands, very silvery, and containing minute garnets.
To these succeed beds like these highly altered bands, but rather
more quartzose. These I suppose to be altered flags. They are
not well exposed in the stream, but there is a good exposure a few
yards from the right bank.

A microscopical section of the purple-brown grit (Pl. XXIII.
fig. 6.) shows large quartz-grains with here and there a felspar, and
highly dichroic brown mica, in flakes about -Olinch long. Amongst
the purple-brown grits are bands and patches, from an inch to a foot
or two broad, containing no mica and much more clayey matter.

The knotted schist is different from that of Skiddaw. It is not so
compact, and the knots are larger, being from 3 to } inch in diameter.
The microscope shows the Skiddaw knots to consist of one or two
crystals of a mineral containing many small inclusions. A few of the
knots in the Knocknairling-Hill rock have the same structure, but the
inclusions are more numerous. Asa rule the knots are only formed
of material much finer in grain than the bulk of the rock. They
are sometimes sigmoidal in form, and their outlines are continuous

with the wavy folds into which the rock has been thrown.

‘The flaggy beds mentioned as containing garnets show in a micro-
scopical section more brown mica than the grit, though they are
grey in colour. From side to side of the slide sweep wavy bands
of minute flakes, polarizing in bright pink and green, probably
sericite. The small garnets, about ‘015 inch across, are colourless
in the section, and fairly well formed. A high power shows them
to contain inciusions, probably of quartz, whose rounded outlines
with bays and gulfs remind one of the outlines of gas- and fluid-
inclusions in quartz.

§$ 3. SHALES TRACED ALONG THEIR STRIKE TO THEIR JUNCTION
WITH THE GRANITE.

The Shales B of the map (fig. 1) are frequently exposed for about
4 of a mile from the granite margin. ‘They are dark shattery
shales, a good deal iron-stained and often crumpled into frills and
zigzags (Pl. XXIII. fig.4). The plications have frequently parted,
and the interspaces been filled with wavy bands and lenticles of
quartz, from an inch or two broad down to microscopic dimensions.

* “ Report on the effects of Contact-metamorphism exhibited by the Silurian
Rocks near the town of New Galloway,” Proc. Royal Soc. vol. xlvi., 1889, p. 200.

NEAR NEW GALLOWAY. 571

The great variation in the amount of effect produced by an
intrusive mass at a given distance has often been noticed. It is
noticeable even in different bands of these shales. Within 100
yards of the granite some bands show no alteration, whilst others
become hardened into a compact, but generally fissile, rock with a
good deal of muscovite in flakes so small as only to show by their
sparkle. For about the last three yards the rock, where the

Fig. 1.—Map of the Knocknairling Hill and Burn, near
New Galloway.

NEW
GALLOWAY

=e Hib oS

‘Tower \Cctrr..4

S eae

of Ocigy?

Op per € arr s 4

Jos ~ -( 60M GN 10
yee ’

ed a G 5 DNceasee

x A AP oy

t cmd
ak

fyue
Ue Ge
\
SONY a)
:

Scale 2Inches toa Mile.

Shales. A. Little altered, but containing bands an inch or two broad,
a in which much white mica and garnets have been developed.
B. Little altered, except at the junction.
C. Altered grits and flags, with narrow bands of unaltered shale and
of chiastolite-mica-schist.
D, HE. An alternating series of shales, flags, and grits. Those at D are
the same as the rocks of the series O, exposed lowest on the hill-

side.
=)S0 ‘ > as
Naga Gramiter te Pedi Pgh an - Contour-lines, in feet.

junction is exposed, rapidly lightens in colour and changes in
character. It finally becomes a light grey, almost white, granular
rock with black patches, of about the size of a sixpenny-piece. It
shows on a cross fracture no signs of foliation, though it has a
tendency to break along planes covered with small flakes of mus-
covite. This rock weathers with the granite so that it is difficult to
tell on a weathered surface where the margin is at the junction.
The microscope, however, shows that that there is no shading off,
and that the altered shale has a marked character of its own.

Q.J.G.8. No. 184. 2p

all

572 MISS M. I. GARDINER ON CONTACT-ALTERATION

A similar rock occurs ona hill to the west of Knocknairling,
where another bed of shale, probably that marked A on the map,
is cut across by the granite.

A microscopical section of the shale B of the map, taken from
about 7 mile from the junction (Pl. XXIII. fig. 4), shows the spaces
mentioned above filled in with quartz. The black colouring matter,
although it is still thickly scattered through the rock, has collected
more thickly down one slope of each wave, so that the section is
crossed by transverse black lines. The rock consists of very
minute grains, probably, from their colours of polarization, quartz
and white mica. It contains also larger flakes of mica, almost
colourless with vibrations parallel to their length, and a light brown
with transverse vibrations, These micas occur in the greatest
quantity on the edges of the quartz bands, and in independent
eyes and bands.

Sections from the more altered bands, nearer the granite, show
that the colouring matter has become still more collected in lines
and granules. One slide shows clear vein-quartz alternating with
thick bands of black colouring matter and a little mica. Another
looks as though the minute quartz-grains and mica-flakes of the
little-altered shale had segregated into separate patches, and here
and there the small mica-flakes had built up an almost perfect
larger flake. A third section from a dark grey rock, with a good
deal of white mica, is figured in fig. 5, Pl, XXIII. Mr. Teall has
kindly looked at this for me; and finds that the lighter oval
patches, of which the rock principally consists, are biaxial. He is
of opinion that the mineral is probably a felspar allied to albite.
The grains are too small and too full of inclusions to yield cleavage-
flakes, by which their nature could be determined with greater
certainty. Occasionally one of these rounded patches contains two
or three white mica-flakes. These flakes have a dappled look, as
indeed much of the white mica has throughout, as though each large
flake consisted of many very small ones turned in slightly different
directions.

In a slide of the light-coloured granular rock, which is the final
stage of alteration (fig. 1, Pl. XXIII.), what first strikes the eye is
the great quantity of white mica, in well-formed flakes, about
-015 inch long. A highly dichroic light-brown mica is also present,
often intercrystallized with the white in such a way that the two
extinguish together. Such intergrowths may be seen at the top
and on the left of the figure. The dark micais indicated by shading.
The brown mica commonly contains spots, not visible with vibra-
tions at right angles to the cleavage, which appear much darker
than the rest, and of a greenish tinge with vibrations in the oppo-
site direction. There are often two or three small black grains,
probably the colouring matter of the rock, in these spots.

The principal part of the rock consists of granules which polarize
in grey tints. Though most of them seem to be quartz, biaxial
grains, probably of felspar, are by no means rare. The smaller
grains are rounded or sub-hexagonal, but the larger, as seen in the

NEAR NEW GALLOWAY. ae

figure, round the large brown mica on the right, are often of very
irregular outline. Here and there is a thick network of black
colouring matter ; other parts are free from it. In parts the quartz —
is quite free from inclusions, but usually contains many highly
refracting grains, too small for their nature to be determined with
any certainty.

In working over this microscopical slide, which is rather less than
1 inch in diameter, one notices that in about half a dozen places the
rock becomes coarser. Two such coarse parts are shown in the
figure: round the largest mica-flake, and on the margin of the slide
diagonally opposite it. They have a very granitic look; but the
brown mica is the same as that in the rest of the rock, and different
from that in the granite, and black colouring matter occurs in
them as well as in the finer parts; so I do not see any reason to
suppose them to be injections of granite, although felspar is more
plentiful than elsewhere.

§ 4. Fracs anp GRITS TRACED ALONG THE STRIKE TO THE JUNCTION.

Less than halfway up the hill a rocky ridge is seen; this, con-
tinued by a series of bosses to the margin of the granite, runs
parallel to the line of shale exposures just described. The ridge
consists mainly of schistose rocks, exactly like those described as
altered flags in thestream. In places this rock is interbedded with
more shaly-looking bands, with chiastolite, and in others with more
quartzose gritty-looking rocks. There are also unaltered shales
amongst these rocks. The bosses, which continue the line up to
the granite, lie a little nearer the shales, and are of a more com-
pact quartzose variety. I suppose them to be the same as the
grits which lie in the stream between the schistose rocks and the
shales.

The main differences between different layers of these altered
grits and flags, from a part of the hill lower than the first cairn,
consist in the character of the garnets and in the nature, size,
and quantity of the mica-flakes. The garnets are sometimes well-,
sometimes ill-formed; sometimes they contain inclusions in
the centre, sometimes in a ring round the centre, rarely none.
The mica is usually the purple-brown variety, but is some-
times greenish. Larger flakes of white mica occur occasionally.
In the more compact rocks the mica is scattered through the rock ;
in the more schistose varieties there are bands of minute flakes, as
in the rock described from the stream. The base is essentially a
fine-grained quartzite.

Fig. 7, Pl. XXIII. gives an idea of the principal varieties. Near
the top is a lenticle of clear, large-grained vein-quartz and garnet ;
below this is a band with well-formed garnets and small flakes of a
greenish mica; then follows one of the bands of minute flakes, and
at the bottom: is a variety with larger brown mica-flakes in more
ecntinuous lines than those above.

Both macroscopically and microscopically the rocks show great

2102

574 MISS M. I. GARDINER ON CONTACT-ALTERATION

signs of contortion. Fig. 2 representsa piece of weathered rock
in cross section. Quartzose layers, of one of which the little
lenticle at the top of fig. 7, Pl. XXIII., is a section, form the
prominent bands; and lines of brown mica weather out, leaving
fine ridges, conforming to the twists and turns of these bands.

Fig. 2.—Altered Grits contorted.

«--------- — — / Foor 3 INCHES. ~--------------4

Weathered surfaces of this kind are common and striking; but
perhaps, considering how quartzose it is, the character of the rock,
which is exposed just below the one E. and W. wall along the hill-
side, is more so. A vertical section shows Vs, of about 3 inch in
length, through whose points the rock cleaves horizontally or nearly
so. This rock (fig. 8, Pl. XXIIT.) consists of the same minerals as
the other altered grits, together with a little chiastolite. The Vs
are formed with thick bands of light brown mica-flakes, always
well-formed and never bent. The cleavage takes place along bands
of quartz-grains, which run through the points of the Vs. This
quartz consists of small granules, such as form the quartzite-like
base of the other altered grits. Chiastolite is seen in the two_
rectangular sections on the left of the slide (fig. 8, Pl. XXIII.).
The light patch at the top, where it is clearly marked by black
lines, consists of large flakes of white mica, probably replacing
chiastolite. It will be noticed that the chiastolite affects the folds,
and that the garnets often lie in small lenticles of quartz.

Following the grit bosses up the hill, at about 200 yards from
the granite junction, the lower cairn (see Map, fig. 1) is reached.
The rock attracts attention by the brilliant sparkle of the small
white mica-flakes. A cross fracture shows the rock to resemble
the more quartzose varieties of the altered rocks just described, but
to be rather coarser in structure, and to contain more white mica.
The mica-flakes are about =), inch in diameter. Though, roughly
speaking, their cleavage-faces are parallel, they, are not in suffi-
ciently continuous planes to make the rock cleave easily. The
rock still has the purplish tint of the grits in the stream.

The microscope shows that the rock varies in texture in different

NEAR NEW GALLOWAY. 575

parts, in the same way as the most altered shale. There are parts
of microscopical slides which could be matched in slides from rocks
farther down the hill, such as fig. 7, Pl. XXIII. Fitted in with
these are bands and patches of a much coarser texture, in which the
quartz is in large pieces. These must be secondary, because they
often embrace large flakes of mica. Especially near the borders of
the less altered parts the large quartz grains form a sort of
ground-mass to quartz (?) granules of such regular oval or circular
outline as to look as if they had been acted on by a solvent. Both
quartz and white mica look thick and cloudy, particularly towards
the centre. A high power shows this to be due to the presence of
a multitude of fine highly-refracting needles, in bands or radiating
bundles, which I take to be sillimanite. All the clear grains con-
taining sillimanite which I have found to give a figure are uniaxial,
so I presume that cordierite is not present. ‘The black mica is very
highly dichroic. Between crossed nicols lath-shaped sections are
of a light yellow in the one direction, and in the other extinguish,
almost as completely as tourmaline does, vibrations in the opposite
direction. It is noticeable that in rotating the colour changes from
the yellow tint to a rich brown, and that just before the maximum
extinction it loses all trace of brown and becomes a dull grey.
This mica often contains black spots ; and sometimes a high power
shows highly-refracting grains in the centre of these. Associated
with the quartz of both finer and coarser parts are occasional
striated felspars. These are rare; and tourmaline, of which a
little has been noticed, is still rarer.

The upper cairn (see Map, fig. 1) stands on another bold crag,
about halfway between the first and the granite. The rock is now
coarser throughout, and, if from an unknown locality, would
probably be described as a fine-grained gneiss. The white mica
is even more conspicuous than before, being present in greater
quantity and in larger flakes. A cleaved surface shows, besides
the white mica, nests of small black micas, just distinguishable as
such without a lens; and between these are patches of quartz and
garnets. ‘These different patches branch, and fork, and jut into
each other, like the counties on a map, the average greatest dimen-
sions being perhaps 4 inch. A cross-section is marked by the black
dashes which give the rock its gneissic look, and which are the
sections of the black mica nests.

Microscopical slides show that more than half the bulk of the
rock now has the character of the coarser parts of that on which the
lower cairn stands. The quantity of sillimanite has consequently
increased. Except for this mineral the quartz is remarkably free
from inclusions, and thus differs from that of the most altered shale.

The granite-junction occurs on the south side of a third boss. As
is shown in fig. 3, light-coloured lenticles are conspicuous in the
weathered cross-section. These are a foot or two long, by about 3 in.
broad. The main part of the rock differs from that of the upper
cairn in being even coarser and more distinctly banded. The white
micas are often as much as } inch in diameter, and form thick piles

576 MISS M. I. GARDINER ON CONTACT-ALTERATION

round the edges of the light lenticles. They are often thickly
studded with small garnets. Branching masses of a somewhat
ivory-like material occur. A lens shows this to contain many very
small flakes of white mica. These are packed in a substance which,
when crushed, breaks into numberless small needles, negative in

Fig. 3.—Junetion of the Granite and Altered Grits, on the
southern side of the Third Boss, showing quartz-garnet lenticles.

—<—S

sign and extinguishing parallel to their length, hence probably
sillimanite. ‘The microscope shows (fig. 2, Pl. XXIII.) that the rock
has lost all signs of its clastic origin. As seen in the upper part of
the slide, it consists of quartz and white mica, both containing
sillimanite, with brown mica and garnets. To the right is indicated
the cloudy look of one of the mica-sillimanite aggregates.

The main part of the lenticles, as seen at the bottom of fig. 2,
Pl. XXIII., consists of garnets. These give to a freshly-broken
surface a delicate pink tint. They are set in clear vein-quartz,
often in large pieces, having an angular outline, and traversed by
lines of liquid- or gas-inclusions. The sillimanite-mica aggregate
just described occurs in large branching masses, often an inch or
two long.

I have had no opportunity of comparing the less altered grits
with the “ quartzite micacé” of Guéméné, which, from the de-
scriptions, they seem to resemble; but I have seen a specimen and
slide of the “ leptynolithe granatifére ” of Rostrenen. The “ lepty-
nolithe ” is a compact dark purple rock, looking microscopically less
altered than the New Galloway rocks ; but the microscope shows it to
be as entirely recrystallized, with these differences,—that it is much
finer in grain, and that the minerals are not so well formed. I sent
a specimen of the most highly altered grit to M. Barrois, and asked
if he would kindly tell me whether it resembled the “ quartzite
sillimanitisé ”’ of Guéméné ; he answered that there was no such
rock amongst the Silurians or Devonians in France, but only
amongst rocks of doubtful origin. He further says that the spe-
cimen is identical with the “ Archeans” of Nantes metamorphosed
by granulite.

NEAR NEW GALLOWAY. 577

§ 5. CarastoLire-mica-Scuists.

Amongst the grits and flags marked C on the map are some
unaltered shales, and others which may be called chiastolite-mica-
schists. ‘These are very black (fig. 9, Pl. XXIIT.), and cleave along
surfaces with the lustre of highly polished black lead. The cleaved
surface is often rough with garnets of very varying sizes, or shows
clusters of chiastolite needles, from 3 to 3 inchin diameter and 1 or
2 inches long. A cross-fracture has a more brilliant lustre, as the
black mica, which forms a great part of the rock, is more conspicuous.
The chiastolite is water-clear, and often shows the pink and green
dichroism as well as the characteristic black figure. Parts of the
crystals are sometimes replaced by white mica, and sometimes by
quartz. The chiastolite usually includes garnets, and often, with
them, little masses of fine-grained quartz. Very rarely it includes
mica, and this is in small flakes.

The garnets are sometimes 7 inch in diameter, but usually
smaller. In sections a dark ring is often seen round the centre,
sometimes due simply to difference of colour, sometimes to inclusions
of black grains. Often on each side of the garnet is a small tri-
angle of quartz, making with it a clear eye.

The main mass of the rock consists of quartz and black mica,
with much colouring matter, which renders much of a slide opaque.

There are quartz-garnet lenticles, like those described in the
gneissic rocks; and round their margins are large masses of chia-
stolite with few or no crystal faces.

§ 6. Aprite VEINs.

On Knocknairling Hill and at other parts of the margin both
granite and sedimentaries are veined by a granite, which would
answer to the description of aplite given by Prof. Rosenbusch, if it
were not that he says that muscovite is present only in small quan-
tities. The rock is usually very coarse, but here and there becomes
fine-grained. It consists of felspar (often in large masses), quartz,
and a considerable quantity of white mica. Tourmaline and gar-
nets are accessory minerals,

The felspar is mostly microcline. In some veins it forms a micro-
pegmatite with the quartz; in others it forms the bulk of the rock.
In one vein, to the west of the granite, there are masses of it 2 or 3
feet across, with continuous cleavage-planes some inches long. The
felspars often include garnets.

The quartz is traversed by many lines of small inclusions. That
associated with the large felspar masses just mentioned can be seen,
with a hand lens, to consist of small, flattened, hexagonal prisms,
with pyramids at one end, built up in parallel rows.

The white mica is often in hexagonal plates, as much as 3 inch
in diameter. Along the edge of one of the veins on Knocknairling
Hill there are triangular flakes arranged in a plumose manner.
The mica feathers point inwards from the edge of the dyke, and are
3 or 4 four inches long.

578 MISS M. I. GARDINER ON CONTACT-ALTERATION

The small garnets are sometimes of a brownish red, as in the
altered grits, and sometimes a bright wine-red colour. Large yellow
garnets occur occasionally.

Tourmaline occurs in the Knocknairling-Hill vein in patches
curiously intergrown with quartz, so as to form what looks like a
graphic granite, with the little hooked letters in dark tourmaline
instead of in quartz (Pl. XXIII. fig. 3). The tourmaline needles are
parallel with each other, instead of radiating as in luxullianite.
Some of it is of an indigo, and some a bottle-glass brownish-green
colour. These tourmaline-quartz patches have an area of 1 or 2
square inches. Groups of tourmaline sections extinguish together,
but the quartz-grains have their axes at all angles.

The fine-grained variety of the aplite has a sparkling saccharoidal
look, and the little pink garnets show conspicuously on the white
surface of a freshly-broken specimen. It consists of about equal
quantities of felspar and quartz in grains. There is a good deal of
white mica, garnets are common, and small needles of tourmaline
occur occasionally. In some places coarser veins shade off in parts
into this fine-grained material ; and in others it occurs in veins by
itself,

$ 7. Agr or tHE METAMORPHOSED Rocks.

The evidence that the metamorphosed rocks of Knocknairling Hill
are of Silurian age is, I think, fairly conclusive.

There can be no question as to the age of the grits and shales of
the stream. ‘They are just like grits “and shales which occur at
various parts of the margin. The amount of mica in the grit varies,
and in some parts the rock differs but little from the unaltered grits
of the district. It is certainly a pity that the schistose beds of the
stream, which I have called altered flags, cannot be traced farther
from the granite; but the way in which they begin by alternating
with unaltered shales renders it unlikely that they have been faulted
in. This alternation is just like that of the flags and shales of the
Ardwells. A similar case of the alternation of thin, highly altered
bands with unaltered shales occurs at a greater distance from the
granite in the shales marked A on the map (fig. 1). In these there
are quartzose bands, an inch or two thick, with much white mica
and garnets.

The grits and shales are Silurian. The mode of occurrence of
the schistose beds in the stream renders it probable that they are
of the same age.

The more altered rocks of the hill-side seem clearly to be the
same series, There are unaltered shales on one side, and altered
flags, like those in the stream, on the other. The strike of the
whole, as given not only by the foliation, but by the shales inter-
bedded with the altered flags, is the normal strike of the Silurians
of the district.

There is also evidence of a different nature. Nowhere else is the
metamorphism of the rocks in contact with this granite-mass so
striking ; but to the south, at the Clints-of-Dromore, the grits, at the

NEAR NEW GALLOWAY. 579

contact, have been altered to a rock very like that of the lower
cairn of Knocknairling Hill without the garnets ; and on the Bennan
Hill to the east, and Laughenghie Hill to the south, there are in
purple-brown grits spots, an inch or so long, closely resembling the
most altered grits of Knocknairling Hill.

§ 8. Remarks.

In connexion with metamorphism the following points seem note-
worthy :—

1. The extreme variation in the amount of alteration undergone
at different places at the same distance from the granite.

a. At the actual contact in different parts of the margin.

b. In the case of beds close together, as on Knocknairling Hill,
where, at a distance of 200 yards, grits are highly altered and shales
little affected.

c. In the case of different layers of the same rock, as on Knock-
nairling Hill, where bands of shale, a few inches thick, are much
more altered than those with which they alternate ; and even more
noticeably in the shales marked A on the map, where, in an exposure
of hardened shale about 8 feet high, are bands, an inch or two thick,
much altered, with white mica and garnets.

2. The way in which the extreme alteration of the grits has
spread from the margin on Knocknairling Hill, the whole being re-
crystallized near the margin, parts of irregular outline similarly
affected at a distance of 100 yards, and smaller portions farther off.

3. That material seems to have travelled through the rock.

a. The larger lenticles of fig. 3, and the smaller of fig. 2, con-
taining quartz, garnet, and sillimanite, as well as the numerous
eyes and lenticles of quartz alone, have the appearance of having
been filled by material which has been brought from the surrounding
rock, |

b. The more altered grits consist largely of clusters of crystals,
here of one mineral, and there of another. It would seem as if
material must have been conveyed from one part of the rock to
another to form such nests of only one mineral.

4. The apparent order of succession of the minerals. Garnets
extremely rarely contain anything but colouring matter and quartz ;
chiastolite contains garnets ; bands of mica bend round both.

5. The microscopical slides give the impression that the minute
folding could not all have been prior to the mineral alteration. One
would suppose that the black colouring matter of fig. 4, Pl. XXIII,
must have been heaped up on one side of the waves during the folding,
and the form of the knots in the knotted schist connect them with the
folding. No inconsiderable part of the rocks consists of twisted bands
and eyes of segregated material. The spaces thus filled might have
been caused by shrinkage in consequence of crystallization in the
more altered rocks, but could not have been so caused in the slightly
altered shales. They suggest easing during folding. ‘The little
garnet quartz-eyes suggest the same idea.

580 MISS M. I. GARDINER ON CONTACT-ALTERATION

Some of the mineral alteration may be due to the energy of the
resisted force which caused the folding; but the main effect must, I
think, be acknowledged to be due to the granite. The mica of the
purple-brown grit is evidently a product of contact-metamorphism,
for there is a zone of this rock almost all round the granite. The
increased metamorphism of the Knocknairling-Hill rocks as the
granite is approached indicates the same cause.

The variation in the amount of alteration at the same distance
from the margin,—the way in which the extreme alteration of the
grits begins in patches which increase in size until the whole is re-
crystallized at the margin,—the way in which the large quartz-grains
of the altered rocks contain little grains which look partly dissolved,
—and the signs of the transference of material, suggest to my mind
the action of highly-heated water.

Folding on the large scale was certainly over when the granite
was intruded, for both on the east and west the granite is constantly
seen cutting across the folds ; but, supposing the contact-effect due
principally to highly-heated water, which would very likely have
been emitted during a long period of time following the injection of
the granite, might not the minute folding have taken place during the
same time, so that dynamic- and contact-metamorphism have taken
place simultaneously ?

EXPLANATION OF PLATE XXIII.

Fig. 1. Most highly altered shale: Xabout 50. Showing white mica, brown
mica (shaded), colouring matter (marked black), and quartz. The
quartz is shaded, and is dotted where it is tull of small inclusions.

2. Most highly altered grit: x about 50. The upper part of the slide
represents the main mass of the rock; the lower, part of a quartz-
garnet lenticle. The minerals are whife mica and quartz con-
taining sillimanite needles, brown mica (shaded), and garnets. The
cloudy-looking portions on the right, both in the rock itself and
in the lenticle, represent the mica-sillimanite aggregates described
in the text (p. 576).

3. “Graphic” arrangement of tourmaline: X about 6.

4, Altered shale ; drawn witha hand-lens: X about 2. Showing quartz
veining and arrangement of colouring matter along folds.

5. Altered shale: x about 10. Showing elongated irregular patches of
a biaxial mineral, probably a felspar, and bands of large-granular
quartz.

6. Purple-brown grit: X about 50. Showing quartz-grains, brown mica,
and a few felspar-grains ; one lies S.H. of the centre.

7. Altered grit; drawn with a hand-lens: xX about 4. Showing garnet,
mica, and quartz.

8. Altered grit, with secondary cleavage; drawn with a hand-lens: X about
2. The shaded bands forming the Vsare masses of small light-brown
micas, and the interspaces fine-granular quartz. Chiastolite to the
left.

9. Chiastolite-mica-schist ; drawn with a hand-lens: x about 2. Chias-
tolite, dark-brown mica, colouring matter, and garnets. A good
deal of quartz in the light bent band in the middle.

NEAR NEW GALLOWAY. 581

Discussion.

The Cuarrman (Mr. HupiEston) remarked on the satisfaction he
felt in seeing microscopic examination of rocks taken up by ladies.
He noticed that there were no chemical analyses given in the paper.

Mr. Harxer had never seen gritty rocks so highly metamorphosed
as those laid upon the table. The mode of occurrence of nodular
masses of garnet and quartz struck him as interesting, and he would
ask whether it was concretionary or connected with folding. Highly
granatiferous rocks were found elsewhere, as in the Ardennes,
coming in in a lenticular fashion. The large quantity of mica would
seem to indicate an arkose rather than a grit, but he would await
the publication of the paper.

Prof. Hueurs thought that whatever may have been the origin
of the gneissic rocks exhibited they had certainly been much affected
by dynamical metamorphism, and that the Author had made out a
good case for contact-metamorphism also, though he believed she did
not profess to have traced the ordinary sedimentary grits continuously
into the highly altered rocks.

Mr. Tratt explained that though he had communicated the
paper, he had no special knowledge of the locality. He felt that
the Author was perfectly well able to examine rocks microscopically,
and she had also done a considerable amount of field-work. He
very much regretted the absence of the Author.

582 MR, 0, A. SHRUBSOLE ON THE

36. On the Vautny-cRavets about Reavine, with especial reference
to the Patmoutraic ImpitemEents found in them. By O. A.
SHRUBSOLE, Hsq., F.G.S. (Read June 18, 1890.)

ConvTENTS.

§ 1. Introduction.

§ 2. Gravels North of the Thames.
1. Toots Farm, Caversham.
2. Henley Road, Caversham.
3. Shiplake.

§ 3. Gravels South of the Thames.
1. Tilehurst Road, Elm Lodge, Reading.

. Norcot Brickyard.

. Redlands, Reading.

. Kennet Mouth.

. Southern Hill and Earley.

Sonning Hill.

. Charvil Hill, Sonning.

. Ruscombe, Twyford.

§ 4. General Considerations.

WH ~A GD or pa 09 bo

§ 1. Inrropuction.

Havre had the Pleistocene deposits of this part of the Thames Valley
under observation for some years past, and more particularly (since
first finding worked flints here fifteen years ago) in reference to the
_ evidence which they afford of the former presence of Man in the
district, I desire to offer to the Society a few notes on some of the
sections which have proved of especial interest. It is not
pretended that this communication aims at presenting a complete
view of the subject ; but, as sections are liable to be covered up or
to change their character in the course of time, I have thought it
well to put on record what has come under my own observation, as
it may serve to present a general view of the manner of the occur-
rence of the relics of Man within a definite area.

The Valley of the Thames in this vicinity forms in the deepest
part a trough, cut in the Chalk, about a mile and a half wide, beyond
which the levels ascend more gradually. Gravel is found here as
elsewhere at various elevations, creeping up the valley-slopes, often
for a considerable distance where the form of the ground has been
such as to retain it.

Of the plateau- and hill-e fas which succeed the valley-terraces
I do not here speak; but there is often some difficulty in making
out a clear line of demarcation. At about the 300-feet contour-line
or less, however, we find that we have to deal with what are
generally known as the plateau-gravels.

§ 2. Graves Nortu oF tHE THAMES.
1. Toots Farm, Caversham.

There is a considerable spread of valley-gravel around the village
of Caversham. On the hill about a mile north of the river, at an

VALLEY-GRAVELS ABOUT READING. 583

elevation of about 269 feet above sea-level, a section shows about
8 feet of irregularly-bedded, ochreous, subangular flint-gravel, with
pebbles of flint, a few quartzites, &c. There are various other
sections at about this elevation within a mile or two; but the only
one of special interest is at a somewhat lower level, near Caversham
church, in a pit on Toots Farm at a height of 235 feet above sea-
level, and 114 feet above the adjacent river-surface.

The section shows about 8 feet of slightly-bedded, subangular,
flint-gravel, containing many large flints in a light-coloured sandy
matrix, together with occasional fragments of felsitic and other rocks,
and a considerable number of the usual pebbles of quartz, quartzite,
sandstone, &c¢., which are found in our valley-gravels at all levels,
and which are generally admitted to have been derived from the
waste of a Triassic coast-line further north. The gravel has
many pot-holes, filled with a compacted clayey and gravelly loam.

It rests on the Chalk, and, beyond the occasional bending of its
bedding-planes, which may have been subsequent to its deposition,
it does not present evidence of any unusual or violent action.

In this pit a large number of flint implements have been found.
They occur mostly in a definite zone, which follows the bedding of
the gravel, and is usually only 1-3 feet from the surface. I
have caused excavations to be made down to the Chalk, and the
result has confirmed the statements made by the men. The imple-
ments occur in considerable numbers, so that it is not difficult to
obtain specimens 7m situ; and I have repeatedly taken them from
the gravel face.

Some years ago I visited the pit when it was not being worked,
and no good section was visible; but subsequently Dr. Joseph
Stevens was more fortunate, and obtained implements from this pit
and from the gravel thrown out in digging the foundations for a
house nearer the river, in the same deposit; and a considerable
number have been secured for the local Museum by carefully turning
over the upper portion of the gravel.

The condition in which the implements are found is such as to
suggest that the greater portion of them have not travelled far.
They are but slightly abraded or worn, as a rule, and there is more
or less unity of character in the forms, and similarity of surface-
condition. The sharp-pointed type is of general occurrence. They
are of various degrees of finish, some being worked but very slightly
indeed, or perhaps spoiled in the working; others are carefully
executed. It seems likely, having in view also their numbers,
that they were made not far from the spot.

These traces of Man do not occur all over the gravel-deposit,
but they do extend over a considerable area, as is proved by casual
openings. At the Toots-farm pit, the gravel occupies a sort of
promontory, bounded on one side by the river, on another by a dry
chalk valley, and on the third side it faces gently rising ground,
—a position in which gravel would readily accumulate.

Selected nodules appear to have been largely used as the material
of the implements. The mineral condition of the surface, where

584 MR. 0. A. SHRUBSOLE ON THE

cut, is generally similar to that of the broken surface of the other
flint fragments with which they are associated, and presents a light-
buff or cream-coloured patination, sometimes bluish, or with the
natural colour of the flint little altered. Frequently one side of
an implement will have a different patination from the other.

The general conclusion seems to be that most, if not all, of the
implements belong to the same paleolithic date. It is worthy of
note that fragments of quartzite are occasionally found which appear
te have been hollowed at the edge and used for scraping or
rubbing. This is of interest as indicating that the fragments in
question, if the hollowing be artificial, were used by Man after such
glacial conditions had set in as produced their transport to this
district.

In order to form an idea of the original thickness of the gravel at;
this point, allowance must be made for the removal of a considerable
quantity by denudation, which, owing to the contour of the ground,
would necessarily be rather severe. That the gravel which has
been removed contained some implements seems probable, from the
occasional occurrence of a specimen at a lower level.

This is, I believe, the highest point at which so far the valley-
gravels of this district have yielded traces of Man. Animal remains
are rare. I have not met with any, but Mr. L. Treacher informs
me that he has found at this pit a much decayed tooth of horse, and
a few small fragments of bone also in a decayed state. Prof.
Prestwich and others have suggested that the rarity of the occurrence
of mammalian remains in the older high-level gravels is due to their
gradual destruction by percolating water.

I have obtained an implement from a casual opening in gravel
about half a mile west of the Toots-farm section and at about the
same level.

2. Henley Road, Caversham.

There is a pit from which gravel and Chalk have been extracted
on the east side of the village, about a mile distant from the Thames
and about 168 feet above sea-level. The section shows a very
uneven surface of Chalk, which is ravined, and overlaid by a clayey
gravel, showing strongly-marked bedding in places, and in other
places looking like a “‘ wash.” In one place there is a thin patch of
sandy gravel resting on the chalk-rubble, which I take to be a relic
of a once larger deposit and to be older than the mass of the gravel.
From this part I have obtained a flat ovoid flint implement, much
abraded, and a few other worked flints. The type is unlike that of
the implements from the Toots-farm gravel, and resembles those
obtained from the opposite side of the valley. A molar of Hlephas
prinugenius, in a decayed state, was found here.

3. Shuplake.

About three miles from the last-mentioned locality there is a
terrace of gravel occupying a level of about 200 feet above sea-level,
a section of which, in a pit by the side of the road to Henley, shows

VALLEY-GRAVELS ABOUT READING. 585

about 8 feet of rather small subangular gravel, mostly of flint, sandy
in the lower portion, and resting on Chalk. The river flows very
near this spot. Implements resembling those from Toots Farm
occur here. Another opening in the ground made during the con-
struction of farm-buildings showed a greater depth of gravel, 15 or
16 feet; and from gravel thrown up from near the bottom I obtained
two implements approximating to the Toots-farm type.

About a mile from this point, near Shiplake Station, and at about
the same level, gravel has recently been dug for the construction of
ayvoad. Itis a small, bedded gravel, containing many small pebbles,
and, in addition to the flint and quartzites, a few pieces of chert,
which may have been derived from the plateau-gravel. I observed
flint flakes in this pit, from which I infer that implements would
be found also,

§ 3. Gravets SourH or THE THAMES.
1. Tilehurst Road, Reading.

On the southern or Berkshire side of the Thames two tri-
butaries join the main stream in this district, namely the Kennet,
which flows through the town of Reading, and the Loddon, which
enters the Thames at Wargrave, about four miles lower down.
There is, of course, a considerable accumulation of gravel about
these rivers. The town of Reading is built on the gravel sheets of
the Thames and Kennet, which unite and spread over the watershed
of the two rivers. There is a good section (see fig.) about a mile

Section of Gravel-pit, Tilehurst Road, Reading.
(Length of section, 63 yards. Maximum thickness of gravel, 22 feet.)

8.

A. Lower ae of the ochreous gravel. A’. Chalky portions of the same
gravel.

B. Ochreous gravel, with a loamy seam, occasionally showing contorted
bedding (“ Trail”’).

C. Whitish clayey gravel, at the top.

D. Woolwich-and-Reading Sand.

HK. Sand-pipe.

from the centre of the town, westward, on the Tilehurst Road, at an
elevation of 197 feet above sea-level, and about 75 feet above the
surface of the Thames at the nearest point, about a mile and a
quarter distant.

The maximum thickness of the sheet here is 14 to 19 feet, and
it thins out in the direction of the Thames and Kennet respectively
by denudation.

The section to which I have referred occurs in a large pit on the

586 MR. 0. A. SHRUBSOLE ON THE

Elm-Lodge estate* which has been largely worked for road-
material; and the sections exposed from time to time have presented
some features of interest. The gravel here rests upon an uneven
surface of the buff-sand of the lower part of the Woolwich-and-Reading
series. It consists of subangular ochreous flints, whiter near the
surface, in a more or less sandy matrix, particularly in the lower
portion of the deposit, with pebbles and boulders of brown and purple
quartzites, white quartz, sandstone, &c., and occasionally fragments
of igneous and metamorphic rocks.

In certain parts of this gravel, however, there are included
masses of a gravel distinct in character, except that quartzites are
foundin both. This is a clean whitish gravel containing many
small water-worn flints weathered white by change in the iron-
oxide, larger fragments of black flint, irregular lumps and pebbles of
chalk, and fine chalk material. Incrustations of calcite appear on
some of the flints. Chalk also occurs in the hollows of others.
It is evidently, as regards the greater portion of it, the result
of the wasting of a Chalk district. These included masses of gravel
vary in size and shape: some are lenticular or flat; others are
roughly circular in section, and the materials composing them lie
at such an angle as seems to require the support of the ochreous
gravel by which they are surrounded. They have the appearance
usually of being contemporaneous with the other gravel, as the lines
of bedding seem frequently to pass through both. Black stains, due
to manganese, also affect both gravels equally.

As the gravel has been worked away eastward the masses of the
chalky gravel exposed have been larger in number and size. The
sketch (fig. at page 585) will give some idea of the manner in which
they occur. Some of these are 10 or 12 feet in diameter in
their shorter axis, and extend some distance horizontally. Many
rest on the floor of Reading Sand; others, as seen in the section,
are entirely inclosed by ochreous gravel. ‘The workmen think that
they all ultimately touch the bottom.

Whether the two different gravels were here laid down contem-
poraneously or not is difficult to decide. Possibly stranded and
piled-up ice inclosed portions of the frozen bottom of another part
of the old river, and melted among the accumulating deposit. But
more probably the chalky gravel may have been an earlier deposit,
partly worn away, and covered unequally by the ochreous gravel.
At all events the chalky gravel was accumulated rapidly, for some
of the fragments of Chalk are angular, and chalky mud still fills
cavities in the flints.

The patches are most numerous near the base of the gravel and

* Sometimes called the “ Grovelands Pit.” See Dr. Stevens’ notes in the
Transact. Brit. Archseol. Assoc., March 1881; Proceed. Geol. Assoc. vol. viii,
1884-5, p. 347; and Jbzd, vol. ix. 1886-7, p. 211; and Journ. Anthrop. Instit.
for 1884, pp. 192-200.

Grovelands is the next farm westwards, where there are other gravel
sections of less interest, although I have found a few worked flints there. The
prominent gravel ridge commences with the Elm-Lodge Estate, occupies its
southern boundary, and extends also further east.

VALLEY-GRAVELS ABOUT READING. d87

in a line parallel with the direction of the present river, near where
the upper gravel thins out on the valley-slope and leaves them near
the surface. Further back in the gravel-working they he under
many feet of gravel, but finally disappear.

It will be seen by reference to the figure, p. 585, that relatively
tranquil conditions of deposit supervened, as shown by a sandy seam
(between a and p) near the top. Some years ago this was exposed
as a very distinct bed of greenish sandy clay with small pebbles. As
it passed over one of the masses of chalky gravel its level was con-
siderably raised, as if on account of the latter. A non-ochreous
gravel, apparently of more recent date, comes in above (c in the fig.).

Resting on the Tertiary Sand (D) at the base of the gravel are
many massive flints and some sarsen-stones.

Flint implements are sparsely scattered in the gravel, and it is
not easy to obtain a specimen wm situ; but, owing to the quantity -
of gravel removed, a considerable number have been secured. Some
of the forms have been described by Dr. Stevens *. Though chiefly
found in that part of the gravel which is associated with the in-
cluded masses of a chalky gravel, yet they occur in both kinds of
eravel (A and B), and some few have been found in the uppermost
gravel (c) which covers the greater portion of the sheet.

As a rule the implements are much worn by attrition, and the
appearance of many of them further suggests that they have had
continued use. Flakes and fragments with sharp edges are, how-
ever, by no means uncommon. ‘The surface-colouring varies. Some
of the tools are of black flint, little altered, and these seem to be
confined to the chalky gravel (a4'). A common tint is a deep
ochreous brown. Others are lighter, and some are of a uniform
dirty white. In some cases the mineral condition of the surface
is sufficiently accounted for by -the position of the implements
in the present gravel, the matrix in which they are embedded,
and their nearness or otherwise to the surface of the ground.
There are cases, however, which are not fully explained in
this way. It is not unusual in gravels of this kind to find
unworked stones, which have apparently come from an older
eravel, as they exhibit fractures of two distinct ages. In the
chalky gravel some of the implements are of black flint, slightly
altered on the surface, while others are more or less ochreous.
Cases of this kind are by no means clear or conclusive. One
implement, however, had evidently been abraded and had ac-
quired its present coloration before it was swept into this gravel
deposit. It has been much worn, so that the marks of chipping
are almost obliterated. Its surface is an opaque whitish colour,
slightly mottled with light brown. It has escaped any serious
fracture ; but small pieces have been knocked off its edges, and
where that has occurred quite a different patination is apparent
which shows the extent to which the surface has been modified in
the present gravel. It appears, therefore, that this tool has been

* Journ. British Archzol. Assoc. 1881. .
Q.J.G.8. No, 184. 2u

588 MR. O. A. SHRUBSOLE ON THE

derived from some older gravel where it had suffered abrasion and
had acquired, in the main, its present alteration of surface. The
adherent matrix shows it to have come from the ochreous part of -
the gravel. It does not differ in type from other implements found
in the same deposit.

Indications of this kind suggest caution in our attempts to
synchronize a deposit, particularly a deposit of so shifting a character
as gravel, with its inclusions organic or otherwise, or the inclusions
with each other. Evidence of the same kind is afforded by the
fragments of Lower Cretaceous and Oolitic fossils which are found
in this gravel.

There is, however, an indication that some of the tools were
fabricated since the dispersal of the Triassic conglomerates, and the
partial submergence which aided that dispersal. It is not unusual
to find fragments of quartzite that have been hollowed out artificially,
to all appearance, so as to form a scraping or polishing tool. I
have found several specimens of this sort, and a hatchet of brown
quartzite, found in this deposit by Dr. Stevens, is now in the
Reading Museum.

With regard to the type of the implements found here, the most
characteristic form is the ovoid ; but more pointed forms, generally
in a damaged state, occasionally occur.

Flakes, sometimes of large size, which have been used as scrapers
are common, and massive rudely shaped implements are not un-
usually found associated with the large flint fragments at the base
of the gravel. The implements, as a whole, have an entirely different
facies from those of the Toots-farm deposit. In the latter the flat
obtusely pointed tool is practically unknown; and the Caversham
workers appear to have operated, as a rule, on smaller nodules, and
to have been more sparing in their use of the material. The non-
descript tools and large scraping and chopping flakes are also rela-
tively more abundant here (Tilehurst Road).

The organic remains found here include so far as Pal own obser-
vation has extended :—

Elephas primigenius. Teeth and fragments of bone not
uncommon.

Rhinoceros. A worn molar.

Bos primigenius. Bone fragments and teeth.

Equus caballus. Teeth rather common.

Cervus elaphus. Portions of antlers.

I have two fragments of bone, which have been cut as if by a
flint implement; and, when put together, they are seen to have
formed part of the same bone—a radius of Bos, which had evidently
been split before it became embedded in this gravel*. The
separate pieces, perhaps, have not been subjected to much rolling,
or they would probably not have been found near together. Mam-
malian remains occur both in the ochreous and the non-ochreous
parts of the gravel.

* Journ. Anthrop. Instit. 1884, p: 199, pl. xi. figs 8 a, 8.

VALLEY-GRAVELS ABOUT READING. 589

In the same field as that in which the gravel occurs, but at a
lower level, about 144 feet above the sea-level, a very good section
Was exposed in digging a foundation. It appeared to indicate
that, at the later period of the deposition of this lower-level gravel,
somewhat similar energetic denuding agencies were at work in the
valley. The section has since been covered up. The buff sand
occurred very irregularly. The pebbles of Chalk in the chalky gravel
below were flat and covered with cracks, somewhat suggestive of the
action of frost. Some fragments of mammalian bone were obtained
from this opening ; one of them is referable to the Mammoth.

2. Norcot Brickyard.

At this place, about three-quarters of a mile westward of the
above-mentioned locality, there is a section of a gravel at a higher
level than that in the Tilehurst Road, namely about 288 to 294 feet
above sea-level. At present there is a thickness of about 6 feet of it
overlying the lower part of the London Clay and the Woolwich-and-
Reading beds at this place. It is evenly bedded, but the flints are
in much smaller proportion than in any other gravel in the district.
The pebbles and boulders of quartz, quartzite, &c., are numerous,
and there are boulders of various igneous rocks, a kind resembling
diorite deeply weathered being common, and occurring in rounded
masses of considerable size.

No trace of Man or any other mammal has been found here.

Such a deposit as this would approach more nearly in point of
date, probably, to the era of the wearing away of the Triassic coast-
line of Warwickshire &e.

The gravel at the Tilehurst Road section (page 585) may have
been derived to a small extent from such a gravel as this.

As this gravel comes into the valley as far as to about 288 feet above
the sea-level, I have taken it as a sort of datum-line for the purpose
of comparison. As it ranges over the higher ground of the Tile-
hurst Tertiary outlier to 340 feet above the sea-level it has the
character of a plateau-gravel, and becomes very variable in its
composition, consisting in places of finely comminuted material ©
and layers of clayey or sandy loam of considerable thickness.

3. Ltedlands, Reading.

Crossing over the Kennet we come to a sheet of gravel south of
the Thames and Kennet, near the point of junction of the latter.
The ground is now mostly built over, but the section seen in a large
pit has been fully described by Mr. E. B. Poulton*. It showed a
considerable amount of local disturbance of the beds beneath the
gravel. The level is low, being 156 feet above sea-level, and 40 feet
above the surface of the Kennet. In gravel taken from this pit I
found the first flint implement discovered in this district. By
further search I obtained a miscellaneous collection of about a dozen
implements and only two flakes. These varied in their types, and

* Quart. Journ. Geol. Soc. vol. xxxvi. 1880, pp. 296-306.
. tao eg

590 MR. 0. A. SHRUBSOLE ON THE

in the amount of abrasion they had suffered. In all cases but two
I found them in the heaps of gravel, but the workmen who discovered _
these two informed me that. they came from the deepest part of the
2 avel. One of these two specimens is a large pointed implement.
his terrace of gravel is continuous to the point where the Kennet
enters the Thames. ;
From another pit a short distance off, near the cemetery, a tooth
of Mammoth was found some years ago.

4. Kennet Mouth.

Close to the mouth of the Kennet, gravel has been extracted for
many years, as shown by the old workings. The present pit shows
the gravel to be here about 16 feet thick, resting on Chalk, at
a height of 30 feet above the river-surface. It is a water-worn,
non-ochreous gravel, containing, in addition to the flints, the usual
quartzites. At the upper part are numerous furrows filled in by
washes of surface-soil. Fragments of shells and of mammalian
bones have been met with. The only species of mammal determinable
is the Mammoth. No traces of Man have been found. Hlephas
prumigenius has occurred at three different points in this terrace of
gravel.

5. Southern Hill and Earley.

As we pass to the higher ground between the Kennet and the
Loddon, this gravel ends against the valley-brow, and is succeeded
by the gravel of the watershed. A section through the lower part
of this is afforded by the cutting on the South-Western Railway at
Earley, where it is seen to be 7 or 8 feet thick, and to consist of
worn and comminuted material, principally flint, at 212 feet above
sea-level.

At the edge of the terrace overlooking the Thames, an opening
for sewerage purposes showed gravel, 9 or 10 feet thick, of the ordi-
nary mixed kind; and from this I have obtained a few flint chips
and a rude implement. The level is about 223 feet above sea-level.

6. Sonning Hill.

A section is here afforded of the gravel of the Thames-and-
Loddon watershed at a level of about 185 feet above sea-level. A
pit by the road-side, close to the railway, shows about 10 feet of
clayey ochreous flint gravel, with quartzites. The line of the
Great-Western Railway passes this spot in a deep cutting, and a
spoil-bank formed of the surplus material has for many years been
worked for brick-making. From the gravelly part of this soil-heap
a few flint implements have been obtained, and are in the Reading
Museum. One of them is a large ovoid implement, ochreous in
colour.

7. Charvil Hill, Sonning.

From Sonning Hill the ground gradually descends towards the
point of confluence of the Loddon with the Thames. A terrace of
gravel occurs at Charvil Hill, near Sonning, at 171 feet above the
sea-level. A pit by the side of the road from Reading to Twyford

VALLEY-GRAVELS ABOUT READING. 591

exhibits a bedded gravel, with a few thin layers of clay. Mr. L.
Treacher, of Twyford, informs me that he has here obtained two
flint implements somewhat abraded. He observed on one occasion
a lump of mottled clay, about 4 feet in its longest diameter, em-
bedded in the gravel.

8. Ruscombe, Twyford.

Continuing in a north-easterly direction by the road from Read-
ing, and crossing the Loddon at Twyford, a higher and lower ter-
race of gravel are met with. The former is seen at the Ruscombe
brick-works, where it overlies the Woolwich-and-Reading beds at
an elevation of 167 feet above sea-level, and 60 feet above the sur-
faces of the Loddon and Thames. Owing doubtless to denudation,
it is a thin deposit, being in places only 2 or 3 feet thick; but it
fills up hollows of considerable size in the underlying sands or clay.

The brickyard itself affords a fine section of the variable Wool-
wich-and-Reading series, apparently with a N.E.-S.W. fault.

I was led to examine the gravel here by finding a flint implement
in the village, where some road-material had been laid down; and
from time to time [ have obtained a few specimens from the gravel
thrown out. Others have been obtained by Mr. Treacher, who re-
sides close by. Some of these are stated by the workmen to have
been obtained from the clay itself, at some slight distance from the
gravel. ‘There is no real improbability in this, for the gravel enters
the clay, as stated above, and its heavier materials would have a
tendency to sink the farthest in the clay. Some of the implements
found thus are quite sharp and unworn.

The implements found here are various in character and do not
belong to any one type; but pointed tools are well represented.
Some of the implements are buff in colour, others nearly black.

Although this would seem at first sight to be a gravel of the
Loddon, which flows past the village, it may perhaps be related
rather to the Thames, which is at no great distance, and towards
which the ground slopes. At Hurst, further up the Loddon-valley,
the gravel is at a lower level and is of a different character, as it
contains many fragments of chert, and quartzites appear to be
absent.

§ 4. GrnERaL ConsIDERATIONS.

With so few data within a limited area, it would be rash to make
large generalizations. It may be well, however, to consider whether
any, and what, significance attaches to the different levels at which
gravel containing palolithic implements occurs. The highest
gravels of the valley, those, namely, which lie between 2385 feet
and 269 feet above sea-level, do not contain, as far as my observa-
tion has extended, any traces of Man, or indeed any contempora-
neous organic remains. In the neighbourhood of Caversham,
gravels, only 20 feet higher than that at Toots Farm, appear to have
been accumulated under similar conditions, yet they have not yielded
any implements.

Assuming the highest gravels of the valley to be the oldest, the

592 MR. O. A. SHRUBSOLE ON THE

indications are that a considerable amount of valley-erosion must
have taken place before the implements now found at 235 feet above
sea-level were placed there. A still greater amount of erosion had
taken place before the implements and mammalian remains now
found at 197 feet above sea-level reached their present position.

With regard to any indications that are afforded as to former
climatic conditions, it is not until we reach the level last mentioned,
in descending order, that any very marked irregularities in the
deposit of gravels occur; the higher-level valley-deposits, like the
plateau-gravels and the hill-gravels, presenting no marked difference
from the results of ordinary water-action. Irregular bedding is
again observable as belonging to the considerably later epoch when
the valley had been lowered to about 150 feet above sea-level.

The very large percentage of quartzites and other rocks not occur-
ring i situ in the Thames-valley in the composition of the gravel
at Norcot (page 589), 294 feet above sea-level, may be taken as an |
indication that glacial action and submergence had taken place at no
distant interval from the time when it was laid down.

So far, then, as the gravels of the valley can be considered repre-
sentative of important stages in its history, the indications are of a
severe climate occurring at an early stage and recurring later
on. ‘Traces of Man occur in many of the stages intermediate be-
tween the Norcot gravel and that of the comparatively low-level at
Elm Park and Kennet Mouth. Traces of other mammalia are found
at those last-mentioned localities, but not of Man.

A comparison of the types of the implements found at the different
levels shows that, assuming the highest level to be the oldest, the
pointed type, with a thickened butt, might be adjudged to be the
most ancient in the district. On the other hand, the Ightham im-
plements, found at heights of from 380 to 500 feet above sea-level,
described by Prof. Prestwich*, and considered by him to be ‘‘ pos-
sibly pre-glacialt”, do not differ in any special manner from those
found in this district at levels lower than that of Caversham.

This similarity was alluded to by Dr. Evans{; and, as there
is reason for supposing the Ightham implements to have formed
part of gravels which have been in a great measure removed by
denudation, it is probable also that many of the implements found
in the lower levels at Reading have been derived from gravels which
have been swept away. This is the more likely when we have regard
to the mixed character of the types generally found in the lower
levels, and to the fact that a river can accumulate a considerable
thickness of gravel in a short time. It is not likely, therefore, that
the implements of various types found at any particular place repre-
sent the gradual entombment of the specimens ina slowly accumu-
lating deposit spread over a considerable interval, but rather the result
of a mixing-up of materials derived from gravels of various dates and
from various levels.

The position in which the implements occur in these lower-level
gravels is also worthy of notice. Wherever the gravel attains any

* Quart. Journ. Geol. Soc. vol. xlv. 1889, pp. 270-296.
t Ibid. p. 292. t Ibid. p. 295.

VALLEY-GRAVELS ABOUT READING. 593

considerable thickness, they occur near the bottom of the depcsit,
as a rule, but occasionally dispersed in the mass. At Ruscombe
they are found, as stated (page 591), in the underlying clay. In
consequence of the discontinuity of the several gravels, there is
great difficulty in obtaining from them detailed and consecutive
data. Juxtaposition in a gravel does not necessarily imply con-
temporaneous origin; and, as we might expect, there has been a
dovetailing of deposits, and a destruction and mixing together of
gravels formed at various dates.

A list of localities exhibiting the typical gravels of the valley,
excluding those of the lowest levels, is appended herewith in order
to show at one view their approximate height above the ordinary
river-level at the nearest point, and their relation to the occupation
of the valley by Man and the other mammalia, so far as I have been
able to ascertain.

It should be mentioned that the levels have been taken from
usually the highest point of each section at the surface; but aliow-
ance must be made for the varying contours of valley-deposits, and
for the fact that it has not been practicable in all cases to get the
exact level surveyed.

I have, through the kindness of Mr. Thomas Reed, of the Ord-
nance Survey at Reading, obtained the exact height above the sea-
level of the river-surface at two points, namely, at the junction of
the Thames and Kennet (116 feet), and at Caversham (120°77 feet).
Below those points the level of the river has been estimated.

I take this opportunity of acknowledging my indebtedness to
Messrs. William Davies, F.G.S., A.S. Woodward, F.G.S., and E. T.
Newton, F.G.S. for the identification of mammalian remains at
various times.

Traces of
Above te Man, * ;
sea-level. te other mam-
ames.
malia, Tt.
feet feet
North of Thames.
pvorela my EM oi ccc.csctecnsannecacvens 269 148
Wwialiimetord Road ...,.....c15..s.0ceces- 255 133
Toots Farm, Caversham.................. 2350) «| V1 etal
roo.0 1) SIEGE? yes Ae ea aa a 200 92 *
SSHORt/0 G/KG Os ee ee re 194 87 %
RUMMACR atte ds. Codonendaseasemanese ssee~ 184 17 sf
Henley Road, Caversham ............... 168 52 Si
South of Thames.
Momeot: (ie laetal e So. iscSeecdlssenitien's adele. 294 172
southerm Hill Reading ...c.s.00.2.cme 223 107 i
Tilehurst Road, Reading ............... 197 79 ea
OMIM HIME We. tea seunet oan aens seacenete 185 70 x
OG raer alle Hie ft movant eeacasdessoedenne Rae 64 =
ISU COMADO shores Seas ston seeaslaaietdavigitadembinaoas 167 60 x
Redlands, Reading y.....2cssacecnernaesne. 156 40 mits
Kennet Mouth, Reading ...............00 146 a0 t
Elm Park, Reading (lower level) ...... 144 . 22 -

594 ON THE VALLEY-GRAVELS ABOUT READING.

It will be seen from this Table that there is a somewhat wide
range of height above the nearest river-level in the case of the |
gravels containing relics of Man, namely from 40 feet to 114 feet.
While it is evident that Man was in the valley certainly as far back
as when its level stood 114 feet higher than at present, we cannot,
owing to the shifting nature of valley-deposits, positively say that
the occupation continued down to the date represented by the lower
level of 40 feet, although it may have been so.

With regard to the larger mammalia, the evidence here seems to
accord with that from other districts, their remains having been
found at lower levels than the implements fabricated by Man. It
may therefore be inferred with some degree of probability that those
animals remained in the valley for some time after Man had left,
if the chronological indications of valley-deposits could in all cases
be relied on.

Discussion.

Mr. Moncxton had noticed great variability of the gravels around
Reading, and would like to learn whether it was possible to trace
the gravels shown in the section at Grovelands for any distance
laterally.

Mr. Axssorr could not understand from the section displayed that
the Groveland gravel belonged to the Thames system, dipping, as it
did, to the valley of the Kennet; a continuation of the line of dip
appeared to take it over to the higher-lying gravel on the north,
making it appear as if the two gravels were the same, and had been
cut through by the Thames valley.

The AuruHor said that the variations had, to some extent, been
traced laterally. The appearance of dip towards the Kennet in
the section referred to by Mr. Abbott was misleading, as the section
was diagrammatic. He did not expect contemporaneous gravels to
be discovered on both the Oxford and the Berks side of the river.
The gravel referred to was distinct from that at Caversham, and
both were essentially valley-gravels.

BURROWS AND TRACKS OF INVERTEBRATE ANIMALS, ETC. 595

37. On Burrows and Tracks of InvertEpratE ANimMALs 7 Patmo-
zorc Rocks, and other Marxines. By Sir J. Wittiam Dawson,
LL.D., F.R.S., F.G.8. (Read May 14, 1890.) At. Ain/'7 840

ConrTENTSs.
Page
§ I. PE ROOUIC HOM Sak INe Mee hia seculecahonds Hlth toad todenonston dees 595
§II. Bilobites, Rusichnites, Arthrichnites, Protichnites, and Cli-
BITC CITIES ee Beek whee ts crated ossie seeieire levine ntaieoio tt Me oad de UaEe os 595
PE MESO MUNG Pome Fee te cece csecioins qbotinnien tisweysiijciens «eae atnauwine adesiears tl 602
CRIM PME SC IBCLIAIULCS cot vache deca enesiccutes tery eveccsticenccsnoateameaacane se: 605
§V. Trunk-like Concretions in the Potsdam Sandstone ............ 609
§ VI. Combinations of Worm-tracks with Ripple-marks and Shrink-
PIPE =CIAG sae E ties b Ma seuccd wags sauces klscat nat neoa- eat eeieeeintets 610
SIL, © Tsiieinfel mien: lee Ke) Baponacerense se ccansocpegdocee 3doeecesboudecclicdce su 613
Sevadue Rill-marks ....0... e600. Rr eerie ONT Ie ae ralee eticate teint at a ame toa ces 614
Srieemme C@orelucine INOUE fita.+...ccc-ssmereereserees- seers Nida dectot ogee 617

§ I. Lyrropvction.

THE present paper isintended to contribute some recently acquired
facts to the solution of questions connected with these often proble-
matical markings ; and it will consist rather of short notes, illustrated
by photographs, than of a connected discussion of the subject. I
propose to notice the nature of certain markings sometimes referred
to plants, under the name of Bilobites,—to the true nature of the
Scolithus canadensis of the Potsdam Sandstone,—to certain tubes
similar to those of modern Sabellce,—to cylindrical concretions resem-
bling trunks of trees,—and to imitative markings, and peculiar trails
of doubtful origin.

§ IJ. Binosrrss, Rustcunires, Proticunires, and CrimacricHNirss.
(Figs. 1 to 6.)

The name Bilobites, proposed by Dekay in 1823, was, as Newberry
has shown,” originally applied not to objects of this kind, but to
casts of certain bivalve shells. It was therefore dropped in America ;
but it has been revived and has gained currency in Europe 7, as
a term including various forms of markings referred to different
genera. The dominant characters are a band, or an oval mass, with
a median longitudinal furrow or ridge, and marked with transverse
or oblique furrows or striz, and with or without a marginal ridge.

The writer was enabled to show in 1864 ¢ that one of the most
remarkable of these impressions, Rusophycus grenvillensis of Bil-
lings, and Cruziana-like markings associated with it, were really

* “Science, vol. v. no. 124, 1885, p. 508.

Tt In Senhor J. F. N. Delgado’s ‘ Etude sur les Bilobites et autres Fossiles des
Quartzites dela Base du Systéme Silurique du Portugal,’ 4to, Lisbon, 1886,
and the ‘ Supplément,’ 1888, numerous bibliographic references to other authors
treating of these and some allied fossils are given in full.

¢ ‘Canadian Naturalist,’ n. s. vol. i. pp. 368, 458.

596 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

burrows and tracks of marine animals, probably Crustaceans. He
arrived at this conclusion by a careful study of the impressions made
by the recent Limulus polyphemus on muddy and sandy bottoms,
and by the application of these results to the explanation of a very
fine exposure of the impressions above-named in the works under-
taken for the enlargement of the Grenville Canal, on the Ottawa
River. In this paper, descriptive of the facts observed at Grenville,
it was proposed to substitute the generic name Lusichnites for Ruso-
phycus or Rysophycus, and it was pointed out that the so-called
fucoids of the genus Arthrophycus were probably of like nature, and
might be placed in the same category with the impressions described
by Logan as Climactichnites from the Potsdam-Sandstone *. These
observations were supposed to have conclusively settled the question
as to the nature of all the Bilobites; but little attention seems
to have been given to them by European Paleontologists. Nathorst
has, however, arrived at similar results, in a somewhat similar
manner, by comparison with modern impressions f ; and Williamson
has described as casts of animal-tracks markings of this nature
from the Yoredale rocks t+. Bureau has also adduced some striking
evidences in favour of the theory that some at least of the Bilobztes
are the work of Phyllopod Crustaceans §. Saporta, Delgado, and
others still regard the Bilobetes as true Alge, and Schimper
describes one form as a plant, under the name Crossochorda. In
so far as American examples are concerned, it may be considered
as settled that they may best be explained in the way above in-
dicated. The following genera may be included in this general
statement :—

Rusichnites = Rusophycus, Hail.
Arthrichnites = Arthrophycus, Harlan.
Cruziana, D’Orbigny.

Climactichnites, Logan.

Freena, ltouault.

Crossochorda, Schimper (in part).

These impressions pass into Protichnites of Owen through such
forms as P. Davisi of Williamson ||, and the Serichnites of Billings§]
and Diplichnites of the author**. They are connected with the
undoubted worm-tracks of the genus Nereites by specimens of
Arthrichnites, of which I have several in my collection, and in

* Canad. Nat. Geol. vol. v. p. 279.

t Kongl. Svenska Vetenskaps-Akad. Handlingar, vol. xviii. No. 7, 1881; eleven
plates, 104 pages, including an Abridgment in French. The List of Books and
Memoirs treating of Trails and Tracks, from 1823 to 1881, occupies six of the
quarto pages in this work. Also ‘ Nouvelles Observations sur les Traces des
Animaux ;’ Stockholm, 1886.

t+ Mem. Manchester Lit. & Phil. Soc. 3rd series, vol. x. 1885, pp. 19-29,
3 plates.

tS Comptes-rendus, vol. 104, 14 Février et 4 Juillet, 1887, page 7 of the
author’s reprint.

|| Op. cit. pl. i. fig. 4. @ Catal. Sil. Foss. Anticosti, 1866, p. 73.

** Amer. Journ. Sci. ser. 3, vol. v. 1873, p. 19, and p. 23, fig. 3.

INVERTEBRATE ANIMALS IN PALZXOZOIC ROCKS. 597

which the central furrow becomes obsolete, and by the genus
Gyrichnites of Whiteaves, and other forms destitute of a median
groove *.

They cannot be sharply divided into genera or species, because of
their variability in passing over different kinds of bottom, and of
the changes which occur in consequence of the various modes of
progression employed by the animals.

Fig. 1 represents a typical specimen of Rusichnites, from my paper

Fig. 1.—Rusichnites grenvillensis. The cast of a Crustacean
Burrow, with part of a trail leading to it, or from it, at. a.
Cambro-Silurian ; Grenville, Canada.

of 1864, and shows traces of the trail leading to or from the cast of
the deep burrow or excavation. Fig. 2, Rusichnites acadicus, from
the Carboniferous, I now regard as a result of successive strokes of a
crustacean tail, with marks of the carapace and limbs. The speci-
men represented in fig. 3, which is from the Clinton Formation of
Canada (and from the collection of Lieut.-Col. Grant, of Hamilton,
Ontario), illustrates the probable origin of these markings, but also
suggests the idea of some of them having been the trails or castings
of worms rather than marks of crustaceans. It is evident indeed
that these markings are closely connected with those named Nerettes
by Hall, and of which he has figured several kinds from the Clinton
formation, ascribing them to Molluscs. Similar objects have been
named Psammichnites by Torell, and are supposed by him to resemble

* Trans. Roy. Soc. Canada, vol. i. 1883 ; Section iv. 1882, pp. 109-111.

598 SIk J. W. DAWSON ON BURROWS AND TRACKS OF

Fig. 2.—Rusichintes acadicus. A Crustacean Track, showing the
marks of the edge of the carapace. Carboniferous; Cape Breton.

YF, Fa

f

WT
fp UY Uf
U7,

Fig. 3.—Rusichntes (Psammichnites) clintonensis, sp. nov.
Silurian of Ontario, Canada. (From a Photograph.)

INVERTEBRATE ANIMALS IN PALHOZOIC. ROCKS. 599

castings of the Lobworm*. I am indebted to Lieut.-Col. Grant for
an extensive series of these markings, on which it can be seen that
the same trail often assumes very different characters, sometimes
resembling Crossochorda or Cruziana, and at others passing into the
ordinary Nerettes or even into a simple trail.

The Protichnites + of the Potsdam Sandstone are indubitable
tracks of Crustaceans ; yet it is possible, as I have shown in the case
of Limulus, that the same animals which produced Protichnites may
also have been the authors of the transversely ridged Climactichnites
so often associated with them (figs. 4 and 5). It is also to be ob-
served that such forms as my Protichnites acadicus t or the Pr.
scoticus of Salter § form connecting links between this kind of track
and Cruziana.

To the same category may be referred the trails with wave-like
transverse markings and no central line, found both in the Upper
Cambrian and Devonian, and which Whiteaves has named Gyrich-
nites ||.

I copy here the remarks on Husophycus (Bilobites) in my paper of
1873, merely adding that I now believe some markings of this kind
may have been produced by Cheetopod Worms, as well as by Phyl-
lopods :—

‘Tn a paper published in the ‘ Canadian Naturalist,’ 1864, I showed
that the singular bilobate markings with transverse strie, named
Rusophycus by Hall, and found in the Chazy of Canada and the
Clinton group of New York, are really casts of burrows connected
with footprints, consisting of a double series of transverse markings,
and that a comparison of them with the trails and burrows of Zz-
mulus justified the conclusion that they were produced by Trilobites.
I proposed for these, and for similar impressions of small size found
in the Carboniferous, the name given above. The Carboniferous
examples, I supposed, might have been produced by the species of
Phillzpsia found in these beds. A specimen recently obtained from
Horton shows this kind ofimpression passing in places into a kind
of Protichnites, as if the creature possessed walking feet as well as
the lamellate swimming feet which it ordinarily used.”

I can scarcely doubt that the Cruziana semiplicata of Salter, and
O. similis of Billmgs from the Primordia! of Newfoundland, must
have been produced by Crustaceans not dissimilar from those to which
Rusichmtes belongs. ;

To Rusichnites, rather than to Protichnites, ought perhaps to be

* Lunds Univ. Arsskrift, vol. vi. p. 34, 1869.

t+ Logan and Owen, Quart. Journ. Geol. Soc. vol. viil. 1852, pp. 199-225.
In the ‘ Geologist,’ vol. v. 1862, pp. 128-139, and pp. 454-456, the proba-
bility of Climactichnites having been the infallen gallery-tracks made by Para-
doxides burrowing in the sand of the old sea, like Su/cator and Kroyera (as
shown by Albany Hancock) burrow in the present sea-sands, has been suggested.
A similar explanation was given in Prof. Dana’s ‘ Manual of Geology,’ 1863,

. 189. This does not, however, seem applicable to the Canadian specimens.
See figs. 4 & 5, and further on.
t Amer. Journ. Sci. ser. 3, vol. v. 1873, pp. 17,18, 23, fig. 2.

§ Quart. Journ. Geol. Soe. vol. xii. p. 248, fig. 2.
|| ‘Trans. Roy. Soc. Canada,’ loc. cit.

600 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

Fig. 4.—Climactichnites and Protichnites, associated on the same
slab. From the Potsdam Sandstone of Ontario (in the Peter-
Redpath Museum). About +, of natural size. The large slab
is the overlying impression ; the small one, placed below, is the
underlying surface. (From a Photograph.)

f KWNTERDVE Bash

INVERTEBRATE ANIMALS IN PALAZOZOIC ROCKS. 601

Fig. 5.—a, Protichnite-like ; 6, Climactichnite-like Trails of
Limulus polyphemus. Modern. Coast of Maine.

NN f
Vw

S A}
SANISIQQ TIS MS
SNA:
ay NY v
SINGINTIN
ys
f

“A
GZ 25
Z Z
LE. y 4
z LY

FIN
BN
iN

VI

referred certain transverse linear impressions with a broad central
groove from the Lower Carboniferous of Horton, which occur at
that place under different modifications, and sometimes seem to
change into light scratches, or touches of feet employed in swimming,
or end abruptly, as if the animal had suddenly risen from the bottom.

Nathorst * and Bureau have further shown that impressions-
similar to Bilobites may be produced by the successive strokes of the:
tail of certain Crustaceans (Crangon and Palemon). From all the
phenomena attending the Potsdam Climactichmtes, 1 am now in-
clined to regard them as of this nature, and as implying the existence:
of a large Crustacean with a truncated tail divided into two movable:
lobes. This would account for the ridge sometimes dividing the
furrows and transverse ridges, and for its change of position from.
side to side of the mesial line,—also for the interrupted ridges on
each side of the trail, which would be the natural result of the suc-
cessive strokes of a flat organ,—and for the appearances presented!
when the tracks turn abruptly f (see fig. 4).

There is confessedly some difficulty in separating the marks known'
as Phymatoderma from Fucoids allied to Caulerpa, and even from:

* Trans. Roy. Acad. Sweden, vol. xviii. no. 7, 1881.
_ + “Impressions of Aquatic Animals,” ‘Amer. Journ. Sci.’ ser. 3,. vol. v..
1873, p. 16.

602 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

stems of the coniferous genus Brachyphyllum; but Zeiller has re-
cently described a roofed tunnel or burrow made by the mole-
cricket, which completely reproduces some of the forms known under
the name Phymatoderma.* I have in my collection (fig. 6) a

Fig. 6.—Roofed Burrow: Phymatoderma. Silurian; Ontario,
Canada. (From a Photograph.)

ee A
aa NG

specimen, collected by Col. Grant in the Clinton formation, |
shows that some Silurian animal, possibly a Crustacean, made
covered burrows of this kind.

§ III. Scorrravus, &. (Figs. 7 to 10.)

This genus, proposed by Haldimand as early as 1840, though the
name would indicate that it refers to a worm, was originally placed
with Fucoids ; and both Halil and Billings regarded the cylindrical
cavities, designated by the title, as representing ‘‘ stems.” No evi-
dence, however, has been found of any organic matter in connection
with Scolithus ; the tubes being usually filled with a sandy argilla-
ceous or calcareous material, which weathers out of the hard matrix,
leaving cylindrical holes.

* Bull. Soc. géol. France, sér. 3, vol. xii. 1884, pp. 676-680.

INVERTEBRATE ANIMALS IN PALZXO0ZOIC ROCKS, ° 603°

- Two species have been recognized in the Potsdam Sandstone of
Canada and the United States, Scolzthus linearis of Hall and
Se. canadensis of Billings. The former is usually straight, at right
angles to the bedding, and smooth, or with obscure striation. . The
latter is rather smaller, tortuous, and unequal in diameter, sometimes
branching and curving, and occasionally showing slight transverse
ridges on the sides of the cylinders.

The latter species is very abundant in the Potsdam of St. Anne’s:
on the Island of Montreal, where many varieties can be collected ;
but none of them shows any distinct structure. So far as indicated
by the ordinary specimens, they may be moulds left by the decay
of plants, sponges, or corals, or by the stems of Lingule, or the
burrows of worms.

Fig. 7.Slab with castings of Scolithus. Perth, Ontario.
(From a Photograph.)

Their true nature is made evident by a fine slab kindly presented
to the Peter-Redpath Museum by Mr. W. J. Morris, of Perth, On-
tario. A portion of the upper surface of this slab is represented in
fig. 7, which shows rounded pellets and ridges of. hardened sand, very

Q.J.G.8. No. 184. 2x

604 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

similar to those ejected by many modern worms from their burrows.
From these the tubes of Scolithus descend into the sandstone in the
manner represented in fig. 8. Itis, I think, quite evident that this
variety of Scolithus represents burrows with castings at their en-
trances; and, since it is referable to Sc. canadensis, I have no
hesitation in affirming that this interesting specimen indicates that

Fig. 8.—Sectional view of Scolithus, showing castings at the orifices,
Perth, Ontario.

that species at least must be regarded as a worm-burrow. From the
forms of these burrowsit is not improbable that they may have been
lined with a fine membrane sufficient to protect the body of the
animal from the roughness of the sand, and that this lining may
have aided in preserving their forms.

It is to be observed with reference to burrows of this kind, that
under different circumstances their orifices may present very dif
ferent appearances. Where the castings from them have been removed
by a rapid current, they may have merely a simple opening at the
summit. Where the animal has moved inward and outward, en-
larging the opening, they may be funnel-shaped at top, like the
burrows to which the term Monocraterion (Torell) has been applied ;
and, where the worm has made grooves radiating from the orifice,
forms similar to Scotolithus mirabilis of Linnarsson *, or the forms
which have been named Pyrophyllites and Asterophycus, may have
been produced. Ido not maintain that the forms indicated by the
above names are identical with Scolithus canadensis, but I have seen
in connection with that species appearances resembling these forms,
Fig. 9 shows aform of this kind; but it is from a higher horizon, the
Clinton, from which formation I have also funnel-topped burrows,
like those of the Cambrian Monocraterion.

The singular radiating markings, from the Cambrian of Nova
Scotia, which I have described as Astropolithon Hindii, and which

* Trans. R. Swed. Acad, Sci. vol. ix. 1871, p. 18, pl. v. figs. 21, 22.

INVERTEBRATE ANIMALS IN PALZOZOIC ROCKS, 605

Fig. 9.—Radiating Burrow. Silurian; Ontario, Canada.
(From a Photograph.)

also ovcur in the Quebec Group at Metis, Canada, may possibly
have the character of mouths of large burrows with radiating trails,
though the radiating marks in this case seem to be of the nature of
vertical plates, rather than of grooves (see fig. 10),

§ IV. Sapetzarires, gen. nov. (Figs. 11 & 12.)

The modern genus Z'erebella, which constructs tubes of grains of
sand and fragments of shells attached to a membranous lining, has
been recognized by its tubes as low as the Lias ( 1’. capilloides, Goldf.),
and I have ascertained the existence of similar tubes as low as the
Siluro-Cambrian ; though, as the tubes do not necessarily indicate
the precise affinities of the animal, I prefer to designate them by
the name above given, and to define this as indicating elongated
tubes composed of grains of sand and calcareous orgauic fragments,

2x2

606 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

associated with carbonaceous flocculent matter, indicating a horny
or membranous sheath. I have long suspected the existence of
such tubes, and their connection with many of the cylindrical bodies
often confounded with fucoids of the genera Palwophycus and
Buthotrephis, but have only recently been able actually to demon-
strate the fact.

Fig. 10.—Astropolithon Hindi, a burrow or organism from the
Lower Cambrian of Nova Scotia. (‘ Acad. Geol.’ 3rd ed. Suppl.
1878, p. 83.)

In the Black-River Limestone (Trenton group of the Siluro-Cam-
brian) at Pointe Claire, on the St. Lawrence, near Montreal, certain
layers of grey limestone sisi numerous dark-coloured, cylindrical,
tortuous bodies, from ;4th to $th of an inch in diameter When
broken across, they are seen to be filled with crystalline calcite, as if
they had been tubes; and, when thin slices are prepared for the
microscope, the character of their walls, as’ composed of fragments of
stone and broken shells &c., cemented by an organic nisin now
carbonised, becomes apparent. Figs. 11 and 12 show the appearance
of the tubes on the weathered surfaces, and in section. The species
may be thus described :-—

The tubes are 1 to 3 millimétres in external diameter, and 3
centimétres or more in length, tortuous, irregular as if sometimes
compressed, and sometimes in groups of two or more attached
together. This would show a fixed or sessile condition as in
Sabellaria or Sabella, rather than freedom, as in the Terebellide.

INVERTEBRATE ANIMALS IN PALZOZOIC ROCKS. 607

Fig. 11.—a, 0, ¢, Sabellarites trentonensis. a. On a weathered
surface; nat.size. b6andc,enlarged. Black-river Limestone ;
Pointe Claire, near Montreal.

a

Fig. 12.—a, b, Transverse and Longitudinal Sections of Sabdellarites.
(Enlarged. )

608 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

The wall of the tube is somewhat thick and composed of fragmental
matter, cemented by a dark-coloured organic substance. It is to
be observed that in the case of tubes, as distinguished from mere
burrows, like Scolithus, when two or more are attached together an
appearance of branching results.

Tubes apparently of similar character, but of considerably larger
size, occur in the same formation ; and many obscure cylindrical or
flattened bodies, not distinguished from branches of Algz, may be
of the same nature. I would also refer to a similar origin, and
provisionally to this genus, the curious primordial burrows from the
Hastings group described in the Quarterly Journal of this Society *
in 1866, and the phosphatic tubes from the limestone of the Quebec
group at Kamouraska, described in the Quart. Journ. Geol. Soc. in
18767. The latter, however, I fancy are composed of excremen-
titious matter, or débris of the food of worms feeding on Lingu-
loid shell-fish. .

While preparing this paper, I have re-examined these tubes, and
have had some new slices prepared. These confirm my previous
statements. The thick walls of the tubes are destitute of lamination,
and have a finely granular texture, resembling that of the paste of
coprolites. They contain a few fine grains of sand, and minute
fragments of shells and of carbonaceous fibres. The whole seems to
indicate that they are formed, as already stated, of the phosphatic
dejections of animals subsisting on Lingule, Trilobites, Hyolithes,
and other creatures having coverings of calcium-phosphate.

In the same paper I referred to the fact that the shells of Hyo-
lithes t [Hyoltthellus, and Salterella] are rich in phosphates, and that
some of these shells are thick-walled with concentric lamination and
with tubes or pores penetrating their walls, suggesting the idea that
they may be shells of Worms rather than of Pteropods. I have since
compared them with specimens of the singular phosphatic tubes
found not infrequently in the Trenton and Chazy formations, and
described by Billings under the name Serpulites splendens and S.
dissolutus. Specimens of these tubes, when sliced, show a structure
not fragmental, but composed of very fine concentric lamine, with
indications, in some specimens, of minute sinuous tubuli. They are
smooth internally, and without show indications of thickened ridges
and of transverse lines of growth. One of my specimens has been
coated externally with a thin layer of some Monticuliporid coral.
If these are worm-shells, of which there seems little doubt, they
suggest affinities with the phosphatic Hyolitheilus and Salterella.

It may, perhaps, be useful to suggest provisional names for the
arenaceous and phosphatic worm-tubes resembling those of Sabellaria
and here described. Those from the Black-River formation may be
named Sabellarites trentonensis; and the thick-walled phosphatic
tubes, from the Quebec group, S. phosphaticus.

* Vol, xxii. p. 608. In the paper of 1866 these are referred to as from
the Laurentian of Madoc, Ontario. Since then these beds have been recog-
nized as being later than Laurentian, possibly Huronian, and designated the

“Hastings group.”
t Vol, xxxii. p. 286. t Op. cit. p. 288.

SSS —“‘ (e'é‘ (!™:;ti‘i:;:;f

INVERTEBRATE ANIMALS IN PALZOZOIC ROCKS. 609

§ V. Trounk-Like Concretions In tHE Porspam SanpsTone.
(Fig. 13.)

Many years ago specimens were obtained from the Potsdam
Sandstone of Ontario, by the late Sir William Logan, which presented
the aspect of large cylindrical trunks, a foot or more in diameter.
They were casts in sandstone, without any external bark or or-
ganic matter, though showing obscure concentric lines on the ends.
No opinion was, I believe, hazarded at that time respecting their
origin; and more recently fine specimens have been collected by Dr.
Selwyn on the bank of the Rideau Canal near Kingston; and Mr.
A. Young, a student of McGill University, obtained others at
Almonte, which he presented to the Peter-Redpath Museum. One
of these is represented in fig. 13.

Fig. 18.—Trunk-like Concretion. Potsdam Sandstone; Almonte,
Canada. inat.size. (From a Photograph.)

An incidental light seems to have been thrown upon their nature
by the study of certain recent concretions, now forming in the
alluvial clay of the St. Lawrence, by Rev. Prof. Kavanagh, of
Montreal. These are small cylindrical bodies with a minute per-

610 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

foration in the centre, often ee a little Mh ote matter.
They were thus described * :

‘“‘ These little bodies are seidinile clay concretions formed around —
vegetable fibres, and hardened by a small percentage of calcium
carbonate, since when treated with hydrochloric acid they effervesce
feebly and become disintegrated. They probably originate in the
molecular aggregation of the calcareous matter in the clay around
any foreign body included in it. They are about half-an-inch in
diameter, and the largest may have been two inches in length; with
rounded ends. When broken, they show a small central canal con-
taining a little sand and strips of epidermal tissue, the remains of a
root orstem. One shows three branches, apparently proceeding in a
verticillate manner from a central stem. In the centre, the light
reddish-brown colour of the clay has assumed a greenish hue, owing
to deoxidation of the peroxide of iron by decay of the vegetable
nucleus.”

On comparison of these recent concretions with the Potsdam
cylinders, it becomes apparent that they resemble each other very
closely in form and structure, and that the older cylinders may have
been formed in a similar manner, though on a gigantic scale. In
confirmation of this view, it may be mentioned that in the Pleisto-
cene clays of Green’s Creek, on the Ottawa, cylindrical concretions
surround twigs of poplar, which have been imbedded in the clay,
and that in the Permian Sandstones of Prince-Edward Island
ferruginous matter has cemented the sand into cylindrical concretions
around stems of Calamites. This view as to the origin of the Pots-
dam cylinders is further confirmed by the rounded ends of some of
them, and by the conformity of the internal concentric structure to
this rounding. One of the smaller specimens in the Peter-Redpath
Museum shows this peculiarity very well.

In the case of the Potsdam concretions, the nucleus of the con-
cretion must have been an erect stem of some kind, possibly a Chorda-
like Alga. So far as appears, this central stem must have been very
slender, but no distinct traces of it have yet been observed. Per-
haps the most remarkable fact in the case is that these cylindrical
bodies are sometimes several feet in length, and pass through more
than one bed of the sandstone. Another peculiarity is the presence
is some of them of irregularly rounded cavities, apparently indicating
the presence of bodies either concretionary or organic which have
been removed by solution or decay. These, however, are very rare.

§ VI. Compryations or Worm-tTRAcKsS witH RipPLE-MARKS AND
SHRINKAGE-cRAcKS. (Figs. 14 & 15.)

Fig. 14 shows a rippled surface in Potsdam Sandstone with marks
of worms or molluscs, arranged in the hollows of the ripples. The
marks are simple trails, of that curious circular or chain-like form
sometimes observed, and seem to have been made by animals creeping
in the furrows between the ridges of the ripple-marks.

* «Canadian Record of Science,’ vol. iii. No. 5, January 1889, pp. 292-294.

———E ee

INVERTEBRATE ANIMALS IN PALHOZOIC ROCKS, 611

. Photograph No. x1. (not figured) shows another combination,
where numerous trails formed in soft sediment have been affected
by shrinkage-cracks, produced by the drying of the mass, in such a
manner as to present a very complicated appearance.

Fig. 14.— Combination of Worm-trails and Fiapple-marks.
Potsdam Sandstone; Canada. 43 nat. size. (From a Photograph.)

-

Still another appearance which may be placed under this head 1s
that in fig. 15, which represents part of the surface of a large slab
of Calciferous Sandstone from St. Anne’s. At first sight it seems
to be covered with a network of shrinkage-cracks, but on closer
inspection these are seen to be cylindrical worm-tracks or burrows
planed off and flattened on one side, as if a slab covered with casts
of worm-tracks had been rubbed or ground down till the originally
rounded sides of all the more prominent were flattened. The
only way in which it seems possible to account for such an ap-
pearance is to suppose that the tracks were partly filled with mud
incapable of hardening into stone, and then completely filled and

612 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

covered with a bed of sand, hardened afterwards into rock. The
effect would be that, on weathering, all the prominent parts filled
with mud would disappear, leaving the slab in its present state.

Fig. 15.— Worm-burrows seen in section, owing to the manner of
preservation and weathering. Calciferous Sandstone ; St. Anne’s.
(From a Photograph.)

All of these tracks or burrows are of the plain cylindrical forms to
which the terms Planolites, Nicholson *, and Arenicolites, Salter t,
have been applied, and which differ from Scolithus only in their
more tortuous character, and in their usually being casts of mere
trails on the surfaces of beds, rather than burrows or tubes pene-
trating them. I cannot doubt the origin of these markings, if for
no other reason, on account of their covering such great surfaces of
strata in a uniform manner.

* «Proceed. Roy. Soc.’ vol. xxi. 1873, p. 289; ‘Manual Paleont.’ edit. 2
vol. i. p. 320.

t ‘Quart. Journ. Geol. Soc.’ vol. xiii. 1857, p. 204... |

INVERTEBRATE ANIMALS IN PALZOZOIC ROCKS. 613

§ VII. Brancuine Tracks. (Fig. 9, page 605.)

It is very puzzling to the Ichnologist to findso many impressions
which he would regard as of animal origin branching in a manner
to simulate plants. The distinction, however, between branching
plants and branching tracksis usually sufficiently obvious to an ex-
perienced eye. The latter are generally of the nature of more or less
cylindrical bodies, diverging or radiating from a commoncentre ; while
the former display either alternate ramification or bifurcation. As
examples I may refer to Photograph No. xuu1. (not figured) of Bu-
thotrephis gracilis, and B. Grantw, figs. 16 and 17, true Fucoids, in

Fig. 16.—Buthotrephis Grantw. <A true Fucoid, from the
Silurian of Canada.

comparison with fig. 9 (above referred to), of radiating Annelid
marks, or Photograph No. xv. (not figured), which represents a
Lncrophycus, probably a burrow with diverging tracks. Simple
and branching trails of these kinds cover large surfaces of the Cal-

.614 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

ciferous formation at St. Anne’s, and are similar to markings of this
kind which I have described from the Lower Carboniferous of Nova
Scotia *,

Fig. 17.—Buthotrephis Grantit. A true Fucoid: carbonaceous.
Niagara Formation. 4 nat. size. (From a Photograph.)

§ VIII. Ritt-marks, as DIstinevIsaED FROM ANIMAL- oR PLANT-
IMPRESSIONS. (Figs. 18 & 19.)

In my ‘ Acadian Geology ’ I have described the remarkable appear-
ances simulating Alge, or even gigantic trees, produced in the sloping
banks of fine mud in the tidal channels of the Bay of Fundy. These
are formed by minute rills, oozing from the wet sand or mud, and
trickling in fine streams along the slimy surfaces, and uniting into
larger and larger streams so as at length to produce the likeness of
impressions of flattened trees, with large trunks and branches, divi-
ding into twigs of extreme tenuity. Similar surfaces are often
found in the Coal-formation, and sometimes on quite as large ascale
as in modern tidal estuaries. Their forms and arrangement differ
according to the slope and character of the sediment, and the amount
of water it contains; but all show very delicate and often regular
branching impressions. Figs. 18 and 19 represent two types of
these in my collection from the Carboniferous of Nova Scotia, and

* * Acadian Geology,’ p. 256.

INVERTEBRATE ANIMALS IN PALMOZOIC ROCKS. 615

taken from surfaces unquestionably sculptured by water. A curious
complication of such markings sometimes occurs when shrinkage-
eracks, overflowed by a succeeding tide, have their edges sculptured
by minute rill-marks. Dvictuolites Beckwi, of Hall*, is a remarkable
example of this.

Fig. 18.—Rill-mark. Carboniferous; Nova Scotia.
3 hat. size. (From a Photograph.)

It would be invidious to refer to the numerous species of ima-
ginary fossil plants that have been founded on such markings as those
referred to above and shown by figs. 18 and 19. IL may merely
mention the genera Dendrophycus, Delesserites, Veawillum, Aristo-

* ‘Paleontology of New York,’ vol. ii, 1852, p. 6, pl. 2. fig. 1.

616 SIR J. W. DAWSON ON BURROWS AND TRACKS OF

phycus, Chloéphycus *, Tricophycus of authors as examples of Gentes
which contain, or consist of, examples of Rill-marks.

I may add that I have discussed other forms of such i impressions
in my papers on Footprints of Limulus, and on the genus Rusichnites,
in the ‘ Canadian Naturalist,’ and in that on “ Impressions of Aquatic
Animals in the Carboniferous Rocks”. In my work, ‘The Geological
History of Plants’, I have also endeavoured to state the criteria for

Fig. 19,—Rill-mark, Carboniferous; Nova Scotia,
3 nat. size. (From a Photograph.)

separating such markings from true Alge, and have referred to in-
stances in which, while, on the one hand, mere markings have been
elevated into marine plants, on the other, true land plants, imper-
fectly preserved, have been degraded into Algw. I may also state
that in America the Clinton tormation, intervening between the
Medina Sandstone and the Niagara Limestone, and containing many
thin-bedded arenaceous and argillaceous deposits, is remarkably rich
in such impressions, Many of these have been figured by Prof.
Hall+ and referred to worms, crustacea, and gastropods. In the
vicinity of Hamilton, Ontario, large collections have been made by
Lt.-Col. Grant, who has enriched the Peter-Redpath Museum of
* Miller now admits that this is not an Alga.

t Amer. Journ. Sci. ser. 3, vol. v. 1873, pp. 17, &e.
t ‘Paleontology of New York’, vol. 11. 1852,

INVERTEBRATE ANIMALS IN PALZOZOIC ROCKS, 617

McGill University with a very large and instructive series of slabs
including a vast variety of forms, a few only of which have been
noticed in this paper.

[I desire also to remark that the facts above detailed, together
with the discoveries of Annelid-jaws by Hinde and others, show
that the Marine Worms must have culminated, in regard to size,
abundance, and range of organization, at a very early geological
period.—September 9th, 189v. ]

I need not refer to the well-known and important observations of
Nathorst, Williamson, Owen, Miller and James of Cincinnati, Zeiller,
Salter, and others on this subject, or of the able defence of the
Algoid nature of some of them by Delgado, Saporta, and Crié. My
object has been merely to give some clear and instructive examples
which may tend to settle some of the points which have been in
dispute.

The whole of the specimens referred to in the above paper are,
with many others, in the Peter-Redpath Museum of McGill Uni-
versity. Anumber of them are large slabs, of which only a portion
or a reduction could be given in the photographs.

§ IX. Norzs.—I append, as an interesting impression, Photograph
xx. (not figured), which shows part of a rain-marked surface from
the Devonian of Gaspé, which has subsequently curled up and
cracked in drying, in the manner which may often be seen in modern
pools, when dried up.

I should perhaps add that, after many unsuccessful attempts, I
have been able to find vegetable structure on only one specimen of
any of the so-called Algze of the Lower Paleozoic rocks. This is a
flattened cylinder referable to the genus Palwophycus, from the
Trenton Limestone. Its structure is somewhat imperfect, but
shows long sinuous tubes like those in the stems of some Laminarie.
All the other Algz of these older formations that I have met with
are either reduced to carbonaceous films destitute of structure or are
mere impressions without organic matter.

[Since the above paper was written Mr. G. F. Matthew has
given (Amer. Journ. Science, ser. 3, vol. xxxix. 1890, p. 145) a
notice of some worm-burrows, from the Lower Cambrian of New
Brunswick, which he regards as similar to those described by
Torell from the EKophyton- and Fucoid-sandstones of Sweden, and
certain remarkable markings from the still older Animikie forma-
tion of Lake Superior. These last are of two kinds, curved divergent
marks (T'aonichnites), and straight strie, crossing at acute angles
(Ctenichnites). The specimens, from the Cambrian of Canada, re-
ferred to Hophyton seem, so far as known, to be of the nature of the
straight markings which I have elsewhere named Rhabdichnites.—
J. W. D., September 9th, 1890. ]

[Norr.—Lesley (‘ Dictionary of Fossils,’ p. 1195) refers to a
specimen, found by Walcott, showing the shell of a large Mollusk
at the end of a track resembling J?usichnites. Billings and Nathorst
have shown that some transversely-wrinkled tracks may have been
produced by the foot of Gastropods.—J. W. D., October 2nd, 1890.]

618 BURROWS AND TRACKS OF INVERTEBRATE ANIMALS, ETC.

Discussion.

Prof. Huenes would like to see a combination of geologists and ~
zoologists discussing each one of the various marks. He had paid
most attention to Cruziana, and was glad to find that the Author
agreed with him that it was impossible to refer it to any surface-
track, and difficult to explain it on the hypothesis of its representing
the form of any soft-bodied animal such as Nerevs.

Dr. H1yve observed that for many years the origin of these marks
had been discussed. He thought that most of them were the
tracks and filled-up burrows of marine organisms. The fact that no
carbonaceous matter had been found with these forms in the ditferent
countries where they occurred was opposed to the theory of their
plant-origin. On the other hand, he had obtained undoubted
Annelid remains from some of the very beds containing these
markings.

Quart. Journ. Geol. Soc. Vol. XLVI. Pl. XXIV.

SCAMS ONS IEEE DO) an sna
from the Red-Hill and Olivine Ranges, South Island, New Zealand.

ON THE NICKEL-IRON ALLOY AWARUITE OF NEW ZEALAND, 619

38. On the Discovery, Monz or Occurrence, and DistRiButTion of
the Nicxet-IRon AtLoy AwaRviTE, on the West Coast of the
South Isranp of New Zeatanp. By Professor G. H. F.
Utricu, F.G.S. (Read June 4th, 1890.)

[Puate XXIV. ]

i ConTENTS.
PPM Tas PRIN NOTA Mcc A ase cecct csc claxane bicce: vss ve cuin« cae scjnceesvedeunnaesndaee 619
2 Geolosy and Description of the Rocks ...... 0.600. .00. 2. ceceasenseooebens 622
8. Mode of Occurrence and Distribution of the Awaruite ............... 629
PE age errr ap LOM OL GWE PIAHC) oye «are cniewns sencerenveseebacesvsiesseecues howsline ne 650
Introductory.

In October 1885 Mr. W. Skey, Government Analyst, read a paper
before the New Zealand Philosophical Society, Wellington, an-
nouncing the discovery of a Nickel-Iron Alloy, which he recognized
as anew mineral species and named “‘ Awaruite.” The discovery was
made in a collection of minerals sent to the Government Laboratory
by Mr. Macfarlane, the Warden of the Jackson’s Bay District, which
includes Big Bay (Maori name,“ Awarua”’), Barn Bay, and other Bays
in that part of the West Coast of the South Island. Mr. Skey found
the new mineral as small grains or scalesina sample of heavy black
sand, reported as saved by alluvial miners in Barn Bay; and he gave
in his paper, besides descriptions of the physical character of the alloy
and its mineral associates, interesting particulars concerning its
behaviour towards a solution of cuprous sulphate acidulated with
hydrochloric acid, and its quantitative chemical composition as :—
Ni=67:63, Co=0°70, Fe=31:02, S=0-22, 810,=0°43 ; Formula
=2Ni+Fe; Sp. Gr.=8-1; Hardness about 5. He considered the
alloy as the second of its kind, of terrestrial origin, so far discovered,
under the impression that the known Nickel-Iron ‘“ Oktibbehite ”
(Ni+Fe), which is a meteorite found in Oktibbeha City, North
America*, was the first alloy of this kind of terrestrial origin ; and
he also suggested that the mineral would be found in some basic
rock in the vicinity of Barn Bay. Mr. Skey’s paper appeared in the
Transactions of the New Zealand Institute for 1885, and was
reprinted with some additions in the Annual Report, for 1885-86,
of the Colonial Museum and Laboratory, Wellington. The additions
concerned the results of Mr. Skey’s examination of other three
samples of heavy black sand: namely, no. 1, from Barn Bay, con-
tained no Awaruite; no. 2, from Callery’s Creek, contained 4°/ ;
and no, 3, from the Gorge River, 45°36 °/,.. Amongst other minerals
sent with the samples of black sand Mr. Skey mentions a hydrous
ferruginous serpentine ; and in a footnote he states “this serpeutine
proves to be the matrix of the nickel-mineral Awaruite, in which

* Wadsworth’s ‘ Lithological Studies,’ Table II, p. xiv.
Q.J.G.8. No. 184, 2x

620 PROF. G. H. F. ULRICH ON THE

it is dispersed in minute grains, in the same manner as metallic
copper occurs in serpentine in Aniseed Valley near Nelson.”

On seeing the notices about Mr. Skey’s first paper (October
1885), giving full particulars regarding discovery, composition, &c.,
of the new mineral, in the daily newspapers, and being cognisant
of the fact of Oktibbehite being a meteorite, and therefore
Awaruite not being the second (as Mr. Skey supposed), but
really the jirst nickel-iron alloy of telluric origin, a fact that
greatly heightened the scientific interest attaching to it, I at once
communicated with some friends at Hokitika and Ross on the
West Coast, and was successful in procuring, through their
agency, a small parcel of the nickeliferous sand. In order to gain
information regarding the special locality of occurrence of the alloy,
and, what was of most importance, about the nature of the rocks in
the vicinity from which it was likely to be derived, I also wrote to

Ir. Gerhard Mueller, Chief Surveyor, Hokitika, and Mr. D. Macfar-
lane, Warden of Jackson’s Bay, two men to whom before all others
belongs the credit of having by dangerous explorations procured
nearly all the reliable information we have of the topographical and
geological features of that wild part of the West Coast in which the
new mineral was found.

Mr. Mueller kindly responded by furnishing me with a copy
of the topographical plan (p. 624) of the country under notice,
which he had prepared from his surveys and explorations,
and also with his Report thereon ; while Mr. Macfarlane was good
enough to inform me that the Red-Hill mountain-complex aud the
Olivine Range, depicted on Mr. Mueller’s plan, largely consisted of
olivine-rock, which he was the first to recognize as such, and on
account of which Mr. Mueller adopted the name Olivine Range.
Regarding my request for specimens of the rocks from the locality
where the Awaruite occurs, be intimated his intention of shortly
making a journey through the district, when he would specially col-
lect for me the specimens asked for. This journey did not, however,
take place, and no further information was received until the begin-
ning of May 1886, when two of my students, Messrs. Henderson and
Batement, submitted to me a small collection of rocks and mineral
specimens which during the early part of the year they had brought
from an exploring-trip extending from the head of Lake Wakatipu
across the Dividing Range and through the Red-Hill district down
to the west coast of the Island. They had spent several weeks in
exploring the wild, inhospitable region of the Red Hill, an enterprise
ouly rendered possible through the fortunate circumstance that just
at that time a well-equipped party of gold-prospectors were camping
on the Red Hill, at a height of near 3000 ft. To one of them, Capt.
Malcolm, I am indebted for several rock-specimens mentioned further
on. The collection mentioned, owing to difficulty of carriage, consisted
mostly of chips and small pieces, amongst which varieties of peri-
dotite and serpentine claimed most attention. The several speci-
mens are more specially described in the sequel. They were obtained
in various places on the Red-Hill Range, along the red-weathered

NICKEL-IRON ALLOY AWARUITE OF NEW ZEALAND. 621

outcrop (hence the name “ Red-Hill ”) of the peridotite ; but those of
the serpentine varieties come principally from the slope of the range,
falling towards the Jerry River, a tributary of the Gorge River,
One of these latter specimens, of thin lamellar (antigorite-like) struc-
ture, was found to be impregnated with fine specks, of silvery-white
colour and metallic lustre, which on examination proved to be the
new mineral Awaruite. In most of the other serpentine specimens
whitish metallic-looking specks were also discovered, but they all
turned out to be pyrite, except in one piece of common dark green
serpentine, which yielded after crushing and washing, from amongst
a small amount of pyrite-powder, a small hackly grain of the alloy.

Up to the time of this discovery of the matrix-rock of the Awa-
ruite nothing was known or had been published about a similar
discovery by anyone elsewhere *; but in answer to a letter I wrote
to Mr. Macfarlane, pointing out the discovery and asking for any
specimens of peridotite and serpentine he might have preserved from
his previous explorations, he informed me that he had also noticed
the metallic specks and would send a number of specimens contain-
ing them. ‘These I received some months later, but found only two
specimens (dark-green serpentine) with unmistakable Awaruite in
them, the metallic specks in the remainder proving to be pyrite.
Considering the great scientific interest attaching to the discovery of
‘the mineral and its matrix combined, because of the apparent close
relationship of the occurrence to certain of the stony meteorites, and
apprehending the find in danger of being quite overlooked, from the
fact that, although made public in New Zealand nearly a year pre-
vious, no notice of it had up to that time appeared in ‘ Nature’ and
other English and foreign scientific journals of eminence, I wrote
letters to a number of distinguished authors, specially interested in
the study of the peridotite rocks in England, America, and Germany,
giving the main particulars of the occurrence of the mineral and
the results of Mr. Skey’s work. The President of the Geological
Society at that time, Professor Judd, being one amongst the number,
considered my communication of sufficient interest to be brought
before the Society, and announced at the same time my intention of
submitting a paper regarding the discovery, provided I was success-
ful in procuring more detailed information about the geology of the
country in which it was made, and more material to work upon f. In

* Mr. Skey’s footnote to his second paper in the ‘ Annual Report of the Colo-
nial Museum and Laboratory,’ quoted in the foregoing, appeared several months
after my find became known.

t In the ‘Abstract of the Proceedings’ of the Society at that Meeting,
Quart. Journ. Geol. Soe. vol. xlii. 1887, Proceed. p. 3, the credit of having dis-
covered the Awaruite is given to me, no doubt through some misunderstanding,
whilst Mr. Skey, as the analyst and namer of it, is not mentioned ; and it is further
stated that I consider Awaruite and the meteorite Oktibbehite as identical in
chemical composition. In consequence of these mistakes Sir James Hector, the
Director of the Geological Survey of New Zealand, in a letter in the March
number of ‘ Nature’ 1887, casts a suspicion of piracy upon me regarding the
discovery of the mineral, and accuses me of ignorance as to the second point,
although perfectly innocent on both these charges, as my letters to Professors

2¥ 2

622 PROF. G. H. F. ULRICH ON THE

pursuance of this project I have since written to and interviewed a
number of persons who, I thought, could aid me inthe matter. The.
results of these endeavours have not, however, I am sorry to say,
come up to my expectations, owing to loss and damage of specimens
sent to me, and various other mishaps. Thus my hope that some,
from amongst quite a little army of prospectors (about 150 men)
who, aided by the Government, landed towards the end of 1886 in
Big Bay, would collect and send specimens was quite disappointed,
as not one of the party penetrated as far inland as the Red Hill.
In fact they soon became so dissatisfied with the hard work of exploring
the rough country that they hurriedly left the district in troops, and
very soon after not one of them remained. In 1887 1 was, how-
ever, gratified in receiving from Mr. Macfarlane a larger sample of
the Awaruite-bearing sand from the Gorge River, together with
portion of a serpentine pebble of nephritic aspect, containing
small specks of Awaruite. During the same year, and again in
1888, an intrepid, enterprising prospector, Mr. Robert Paulin, with
several hired men, traversed the Red-Hill district in various direc-
tions, prospecting the rivers and creeks; and from him I received
last year, besides a few more specimens of serpentine and other rocks,
some valuable notes, accompanied by a sketch-plan of the district,
indicating the distribution of the Awaruite and the extent of the
peridotite and serpentine rocks. The several small rock-samples
so far enumerated, of which the collection brought by Messrs. Hen-
derson and Batement was the most diversified and important, have
thus been all the material available to work upon; whilst regarding
the general geological structure of the country, and more especially
the mode of occurrence and extent of the peridotite and derived
serpentine rocks, I can only give an imperfect outline, gathered
from the reports and notes received from Mr. Gerhard Mueller,
Messrs. Henderson and Batement, Mr. Macfarlane, Capt. Malcolm,
Mr. Paulin, and several other persons I met since who have traversed
the district.

2. Geology and Description of the Rocks.

Regarding the general geological structure of the country it is
reported that the ranges from near the sea-coast inland to the ice-
clad Dividing Range, except where broken through by the peridotite
and derived serpentine rocks, consist of metamorphic schists (gneiss,
mica-schist, and chlorite-schist) with occasional massive protrusions
and probably large dykes of granite and quartz-porphyry. Judging
from a few small specimens obtained from Mr. Paulin, the granite is
medium-grained and rather felspathic (felspar flesh-coloured), with
principally dark mica; whilst the gneiss and mica-schist are of
ordinary character, showing also mainly dark mica. Where the

Judd, Bonney, and others can prove. I have nevertheless considered it neces-
sary to lay before the Society the foregoing succinct statements of. facts
relating to the matter, which will afford the explanation which Sir James
Hector says the case requires.

NICKEL-IRON ALLOY AWARUITE OF NEW ZEALAND. 623

spurs from the high ranges do not directly dip steep into the ocean,
massive deposits of sandstone and shale and in some cases limestone,
of probably older Tertiary age, overlie the old rocks along the coast
to pretty high up the easy slopes of the spurs ; whilst down the main
river-valleys, mostly on both sides, descend extensive high terraces
of boulder-drift and hard conglomerates, of morainic character in
the higher parts of the valleys. In the embouchures of the rivers
there are generally bars or delta-like accumulations of more recent
drift. The prospecting of the terrace-drifts for gold and tracing
the gold to its original deposits (quartz-reefs) was the main object of
the large prospecting party previously referred to.

Coming now to the peridotite and serpentine rocks, the following
extracts are of importance. The Chief Surveyor, Mr. Gerhard
Mueller, in his report of his explorations *, states on this head as fol-
lows :—‘ The most remarkable feature about the district appears to
me to be that of the Olivine Range on the Hast of Cascade River.
It is a red and violet looking mass, and, from about 1000 ft. above
the river, devoid of almost every vestige of vegetation. It is of the
same formation of which the Cascade Plateau and a great part of the
country of the Gorge and Jerry valleys consist. The Red Hill
(5000-6000 feet) itself is olivine-rock, whilst the spurs running
therefrom are a sort of greyish slate with grey granite belts here and
there through them. An extraordinary red granite belt is seen in
the Jerry River a little above the proposed road-crossing. The
olivine formation is traceable as far as the Humboldt Mountains;
the last indication of it I saw on the Cow Saddle, from which the
Barrier and Olivine Branches (Creeks) and the Hidden-Falls Creek
rise; the extent of it there does not exceed a couple of acres, but it
is very marked and distinct.” Ina letter to me, August 1st, 1889,
Mr. R. Paulin, in explanation of his sketch-plan (p. 624), states :—
“The Red-Hill formation (olivine and serpentine) occurs all over
the parts | have marked with red lines. The Red-Hill and Olivine
Ranges are for the most part bare of timber, and the formation is
very conspicuous, owing to the burnt-brick colour which the rock
assumes where exposed to the atmosphere. Both the Olivine and
Hope Ranges are very much broken and shattered, containing no
mass of rock that has not cracks in all directions. This is not so
much the case in the Red-Hill Ranges.”

From these extracts, together with Mr. Paulin’s plan, it will
be seen that the rocks under notice compose, in the region of the
Awaruite discovery, a complex of high massive ranges, the most
prominent of which are the Red-Hill and Olivine Ranges, and
which comprise, according to Mr, Paulin’s plan, an area of about
25 miles in length north and south, and 16 miles in width east
and west. The rocks, however, doubtless extend (probably with
interruptions and for certain much contracted in width) much further
southward, even beyond the point Mr. Mueller mentions near the

* Report on West Coast between Cascade Plateau and Jackson’s River on the

North, and Lake M’Kerrow and Hollyford Valley on the South ; in the ‘ Report
of the Survey Department of N.Z. for the year 1883-84,’ p. 73,

624 PROF. G. H. F. ULRICH ON THE

Geological Sketch-plan of a Part of the West Coast of the South
Island, New Zealand, by R. Paulin; based on Mr. G. Mueller’s
Topographical Plan of the Country between Jackson’s River

and the Hollyford Valley.

AWA PN

=
oc
= 0

“> R
GRE RNR
tT
\S
i}

ll
a

{

K
MARTIN. |

Vy
desi)
C~ °- Be
3

=>

ae

i
€

-

iy)

Y

yi f;
i)

Ss,

<=
ES

t

Y)

SCALE OF MILES
2 4 6 8

v
if SS *
BSS wp faivine BME DE

°
o

Localities where Awaruite has been found.

Area of the Serpentine and Olivine Rock (Peridotite).

Ground covered by Mineral-leases for working the Nickel on the
Gorge River.

Cow Saddle. Mr. Mueller’s last indication of the Olivine Rock.

+ [ii] «

NICKEL-IRON ALLOY AWARUITE OF NEW ZEALAND. 625

Humboldt Mountains (about 64 miles 8. by W. from the junction
of the Barrier Creek with the Pyke River). What leads to this
conclusion is, that Messrs. Henderson and Batement saw con-
spicuously bare and red-coloured mountains and ridges (like those
of the Red-Hill Range) further southward, near Lake-Harris Saddle,
the watershed between the Route Burn (a tributary of the Dart
River falling into Lake Wakatipu) and the Hollyford River; and
that they found boulders of olivine rock and serpentine in one of
the creeks rising near that saddle and falling into the Hollyford
River. Still another important proof is that at the head of the
Caples River (about 22 miles 8. of the junction of Barrier Creek
and Pyke River) there occurs in massive outcrops a dark-green ser-
pentine, closely resembling that of the Red Hill and enclosing
veins and bunches of compact talc (steatite).

With regard to the geological relations of the peridotite and
serpentine rocks to the enclosing crystalline schists, there can be no
doubt, according to Messrs. Henderson’s and Batement’s observations,
that the former are intrusive through the latter; several places
having been observed by them where the strike of the schists was
right against the peridotite and serpentine outcrops.

Judging from examination of the specimens available, the unal-
tered peridotite, in its petrographic character, is always holocrystal-
line, and its main constituents (olivine and enstatite) are allotrio-
morphic. It shows, however, various modifications. On the Red
Hill it conforms toWadsworth’s species “‘saxonite,” is of light-greenish
colour, and varies from coarse to fine granular in texture. The
olivine and enstatite vary much in relative proportions; while in
some specimens the former greatly predominates over the latter,
in others the reverse is the case. This can be well seen on the red-
weathered surface of the rock, which shows the enstatite in out-
standing angular particles of irregular size and form; the olivine
once connecting them haying been decomposed and removed. Chro-
mite, though in some parts abundant, appears on the whole rather
sparingly distributed throughout the rock; partly and more fre-
quently in larger and smaller grains of irregular contours ; partly in
small perfect octohedrons. These grains and crystals are easily
identified by their lustre, together with the green colour imparted
by the powder to the borax bead. Several specimens with pre-
dominating enstatite show on the surface light to dark emerald-green
portions which do not seem to occur in the interior of the rock, as I
found on cutting two such pieces in various directions. Although
they seem at first sight to belong to a different species of pyroxene
(diallage), closer examination proves them to be so similar in lustre
and structure to the associated, common, yellowish or brownish
enstatite, that I suppose they most probably represent only a green-
coloured variety of the latter. Owing to the failure of several attempts
in preparing thin sections showing the green mineral, through the
latter unfortunately breaking away or quite disappearing during
the grinding, and not liking to destroy any more of the remaining
specimens, reserved for transmission with this paper, I have not

626 PROF, G. H. F, ULRICH ON THE

been able to test the correctness of my supposition by microscopic
examination. In thin sections both olivine and enstatite become ~
nearly or quite colourless and transparent, the former in parts with a
faint greenish, the latter more generally with a feeble brownish-yellow
tint ; and they are on the whole rather free from inclusions, chromite
and picotite excepted. In Pl. XXIV., figs. 1, 3,5, grains of greenish
olivine are indicated by the letter 0. I suspected these at first to be
the green mineral before mentioned, but their rough surfaces and high
brilliant polarization-colours unmistakably proved them to be olivine.
Between crossed Nicols the enstatite, determined by always extin-
guishing parallel to the main cleavage-cracks, shows in some grains
throughout, in others in parts, a closely and sometimes slightly-curved
fibrous structure, which may indicate its alteration into bastite*.
On looking straight through a mounted section towards the light
with the naked eye, enstatite and olivine are often indistinguishable
from each other, if both are clear and colourless; but on looking
obliquely down upon the section, whilst turning it in different direc-
tions between the fingers, the grains of enstatite are recognizable
by a peculiar brightening-up like opalescence, caused by internal
reflections. Chromite and picotite, in opaque black and brownish
translucent crystals and irregular grains, occur in moderate number
in every section. The dark-green translucent serpentine from the
Red Hill becomes, in thin sections, perfectly transparent and nearly
colourless, with scattered patches of a slightly cloudy aspect ; and it
encloses numerous black and brown opaque grains of iron-ores, some
of which on microscopic examination by reflected light generally prove
to be pyrite. Between crossed Nicols the clear substance appears as .
broken up into a confused intermixture of small granules and narrow,
longer and shorter fibrous bodies, most of which (the fibrous bodies
invariably) are anisotropic, by polarizing from bright white or yel-
lowish through ght and dark shades of greyish-blue to black, the
extinction of the latter being in the direction of the fibres. The rest
of the granules that are dark remain so on complete rotation of the
stage, thus proving to be isotropic. Irregularly outlined portions
in the sections, showing more minute granulation, no fibrous bodies,
and polarizing in parallel bands in different shades of blue and grey,
are doubtless indicative of altered enstatite, and conform to the
cloudy patches before adverted to.

It requires now finally to be mentioned concerning the Red- Hill
rocks, that, as far as Messrs. Henderson and Batement “could observe,
there exists no defined boundary between the unaltered peridotite
and the serpentine. The two rocks seemed to be quite irregularly
intermixed. Rock-masses which at a distance they took to be
peridotite proved on examination to be serpentine and vice versd, the
recognition being always easy on near approach, even without break-
ing the rock, by the rough surface of the peridotite and the smooth sur-
face of the serpentine. They came in their traverses through the
district at several places, pretty far apart, across the boundary of the
schist and peridotite rocks (including serpentine) ; and, judging from

* J.J. H. Teall’s ‘ British Petrography, p. 88.

NICKEL-IRON ALLOY AWARUITE OF NEW ZEALAND. 627

the few specimens they collected, it may fairly be concluded that per-
haps all along that boundary there occur certain gabbro-rocks, either
as irregular intrusions and dykes, or as formed by gradual transition
from the peridotite through accession of plagioclastic felspar, disap-
pearance of the olivine, and exchange of the light coloured enstatite
tor the dark ferriferous bronzite, and may be hypersthene and
diallage. Which of these suppositions is the correct one is doubtful.
Both kinds of relations between peridotites and gabbros have been
described by Professors Judd* and Bonney f from Scotland and
Cornwall respectively, and are also known from several European
districts. From the travellers’ descriptions the intrusive mode of
occurrence of the gabbro seems the more probable. At uncertain
distances away from the peridotite-boundary, within the schist-
rocks, they found dykes of augite-porphyry and felspar-porphyry,
and bosses of a peculiar rock consisting of a white felspathic base
with long, thin, prismatic crystals of a fine green colour, reminding
us of epidote or actinolite. Of this unfortunately they lost the
sample ¢.

We now come to the peridotite of the Olivine Range. Of this
there are only a few specimens available, and these present two va-
rieties very different in microscopic aspect, and also easily distinguish-
able from any of the Red-Hill rock. The variety said to be most
abundant on the range has a greenish ash-grey colour, looks very
close and dense, and consists of olivine and enstatite, the former
much predominating. Its special texture is, doubtless, owing to the
advanced degree of serpentinization it has undergone, though micro-
scopic examination of a number of thin sections, cut at various
angles from a specimen, seems to indicate that the enstatite has, in
the aggregate, suffered by this process quite as much as, if not more
than, the olivine; this is an occurrence rather at variance with what
is usually observed and with the stronger tendency of the latter
mineral to decompose by atmospheric action, as shown by its
removal from between the grains of enstatite on the surface of
these rocks. Every grain of enstatite is more or less attacked along
eracks of cleavage and cross-cracks. Some appear broken up, as it
were, into a multitude of longer and shorter columnar pieces of
varying width, occupying collectively much less space than the
serpentine between them (see Pl. XXIV. fig. 7). A small pro-
portion are wholly converted into this mineral, which, in most cases,

* Quart. Journ. Geol. Soc. vol. xli. 1885, p. 583.

+ Zoid. vol. xxxiii. 1877, p. 904, and vol. xxxiv. 1878, pp. 778, 779.

¢{ Among the specimens sent from the Red Hill are examples of varieties
of serpentine allied to picrolite, marmolite, and antigorite, with the common
dark-green type of the mineral, the latter sometimes containing specks of
Awaruite as well as of pyrite and magnetite. In small nests and veins of the
serpentine of the Red Hill the following minerals were found :—Garnets (both
of light-brown and light-green colour), quartz, a chlorite (probably ripidolite),
asbestos or mountain-leather (probably chrysotile), magnetite, and massive tale
(steatite or soapstone). From massive outcrops in the same district rock-
specimens were collected, which are referred to bronzite-gabbro, common gabbro,
augite-porphyry or melaphyre, and labradorite-porphyry.

628 PROF. G. H. F. ULRICH ON THE

is dusky, sometimes nearly opaque. With the olivine the case is
different. While in parts of the sections it is traversed by an
irregular network of veins of serpentine, in other parts, of about
similar extent, such veins are scarce, smaller, or quite absent, and
there are only noticeable scattered patches with more pronounced
cracks and of slightly impaired transparency, caused by a minute
dust or granulation, and which show mostly aggregate polarization
between crossed Nicols; the brilliancy of the polarization colours is,
however, quite unaffected. Regarding the serpentine of the veins,
it is different from that formed from the enstatite, being perfectly
transparent and nearly colourless throughout ; and its behaviour, as
well as the structure of the veins in polarized light (between crossed
Nicols with rotation of the stage), accord perfectly with the descrip-
tions given by Prof. Bonney iu his paper on the serpentine of the
Lizard district, Cornwall *, and therefore need not be detailed here.
Only I may mention that in some of the veins the arrangement of a
granular dark layer in the centre and a transversely-fibrous layer
along each side is very regular, reminding us of the symmetrically
banded structure observed in some ore-lodes; also that in parts of
some veins the fibrous bodies are more or less regularly radiating
(star-like) from dark ferruginous granules. Inclusions of grains of
chromite, &c., in the olivine and enstatite are, according to the pre-
pared sections, very scarce indeed; one pretty large section shows
not a single grain, and none of the others contain more than three
or four. The specific gravity of the rock, as determined on dif-
ferent specimeus, ranges from 2°81 to 3:13; and regarding its
solubility in HCl, some determinations by Mr. Thomas Batement
gave the following results :—

No. 1. No. 2. INO, 3:
Sn 80:08°/, 83739, 84119
Insoluble. ....- 19°92 ,, LGO?2 G45 15:89 5
100:00 100-00 100-00

The soluble portions here evidently represent olivine and serpen-
tine ; the insoluble enstatite, with a small percentage of chromite, &e.
Judging from what the sections show, the relative proportions of
olivine and enstatite in the unaltered original rock may be taken to
have been as 2: 1, or at the outside 3:1, say as 70 °/, : 30°/,; there-
fore the above results would indicate that in the present rock nearly
one-half of the enstatite has been converted into serpentine. As
already mentioned when describing the thin sections, it is rather
questionable whether the olivine has suffered to a like extent.

The second variety of rock from the Olivine Range is of medium-
grained, granitoid texture, dark greyish-green colour, and very tough.
The amount of outstanding grains of enstatite on the brown-
weathered surface of the rock points to this mineral predominating
over olivine, and this is confirmed by examination of the several

* Quart. Journ. Geol. Soc. vol. xxxiii. 1877, pp. 907 & 916.

NICKEL-IRON ALLOY AWARUITE OF NEW ZEALAND. 629

thin sections cut from a specimen at various angles. These sections
look under the microscope much like those prepared of Red-Hill
rock similarly constituted ; the only difference being a more pro-
nounced brownish-yellow colour of the enstatite and a greater
quantity of dark ore-grains (chromite &c.). In one section, how-
ever, there are seen four small, irregularly-outlined grains of a trans-
parent green mineral, which certainly is monoclinic, though whether
it be hornblende or a pyroxene optical examination leaves undecided.
Two of the grains, showing a few parallel cleavage-cracks, and
parallel to these a slightly fibrous structure, extinguish one at
an angle of about 12°, the other at about 17° with these cracks,
and are slightly pleochroic, changing from bluish green to yellowish
green ; the third grain shows only irregular cracks and hardly any
pleochroism ; but in the fourth grain, rendered rather dusky by fine
black dust, there are a few, though very indistinct, cracks, apparently
crossing each other at approximately right angles, and the extinction
makes nearly equal angles with these cracks; itis feebly pleochroic,
the green colour becoming fainter. The employment of conver-
gent polarized light gave no definite results for any of the grains.
Accepting the cracks in the fourth grain as really indicating cleavage,
the mineral is doubtless a pyroxene, and probably diallage. The
specific gravity of the rock is 3°17—-3°35, and its chemical com-
position, according to a bulk analysis by Mr. Thomas Batement, as
follows :—

SOP sriersh2 39°99
HAN Oise ated 3°50
CrOie nek Strong traces
eC Og ps2) 2: 8°56
MnO. ....traces
CaO sean 4:19
MeO.) ois < 41°26
ET ON ree 240) 2°07
99-62

Among the specimens from the Cascade River at the foot of
the Olivine Range are pieces of a hard nephrite-like serpentine
(bowenite ?), containing small specks of Awaruite embedded in it.
The specimens are evidently portions of rolled pebbles.

3. Mode of Occurrence and Distribution of the Awaruite.

The first sample of the Awaruite-bearing black sand examined by
Mr. Skey was supposed to have come from Barn Bay (p. 619); but
it was subsequently proved to have been washed from the drift of
the Gorge River. The valley of this river has since generally been
considered to be the only place of occurrence of the mineral, and is,
indeed, the one in which it has so far been proved to exist in largest
quantity. Mr.G. Mueller, the Chief Surveyor, in answer to my en-
quiries on this point, states: ‘‘ The mineral is found in the bed and

630 PROF. G. H. F. ULRICH ON THE

the banks of the Gorge River, and the ground covered by the mineral-
leases applied for with the view of working the nickel is marked in
red on the lithograph-plan enclosed [see the indication on the
sketch-plan, p. 624]. These deposits have evidently been brought
across the saddle into the Gorge River from the Olivine Range
at the back of it.”

As, in consideration of the large extent of the peridotite or serpen-
tine rocks, it seemed to me very unlikely that the occurrence of the
mineral should be confined to the Gorge River only, I specially
requested Mr. R. Paulin, before he set out on his exploring and
prospecting trip, to look out for the alloy in the olivine and serpentine
rocks and the drift of the rivers and creeks he prospected. The
results of his examinations in this respect are given on the sketch-
plan previously alluded to (p. 624),—the many places where he found
Awaruite being marked by black crosses. In his explanatory letter
to me he states as follows :—‘I have found small specks of nickel
in the rocks of various localities, most conspicuous at Silver Creek
(a tributary of the Jerry River rising in the Red-Hill Range), and I
think that it occurs throughout the whole formation. The free
nickel found in different river-beds is much coarser than any I
have seen in the stone. On the Red Hill itself 1 found nickel
2400 feet above sea-level.”” The area of distribution of the Awaruite
is thus by Mr. Paulin’s observations proved to be far more extensive
than first imagined, and it may be larger still, for I see nothing
unreasonable in his belief that the mineral occurs in the impreg-
nated matrix throughout the whole extent of the peridotite and ser-
pentine rocks ; and, inferentially, in the liberated state in the drifts
derived therefrom. The gradual gathering of practical proof of this,
however, will, I fear, take a long time, owing to the great hardships
and dangers connected with prospecting in that wild, inhospitable
district. The supposed recognition of Awaruite distributed through
the rock will also, in many cases, not be free from doubt, unless the
specks be detached and specially tested. This is on account of the
smallness of the specks, and their frequent association with, and
general resemblance in colour to, grains of pyrite, which may there-
fore be easily mistaken for it. The simplest test in the case of de-
tached specks is by application of the magnet, which energetically
attracts the Awaruite specks, but leaves those of pyrite unaffected.
The malleability of the specks affords another proof of their identity.

EXPLANATION OF PLATE XXIV.

Figs. 1, 2, 3, are drawn in ordinary light from thin slides cut in different direc-
tions froma piece of medium-grained Peridotite from the Red Hill;
magnified 20 diams.

Fig. 1. In this both the Olivine and Enstatite are remarkably clear, and the latter
is only distinguishable from the former by a faint brownish-yellow tint
and parallel cleavage-cracks. The large cross-shaped grain in centre
of the figure is Enstatite, showing between crossed Nicols in patches
a slightly curved fibrous structure with wavy extinction parallel to the
fibres. Polarization-colours yellow, orange to brown. At lower right-

NICKEL-IRON ALLOY AWARUITE OF NEW ZEALAND. 631

hand corner of centre bar of cross is seen in convergent polarized light
a fine optic axis with p< v. Above the cross-shaped grain, sepa-
rated from it by a narrow band of Olivine, there is another grain of
Hnstatite showing a number of well-marked cleavage-cracks. In
several parts of the Olivine are seen in convergent. polarized light fine
optic axes, and two light yellowish-green grains of it, near the centre
of the figure, adjoining the Enstatite, are indicated by a line and the
letter o.

Fig. 2. In this the Olivine is, if anything, clearer and less cracked than in fig. 1.
There is only one grain of Enstatite shown in upper part of the figure,
recognizable by its numerous parallel cleavage-cracks, in the line of
which it extinguishes between crossed Nicols. The large irregularly-
contoured black grain and several far smaller black grains near it are
feebly brown, translucent, and consist either of Picotite or Chromite,
probably the former.

Fig. 3. This shows two grains of Enstatite divided near centre of the figure by
fine-granular Olivine, full of minute black opaque and dark brown
trauslucent particles of either Picotite or Chromite. The largest grain of
Enstatite is very clear, and shows only a few cleavage-cracks; at the
margin of the figure it becomes slightly dusky. The other grain of
Enstatite on the left shows both prismatic and brachy-pinacoidal
cleavage-cracks, and is therefore a basal section, disclosing in conver-
gent polarized light between crossed Nicols a pretty perfect interference-
figure ; at the upper end it is broken into by a grain of Olivine. The
green-coloured grain (0) below the last-noted Enstatite-grain is Olivine,
like those in fig. 1, characterized by a rough surface and the same
range of brilliant polarization-colours as the neighbouring colourless
Olivine. The two black opaque grains at bottom of the figure are
probably Chromite.

Figs. 4, 5, & 6 are drawn in ordinary light from sections cut in different direc-
tions from a piece of medium-grained, though rather dull and com-
pact-looking Peridotite from the Red Hill. Magnified 20 diams.

Fig. 4. In this are shown two grains of Enstatite, a large one in the upper
part, and a smail triangular one at the lower margin. Both these
grains are more or less fibrous, and show streaks parallel to fibres
densely filled with a fine, dark dust, probably the commencement of
serpentinization. The Olivine is in parts very clear and not much
cracked; but in others it is slightly (on the right-hand edge of the
figure very densely) filled with fine, dark dust, asin the case of the En-
statite. The large black grain within the Olivine is quite opaque, and
probably consists of Chromite.

Fig. 5. This shows on the left side a large grain of Enstatite, very clear and
with well-pronounced cleavage-cracks. On the right-hand edge there
is a smaller grain of this mineral, also clear, showing faint cleavage-
cracks ; and across the middle a row of small, feebly brown, translucent
grains of probably Picotite. In the centre of the figure, and in contact .
with the large grain of Enstatite, there are grains of light yellowish-
green Olivine, similarly characterized as the grains in figs. 1 & 3. The
Olivine (0, 0) in the lower part of the figure is very clear, but that in
upper part is dusky and more fissured. The large irregularly-shaped
black grain is in parts faintly brown translucent, the small adjoining
one is quite opaque; they probably consist respectively of Picotite and
Chromite.

Fig. 6. This shows the grains of Enstatite, one on the lower right-hand edge,
the other on the left-hand edge. Both are rather fibrous, and in the
lower one a dusty streak (similar to those in fig. 4) runs in the line of
the fibres ; in the other grain such a streak runs across the fibres, and
there are also dusty patches and several strong dark irregular cracks.
The Olivine between these Enstatite grains is also in parts more or less
dimmed by dark dust. The black grains are opaque and probably
Chromite.

632 ON THE NICKEL-IRON ALLOY AWARUITE OF NEW ZEALAND.

Figs. 7, 8,9 are drawn from sections cut at nearly right angles to each other
from a specimen of the Peridotite described as the first variety from
the Olivine Range. Magnified 20 diams.

Fig. 7 represents portion of a large Enstatite grain, broken up more or less
parallel to the chief cleavage, and converted in this direction for more
than half its original bulk into Serpentine. The remaining columnar
Enstatite portions polarize in light yellow to orange, and extinguish
between crossed Nicols parallel to their longitudinal extent. They are
much broken transversely in various directions. The Serpentine
between is more or less densely charged with a fine, dark dust, with
occasional larger dark particles, probably Magnetite. Under a high
power (700) the dust is seen to be arranged streak-like, parallel to the
columnar Enstatite portions.

Fig. 8. The large grain of Enstatite in the upper part of the figure is for the
greater part closely fibrous (well seen between crossed Nicols) and
densely filled with fine, dark dust. Portions polarize like the Serpen-
tine in fig. 7. Small veins and a larger patch of colourless transparent
Serpentine are seen in it near the upper left-hand margin. The Olivine
below the Enstatite is much fissured, and in parts more or less densely
filled with fine, dark dust. Near the left-hand margin it is traversed
by a large vein of clear colourless transparent Serpentine; and small
patches and interrupted veins of such Serpentine are shown in the
centre and close to the right- and left-hand edges of the figure. The
large vein shows between crossed Nicols a dark, fine-granular layer in
the centre, and transversely fibrous layers on each side.

Fig. 9. In this the Olivine is much fractured, and in parts densely filled with
dark dust, and traversed by strong serpentinous cracks,which in ordinary
light and between crossed Nicols are nearly opaque. The Enstatite
grains—one shown at the upper edge, one in the centre, and a large
one in the lower part of the figure—are closely fibrous, and traversed
by irregular veins of dusky Serpentine. In the central grain oblong
patches of dusky Serpentine appear also in the line of the fibres.

Discussion.

The PresipEenr noted the interest attaching to the gradual deve-
lopment of our knowledge of native iron of terrestrial origin.

Prof. Jupp was glad to have the present opportunity of removing
a misconception that had arisen concerning this mineral. In bringing
the matter before the Society on a previous occasion he dwelt upon
the facts of special geological interest, and Mr. Skey’s name was not
mentioned in the few lines placed on record in the ‘ Proceedings.’
No attempt, however, had been made by Prof. Ulrich to claim the
discovery of this mineral, though he appeared to have been the first
to record its peculiar occurrence in the ultrabasic rocks. In the
South Island were the well-known chromite-bearing olivine rocks of
the Dun Mountain, but the rock now described was in a distant part
of the same island. An interesting series of serpentines derived
from peridotites had been sent over by the Author, and these speci-
mens contained the ‘ Awaruite.” A number of garnets and chlorites,
with chrysotile, talc, and magnetite, had been found in the Red Hill.
He was not aware that any “ Awaruite ” had been discovered in the
peridotite; but this was probably due to the softer nature of the
serpentine, where it could be more easily detected. He had recently
heard that one of the serpentines of Norway had yielded a similar
alloy.

GENERAL INDEX

THE QUARTERLY JOURNAL

AND

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

[The Fossils referred to are described ; and those of which the names are printed
in italics are also figured. |

Atchmina Byrnesi, 3, 12; spinosa, 3,
ie

Africa, South, a new Labyrinthodont
from, 291.

Ailurus anglicus, 451 ; fulvens, 452.

Alloy of nickel and iron from New
Zealand, 619.

Almonte, trunk-like concretion from,
609.

Alp Vitgira, schists of the, 214, 217,
235; section on, 217.

Alps, Professors Heim and Bonney on
the crystalline rocks of the, 236-
238.

Altered rocks near New Galloway,
569.

America, the Great Lakes of North,
5238, 524.

Amphibole-andesites, 349, 358.

Andermatt, Jurassic rocks of, 191,
222; section at, 191.

Andesites of South Devon, 76; of
the Western Isles of Scotland,
358, 3861, 378.

Anniversary Address of the President,
Proc. 43-110. See also Blanford,
Dr. W. T.

Anticosti, Ostracoda from, 545, 546.

Aplite veins, 577.

Ardnamurchan, section of Ben Hiant
in, 375.

Arenicolites, 612.

Aristophycus, 615.

Armenia, catastrophe of Kantzorik in,
32.

Arthrichnites, 596.

Ascot, gravels at, 560.

Ashprington Volcanic series, 493, 504.

Astropolithon Hindii, 604, 606.

Augite-andesites of the Western Isles,
361, 371, 377. }

Augite-diorites of the Western Isles,
365.

Awards of Medals and Funds, Proc.
34-42.

Awaruite of New Zealand, Prof. G. H.
F, Ulrich on, 619.

Bacton Cliff, section at, 104.

Bagshot Gravels, Dr. A. Irving on the,
557.

Bairdia anticostiensis, 548.

Barlow-Jameson Fund, award from
the, to Mr. W. Jerome Harrison,
Proc. 42.

Basal Cambrian Rocks of the Long-
mynd, Prof. Blake on the, 386.

Basins of the Great Lakes of America,
Dr. Spencer on the, 523.

Bather, Mr. F. A., on Herpetocrinus,
POE

Bearwood, gravels at, 560.

Belemnite-slates of Scopi, 223.

Ben Hiant, map of, 374; section of,
379.

Bentley Priory, section near, 166.

Berkshire, gravels of Hast, 557; the
Southern Drift in, 156; the Wes-
tleton Beds in, 141.

Berry Park, Devonian rocks at, 502.

634

Beyrichia equilatera, 4, 18, 28, 552;
Buchiana (?), 4, 16; ciliata, 4, 19;
Clarkei, 4,17; devonica, 586; dif-
fissa, 546; granulata, 4,15; Guil-
lieri, 554; Halli, 4, 15; Hamil-
tonensis, 4,19; Kledeni, var., 538;
Kolmodini, 538; oculifera, 4, 21;
oculina, 4, 16; parasitica, 4, 16;
reticulata, 5389; sp., 553; subquad-
rata, 537; trisulcata, 4, 14; tuber-
culata, and var. Bronni and pustu-
losa, 582; tuberculata, var. pustu-
losa, 4, 18, 28.

Bibliography of the Cretaceous Poly-
zoa. 458.

Bilobites, 595, 599.

Blake, Prof. J. F.,on the Monian and
Basal Cambrian Rocks of Shrop-
shire, 386.

Blanford, Dr. W. T. (President),
Address on handing the Wollaston
Medal to Prof. Judd for transmis-
sion to Prof. W. Crawford William-
son, Proc. 34; Address on pre-
senting the Murchison Medal to
Prof. E. Hull, Proc. 35; Address
on presenting the Lyell Medal to
Prof. T. Rupert Jones, Proc. 37;
Address on presenting the balance
of the Wollaston Donation Fund
to Mr. W. A. E. Ussher, Proce. 3 ;
Address on presenting the Balance
of the Murchison Donation Fund
to Mr. HE. Wethered, Proc. 40;
Address on presenting the Balance
of the Lyell Donation Fund to
Mr. C. Davies Sherborn, Proc. 41 ;
Address on presenting the Award
from the Barlow-Jameson Fund to
Mr. W. Jerome Harrison, Proc.
42 :—Anniversary Address, Feb. 21,
1890: Obituary Notices of Deceased
Fellows: —Archdeacon B. Philpot,
Proc. 43; Mr. Robert Damon, Proce.
43; Mr. J. F. Latrobe Bateman,
Proc.44; Mr. Henry William Bris-
tow, Proc. 44; Dr. John Percy,
Proc. 45: Rev. J. EH. Tenison-
Woods, Proc. 48; Mr. Daniel Adam-
son, Proc. 49; Dr. Heinrich von
Dechen, Proc. 49; Prof. Friedrich
August von Quenstedt, Proc. 51;
Prof. Luigi Bellardi, Proc. 52; Prof.
Leo Lesquereux, Proc. 53; Dr.
Melchior Neumayr, Proc. 54; Mr.
Thomas H. Cockburn-Hood, Proc.
56; and Mr. James Radcliffe, Proc.
56. Address on some new Geolo-
gical works; the discovery of Coal
near Dover; and the permanence
of Ocean-basins, Proc. 56,

GENERAL INDEX.

Bollia bilobata, 540; Hindei, 540;
lata, 3, 12; semilunata, 548; (?)sp.,
540; symmetrica, 3, 12.

Bonney, Dr. T. G., and Dr. A. Heim,
on the Crystalline rocks of the Alps,
236-238.

Bonney, Dr. T. G., on the Crystalline
Schists, and their Relation to the
Mesozoic Rocks in the Lepontine —
Alps, 187.

Borings, Valleys revealed by, 527.

Borrowdale, the plumbago of, Proc.
124.

Braintree, section at, 133.

Branching Tracks, 613.

Brandeston, section at, 125.

Breccias and Conglomerates of South
Devon, 69, Proce. 120.

Brentwood, Preglacial Gravels of, 162.

Brentwood Common, section at, 164.

Beene Beyrichia Guilliert from,

4.

Broadmoor, gravels at, 560.

Browne, Mr. R. M., as to certain
“‘Uhanges of Level” along the shores
on the western side of Italy, Proc.
Loe:

Bryozoa, Mr. A. W. Waters on North-
Italian, Proc. 123.

Buckhurst Hill, gravels at, 560.

Buckinghamshire, the Westleton Beds
in South, 139.

Buckman, Mr. 8. 8., on the so-called
: Upper-Lias Clay ” of Down Cliffs,

18

Bure-valley Beds, 89, 91, 95.

Bure-valley Crag, 92, 110, 112.

Buried Valleys revealed by Borings,
527.

Burrows, tracks, and other markings
in Palzeozoie Rocks, Sir J. W. Daw-
son on, 595.

Buthotrephis Grantii, 613, 614.

Bythocypris (?) Lindstremi, 548; (?)
obtusa, 549.

Caerbwdy Valley, Pebidian in, 244.

Cesar’s Camp, Aldershot, 559, 560;
Easthampstead, 560.

Caleareous Grit, siliceous
from the, 54.

Calceolen-Kalk, 491; Schiefer, 49].

Cale-mica Schist, 228.

California,.-composite spherulites in
Obsidian from, 423.

Camberiey, gravels at, 560.

Cambrian and Pebidian, 248, 253 ;
Cambrian conglomerate at St.
David’s, 243, 252; overlap, 259;
Rocks of Shropshire, Prof. Blake on
the Basal, 386.

sponges

GENERAL INDEX.

Cam, channel of Drift in the valley of
the, 333, 338.

Canada, Devonian and Silurian Ostra-
coda from, 554, 545, 551.

Carboniferous Cyphaspts, a new, 421;
of Scotland, a Labyrinthodont man-
dible from the, 282; volitic lime-
stones, 271.

Cardington, section at, 412.

Carnassial teeth of Hyena striata, 63.

Catastrophe of Kantzorik, Armenia,
32.

Caversham, gravels at, 584.

Ceriopora, genus, 480; micropora (?),
480.

“Changes of level” in Italy, Proc,
122),

Chanter's Seat, grit beds at, 266.

Charlton Lane, section in, 409.

Charvil Hill, gravels at, 590.

Chenaillet Ridge and Valley of Mont
Genevre, 299, 304.

Chiastolite-mica-schists, 577.

Chideock Hill, strata of, 519.

Chloéphycus, 616.

Chobham Ridges, 560.

Chudleigh limestone, 507, 511.

Church Stretton, section near, 409.

Cimoliosaurus portlandicus, 47 ; dorsal
vertebra of, from the Purbeck of
Beds of Portland, 48.

Clacton, section near, 129.

Climactichnites, 600.

Coccodus armatus, 567; Lindstremi,
565, 567.

Cockington Beds, fossils from the,
489, 516.

Coignou, Miss C., on a new species of
Cyphaspis from the Carboniferous
Rocks of Yorkshire, 421.

Cole, Mr. G. A. J.,and Mr. J. W.
Gregory, on the Variolitic Rocks of
Mont Genévre, 295.

Collieries in Derbyshire, Wash-out in,
Proe. 1.

Composition of the propylites, 349.

Concretion, trunk-like, 609.

Conglomerate, Cambrian, at St. David’s,
243, 252.

Conglomerates and Breccias of South
Devon, 69, Proc. 120.

Contact-Alteration near New Gallo-
way, Miss M. I. Gardiner on, 599.

Contact-Metamorphism as producing
propylites, 370.

Corallian formation, siliceous sponge
from the, 59.

Coralline Oolite near Weymouth,
Girvanella in the, 277.

Corniferous Chert, Ostracoda from
the, 534, 535, 536.

Q, J. G. 8. No. 184.

635

Corpi, F. M., on the Catastrophe of
Kantzorik, Armenia, 32. ;
Course of the Valley of Smitham
Bottom, restored, 172.

Covehithe Cliff, section in, 99.

Crocodilian Jaws from the Oxford
Clay, Mr. R. Lydekker on, 284,
285.

Crossochorda, 596.

Cruziana, 9596 ;
similis, 599.

Crystalline rocks of the Alps, Profes-
sors Heim and Bonney on the, 238,
238 ; schists of the Lepontine Alps,
Prof. Bouney on the, 187.

Ctenichnites, 617.

Culm-measures, 492.

Cupola in Mull,-355.

Cyphaspides, structure of some, 422.

Cyphasphis acanthina, 422; Cerberus,
422; coronata, 422 ; Davidsoni, 422 ;
megelops, 422.

Cypridinen-Schiefer, 493, 512, 513,
514.

semiplicata, 599 ;

Daddyhole Knol), fossils from, 501,
515.

Dallas, Mr. W.S., Resolution of the
Council respecting the Death of,
Proc. 121.

Darent Valley, section of the, 170.

Dartington limestones, 502.

Dartmoor, period of the elevation of,

Il

Davis, Mr. J. W., on a new species of
Coccodus (C. Lindstremi), 5665.

Dawson, Sir J. W., on Burrows and
Tracks of Invertebrate Animals in
Palzxozoic Rocks, and other Mark-
ings, 295.

Deep Channel of Drift in Essex, Mr.
W. Whitaker on a, 333, 338.

Deformation of the Lake Region, 529.

Delesserites, 614.

Dendrophycus, 615.

Denudation of the Weald, 84.

Devon. some raised beaches of, 438,

Devon, South, Devonian Rocks and
Fossils of, 487; Triassic Breccias
and Conglomerates of, 69, Proc. 120,

Devonian Ostracoda from Lake Erie,
N.Y., 5384, 535; from Clarke Co.,
Indiana, 534, 535 ; from the Corni-
ferous Chert of Ontario Co., N.Y.,
584, 585; from Thedford, Ontario,
Canada, 534, 535, 542.

Devonian Rocks, Lower, 495, 494;
Middle, 493, 499, 501, 503; of
South Devon, Mr. W. A. E. Ussher
on the, 487; Upper, 493, 503, 506.

Diagram of the lines of Elevation

22

636

bounding the Tertiary Basin of the
Thames, 178.

Diagrain-section across Lake Ritom,
200; across St. David’s Promontory,
257; across the Gorge of the
Thames through the Escarpment of
the Chalk at Goring, 149; from Pian
Alto across the summit of Fongio,
208 ; from the Gorge of the Thames
at Goring to the Oolitic hills near
Oxford, 151; of the Valley of the
Lea at Ware, 150; on Alp Vitgira,
217; on the west flank of Scopi, 215.

Diastopora foecunda, 476; genus, 474;
hunstantonensis, & var. A, 475;
Jessoni, 478; papillosa (?), 477;
radians (?), 477; regularis, 476.

Dictuolites Beckii, 615.

Dimetian and Pebidian, 263.
Dinosaurian horn-like bone or horn-
core (?), from the Wealden, 185.
Dinosaurs, small Sauropodous, from
the Wealden, 182; of the Wealden,

36.

Diorites of the Western Isles of
Scotland, 358, 360, 361.

Diplichnites, 596.

Diorites of the Western Isles, 358,
360, 361,

Dislocated strata of N.W. Germany,
Proc. 116.

Disthene schist, 227.

Down Cliffs, near Seatown, strata of
the, 518, 519.

Drainage, lines of, in 8.E. England,
176.

Drift, deep channel of, in Essex, 338,
338.

Dumb Fault or Wash-out in Derby-
shire, Proc. 1.

Dundas, Canada, Ostracoda from, 545,
550

Durance, Variolite of the, 295.

Dykes, Pebidian felsitic, 260; volcanic
of Mont Genévre, 306.

Earley, gravels at, 590.

Easthampstead, section near, 161.

Edgebarrow, gravels at, 560,

Fifelian slates, 493, 499, 560.

Eighteen-mile Creek, Lake Erie, N. Y.,
Ostracoda from, 28, 534, 535.

Elevation, lines of, in the South-east of
England, 176, 178; of the Weald,
84, 155.

Entelophora (?), 479.

Entomis gyrata, 514; rhomboidea, 38,
10; serratostriata, 514.

Entomis-Slates, 493, 512, 513, 514.

Entomostraca, range of some Palzxo-
zoic, 2.

GENERAL INDEX.

Hrie Basin, 525.

Eryops Owenii from South Africa,
293. ;

Escarpments of the Chalk and Oolite,
relative age of, 150. |

Essex, deep channel of Drift in, 338,
338 ; the Westleton Beds in, 128.

Eurychilina, genus, 538; reticulata,
539.

Eurycormus grandis, Proc. 8.

Exton, H., on the Witwatersrand
Gold-field, Proc. 3.

Fault at Ogof Goch, 257, 258.

Felsites of South Devon, 73, 81.

Felsitic dykes, Pebidian, 260. :

Felspathic traps of South Devon, 81.

Finchhampstead Ridges, 560.

Fish fossil, from Lebanon, 565.

Fish-remains, some Jurassic, Proc. 8.

Flint Implements, 584, 587.

Fongio, section near the summit of,
208.

Forest-bed series, 95, 103-111, 114.

Fossils of South Devon, 495-514.

Fox Hills, gravel of the, 560.

Frena, 596.

France, Beyrichia Guilliert from, 554.

Frimley Ridges, 560.

Gabbro and serpentines of Mont
Genévre, 302.

Gardiner, Miss M. I., Contact-Altera-
tion near New Galloway, 569.

Gastaldi, Prof., his views on the
Geology of Mont Genévre, 320,
321.

Genesis of the Thames, 155.

Geology of part of the South Island,
New Zealand, 622.

Germany, disturbed rocks of North-
western, Proc. 1.

Gimont Valley of Mont Genévre, 301.

Girvanella Ducii, 272, 274, 280;
zncrustans, 273, 280; wncrustans,
var. Lucti, 280; in Oolitic Rocks,
270; intermedia, 278, 281; minuta,
280 ; pisolitica, 274, 276.

Glacial and Post-glacial denudation,
measures of, 150.

Glaciation in Kashmir, 66; in the
gravels, evidence of, 561; of North
America, 529.

Gloucestershire, Carboniferous Oolitic
limestones of, 271 ; Jurassic Oolites
of, 274.

Gold-field of Witwatersrand, Proc. 3.

Gondran Valley of Mont Genévre,
299, 301.

Goniatite Limestone, 493, 506, 507,
508, 511, 515.

GENERAL INDEX,

Gorge River, Awaruite from the, 622,
630.

Goring, gorge of the Thames at, 148,
251; section near, 140, 149.

Granite near New Galloway 569.

Granites of South Devon, 72, 81.

Graphite of Borrowdale, Proc. 124.

Gravels at and near Reading, Mr. O.
A. Shrubsole on the, 582; north ot
the Thames, 582; of East Berks
and West Surrey, D. A. Irving on
the, 557; south of the Thames, 585,

Great Lakes, map of the, 524.

Great Oolite, oolitic structure in the,
278.

Gregory, Mr. J. W., and Mr. G. A. J.

Cole on the Variolitic rocks of
Mont Genévre, 285.

Gresley, Mr. W. 8S. Evidence fur-
nished by the Quaternary Glacial-
Epoch Morainic Deposits of
Pennsylvania, U.S.A., for a similar
mode of formation of the Permian
Breccias of Leicestershire and South
Derbyshire, Proc. 114.

Grits, altered, near New Galloway,
573, 576.

Gyrichnites, 597, 599.

Haldon Hills, Devonian Rocks near
the, 490.

Hampshire, the Southern Dritt in,
156; the Westleton Beds in, 148.
Harrison, Mr. W. Jerome, award from

the Barlow-Jameson Fund to, Proc.

42.

Hatfield, section at, 138.

Heights of the Plateau-gravels of
Berks and Surrey, 560.

Heim, Prof., and Prof. Bonney, their
views as to the crystalline rocks of
the Alps, 236-238.

Hendy, J. C. B., on a Dumb Fault or
Wash-out in the Pleasley and
Teversall Collieries, Derbyshire and
Nottinghamshire, Proc. 1, 432. °

Henley Road, gravels at, 584.

Herpetocrinus, Mr. F. A. Bather on,
Proc. 5,

Hertfordshire, the Westleton Beds in,
137.

Heteropora (?), 480.

Highweek, fossils at, 514.

Himalayas, glaciation in the, 66.

Hinde, Dr. G. J., on a new genus of
Siliceous Sponges from the Lower
Caleareous Grit of Yorkshire, 54;
On specimens and microscopic
sections of Radiolarian Chert frova
the Ordovician Strata (Llandeilo-
Caradoc) of the Southern Uplands

637

of Scotland, Proc. 111 ; on the Cor-
niferous Chert, 536.

Hippothoa simplex, 486.

Hook-wood gravels, 560.

Hope’s Nose, fossils from the lime-
stone of, 500; raised beaches of, 438.

Horderley Inlier, section of the, 392.

Hornblende-Andesites of the Western
Tsles, 349, 358.

Horn-core (?) or horn-like bone of a
Dinosaur, 185.

Hot-Springs, Spherulites in Obsidian
from, 423.

Hull, Prof. E., award of sthe
Murchison Medal to, Proc. 85.

Human Skull from the Manchester
Ship-canal, Proc. 112.

Hunstanton, Polyzoa of the Red
Chalk of, 454.

Huntingdonshire, Mr. R. Lydekker on
some Ornithosaurian remains from,
429,

Huron Basin, 526.

Hyena in the Tertiary of the Val
d’Arno, 62.

Hyena striata, carnassial teeth of,
from the Val d’Arno, 63.

Hypsocormus Leedsii, Proc. 8; tenui-
rostris, Proc. 8.

Igneous constituents of the Breccias
and Conglomerates of South Devon,
69.

Iguanodon, bernissartensis, ilium of,
37; cervical vertebra of an, from
Hastings, 44; Dawsoni, 37, 38;
Fittoni, 38 ; ilium of, 387 ; hollingtoni-
ensis, femur of, 41; ilium of, 37;
left ilia of, 87; Mantelli, ilium of,
oT.

Tguanodonts of the Wadhurst Clay,
36

Imosthay Quarry, Portland, 279.

Indiana, Ostracoda from, 534, 535.

Inferior Oolite, upper beds of the,
519,

Invertebrate animals, burrows and
tracks of, 595.

Ipswich, section near, 127.

ne Palzxozoie Ostracode from, 1,

8.

Irving, Dr. A., Note on the Plateau-
gravels of Hast Berks. and West
Surrey; their Age, Composition,
and Structure, 557.

Isle of Wight, Dinosaurian Horn-core
(?) from the, 185.

Isochilina cristata, 4,23; (?) fabacea,
4, 22; gregaria, 4, 22; lineata, 4,
21; ottawa, var., 551, 553; Sceelyi,
4, 22; (?) sp., 4, 28.

638

Italy “changes of level ” on the shores
of Western, Proc. 122.

Jhelam Valley, Glaciation in the, 66.

Johannesburg, Gold-field near, Proc. 3.

Jones, Prof. T. Rupert, award of the
Lyell Medal to, Proc. 37; on
Palzxozoic Ostracoda from North
America, Wales, and Ireland, 1; on
some Devonian and Silurian Ostra-
coda from North America, France,
and the Bosphorus, 534.

Judd, Prof. J. W., on the Propylites
of the Western Isles of Scotland,
and their Relations to the Andesites
and Diorites of the District, 341.

Junction of Grits and Granite near
New Galloway, 576; of Slate and
Grit near Narnell’s Rock, 395.

Jurassic and Crystalline Rocks near
Andermatt, 191, 222; Fish-remains,
some British, Proc. 8; Oolites of
Gloucestershire, 274; rocks con-
taining fossils and minerals, 213.

Kantzorik, Catastrophe of, 32.

Karoo beds, a new Labyrinthodont
from the, 291.

Kashmir, glaciation in, 66.

Kennet Mouth, gravels at the, 590.

Kent, the Southern Drift in, 156; the
Westleton Beds in, 148.

Kessingland Cliff, section at, 101.

Kingsteignton, Devonian Rocks near,
490, 507.

Kledenia notata, 3, 138; var. ventri-
cosa, 3, 14.

Knocknairling Burn, 569; hill, 569;
altered rocks on, 572.

Knollen-Kalk, 492, 509.

Konen, Prof. A. von, on the Disturbed
Rocks of North-western Germany,
Proc. 116.

Labradorite-andesites, 364.

Labyrinthodonts, Mr. R. Lydekker on
two new species of, 289.

Laccolites in the Western Isles, 356.

Lake Hrie, 525 ; Huron, 526 ; Michi-
gan, 526; Ontario, 525.

Lakes, the Great, of America, 523.

Laurentian Valley, Map of the
Ancient, 524.

Lea Valley, section across the, 150.

Lebanon, fossil fish from, 565.

Leiston Common, section at, 124.

Lenham Sands, the, 168 ; section near,
168.

Leperditia alta, 5, 25, 28; Claypolei,
5, 25; frontalis, 547; hudsonica, 4,
24; Jonesi, 5,25, 28; nana (?), 5,

GENERAL INDEX.

27; (?) seneca, 4,23; (?) stnwata,
4,23; sp., 553, :

Lepontine Alps, the Crystalline Schists
of the, 187

Licrophycus, 613.

Limulus, marks made by, 601.

Lincombe Hill, fossils from, 495.

List of the Mollusca of the Southwold
and the Bure-Valley Beds, 93;
Weybourn Crag, 111; Organic Re-
mains of the Westleton and Mun-
desley Beds, 115-117.

Lists of local Devonian Fossils, 495-
514; of Paleozoic Ostracoda from
North America and elsewhere, 3,
535, 545, 550.

Littlebury, Essex, deep channel of
Drift at, 336.

Livaton, fossils near, 514.

Long Down, gravelsat, 560.

Longmynd Hills, stratigraphy of the,
386, 888, 404, £16; Massif, west-
ern part of the, 397, 402; sections
of the, 392.

Lory, Professor, his views on the
geology of Mont Genevre, 320.

Lukmanier Pass, the, 214, 222, 232.

Lummaton limestone, 503.

Lutra dubia, 444; Reevei, 446.

Lydekker, Mr. R., on a Crocodilian
Jaw from the Oxford Ciay of Peter-
borough, 284; on a peculiar horn-
like Dinosaurian bone from the
Wealden, 185; on Ornithosaurian
Remains from the Oxford Clay of
Northampton [Huntingdonshire],
429; on Remains of small Sauropod-
ous J)inosaurs from the Wealden,
182; onthe Dinosaurs of the Weal-
den and the Sauropterygians of the
Purbeck and the Oxford Clay, 36;
on the occurrence of the Striped
Hyena in the Tertiary of the Val
d’ Arno, 62; on two new species of
Labyrinthodonts, 289.

Lyell Geological Fund, award of the,
to Mr. C. Davies Sherborn, Proce.
41; Medal, Award of the, to Prof.
T. Rupert Jones, Proc. 37.

Macrocypris (?) subcylindrica, 549.

Macromerium scoticum, 291,

Main reef of the Witwatersand Gold-
field, Proc. 3.

Mammalia of the Westleton and Mun-
desley Beds, 117.

Mammals from the Red and Norwich
Crag, Mr. E. T. Newton on some
new, 444.

Mandibles and teeth of Suchodus duro-
brivensis, 285.

GENERAL INDEX.

Map of a part of the South Island of
New Zealand, 624; Littlebury, with
the sites of wells, 336; Mont Gené-
vre, 3800; by Professor Lory, part
of, 8322; by Zaccagna and Mattirolo,
part of, 322; Distribution of the
Devonian Rocks between the River
Teign and the Haldon Hills, 490 ;
Distribution of the Devonian Rocks
west of Torquay, 490; district from
Charlton Hill to Wellington, 410;
Drainage of the Ancient Laurentian
Valley, 524; Great Lakes of Ame-
rica, 924; Knocknairling Hill and
Burn near New Galloway, 571.

Mark’s Tey, section near, 132.

Mattirolo, M., & M. Zaccagna, their
views on the Geology of Mont
Genévre, 321.

Meadfoot Beds, fossils from the, 495.

‘Medals, Awards of, Proc. 34-38.

Megalosaurus Dunkeri, metatarsals of,
46; metatarsus of a, from the
Wadhurst Olay, 45.

Membranipora elliptica (?), 485; fra-
gilis, 485; gaultina, 484; genus,
484; obliqua (?), 485.

Merstham, section above, 173.

Mesoplodon floris, 448; scaphoides,
450.

Mesozoic rocks of Lepontine Alps,
137, 191, 222, 232.

Metamorphosed rocks near New Gal-
loway, 569.

Metriorhynchus Moreli, mandible of,
285.

Mica-Andesites, 358, 360.

Michigan, Lake, 526.

Microscopic sections of peridotite,
630-632.

Microscopic structure of the altered
rocks near New Galloway, 572, 580;
of the Jurassic Rocks of the Lepon-
tine Alps, 232; of the Rauchwacké,
230; of Rocks from the South
Island, New Zealand, 625; of the
Schists of Val Piora, 224, 229.

Microscopical characters of the Scot-
tish Propylites, 350.

Middlesex, the Westleton Beds in,
136.

Mollusca of the Bure-Valley Beds,
93; Southwold Beds, 93; Westle-
ton and Mundesley Beds, 113, 116 ;
Weybourn Crag, 111.

Monian Rocks of Shropshire, Prof.
Blake on the, 386,416. ~

Monocraterion, 604.

Mont Genévre, map of, 300; Vario-

litie Rocks of, 295; village, pass,
and valleys of, 229.

639

Moorea Kirkbyi, 542.

Morainic deposits in Pennsylvania,
Poe: T14,

Morgan, Prof. C. Ll., on the Pebidian
Volcanic Series of St. David’s,
241.

Mull, augite-propylite of, 350; cupola
in, 355; diorites of, 361; horn-
blende-propylite of, 348.

Multicrescis variabilis (?), 482.

Mundesiey beds, 95; section near,
106.

Murchison Geological Fund, award of
the, to Mr. E. Wethered, Proc. 40 ;
Medal, award of the, to Prof. E.
hull? Proc, 3h:

Nereites, 597.

New Galloway, altered rocks near,
569; aplite veins near, 577; gra-
nite near, 569; metamorphosed
rocks near, 569 ; mica-schists near,
577.

Newport in the Valley of the Cam,
Essex, wells at, 334.

Newton, Mr. EH. T., on some New
Mammals from the Red and Nor-
wich Orags, 444.

Newton-Abbot, Devonian Rocks at,
492, 507, 508, 511, 514.

New Zealand, Awaruite from, 619 ;
geology of a part of the West Coast
of the South Island of, Prof. Ulrich
on the, 619-630.

Nickel-iron alloy of New Zealand, 619.

Norcot, gravels, at 589.

Norfolk, Pebbly sands of, 84.

North America, former elevation of,
929; glaciation of, 529; Paleozoic
Ostracoda from, 534.

North-Italian Bryozoa, Proc. 123.

Norwich Crag, new Mammals from
the, 444.

Nufenen Pass, the, 217, 222, 232.

Obelisk Hill, Camberley, 560.

Obituary Notices, Proc. 48-56.

Obsidian, composite Spherulites in,
423.

Ocean-basins, Dr. W. T. Blanford on
the permanence of, Proc. 59.

Octonaria Linnarssoni, 541.

Ogof Goch, the fault at, 257, 258.

— Golchfa, Pebidian at, 247, 248.

Llesugn, Dimetian at, 264.

Olivine rocks of the South Island, New
Zealand, 623.

Ontario Basin, 525.

Oolite, Girvanella in, 270.

Oolitic structure, Mr. H. Wethered on,
270.

640

Ordovician chert-beds of Scotland,
PPOG. ALY.

Origin of the Great Lakes of America ;
Dr. Spencer on the, 523; of serpen-
tine, 324; Southern Drift, 168,
Variolitic rocks of Mount Genévre,
324.

Ostracoda, Devonian and Silurian, 7,
534.

Overlap, the Cambrian, 209.

Oxford, section near, 151.

Oxford Clay of Huntingdonshire, Orni-
thosaurian remains from the, 429 ;
Peterborough, Crocodilian jaw from
the, 284; Peterborough, Pliosaurus
from the, 49 ; Wiltshire, Crocodilian
jaw from the, 285 ; Sauropterygians
from the, 36, 49.

Oxfordshire, the Westleton Beds in
South, 140.

Paignton, Devonian rocks near, 496.
Pakefield, section near, 102.
Paleolithic Implements, 583, 587.
Palxophycus, 606, 617.

Palzozoic burrows, tracks, and other
markings, 594; Entomostraca, range
of some, 2; Ostracoda from North
America, Wales, and Ireland, 534 ;
Radiolarian Chert from Scotland,
Proc. 112.

Pebidian in Caerbwdy Valley, 244;
in St. Non’s Bay, 244; relation of
the, to the Cambrian, 248, 253;
to the Dimetian, 263; succession,
the, 255.

Pennsylvania, some glacial deposits in,
Proc, 114.

Peridotite, microscopic sections of,
630-632; of the South Island, New
Zealand, 623, 626.

Permanence of Ocean-basins, Dr. W.
T. Blanford on the, Proc. 59.

Permian Breccias, Mr. W. 8. Gresley
on the, Proc. 114.

Peterborough, Crocodilian jaw from
the Oxford Clay of, 284; Pliosau-
rus ferox from, 49.

Phoca Moori, 446.

Phocanella minor, 447.

Phymatoderma, 602.

Pidgeon, Mr. D., on certain Physical
Peculiarities exhibited by the so-
called ‘ Raised Beaches” of Hope’s
Nose and the Thatcher Rocks,
Devon, 438.

Pitchstones of the Western Isles, 371,
379.

Plan of the Plain of Tortoum, Arme-
nia, 33; Teversall and Pleasley Col-
lieries, showing the Wash-out, 433.

GENERAL INDEX.

Planolites, 612,

Plants, fossil, of the Westleton and
Mundesley beds, 115. .

Plateau-gravels of Berks and Surrey,
Dr. A Irving on the, 557.

Localities of Sections of the, 560.

Pleasley Colliery, Wash-out in, Proce. 1,
432.

Piewrocelus valdensis, 182, 184.

Pliosaurus ferox, 49, 50.

Plumbago of Borrowdale, Mr. J. Pos-
tlethwaite on the, Proc. 124.

Polycope sublenticularis, 550.

Polyzoa North-Italian, Proc, 123; of
the Red Chalk, Mr. G. R. Vine on
the, 454.

Porphyry Crags of Treginnis, 257 ; in
Grit, section of, 412.

Porth Clais, the Dimetian in the Allan
Valley at, 264.

Porthlisky Bay, the red quartz-ande-
site of, 258; the Dimetian in, 263.
Portland, Czmoliosaurus from the

Purbeck beds of, 47.

Oolite, structure of the grains of,
279.

Postlethwaite, Mr. J., on the Borrow-
dale Plumbago, its mode of occur-
rence and probable origin, Proc. 124.

Potsdam Sandstone, concretions in the,
609; tracks and other markings in .
the, 599, 609.

Pre-Cambrian Rocks of the Long-
mynd, 386, 413.

Preglacial Drifts and the Westleton
Shingle, 155; Hill-gravels, 162.
Prestwich J., on the relation of the
Westleton Beds, or Pebbly Sands of
Suffolk, to those of Norfolk, and on
their extension inland, with some
Observations on the Period of the
Final Elevation and Denudation of
ThamesValley, Part. I., 84 ; Part II.,
120; on the relation of the West-
leton Shingle to other Preglacial
Drifts in the Thames Basin, and on
a Southern Drift, with Observations
on the Final Elevation and Initial
Subaerial Denudation of the Weald,
and on the Genesis of the Thames,

Part IIL, 155.

Primitia Billingsii, 547 ; Clarkei, 535 ;
humilis, var. humilior, 3,5; minuta,
3,7; Morgani, 3,5; mundula, 551,

. 592, 553; mundula, var. cambrica,
3,5; ovata ?, 552; seminadum, 3, 5;
sp., 553 ; Ulrichi, 3, 6,551; wnicornis,
3, 7; (?) Walcotti, 543; Whitfieldi,
3, 9

Primitiopsis punctulifera, Oy) Del Os
542.

GENERAL INDEX,

Proboscina angustata, 467; bohemica
(?) var., 472; dilatata (?) and var.
cantabrigiensis(?), 473; genus, 466 ;
gigantopora, 471; gracilis, var.
Reussii, 469; hunstantonensis, and
var. ampliata, 470; irregularis, and
var., 468 ; Jessoni,471; ramosa (?),
473; rugosa (?), 468; subelegans,
470; Toucasiana (?), 572; uberrima,
469,

Profile-diagram of Ben Hiant, 375.

Propylites, composition of, 349;
geological age of the Scottish, 353 ;
microscopical characters of the,
350; of the Western Isles of Scot-
land, Prof. J. W. Judd on the, 341,
345 ; origin and original condition
of the Scottish, 354, 356, 367 ; struc-
ture of the, 354; Propylitic modi-
fication, causes of, 366.

Protichnites, 600; acadicus, 599.

Psammichnites, 597.

Purbeck beds, Cimiliosaurus from the,
47 ; Sauropterygians of the, 36, 47.

Pyroxene- -andesites, 361, 371, 377.

diorites, 461, 365.

Quartz-andesite of Porthlisky Bay,
253.

Quartz-diorites of Mull, 361.

Quartzite of the Longmynd, 414.

Quendon and Rickling, in the Valley
of the Cam, wells at, 334.

Radiating Burrow, 605.

Radiolarian Chert from Scotland, Dr.
G. J. Hinde on some, Proc. 111.

“ Raised Beaches,” so-called, of Hope’s
Nose and the Thatcher Rock, Mr. D.
Pidgeon on the, 438.

Raised Shores and Beaches of the
Great Lakes, 529.

Ramsleigh limestone, 508.

Range of some Paleozoic genera of
Entomostraca, 2; of the Polyzoa
of the Red Chalk, 460; of the
Westleton Beds inland, 124.

Rapids of the St. Lawrence, 530.

Rauchwacké, microscopic structure of
the, 230 ; the, and its relation to the
Schists, 204, 230.

Reading, gravels near, 560, 582; Mr.
O. A. Shrubsole on the evavels
about, 582.

Red Chalk, Polyzoa of the, 454.

Red Crag, new mamunals from the, 444.

Red Hill, rocks of the, New Zealand,
628.

Red quartz-andesite of Porthlisky
Bay, 258.

Redlands, gravels at, 589.

641

Relation of the Pebidian to the Cam-
brian at St. Davids, 241, 253; of the
Variolitic and other rocks of Mont
Genévre, 319.

Reptomulticava collis (?), 481; genus,
481; simplex (?), 481.

Resolution of Council respecting the

* Death of Mr. Dallas, Proc. 121.

Rhamphorhynchus Jessoni, 430.

Rhaxella perforata, 59.

Rill-marks, 615.

Ripple-marks, worm-tracks,
shrinkage- -cracks, 610, 611.

Ritom, section across Lake, 200.

River St. Lawrence, 525,

Ruscombe, gravels at, 591.

Rusichinites, 596 ; acadicus, 598,

Rusophycus, 596.

Rutley, Mr. F.,on Composite Spheru-
lites in Obsidian from Hot Springs
near Little Lake, California, 428.

and

Sabellarites, 605, 607 ; phosphaticus,
608 ; trentonensis, 607.

Seerichnites, 596.

St. Davids, Pebidian Volcanic series
at, 241 ; Promontory, section across,
207.

St. Lawrence, the river, 525.

St. Non’s Arch, sketch of, 246.

St. Non’s Bay, map of the Pebidian
and Cambrian in, 244.

Saltern Cove, 497, 508.

Sandhurst, gravels at, 560.

Sauropodous Dinosaurs from the
Wealden, Proc. 6, 182.

Sauropterygians of the Purbeck and
the Oxford Clay, 36, 47, 49.

Scarborough, siliceous sponges from
the Calcareous Grit of, 59.

Schists near Andermatt, 191; of the
Val Piora, 199, 244.

Schorlaceous Felsites, South Devon, 75.

Scolithus, 602, 605, 607 ; canadensis,
604; linearis, 603.

Scopi, schists of the, 214; section on
the, 215.

Scotland, a new Labyrinthodont from,
289 ; Propylites of the Western Isles
of, 341, 345; Radiolarian Chert
from, Proc. 111.

Scotolithus mirabilis, 604.

Section across Littlebury, Essex, 337 ;
the extreme south part of the Long-
mynd, 892; the southern part of the
Longmynd, 392 ; the Volcanic Hills
near Church Stretton, 409 ; along
Smitham Bottom, 172.

Sectional list of beds at Chideock Hill
and Down Cliffs, 519; of the Port-
land beds, 279.

642

Section at Bacton Cliff, 104; Brandes-
ton Brick-pit, 125; Burnt House
near Stoke, 131; the base of the
Cliff near Trimlingham, 100; the
base of the Cliff north of Pakefield,
102 ; the north end of the Railway
Section between Chettle and Mark’s
Tey, 182; the Railway ballast-pit,
Braintree (south end), 133; the
south end of Kessingland Cliff, 101 ;
West-Runton Gap, 110; Woman-
Hythe Gap, 110.

Section (diagram) across Lake Ritom
and the Val Piora, 200; across the
pass between Pian Alto and Fongio,
208; from Ogofau-Dduon to Ogof
Llesugn, 257; of Ben Hiant, Ardna-
murchan, 3875; on Alp Vitgira,
217; onthe west flank of Scopi, 215.

Section from Charlton Hill to the
south end of the Wrekin, 411;
Hatfield Brick-pit to the Great-
Northern Railway near Digswell
Junction, 188; in Charlton Lane,
showing the Grit, 409; Covehithe
Cliff, north of Easton Bavant, 99;
front of the Chalk-escarpment
above Merstham, 173; ravine,
Val Canaria, 210; the Brickfield to
the West of Bentley Priory, Stan-
more, Middlesex, 166; near
Thaxted, 1384; of a gravel-pit on
West-Ho Hill, 158; disturbed
pebble-bed in the Railway-cutting
(west end), Brentwood Common,
164; porphyry intrusive in Red
Grit at Cardington, 412; Chalk-
escarpment above Lenham, show-
ing the former extension of the
Lenham Sands, 168; Cliff about 4
mile north of Mundesley, 106;
Cliff east of Walton-on-the-Naze,
128; Cliff one mile south-east of
Clacton, 129; Horderley Inlier,
392; Junction of Slate and Grit
south of Narnell’s Rock, 3895;
Northern part of the Longmynd,
392; Westleton Beds on Westleton
Common, 96; on Gravel-pit Hill,
near Hasthampstead, 161; Rundell’s
Farm, Leiston Common, 125; the
hill above the Thames near Goring,
140; Railway near Ipswich, 127;
Railway one mile north of Witham,
132,

Section, theoretical, across Well Hill
and the old Gravel-stream, 170;
along the summit of Well Hill to
the flanks of the Wealden Range,
170.

Sections in ravine 8.E. of Lake Ritom,

GENERAL INDEX.

206, 207; of the Wash-out in the
Teversall and Pleasley Collieries,
434,

Serpentine, origin of, 324.

Serpentine rocks of the South Island,
New Zealand, 623, 625.

Sherborn, Mr. C. Davies, award of the
Lyell Geological Fund to, Proc. 41.

Shiplake, gravels at, 584.

Shrinkage-creeks, 610, 611.

Shropshire, Monian and Cambrian
Rocks of, 3886; the Voleanic Hills
of, 405, 409.

Shrubsole, Mr. O. A., on the Valley-
gravels about Reading, with especial
reference to the Paleolithic Imple-
ments found in them, 582.

Siliceous Sponges from the Lower
Calcareous Grit, 54. |

Silurian Ostracoda from Anticosti,
545, 546; Canada, 545, 550.

Silver Creek, Awaruite at, 630.

Sind Valley, Glaciation in the, 66.

Sketch from cliff, St. Non’s Bay,
245; of a rock-face showing the
relations of variolitic diabase, dia-
base dyke, porphyritic diabase, and
tuff on Le Chenaillet, 809; faulted
junction of Pebidian and Conglom-
erate at. Ogof Golchfa, 248; St.
Non’s Arch, 246; the Col du
Chenaillet from the North, 305;
west slope of Le Chenaillet, showing
dyke-like forms of the Variolite-tuf’,
318; Variolite-diabase and sphe-
roidal masses on Le Chenaillet,
above the Durance, 311; north end
of Le Chenaillet, 312.

Sketch-map of Ben Hiant, Ardna-
murchan, 374; of St. Non’s Bay,
244.

Sketch-plan of the Plain of Tortoum,
Armenia, 38.

Skull, human, from the Manchester
Ship-canal, Proc, 112.

Smitham Bottom, section along, 172.

Solfataric action in producing pro-
pylites, 367.

Somerset, Westleton Shingle in, 144.

Sonning Hill, gravels at, 590.

South Africa, a new Labyrinthodon
from, 291; gold-field of the Wit-
watersrand in, Proce. 3.

South Devon, Breccias of, 69.

South-east of England, lines of ele-
vation and drainage in, 176.

Southern Drift, characters of the,
155; in Kent and elsewhere, 156;
origin of the, 168; relation of the,
to the Westleton Shingles, 174.

Southern Hill, gravels at, 590.

GENERAL INDEX,

South Island, New Zealand, Awaruite
from, 619; Geology of part of the
West Coast of, 622.

Spencer, Prof. J. W., on the Origin of
the Basins of the Great Lakes of
America, 523.

Spherulites in Obsidian, Mr. Rutley
on some, 423.

Spilosite in Devon, 506.

Sponges, siliceous, from the Lower
Calcareous Grit, 54.

Stanmore, section near, 199.

Stiffe, A. W., cv the Glaciation of parts
of the Valleys of the Jhelam and
Sind Rivers in the Himalaya Moun-
tains of Kashmir, 66; on a Human
Skull from the Manchester Ship-
canal, Proc. 112.

Stoke, section near, 131.

Stomatopora divaricata, 463; genus,
462 ; gracilis, 462; granulata, 464 ;
linearis, 466; longiscata, 465;
ramea, 465.

Strepula plantaris, 540; sigmoidalis,

1

Stringocephalus-limestone, 502, 515.

Striped Hyzna, fossil in the Val
d Arno, 62.

Subaerial Denudation.of the ‘Weald,
155.

Suchodus durobrivensis, 285.

Suffolk, Pebbly Sands of, 84; Westle-
ton Beds in, 124.

Surrey, the Southern Drift.in, 156;
Westleton Beds in, 148.

Swinley, gravel at; 560.

Taonichnites, 617.

Teeth, carnassial, of Hyena striata, 63.

Teign River, Devonian Rocks near,
490, 509, 514.

Tertiary Basin of the Thames, 178;
Hyena in the Val d’ Arno, 62.

Teversall Colliery, Wash-out in, Proc.
I, 432.

Thames-Basin, Preglacial Drifts in
the, 155; genesis of the, 155, 177;
gorge of the, at Goring, 148, 149,
151 ; gravels north and south of the,
582, 585; the Tertiary Basin of the,
178.

Thames-Valley, glacial drifts of the,
144; period of the denudation of
the, 84.

Thatcher Rock, raised beach of the,
438.

Thaxted, section near, 134.

Thedford, Canada, Ostracoda from,
534, 535, 542. -

Tholeites of the Western Isles, 371,
379.

Q.J.G.8. No. 184.

643

Tilehurst Road, gravels at, 384.

Tooth of Pleurocelus valdensis, 182.

Topographical plan of a part of South
Island, New. Zealand, 624.

Torquay, Devonian Rocks near, 490,

494; raised beaches.near, 438.

Tortoum, Sketch-pian of the plain of,
30.

Tourmaline .on Knocknairling Hill,
578.

Tracks, branching, 613.

‘Tracks, burrows, and other markings

in Paleozoic Rocks, 595.
Treginnis, the Porphyry Orags of, 257.
Tricophycus, 610.

Trimlingham, Section near, 100.
Trogontheriwm minus, 447.
Trunk-like concretions, 609.
Twyford, gravels at, 591.

Ugbrooke Park, limestone of, 507.

Ulrich, Prof. G. H. F,, on the dis-
covery, mode of -occurrence, and
distribution of the Nickel-iron Alloy
Awaruite, on the West Coast of
the South Island of New Zealand,
619.

Ulrichia Conradi, 544; genus, 543.

Unicavea collis, 483; genus, 483.

Unitubigera, genus, 479; papyracea,
479.

Upper-Lias clay, so-called, 518.

Ussher, Mr. W. A. H., Award of the
Wollaston Geological Fund to,
Proc. 38; on the Devonian Rocks
-of South Devon, 487.

Val Canaria, sections of, 208, 210, 227,
230.

Val Piora, the ‘Rauchwacké of, 204;
Schists of the, 199, 224; section
across, 200.

Variolite, composition of, 327 ; of the
Durance, 295; origin and modifi-
cation of, 329 ; known localities of
true, 328, /

Variolitic Rocks of Mont Genévre,
Messrs. Cole and .Gregory on the,
295 ; origin of the, 328, 229, 381.

Verde antique of Greece, 364.

Vertebre of Pleurocelus from the
Wealden, 184.

Vertebrata of the Westleton and Mun-
desley Beds, .117.

Vexillum, 615.

Vine, Mr. G..R., A Monograph of the
Polyzoa (Bryozoa) of the Hunstan-
ton Red Chalk, 454.

Volcanic bombs, Pebidian, 258; dykes
of Mont .Genévre, 306; Hills of,

Soe

644

Shropshire, 405, 409; rocks of
Ashprington in South Devon, 493,
504; rocks of N.W. Germany,
Prof. A. von Koenen on the, Proc.
116 ; series of St. Davids, Mr. C. Ll,
Morgan on the Pebidian, 241.

Wadhurst Clay, bone of Megalosaurus
from the, 45; Iguanodonts of the,
36.

Wagbullock Hill, gravels at, 560.

Wales, Palzozoic Ostracoda from,
fab:

Walton-on-the-Naze, section near, 128.

Warberry Hill, fossils from, 495.

Ware, section across the Lea at, 150.

Warley, Preglacial gravels of, 162.

Warping of the EKarth’s Crust, 529.

Wash-outs, Washes, or Drifts in the
Durham and other Coal fields, Proc.
1, 432, 486.

Waters, Mr. A. W., North-Italian
Bryozoa, Proc, 128.

Weald, elevation and denudation of
the, 84, 55; period of the denuda-
tion of the, 84,

Wealden Anticlinal, section of the
slope of the, 170, 172; Area, early
physiographic conditions of the,
166

Wealden, horn-like Dinosaurian bone
from the, 185; Dinosaurs of the,
36; small Sauropodous Dinosaurs
from the, 182.

Well Hill, sections of, 170.

Wells in Essex, indicating deep chan-
nel of Drift, 333-339.

Wenden, Essex, wells at, 335.

West-Ho Hill, section on, 158.

Western Isles of Scotland, the ande-
sites of, 358; the diorites of, 358;
the propylites of the, 341.

Westleton and Mundesley Beds, 95,
114; Mollusca of the, 113; Organic
Remains of, 115.

Westleton Beds, range of, north of the
Thames, 124; south of the Thames,
148.

Westleton Common, section at, 96;
Pebbly Sands of, 84; Shingle in
relation to the Glacial Drifts
of the Thames Valley, 144; to
the other Preglacial Drifts, 155,
174; in Somerset, 144; in Wilt-
shire, 143; origin of the, 145.

West-Runton Gap, section at, 100.

Wethered, Mr. E., award of the Mur-

GENERAL INDEX,

chison Geological Fund to, Proc.
40; on the occurrence of the genus
Girvanella, and remarks on Oolitic
Structure, 270.

Weybourn Crag, 110; Mollusca of
the, 111.

Weymouth, Girvanella in the Coral-
line Oolite near, 278,

Whitaker, Mr. W., on a Deep Chan-
nel of Drift in the Valley of the
Cam, Essex, 333.

Whiteway Farm, Devonian Rocks at,
491, 507, 510, 513, 514, 515.

Whittlesford, well at, 339.

Williamson, Prof. Dr. W. Crawford,
Award of the Wollaston Medal to,
Proc, 34:

Wiltshire, the Southern Drift in, 156 ;
Westleton Shingle in, 143.

Witham, section near, 132.

Witwatersrand Gold-field, Proc. 3.

Wollaston Geological Fund, Award of
the, to Mr. W. A. E. Ussher, Proc.
38; Medal, Award of the, to Prof.
Dr. W. Crawford Williamson, Proc.

A acdiaticdl Mr. A. S., on some British
Jurassic Fish-remains referable to
the genera Eurycormus and Hypso-
cormus, Proc. 8.

Woolborough limestone, 503.

Worm-burrows, 612.

Worm-tracks, _ripple-marks,
shrinkage-cracks, 610, 611.

Worth, R. N., Further notes on the
existence of Triassic Rocks in the
English Channel off the coast of
Cornwall, Proc. 120; on the igne-
ous constituents of the Triassic
Breccias and Conglomerates of
South Devon, 69.

Woman-Hythe Gap, section at, 110.

Wrekin, map of the, 410; section of
the, 411.

Aestoleberis Wrightii, 5, 28.

and

Yorkshire, a new Cyphaspis from,
421; siliceous sponges from the
Lower Calcareous grit of, 54.

Zaccagna, M., his views on the Geology
of Mont Genévre, 321].

Zonopora, genus, 481 ; irregularis (?),
482; variabilis (?), 482.

Zoutpansberg, Mr. CO. Maidment’s
map of, Proc. 9.

END OF VOL. XLVI.

Printed by TAYLOR AND FRANCIS, Red Lion Court; Fleet Street.

A PHYSICAL AND GEOLOGICAL MAP

OF

PNGLAND AND WALES

BY THE LATE

G. B. GREENOUGH, Esq., F.R.S., F.G.S.

ON THE BASIS OF THE

ORIGINAL MAP OF WILLIAM SMITH, 1815.
Revised and Improved under the Superintendence of a Committee

of the Geological Society of London.
Size 84 inches by 63. Scale 6 miles to 1 inch.

eee

Price of the Complete Map in sheets, to Fellows of the Society, £2 2s.;
to the Public, £2 16s.

Mounted in Case, £3 13s. 6d.; Rollers, Varnished, £4 4s.;
Spring Roller, £6 6s.

Separate Sheets at the under-mentioned Prices :

To Fellows. To Public. To Fellows. To Public.

Se) Ge sid. Sead, Sous

Nowe es 4 Ge... 66 Nos ae eat Sie'G 10 6
homes OG os... 4 6 No. 5 Lo yOr 16 0O
Nowore W210 6 hie 6 No. 6 Teh Gure 10 O

PUBLISHED BY THE GEOLOGICAL SOCIETY, AND SOLD AT
THEIR APARTMENTS, BURLINGTON HOUSE.

NATURAL SCIENCE LABORATORY,

22 Newman Street, Oxford Street, London, W.
Director: Prof. J. F. BLAKE, M.A., F.G.S.

For Students and Research work in the various branches of Geology
and Biology. Special courses for the Preliminary Science and other
Examination work may commence at any time.

The naming and description of Fossils, Minerals, Rocks, and Objects of
British Natural History are also undertaken.

’

PASS CORN ESA #0) 2) POTN AT OE Vain hohe ; al ‘ate Ree

een @ cea | 5 y :
watt iti ans VES re i | ti) ‘bree ty) ty 4 , . siasirhbe lee
wh} . oy % ? i, » p ’ Bo mf f a) oh be
0 3 0B. 2a Glee Bea ig (Re POR A Oe RT ae
° + ; te q re f f : Pi ' a “) > in . 4 tai
’ bi ys oe Pe at
i B 4 y & ty, \ p ‘ q fi as 4 i P he) nate i
dh ’ § = A ‘ /
ANE Oat ae ee

ast Thun “GRA

Pe
ie Lat =
~*~

rie 5 Ba ae 5 i ~ to <a =
Saat MRNAS os Cs 3
1S leg Be 4 aie yer tg EA
‘ 4 ? On? 3 in Ae
f ; A : My . fi

“aN ey

si Geiser dla

“
Fis Bs ‘ aes,
Pd
Vey Say e vias ae

x iat Peit ea tae

: oe
ayy 4) oy Diep aa

aS Toe I 2 By a eee
Mh oh TERA Ae

Wives, bh abeatt aire wai vel
OAS Ptr 1 sayy as

2198 ok Site Mat tdaeew he AE

Aury Cet . Rot
ee 7 sthrtitae B 10° 8945 sO te arid: ohio | yo eerie on

} tober. ‘a Yee fag as bie ned:
Hurd Kutiwlns ti F Ex c, ie ie

|

=

» De zi e

ae Marys

1 er . a are

}: ° ; ‘ ihe - iA ) Fa } 3s \ nk ae 2 \
ars 1

a i

Ey ys , ers ae sii ee ae ee ie cS (aoe

bp ee eS Rata ae shetit | * 4 ant Oe, #4) ok Debate
4% 3 lhe rn
. boi iy ot yds e Lal ae ae | ep on :

fe! Vai "e Ania

m

Tapa TS Verhsaey 1 Tues ai titi nit 1H sy RSs Sona rm
4 e 7

if Shieh, Fr, Ky eh AIG hook ee ence: Vit the |
. “~~ ¢ w i Silat et ier » ¢®) - j ; ahs cd ; x. ar: ary
GOO ROL PRL Ta Pls oF ii vy 10 Ala LE aes ¥
; ; i a

my eel few oven ~t Mahe oe See pede gy emetic eieiiiiernas lie. te Sietes nih neem iat oe!
P a3, ‘
'

OLA TORO TO DST

Pier

- i Peas at part" Poe ay Rael <, Sadeghi ‘ ave aw i ies 7
my |

SP Cae ee GMALR Oh loth: thes oa

bis: RCL } ae] Py Ont be oh ae Levit shh bia aleay x
' oe a mits Pap bik OE a Th) eae bint na yk t ;
™ Y ’ ry P:
Rye neue eT he a Pia e at es
ee OGL, tie ¥ hl gagi he. 14: tthtdiziwectly Bde ethan By:
és

posite Mak oi celarane aac ybog ht Lawaalt oa i

eee rvae

-"
, qj Maia Mc

i

PROCEEDINGS

OF THE

GEOLOGICAL SOCIETY OF LONDON.

SESSION 1889-90.

November 6, 1889.
W. T, Branrorp, LL.D., F.R.S., President, in the Chair.

The Rev. D. Charles Evans, Menai Bridge, was elected a Fellow
of the Society.

The List of Donations to the Library was read.

The following communications were read :—

1. “Contributions to our Knowledge of the Dinosaurs of the
Wealden and the Sauropterygians of the Purbeck and Oxford
Clay.” By R. Lydekker, Esq., B.A., F.G.S.

2. “Notes on a ‘Dumb Fault’ or ‘ Wash-out’ found in the
Pleasley and Teversall Collieries, Derbyshire.” By J. C. B. Hendy,
Esq. (Communicated by the President*. )

The “Top Hard” Seam of the district is being worked in ess
collieries at a depth of 500 yards, where it has an average thickness
of 5 feet, with a band of cannelin the middle. In the working it was
found that the coal began to thicken, until it became double the
usual size, the cannel also increasing in the “ Top Seam,” but in
the Lower Seam running out altogether.

This double thickness of coal continued till the “wash-out”
was reached, when both coal and shaly roof disappeared, the space
being replaced by sandstone similar to that of the beds overlying
the shale. The clay floor of the Lower Seam had not been much
interfered with, and this was followed for 60 yards, when the

* This paper has been withdrawn by permission of the Council.
VOL. XLVI. a

2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

doubly thick seam was again met with, and on being followed
gradually assumed its normal thickness.

No fossils have been noted in the ‘‘Wash-out” itself, the —
vertical extension of which is unknown.

' Discussion.

The PresrpEnT considered that more particulars would have been
useful, and that the section should have been drawn to true scale.
He quoted cases in India where there was no thickening of the coal
at the edge; the coal had apparently been washed away and
replaced by sandstone. It was difficult to understand why the coal
washed away should be redeposited at the edges of the stream.

Prof. Grern, with reference to the want of further particulars,
. could only endorse what had been said. He spoke of the possible
existence of little ponds and lagoons where the cannel had been
forming.

Prof. Huexes pointed out that the thicknesses did not give the ori-
ginal measurement of the coal. There was no mention of roots _
going into the floor, which was described as uninterrupted. The
space had been filled up with less compressible material.

Prof. J. F. Buaxe observed that this “‘ dumb fault” was a portion
only of a much larger one. In this Mr. Coke had shown that
pressure from the sides had been brought to bear, which would
account for the thickening observed. Mr. Coke had suggested that
the ‘‘ wash-out” was not due to ordinary denudation, but to an
original depression in an area of sinking.

Prof. Larworrn considered that such ‘“‘ dumb faults” as had been
investigated by himself were due to faulting and to distortion from
pressure. The edges of a “dumb fault” were slickensided. The
missing coal is to be found in the thickened seam.

Mr. J.G. Woop alluded to a “‘ dumb fault ” described by the late
Mr. Buddle about 50 years ago. Subsequently agreat contortion had
been discovered in near proximity to it, the coal being thrown into
an arch with a possible parting asunder.

3. “On some Paleozoic Ostracoda from North America, Wales,
and Ireland.” By Prof. T. Rupert Jones, F.R.S., F.G.S.

The following specimens were exhibited :—

Remains of a Pliosaur from the Oxford Clay of Peterborough, in
the collection of A. N. Leeds, Esq.; the cast of a cervical vertebra
of Iguanodon from the Wealden of Hastings, in the possession of
P. Rufford, Esq.; a cervical vertebra of a Plesiosaurian from the
Purbeck; and a dorsal vertebra of Pelorosawrus (Ornithopsis)
Leedsi, in the collection of A. N. Leeds, Esq.; exhibited in illus-
tration of the paper by R. Lydekker, Esq., F.G.S.

Specimens of Paleozoic Ostracoda, exhibited by Prof, T, Rupert
Jones, F.R.S., F.G.S

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 3

November 20, 1889.
W. T. Buanrorp, LL.D., F.R.S., President, in the Chair.

Nagayuke Asano, Esq., Assoc. R.S.M., care of Marquis Asano,
Hongo, Tokio; Lieut.-Col. T. Couchman, C.E., Melbourne, Victoria ;
Frederic H. P. Cresswell, Esq., Assoc. R.S.M., Chile, Venezuela ;
and Thomas Shilston, Esq., 14 Wentworth Place, Newcastle-on-
Tyne, were elected Fellows of the Society.

The List of Donations to the Library was read.

The Secretary announced that a series of specimens from the
line and the neighbourhood of the Main Reef, Kast and West of
Johannesburg, Witwatersrand Gold Fields. had been presented to
the Museum by Dr. H. Exton, F.G.S., and read the following letter
from that gentleman in explanation of them :—

‘ Johannesburg, Transvaal, South Africa,
7th May, 1889.

«“¢ DEAR Si1z,—

“‘ Having been engaged in making a collection of specimens of
auriferous conglomerate from the principal mines in this immediate
neighbourhood, I have packed a series of these, which are now in
transit and of which you will be duly advised by the transport-
agent. They are designed for the Museum of the Geological
Society.

‘Commencing eastward of Johannesburg, there are examples from
the Black Reef, the Salisbury Mines, Wemmer’s, Robinson’s, Lang-
laagte Estate, and the Paad| Pretoria—this last-named being now
under the new appellation of Langlaagte Consolidated. Excepting
the Black Reef, these mines are all upon the Main Reef. The
Main Reef has a general direction east and west, with a dip
towards the south varying from 45° to 80°. In the Salisbury
claims the reef is practically perpendicular.

“* Qn the south side of the Main Reef, and running parallel to it at
a distance of from 15 to 20 feet, is a narrow reef called by the miners
the south ‘leader.’ This varies from 7 to 15 inches wide, and is
generally much richer than the Main Reef.

‘At the Wemmer’s Co. this south ‘leader’ consists of several
narrow bands in close contiguity, which are so rich that at present
this alone is being worked. I am enabled to send specimens of this
‘leader,’ along with the casing both from the north and south
faces. From severe! other mines there are examples from the
casing of the Main Reef as well as of the ‘leader.’ Among those
from the Salisbury there is a piece of a white friable sandstone,
which runs in a narrow band parallel to the south ‘ leader,’ and
which often runs into the ‘leader,’ still keeping its distinctive
feature,

4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

“ Accompanying these I enclose for the Geological Society a large
plan of the district, with the gold-bearing reef marked upon it, with
the farms through which it runs, and the names of the various ~
companies on the site of their workings. ‘This may be relied upon
as authentic, though a large number of valuable gold properties have
been developed since the publication of this plan.

‘*Upon the plan I have placed a cross section, almost directly north
and south at right angles to the Main Reef. ‘This section covers a
little over four miles, crossing the Salisbury claims and passing
through the town of Johannesburg. At the south limit of this line
I have obtained the specimens A and B, which are at that point in
alternate bands of from 7 to 10 feet thick. A is worked for door-
jambs, lintels, &c.; but the quartzite B is too hard to be worked.
The dip of these rocks is towards the south about 40°. From here
to the Main Reef is a coarse sandstone, with here and there a
narrow reef of barren conglomerate. From the Main Reef north-
wards a similar sandstone prevails, having generally the character
of C, but (with a redder tinge nearer to the Main Reef) with a dip
(southwards) at the northern limit of 75°. Here it is bounded by a
fine-grained purplish-red jaspideous slate (specimen D), permeated by
narrow lines of quartz. The jagged edges of this dark-red slate
protrude above the surface.

‘From personal observation I am enabled to state that wherever
this formation is maintained the reef of gold-bearing conglomerate
is found running more or less parallel to it at a greater or less
distance to the south. I am not prepared to state the converse ;
but the before-named arrangement is true over 20 miles of reef.

‘J trust the specimens and plan may be found helpful towards
elucidating the geological problem of the origin of the gold-bearing
conglomerate, which has hitherto oscillated between the igneous
and aqueous theories,

““T am, dear Sir,
‘* Yours faithfully,
“<H. Exton, F.G.5,"

The PresipEnr considered the occurrence of the gold in large
quantities in such a conglomerate was a remarkable and interesting
ease. The rock was an ancient-jooking one, and the country
appeared to have undergone much disturbance.

Dr. Hiypr remarked that j in Nova Scotia beds of conglomerate of
supposed Carboniferous age were formerly worked for gold, but the
yield had not been very great.

The following name was read out for the first time in conformity
with the Bye-Laws, Section VI. Article 5, in consequence of the
non-payment of his arrears of contributions :—Dr. R. Havsrer.

The following communications were read :—

1. “On the Occurrence of the Striped Hyzena in the Tertiary of
the Val d’Arno.” By R. Lydekker, Esq., B.A., F.G.S.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. ; 5

_ 2. The Catastrophe of Kantzorik, Armenia.” By Mons. F. M.
Corpi. (Communicated by W. H. Hudleston, Esq., M.A., F.R.S.,
Secretary.)

3. “On anew Genus of Siliceous Sponges from the Lower Cal-
careous Grit of Yorkshire.” By Dr. G. J. Hinde, F.G.S.

The following specimens were exhibited :—

Specimens and microscopic sections of Khaxella perforata, Hinde,
gen. ef sp. nov., from the Lower Calcareous Grit of Scarborough (the
specimens belonging to the Natural-History Museums of York and
Scarborough), exhibited by Dr. G. J. Hinde, F.G.S., in illustration
of his paper.

' Specimens of Herpetocrinus Fletcheri, Salter, from the Wenlock
Limestone of Dudley, exhibited by F. A. Bather, Hsq., F.G.S.

With regard to these specimens Mr. Bather said that Herpeto-
erinus of Salter (= Myelodactylus, Hall) was described in Cat. Foss.
Woodwardian Mus. as possessing a coiled cirriferous stem, and
a small crown with dichotomous arms. American authorities,
however, had maintained Hall’s view that the coiled structure was
‘an arm with pinnules. The two specimens belonging to Mr. E.
Hollier, of Dudley, which were on the table, conclusively proved
the correctness of Salter’s position ; one of them was very fine, and
showed the structure of the dorsal cup. A specimen in the British
Museum had quite recently been discovered to possess a crown.
The drawings of stem-ossicles and of sections exhibited showed
that there were strong muscles on the outer curvature of the stem,
which could uncoil it.

December 4, 1889.
W. T. Branrory, LL.D., F.R.S., President, in the Chair.

Montagu Browne, Esg., Aylestone Park, Leicester; Joseph
Howell Bullock, Esq., The Grove, Pelsall, near Walsall; Arthur
Walter Clarke, Esq., Charters Towers, Queensland, Australia; John
Errington de la Croix, Esq., F.L.S., 49 Avenue Bosquet, Paris ;
Henry Nathaniel Davies, Esq., 5 Westbourne Terrace, Weston-
super-Mare; Arthur Dudley Dobson, Esq., Warrnambool, Victoria ;
Charles Henry Dunhill, M.D., Grays Court, York ; George Frede-
rick Lee Giles, Ksq., Memb.Inst.6. K., The Docks, Southampton ;
Henry Francis Hermi age, Esq., J.P., Margate ; Edward Hodges,
Esq., Assoc.M.Inst.C.H., Allahabad, India; Rev. James Hyslop,
4 Stratton Terrace, Tia: : Philip Lake, Esq., B.A., Geological
Survey of India, Calcutta ; Albert Latham, Esq., Memb. Inst.C.E.,
Margate ; J. Bickerton Morgan, Hsq., 30 Severn Street, Welshpool ; ;
Percival Gerard Pochin, Esq., 13 Ranmoor Park, Sheffield; John
Ridyard, Esq., Hilton Bank, Little Hulton, Bolton ; Charles Archi-
bald Ross, Esq., Porlock, Somersetshire ; Andrew Simons, Esq.,

6 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

1 Crescent Place, Plymouth; Evan William Small, Esq., M.A.,
B.Sc.Lond., High School, Nottingham; John William Teale, Esq.,
Bishop Auckland, Durham; J. Egerton Wood, Esq., Assoc.R.S.M., -
143 Regent Road, Salford, Manchester ; and Henry Woods, Esq.,
St. John’s College, Cambridge, were elected Fellows of the Society.

The List of Donations to the Library was read.

The following name was read out for the second time in conformity
with the Bye-Laws, Section VI. Article 5, in consequence of the
non-payment of arrears of contributions :—Dr. R. Hiustmr.

The President stated that a Circular Letter had been received
from the Secretary of the Committee on Geological Photographs,
formed at the last meeting of the British Association for the
Advancement of Science, to arrange for the Collection, Preser-
vation, and Systematic Registration of Photographs of Geological
interest in the United Kingdom, in which the aid and co-operation
of geologists ‘is earnestly requested. Copies of Instructions &e.,
drawn up in order to secure uniformity, are to be obtained on
application to O. W. Jeffs, Esq., Secretary to the Committee,
12 Queen’s Road, Rock Ferry, Cheshire.

The following communications were read :—

1. “On Remains of Small Sauropodous Dinosaurs from the
Wealden.” By R. Lydekker, Esq., B.A., F.G.S.

2. “ On a peculiar horn-like Dinosaurian Bone from the Wealden.”
By R. Lydekker, Esq., B.A., F.G.S.

3. ‘ The Igneous Constituents of the Triassic Breccias and Con-
- glomerates of South Devon.” By R. N. Worth, Esq., F.G.S.

4. “ Notes on the Glaciation of parts of the Valleys of the
Jhelam and Sind Rivers in the Himalaya Mountains of Kashmir.”
By Capt. A. W. Stiffe, F.G.S.

’ The following specimens were exhibited :—

Rock-specimens, exhibited by R. N. Worth, Esq., F.G.S., in
illustration of his paper.

Specimen and cast, exhibited by R. Lydekker, Esq., F.G.S., in
illustration of his papers.

Specimens of Quartz &c., containing Gold, from ‘“‘ Two Brothers ”
Reef, near Southern Cross and Golden Valley, Yilgarn, Western
Australia; and Specimens of “Stream Tin” from the Green
Bushes Tin Fields, Blackwood District, Western Australia, obtained
by M. F. A. Canning, Esq., exhibited by Dr. H. Woodward, F.R.S.,
F.G.S,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. i

December 18, 1889.
W. T. Branrorp, LL.D., F.R.S., President, in the Chair.

Charles Aburrow, Esq., Assoc.M.Inst.C.H., Johannesburg, South
Africa; Henry A. Allen, Esq., Assistant Paleéontologist to the Geo-
logical Survey, Museum, Jermyn Street, 8.W.; Thomas Bennett,
Esq., Assoc.M.Inst.C.E., Cheshunt Local Board, Cheshunt, Hert-
fordshire; and R. Lethbridge Tapscott, Esq., Assoc.M.Inst.C.E.,
41 Parkfield Road, Liverpool, were elected Fellows of the Society.

The List of Donations to the Library was read.

The following communications were read :— _

1. “‘On the Occurrence of the Genus Girvanella, and remarks on
Oolitic Structure.” By E. Wethered, Esq., F.G.S.

2. “On the Relation of the Westleton Beds or ‘ Pebbly Sands’ of
Suffolk to those of Norfolk, and on their extension inland, with some
observations on the Period of the final Elevation and Denudation of
the Weald and of the Thames Valley.”—Part II. By Prof. Joseph
Prestwich, M.A., D.C.L., F.R.S., F.G.S.

The following specimens were exhibited :—

Microscopic specimens and photographs, exhibited by E. Wethered,
Esq., F.G.S., in illustration of his paper.

Block of Quartz from the Plateau Gravel, 34 miles W.S.W. of.
Ascot Station, Berkshire (400 ft. above O.D.), exhibited by H. W.
Monckton, Esq., F.G.S. .

Book of photographs of Baku and the Caucasus, exhibited by
W. F. Hume, Esq., F.G.S.

January 8, 1890.
W. T. Branrorp, LL.D., F.RB.S8., President, in the Chair.

William Andrews, Esq., Gosford Lodge, Coventry; the Earl of
Berkeley, 21 Drayton Gardens, 8.W.; James Wright Croston, Esq.,
3 Egerton Street, Prestwich, Manchester; Walcot Gibson, Esq.,
34 Radnor Street, Chelsea, S.W.; and Arthur Octavius Watkins,
Esq., Assoc. R.S.M., Stow Park, Newport, Monmouthshire, were
elected Fellows of the Society.

The following Fellows, nominated by the Council, were elected
Auditors of the Society’s Accounts for the preceding year :—
H. Bavermay, Esq., H. W. Moncxton, Esq.

VOL. XLVI. b

8 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

The List of Donations to the Library was read.

The following communications were read :——

1. “On some British Jurassic Fish-remains referable to the
Genera Hurycormus and Hypsocormus.” By A. Smith Woodward,
Esq., F.G.S.

[ Abstract. ]

Hitherto our knowledge of the Upper Jurassic Fish-fauna has
been mainly derived from specimens found in fine lithographic stones,
where the various elements are in a state of extreme compression.
Within the last few years remains of similar fishes have been dis-
covered in the Oxford and Kimeridge Clays of England, and these
are of value for the precise determination of certain skeletal features
in the genera to which they belong.

The Author described Hurycormus grandis from the Kimeridge
Clay of Ely, a large species which makes known for the first time
the form and proportions of several of the head-bones in this genus.
A technical description of all the bones the characters of which are
distinguishable was given, and the Author concluded that there is
considerable similarity between the head of Hwrycormus and the
recent Ganoid Amia, even to minute points of detail.

He further described Hypsocormus tenuirostris and H. Leedsix
from the Oxford Clay of the neighbourhood of Peterborough, the oste-
ology of this genus not having as yet been elucidated. Portions of
the jaws have been discovered, affording valuable information asto
the form and dentition of the principal elements.

These jaws are not precisely paralleled by any other Jurassic
genus, though they possess a resemblance to Pachycormus, as also
to the Upper Cretaceous genus, Protosphyranda.

Discussion.

The Prestpent remarked that Amia is a freshwater genus, and
inquired whether the fossil fish was freshwater or marine. .
Mr. EK. T. Newron remarked upon the great interest and import-
ance of the paper.
The AurHor, in reply to the President’s question, said that the
old Ganoids were marine, and it was only in more recent times that
they had become restricted to fresh water.

2. “On the Pebidian Volcanic Series of St. Davids.” By Prof.
C. Lloyd Morgan, F.G.S.

The following specimens were exhibited :—

Head of Eurycormus grandis, A. 8. W., from the Kimeridge

Sk of Ely, exhibited by Prof. T. M°Kenny Hughes, F.R.S.,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 9

Jaws of Hypsocormus Leedsi, A. 8. W., from the Oxford Clay of
Peterborough, from the collection of A. N. Leeds, Esq., exhibited by
A. Smith Woodward, Esq., F.G.S.

Rock-specimens and microscopic sections, exhibited by Prof. C.
Lloyd Morgan, F.G.S., in illustration of his paper.

Specimen showing a new method of mounting Gold-leaf so as to
exhibit the green and yellow colours and transparency at one view,
either by daylight or artificial light, adapted for Museums &c.,
exhibited by 8. H. Needham, Esq., F.G.S.

ve

January 22, 1890.
W. T. Branrorp, LL.D., F.R.S., President, in the Chair.

Edwin Thomas Beard, Esq., The Colonial College, Hollesley Bay,
Suffolk ; William Fairley, Esq., Assoc.M.Inst.C.E., 1 Parliament
Square, Edinburgh ; and Lawrence Morris Lambe, Esq., Geological
Survey of Canada, Ottawa, Ontario, Canada, were elected Fellows,
and M. Gustave Dollfus, Paris, and Prof. A. von Konen, Gottingen,
Foreign Correspondents of the Society.

The List of Donations to the Library was read.

The Secretary, with reference to a Map of Zoutpansberg, presented
by C. Maidment, Esq., of Johannesburg, read a letter from that
gentleman in explanation of some points in the geology of the
district.

The following communication was read :—

‘On the Crystalline Schists and their relation to the Mesozoic

Rocks in the Lepontine Alps.” By Professor T. G. Bonney, D.Sc.,
Mia H.R. F.GS.

The following specimens were exhibited :—

Rock-specimens and microscopic sections, also four Iarge photo-
graphs taken by James Kecles, Esq., F.G.S., exhibited by Prof. T.
G. Bonney, D.Sc., F.R.S., F.G.S., in illustration of his paper.

é

February 5, 1890.
W. T. Branrorp, LL.D., F.R.S., President, in the Chair.

Wheatley James Atkinson, Esq., 76 Christchurch Road, Streatham
Hill, 8.W.; A. E. Gooch, Esq., B.A., B.Sc.Lond., 4 Alwyne Villas,
Canonbury, N.; Bernard Hobson, Esq., B.Sc.Vict., Tapton Elms,

b2

1 fe) PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

Taptonyille Road, Sheffield; Sir James Maitland, Bart., F.LS.,
Stirling ; Hugh Frederick Marriott, Esq., the Manor House, Perry
Hill, $.E.; 8. J. Truscott, Esq., Assoc.R.S.M., care of Messrs. Syme
and Co., Singapore; and John Walter Sugg, Esq., Knollbrow,
Dorking, were elected Fellows of the Society.

The List of Donations to the Library was read.

The following communications were read :—

1. “The Variolitic Rocks of Mont-Genévre.” By Grenville A.
J. Cole, Esq., F.G.8., and J. W. Gregory, Esq., F.G.S., F.Z.S.

2, “The Propylites of the Western Isles of Scotland, and their
Relations to the Andesites and Diorites of the District.” By Pro-
fessor John W. Judd, F.R.S., F.G.S., &c. a

The following specimens were exhibited :—

Rock-specimens and microscopic sections, exhibited by G. A. J.
Cole, Esq., F.G.8., and J. W. Gregory, Esq., in illustration of their
paper.

Rock-specimens and microscopic sections, exhibited by Prof. J.
W. Judd, F.R.S., F.G.8., in illustration of his paper.

ANNUAL GENERAL MEETING,

February 21, 1890.
_ W. T. Buanrorp, LL.D., F.R.S., President, in the Chair.

REPORT OF THE CoUNCIL FoR 1889.

In presenting their Report for the year 1889, the Council have
much pleasure in congratulating the Fellows upon the continued
and apparently increasing prosperity of the Society. The actual
Income of the Society was, indeed, rather less than in 1888, but
notwithstanding the Investment of a sum of nearly £200, and the
considerable expenses incurred in connexion with the Revision of
the Bye-Laws, the Balance at the credit of the Society is fully
maintained.

The number of Fellows elected during the year was 68, of whom
46 paid their fees before the end of the year, making with 15
previously elected Fellows, who paid their fees in 1889, and 1
Fellow re-admitted without payment of Entrance-fee, a total acces-
sion during the year of 62 Fellows. But during the same period
there was loss by death of 38 Fellows, and by resignation ot
13 Fellows, and 5 Fellows were removed from the List for non-
payment of their annual contributions, making a total loss of 56
Fellows. The actual increase in the number of Fellows is thus
only 6. Of the 38 Fellows deceased, 7 were Compounders, 14
Contributing Fellows, and 17 Non-contributing Fellows. During
the year 13 Contributing Fellows sent in their resignations, and 6
compounded for their Annual Contributions, so that the actual
increase in the number of Contributing Fellows is 24, making a
total of 856.

The total number of Fellows, Foreign Members and Foreign
Correspondents was 1373 at the end of 1888, and 1379 at the close
of the year 1889.

At the end of the year 1888 there was 1 vacancy in the List of
Foreign Members, and in the course of 1889 intelligence was
received of the decease of 2 Foreign Members. During the year
3 Foreign Members were elected. At the close of 1888 there was
also 1 vacancy in the List of Foreign Correspondents, and further
vacancies were caused by the filling up of those among the Foreign
Members and by the death of 3 Foreign Correspondents in the

I2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

course of the year. In this way 7 vacancies were caused in the
List of Foreign Correspondents, 5 of which were filled up in 1889,
leaving two vacancies in the list at the end of the year.

The total Receipts on account of Income for 1889 were
£2775 14s. 3d., being £169 19s. 7d. more than the estimated
Income for the year. The current Expenditure of the year, leaving
out of account the sum of £198 5s. 6d. expended in the purchase
of £200 Consolidated 22 per cent. Stock, was £2576 17s. 1d., being
£6 7s. ld. more than the Estimate. The actual excess of Receipts
over Expenditure during the year amounted to £198 17s. 2d., and
the Balance in favour of the Society to £249 4s. 1d.

In accordance with the statement made in the last Annual
Report of the Council several Special General Meetings were held
during the Spring of the year 1889 for the discussion of suggested
amendments of the Bye-Laws. The last of these Meetings was on
May 22nd, when the Bye-Laws as amended were formally balloted
for and carried. The amended Bye-Laws were then immediately
printed and circulated among the Fellows of the Society.

The Council have to announce the completion of Vol. XLYV.,
and the commencement of Vol. XLVI. of the Society’s Quarterly
Journal. .

They have also to mention that Mr. Ormerod has prepared and
sent in a Third Supplement to his Index to the Publications of the
Society, and that this is now in the Printer’s hands,

At the end of last year Prof. Prestwich wrote to the Council on
the subject of a series of MS. notes prepared by Dr. James Mitchell,
a former Fellow of the Society (who died in 1844), containing the
results of his investigations upon the Geology and Botany of the
neighbourhood of London, which were especially valuable as referring
particularly to the Economic Geology of the District. These notes,
having been collected and transcribed, now form five folio volumes,
which have been in Prof. Prestwich’s possession for many years,
and as he now knows of no surviving relatives of the late Dr. Mit-
chell, he desired to deposit the books in the Society’s Library, on
the understanding, however, that should any legitimate claimant
appear and apply for them they are to be given up. As Prof.
Prestwich considered that the notes contained in these volumes
might prove useful to Geologists engaged in similar investigations,
the Council at once accepted his offer, and the books have now been
deposited in the Library.

The Council have awarded the Wollaston Medal to Prof. William
Crawford Williamson, LL.D., F.R.S., in recognition of the valuable

services rendered by him to the study of Natural History and
' Geology, especially by his researches on the Foraminifera and on
Fossil Botany. ;

The Murchison Medal, with the sum of Ten Guineas from the
Proceeds of the Fund, has been awarded to Prof. Edward Hull,
LL.D., F.RS., F.G.S., in testimony of appreciation of the value of
his work as a Geological Surveyor, both in England and in Ireland,
through a long series of years, and also of his recent investigations
upon the Geology of Palestine.

ANNUAL REPORT. I3

The Lyell Medal, with a sum of Forty Guineas from the
Proceeds of the Fund, has been awarded to Thomas Rupert Jones,
Ksq., F.R.S., F.G.8., in recognition of the excellent work done by
him in many departments of Geological Science, but more especially
in connexion with the study of the Foraminifera and Entomostraca.

The balance of the Proceeds of the Wollaston Donation Fund has
been awarded to W. A. E. Ussher, Esq., F.G.S., as a token of
appreciation of the good work done by him during the progress of
the Survey of the South-western Counties of England.

The balance of the Proceeds of the Murchison Geological Fund
has been awarded to Edward Wethered, Esq., F.G.S., in recognition
of the value of his original investigations into the Microscopic
Structure of the Sedimentary Rocks, especially in connexion with
their minute organic constituents, and to aid him in the further
prosecution of his researches.

The Balance of the Proceeds of the Lyell Geological Fund has
been awarded to Charles Davies Sherborn, Esq., F.G.S., as a
testimony to the value of his Bibliographical and Microscopical
work, especially in connexion with the: Foraminifera, and to assist
him in carrying on his investigations.

A sum of £20 out of the Proceeds of the Barlow-Jameson Fund
has been awarded to William Jerome Harrison, Esq., F.G.S., in
recognition of the value of his original researches upon the Geology
of the Midland Counties, and of his efforts to popularize and widen
the sphere of Geological knowledge, and to aid him in further efforts
in the same directions.

14 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Report oF THE Liprary anp Mvusrum Committers.

Labrary.

Since the last Anniversary Meeting many valuable additions
have been made to the Library both by donation and by purchase.

As Donations the Library has received about 152 volumes of
separately published works and Survey Reports, and about 292
pamphlets and separate impressions of Memoirs, also about 149
volumes and 80 detached parts of the publications of various
Societies, and 18 volumes of independent Periodicals presented by
their respective Editors or Publishers, besides 17 volumes of News-
papers of various kinds. This will constitute a total addition to
the Society’s Library of about 352 volumes and 292 pamphlets.

Of Maps, Plans, &c., Geological and otherwise, the number pre-
sented during the past year has not been great. They include sheets
of the maps of the Geological Surveys of Norway, Saxony, Italy,
and Japan; some sheets of the Ordnance Survey Map; and maps
of some Mining Districts in Australia and South Africa.

The Books and Maps above referred to have been received from
173 personal Donors, the Editors or Publishers of 20 Periodicals,
and 190 Societies, Surveys, and other Public Bodies, making, in all,
383 Donors.

By purchase, on the recommendation of the Standing Library
Committee, the Library has received the addition of 41 volumes of
books, and of 93 parts (making about 27 volumes) of various
Periodicals, besides 16 parts of certain works published serially.
Of the Geological Survey Map of France 19 sheets, and of the
smaller Geological Map of France, by MM. Vasseur’ and Carez, 7
sheets have been obtained by purchase, besides a Mineral Map of
the district of Bensberg and Runderoth.

The cost of Books, Periodicals, and Maps purchased during the
year 1889 was £63 Os. 6d., and of Binding £83 3s. 6d., making
a total of £146 4s. Od.

Several of the Periodicals in the Library are still in an incomplete
condition. Inquiry is being made as to the possibility and the cost
of filling the existing gaps; and as there can be no doubt of the
desirability of the Serial Works in the Library being complete, it is
recommended that some provision in excess of former years be made
in the Estimates, so as to allow of the purchase of the Volumes
necessary to complete the sets.

Museum.

During the past year the following additions have been made to
the Society’s Museum :—
1. Fourteen specimens of Gold-bearing Rocks from the De Kaap

ANNUAL REPORT. 15

Gold-fields, South Africa, presented by R. H. Scaddan, Esgq., of
Johannesburg ; and

2, A series of Rock-specimens from the Main Reef, Witwaters-
rand Gold-fields, South Africa, presented by Dr. H. Exton, F.G.S8.

The Collections in the Museum are in good condition, and the
glazing and other protections of the drawers appear to answer their
purpose very well. As intimated at the close of the last Report of
the Committee, the glazing of the drawers in the Lower Museum
was continued in 1889, when 220 drawers, large and small, were
provided with covers at a cost of £5 4s. 5d. To complete the
glazing of the Inner Room of the Lower Museum there still remain
80 large drawers, at least twice the size of any of the others, to be
covered ; the Committee propose to devote a sum of about £5 to this
purpose during the year. The Inner Museum would then be glazed
throughout.

16 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
d

ComMPARATIVE StaTEMENT oF THE NUMBER oF THE Socrery AT THE
CLOSE OF THE YEARS 1888 anp 1889.

Dec. 31, 1888. Dec. 31, 1889.
Compounidersy "soy. tee Rig meerae ote 310
Contributing Fellows...... Coo ener ta 856
Non-contributing Fellows. . A aie aay 135
1295 1301
Foreign Members ........ ian eet cige ge 40
Foreign Correspondents... . Fa Oe A a 8 38
1373 1379

Comparative Statement explanatory of the Alterations in the Number
of Hellows, Foreign Members, and Foreign Oorrespondents at the
close of the years 1888 and 1889.

Number of Compounders, Contributing and Non- 1295
contributing Fellows, December 31, 1888....

Add Fellows elected during former year and paid 15
HHI ots MRRP ASE ra mM hel diet aid yak mor ao
Add Fellows elected and paid in 1889 ........ 46
Add Fellow re-elected and who pays no Admis-
siom Meets for an eeieeite einen enone mee } 1
1357
Deduct Compounders deceased .............. 7
Contributing Fellows deceased ........ 14
Non-contributing Fellows deceased .... 17
Contributing Fellows resigned ........ 13
Contributing Fellows removed ........ 5
— 56
1301

1 Contributing Fellow became Non-Resident, and 1 Non-
Resident Fellow was placed on the Contributing List.
Number of Foreign Members and eal, 9
Correspondents, December 31, 1888 ....
Deduct Foreign Members deceased .. ..... 2
Foreign Correspondents deceased .. 3
Foreign Correspondents at 3

Foreign: Members 27 -..- a. a
—, 8
70
Add Foreign Members elected ........ SoA 3
Foreign Correspondents elected ........ 5
— 78

ANNUAL REPORT. sf

DEcEASED FELLOWS.

Compounders (7).

Cockburn-Hood, T. H., Esq.
Jackson, HK. 8., Esq.
Langdon, Rev. E.

Lendy, Major A. F.

Travers, A., Esq.
Turner, H., Esq.

Woods, Rev. J. E. T.

Resident and other Contributing Fellows (14).

Bateman, J. F. La Trobe, Esq.
Blair, M., Esq.

Boyd, E. F., Esq.

Bristow, H. W., Esq.

Browne, Rev. T. H.

Coke, R. G., Esq.

Crawford, J. C., Hsq.

Damon, R., Esq.
DuSautoy, J. B. A., Esq.
Eversley, Viscount.
Hamand, A. 8., Esq.
Percy, Dr. J.

Radcliffe, J., Esq.
Readwin, T. A., Esq.

Non-contributeng Fellows (17).

Bland, T., Esq.

Brand, G., Esq.
Fisher, J. C., Esq.
Floyer, J., Esq.
Hawkins, T., Esq.
Hertzog, W. F., Esq.
Jennings, F. M., Esq.
Knowles, Rev. J.
Lingwood, R. M., Esq.

McConnell, D. C., Esq.
Mayo, H., Esq. :
Mortimer, W. H., Esq.
Murray, W., Esq.

Nicholson, C., Esq.

Philpot, Ven. Archdeacon B.
Turner, Rev. W.

Watson, Dr. J. G. W.

Foreign Members (2).

Dechen, Herr H. von.

| Meneghini, Prof. G.

Foreign Correspondents (3).

Bellardi, Prof. L.
Lesquereux, Prof. L.

Seguenza, Prof. G.

18 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Fettows Rrstenep (13).

Bourne, A. A., Esq. Meaden, H. P., Esq.
Colebrooke, Sir T. E. Morgan, J. A., Esq.
Dresser, C. L., Esq. Plant, James, Esq.
Eastwood, C., Esq. Robinson, R., Esq.
Gaskin, D. M. F., Esq. Sylvester, J. H., Hsq.
Longe, F. D., Esq. Willacy, Rev. T. R., Esq.

Mackintosh, D., Esq.

Frttows Removen (5),

Brunt, E., Esq. Parnell, G. T., Esq.
Hausler, Dr. R. Wilson, Dr. W. H.
Holme, H. 8., Esq.

The following Personages were elected from the List of Foreign Oor-
respondents to fill the vacancies in the List of Foreign Members
during the year 1889.

Professor Ferdinand Fouqué, of Paris.
Marquis Gaston de Saporta, of Aix-en-Provence.
Professor Karl Alfred von Zittel, of Munich.

The foliowing Personages were elected Foreign Correspondents during
the year 1889.

Professor G. K. Gilbert, of Washington, U.S.A.
Mons. A. Michel-Lévy, of Paris.

Doctor Hans Reusch, of Christiania.

Professor Antonio Stoppani, of Milan.

Mons. R. D. M. Verbeek, of Padang, Sumatra.

ANNUAL REPORT. 19

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

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

It was afterwards resolved :—

That the thanks of the Society be given to Dr. W. T. Blanford,
retiring from the office of President.

That the thanks of the Society be given to Dr. J. Evans, Prof.
T. M*Kenny Hughes, Prof. J. W. Judd, and Prof. J. Prestwich,
retiring from the office of Vice-Presidents.

That the thanks of the Society be given to W. H. Hudleston,
Esq., retiring from the office of Secretary.

That the thanks of the Society be given to Prof. T. M°Kenny
Hughes, Prof. J. W. Judd, Prof. J. Prestwich, Prof. H. G. Seeley,
and the Rev. H. H. Winwood, retiring from the Council.

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

20 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

OFFICERS.

PRESIDENT.
A. Geikie, LL.D., F.R.S.

VICE-PRESIDENTS.

Prot. T. G. Bonney, DiSe., Vi.) Boas,
L. Fletcher, Esq., M.A., F.R.S.
W. H. Hudleston, Esq., M.A., F.R.S.

J. W. Hulke, Esq., F.B.S.

SECRETARIES.

UH Hei ae EES:
J. EK; Marr, Esq., M.A-

FOREIGN SECRETARY.
Sir Warington W. Smyth, M.A., F.R.S.

TREASURER.

|
:

Prof. T. Wiltshire, M.A., F.L.S.

COUNCIL.

Prof. J. F. Blake, M.A.

W. T. Blanford, LL.D., F.R.S.

Prof. T.'G. Bonney, Disc. uD;
F.RS.

James Carter, Esq.

John Evans, D.C.L., LL.D., F.R.S.

L. Fletcher, Esq., M.A., F.R.S.

A. Geikie, LL.D., F.RB.S.

Prof. A. H. Green, M.A., F.R.S.

A. Harker, Esq., M.A.

a? Hicks, Mies EES.

Rev. Edwin Hill, M.A.

W.H. Hudleston, Esq., M.A., F.R.S.

J. W. Hulke, Esq., F.R.S.

Major-Gen. C. A. M*Mahon.

J. KE. Marr, Esq., M.A.

H. W. Monckton, Esq.

K. Tulley Newton, Esq.

F. W. Rudler, Esq.

Sir Warington W.
FBS:

W. Topley, Esq., F.R.S.

Rey. G. F. Whidborne, M.A.

Prof. T. Wiltshire, M.A., F.L.S.

H. Woodward, LL.D., F.R.S.

Smyth, M.A.,

ANNUAL REPORT,

LIST OF
THE FOREIGN MEMBERS

OF THE GEOLOGICAL SOCIETY OF LONDON, ry 1889,

Date of
Hlection.

1827. Dr. H. von Dechen, Bonn. (Deceased.)
1848. James Hall, Esq., Albany, State of New York, U.S.A.
1851. Professor James D. Dana, New Haven, Connecticut, U.S.A.
1853. Count Alexander von Keyserling, Raykull, Russia.
1856. Professor Robert Bunsen, For. Mem. R.8., Hezdelberg.
1857. Professor H. B. Geinitz, Dresden.

1859. Dr. Ferdinand Romer, Breslau.

1866. Dr. Joseph Leidy, Philadelphia, U.S.A.

1867. Professor A. Daubrée, For. Mem. R.S., Paris.

1871. Dr. Franz Ritter von Hauer, Vienna.

1874. Professor Alphonse Favre, Geneva.

1874. Professor EK. Hébert, Pars.

1874. Professor Albert Gaudry, Pars.

1875, Professor Fridolin Sandberger, Wiirzburg.

1875. Professor F. August Quenstedt, Tiibengen. (Deceased.)
1876. Professor E. Beyrich, Berlin.

1877. Dr. Carl Wilhelm Giimbel, Munich.

1877. Dr. Eduard Suess, Vienna.

1879. Major-General N. von Kokscharow, St. Petersburg.
1879. M. Jules Marcou, Cambridge, U.S.A.

1879. Dr. J. J. 8. Steenstrup, For. Mem. R.S., Copenhagen.
1880. Professor Gustave Dewalque, Liége.

1880. Baron Adolf Erik Nordenskidld, Stockholm.

1880. Professor Ferdinand Zirkel, Lezpzzgq.

1882. Professor Sven Lovén, Stockholm.

1882. Professor Ludwig Riitimeyer, Basle.

1888. Professor J. S. Newberry, New York, U.S.A.

1883. Professor Otto Martin Torell, Stockholm.

1884. Professor G. Capellini, Bologna.

1884. Professor A. L. O. Des Cloizeaux, For. Mem. R.S., Paris.
1884, Professor G. Meneghini, Pisa. (Deceased.)

1884. Professor J. Szabé, Pesth.

1885. Professor Jules Gosselet, Zidle.

1886. Professor Gustav Tschermak, Vienna.

1887. Professor J. P. Lesley, Philadelphia, U.S.A.

1887. Professor J. D. Whitney, Cambridge, U.S.A.

1888. Professor Pierre J. van Beneden, Louvain.

1888. Professcr Eugéne Renevier, Zausaune.

1888. Baron Ferdinand von Richthofen, Berlin.

1889. Professor Ferdinand Fouqué, Paris.

1889. Marquis Gaston de Saporta, Adx-en-Provence.

1889. Professor Karl Alfred von Zittel, Munich.

21

22 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
LIST OF
THE FOREIGN CORRESPONDENTS

OF THE GEOLOGICAL SOCIETY OF LONDON, rn 1889.

Date of
Election.

1863. Dr. F. Senft, Evsenach.

1864. Dr. Charles Martins, Montpellier.

1866. Professor Victor Raulin, Montfaucon d’ Argonne.
1866. Baron Achille de Zigno, Padua.

1872. Herr Dionys Stur, Vienna.

1874, Professor Igino Cocchi, Florence.

1874. M. Gustave H. Cotteau, Aaverre.

1874. Professor G. Seguenza, Messina. (Deceased.)
1874. Dr. T. C. Winkler, Haarlem.

1877. Professor George J. Brush, New Haven, U.S.A.
1879. M. Edouard-Dupont, Brussels.

1879. Dr. Emile Sauvage, Boulogne-sur-Mer.

1880. Professor Luigi Bellardi, Turin. (Deceased.)
1880. Professor Leo Lesquereux, Columbus, U.S.A. (Deceased.)
1880. Dr. Melchior;Neumayr, Vienna. (Deceased.)
1880. M. Alphonse Renard, Ghent.

1881. Professor,;E. D. Cope, Philadelphia, U.S.A.
1882. Professor;Louis Lartet, Towlouse.

1882. Professor Alphonse Milne-Edwards, Paris.
1884. Dr, Charles Barrois, Lille.

1884. M. Alphonse Briart, Morlaniwelz.

1884. Professor Hermann Credner, Leipzig.

1884. Baron C. von Ettingshausen, Gratz.

1884. Dr. E. Mojsisovics von Mojsvar, Vienna.
1885. Professor G. Lindstrém, Stockholm.

1885. Dr. A. G.ENathorst, Stockholm.

1886. Professor HB. Rosenbusch, Hetdelbery.

1886. Professor J. Vilanova y Piera, Madrid.
1887. Senhor J. F. N. Delgado, Lisbon.

1887. Professor A. Heim, Zurich.

1887. Professor A. de[Lapparent, Paris,

1888. Professor W. C. Brogger, Stockholm.

1888. M. Charles Brongniart, Paris.

1888. Professor Kdward Salisbury Dana, New Haven, U.S.A.
1888. Professor Anton Fritsch, Prague.

1888. M. Ernest Van den Broeck, Brussels.

1889. Professor G. K. Gilbert, Washington, U.S.A.
1889, M. A. Michel-Lévy, Paris.

1889. Dr. Hans Reusch, Christiania.

1889. Professor Antonio Stoppani, Milan.

1889. M. Rh. D. M. Verbeek, Padang, Sumatra.

ANNUAL REPORT. 23

AWARDS OF THE WOLLASTON MEDAL

UNDER THE CONDITIONS OF THE ‘‘ DONATION FUND”?

ESTABLISHED BY
WILLIAM HYDE WOLLASTON, M.D., F.R.S., F.G.S., &c.

“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.
1835.

Mr. William Smith.
Dr. G. A. Mantell.

1861.
1862.

Professor Dr. H. G. Bronn.
Mr. R. A. C. Godwin-Austen.

1836. M. Louis Agassiz. 1863. Professor Gustav Bischof.
1837 cae T. P. Cautley. 1864. Sir R. I. Murchison.
* | Dr. H. Falconer. 1865. Dr. Thomas Davidson.

1838. Sir Richard Owen. 1866. Sir Charles Lyell.
1839. Professor C. G. Ehrenkerg. 1867. Mr. G. Poulett Scrope.
1840. Professor A. H. Dumont. 1868. Professor Carl F. Naumann.

1841.
~ 1842.

1848.

1844.
1845.

M. Adolphe T. Brongniart.

Baron L. von Buch.

ies Elie de Beaumont. —
M. P. A. Dufrénoy.

Rev. W. D. Conybeare.

Professor John Phillips.

1869.
1870.
1871.
1872.
1873.
1874.

Dr. H. C. Sorby.

Professor G. P. Deshayes.
Sir A. C. Ramsay.
Professor J. D. Dana.

Sir P. de M. Grey-Egerton.
Professor Oswald Heer.

1846. Mr. William Lonsdale. 1875. Professor L. G. de Koninck.
1847. Dr. Ami Boué. 1876. Professor T. H. Huxley.
1848. Rev. Dr. W. Buckland. 1877. Mr. Robert Mallet.

1849.

Professor Joseph Prestwich.

1878.

Dr. Thomas Wright.

1850. Mr. William Hopkins. 1879. Professor Bernhard Studer.
1851. Rey. Prof. A. Sedgwick. 1880. Professor Auguste Daubrée.
1852. Dr. W. H. Fitton. 1881. Professor P. Martin Duncan,
1853, | M. le Vicomte A. d’Archiac. | 1882. Dr. Franz Ritter von Hauer.
M. E. de Verneuil. 1883. Dr. W. T. Blanford.

1854. Sir Richard Griffith. 1884. Professor Albert Gaudry.
1855. Sir H. T. De la Beche. 1885. Mr. George Busk.

1856. Sir W. E. Logan. 1886. Professor A. L. O. Des

1857.

M. Joachim Barrande.

Cloizeaux.

1858 j Herr Hermann von Meyer. | 1887. Mr. J. Whitaker Hulke.
* | Mr. James Hall. 1888. Mr. H. B. Medlicott.
1859, Mr. Charles Darwin. 1889. Professor T. G. Bonney.

1860.

Mr. Searles V. Wood.

VOL. XLYI.

1890.

Professor W. C. Williamson,

¢

24

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

AWARDS

OF THE

BALANCE OF THE PROCEEDS OF THE WOLLASTON
“ DONATION-FUND.”

1831.
1833.
1854.
1835.
1836.
1838.
1839.
1840.
1841.
1842.
1843.
1844.
1845.
1846.
1847.

1848.

1849.
1850.
1851.
1852.
1855.
1854.
1855.
1856.
1857.
1858.
1859.

1860.
1861.

Mr. William Smith.

Mr. William Lonsdale.
M. Louis Agassiz.

Dr. G. A. Mantel.
Professor G. P. Deshayes.
Sir Richard Owen.
Professor C. G. Ehrenberg.
Mr. J. De Carle Sowerby.
Professor Edward Forbes.
Professor John Morris.
Professor John Morris.
Mr. William Lonsdale.
Mr. Geddes Bain.

Mr. William Lonsdale.
M. Alcide d’Orbigny.

Cape-of-Good-Hope Fossils.

M. Alcide d’Orbigny.
Mr. William Lonsdale.
Professor John Morris.
M. Joachim Barrande.
Professor John Morris.

Professor L. G. de Koninck.

Dr. 8. P. Woodward.

Drs. G. and I. Sandberger.

Professor G. P. Deshayes.

Dr. S. P. Woodward.

Mr. James Hall.

Mr. Charles Peach.
Professor T. Rupert Jones.

tent W. K. Parker.

Professor A. Daubrée.

1862.
1863.
1864,
1865.
1866.
1867.
1868.
1869.
1870.
1871.
1872.
1873.
1874.
1875.
1876.
1877.
1878.
1879.
1880.
1881.
1882.
1885.
1884.
1885.
1886.
1887.
1888,
1889.
1890.

Professor Oswald Heer.
Professor Ferdinand Senft.
Professor G. P. Deshayes.
Mr. J. W. Salter.

Dr. Henry Woodward.
Mr. W. H. Baily.

M. J. Bosquet.

Mr. W. Carruthers,

M. Marie Ronault.

Mr. R. Etheridge.

Dr. James Croll.
Professor J. W. Judd.

Dr. Henri Nyst.

Mr. L. C. Miall.

Professor Giuseppe Seguenza.
Mr. R. Etheridge, Jun.
Professor W. J. Sollas.
Mr. 8. Allport.

Mr. Thomas Davies.

Dr. R. H. Traquair.

Dr. G. Je inde:

My. John Milne,

Mr. E. Tulley Newton.
Dr. Charles Callaway. -
My. J. S. Gardner.

Mr. B. N. Peach.

Mr. J. Horne.

Mr. A. Smith Woodward.
Mr. W. A. E. Ussher.

ANNUAL REPORT. 25

AWARDS OF THE MURCHISON MEDAL

AND OF THE

PROCEEDS OF “THE MURCHISON GEOLOGICAL FUND,”
ESTABLISHED UNDER THE WILL OF THE LATE

SIR RODERICK IMPEY MURCHISON, Barr., F.R.S., F.G.S.

“To be applied in every consecutive year in such manner as the Council
of the Society may deem most useful in advancing geological science,
whether by granting sums of money to travellers in pursuit of know-
ledge, to authors of memoirs, or to persons actually employed in any
inquiries bearing upon the science of geology, or in rewarding any
such travellers, authors, or other persons, and the Medal to be given
to some person to whom such Council shall grant any sum of money
or recompense in respect of geological science.” |

1873. Mr. William Davies. Medal. | 1883. Professor H. R. Goppert.

1875. Professor Oswald Heer. Medal.

1874. Dr. J. J. Bigsby. Medal. 1883. Mr. John Young.

1874, Mr. Alfred Bell. 1884. Dr. H. Woodward. Medal.

1874, Professor Ralph Tate. - 1884, Mr. Martin Simpson.

1875. Mr. W. J. Henwood. Medal. | 1885. Dr. Ferdinand Romer.

1875. Professor H. G. Seeley. Medal.

1876. Mr. A. R. C. Selwyn. | 1885. Mr. Horace B. Woodward.
Medal. 1886. Mr. W. Whitaker. Medal.

1876, Dr. James Croll. 1886. Mr. Clement Reid.

1877. Rev. W. B. Clarke. Medal. | 1887, Rev. P. B. Brodie. Medal.

1877. Professor J. F. Blake. 1887, Mr. Robert Kidston.

1878. Dr. H. B. Geinitz. Medal. 1888. Professor J. S. Newberry.

1878. Professor C. Lapworth. Medal.

1879. Professor F. M‘Coy. Medal. | 1888, Mr. E. Wilson.

1879. Mr. J. W. Kirkby. | 1889. Professor James Geikie.

1880. Mr. R. Etheridge. Medal. Medal.

1881. Professor A.Geikie. Medal. 1889. Mr. Grenville A. J. Cole.

1881. Mr. F. Rutley. 1890, Professor Edward Hull.

1882. ProfessorJ.Gosselet. Medal. Medal.

1882. Professor T. Rupert Jones. 1890. My. E. Wethered.

c2

26

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

AWARDS OF THE LYELL MEDAL

AND OF THE

PROCEEDS OF THE “LYELL GEOLOGICAL FUND,”

ESTABLISHED UNDER THE WILL AND CODICIL OF THE LATE
SIR CHARLES LYELL, Bart., F.R.S., F.G.S.

The Medal “to be given annually” (or from time to time) “as a mark of
honorary distinction as an expression on the part of the governing
body of the Society that the Medallist (who may be of any country
or either sex) has deserved well of the Science,’—“not less than
one third of the annual interest [of the fund] to accompany the
Medal, the remaining interest to be given in one or more portions at
the discretion of the Council for the encouragement of Geology or
of any of the allied sciences by which they shall consider Geology
to have been most materially advanced, either for travelling expenses
or for a memoir or paper published, or in progress, and without refer-
ence to the sex or nationality of the author, or the language in which
any such memoir or paper shall be written.”

1876.

1877.
1877.
1878.
1878.
1879.

1879.
1879.
1880.
1880.
1881.
1881.
1881.
1882.
1882.
1882.
1883.
1883.

Professor John Morris.
Medal.
Dr. James Hector. Medal.

Mr. W. Pengelly.
Mr. G. Busk. Medal.
Dr. W. Waagen.

Professor Edmond Hébert.

Medal.
Professor H. A. Nicholson.
Dr. Henry Woodward.
Mr. John Evans. Medal.
Professor F. Quenstedt.
Sir J. W. Dawson. Medal.
Dr. Anton Fritsch.
Mr, G. R. Vine.
Dr. J. Lycett. Medal.
Rey. Norman Glass.
Professor C. Lapworth.

Dr. W.B. Carpenter. Medal.

Mr. P. H. Carpenter.

1883.
1884.
1884.
1885.

1885,
1886.
1886.
1887.
1887.
1888.

1888.
1888.
1889.

1889.
1890.

1890.

M. E. Rigaux.

Dr. Joseph Leidy. Medal.

Professor Charles Lapworth.

Professor H. G. Seeley.
Medal.

Mr. A. J. Jukes-Browne.

Mr. W. Pengelly. Medal.

Mr. D. Mackintosh.

Mr. Samuel Allport. Medal.

Rev. Osmond Fisher.

Professor H. A, Nicholson.
Medal.

Mr. A. H. Foord.

Mr. T. Roberts.

Professor W. Boyd Dawkins.
Medal.

M. Louis Dollo.

Professor T. Rupert Jones.
Medal.

Mr. C. Davies Sherborn.

ANNUAL REPORT. Ae

AWARDS OF THE BIGSBY MEDAL,
“FOUNDED BY

Dr. J. J. BIGSBY, F.B.S., F.GS.

To be awarded biennially “as an acknowledgment of eminent services
in any department of Geology, irrespective of the receiver’s country ;
but he must not be older than 45 years at his last birthday, thus
probably not too old for further work, and not too young to have done

much.”
1877. Professor O. C. Marsh. 1885. Professor Alphonse Renard.
1879. Professor E. D. Cope. 1887. Professor Charles Lapworth.
1881. Dr. C. Barrois. 1889. Mr. J. J. Harris Teall.

1883. Dr. Henry Hicks.

AWARDS OF THE PROCEEDS OF THE BARLOW-
JAMESON FUND,

ESTABLISHED UNDER THE WILL OF THE LATE
Dr. H. C. BARLOW, F.G.S.

“The perpetual interest to be applied every two or three years, as may
be approved by the Council, to or for the advancement of Geological
Science.”

1880. Purchase of microscope. 1884, Professor Leo Lesquereux.
1881. Purchase of microscope lamps. | 1886. Dr. H. J. Johnston-Lavis.
1882. Baron C. von Ettingshausen. | 1888. Museum.

1884. Dr. James Croll. 1890. Mr. W. Jerome Harrison.

28 j PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Estimates for

INCOME EXPECTED.

Compositions sevice sews aie ane ae ake a aang ae tere ea 189 0" OD
Due for Arrears of Admission-fees .......... 75 12 0
Admigsion-fees;, 16907... wey Gee eee eee ake 252 0.0
— $2712 0
Due for Arrears of Annual Contributions ..............6- 105 O O
Annual Contributions, 1890, from Resident Fellows, ad
Non-residents;(1859"to T8619 we Md eae ae ee ee 1600 0 0
Annual Contributions imjadvance yei')).0 Jee. os lene ees 42 0 0
Dividends on Consolidated 22 per Cents. ............5.45 238 12 8
Sale of Quarterly Journal, including Longman’s
ACEOUME, 2 J so bet he Sihenalete cauaae Ruageren tena) oka ane oat 165 0 0
Sale of Geological Map, including Stanford's
QCCOUTE® rear oie eich teeters ie oe eer ap ee tettet tetas LO. kr)
Sale of Transactions, Library-catalogue, Orme-
rod’s Index, Hochstetter’s New Zealand, and
Thistror Bellows s7 sass ago poe eee tenet ao 0 0
——— 178 0 0
£2680 4 8

THOMAS WILTSHIRE, Treas.
25 January, 1890.

FINANCIAL REPORT.

the Year 1890.

“20

EXPENDITURE ESTIMATED.

House Expenditure:

MPS Cees tani sew ak sinccls osiotensonecsenedde

FiEMinIre AMG! TEPAlNS....-.-ec.serecssreens sees
House-repairs and Maintenance.................
PMC LEANING 2. a0 moan cacrceciaensaeiasaeene s
Washing and Sundries........... ne eee io maee
Hiab WUCCUIMOS! 22. \scceecnncungcieiinan-selimpic'ess

Salaries and Wages:

PMs oU stan OECKOLALY o..0 1s oss -eewnceneseterncsemend

Assistants in Library, Office, and Museum

MANGAS EM OUCVGATO fic)acicidacz cece vaste ssesccsceavecduccs
eM GMEse NATO A Wh. Swe eee cdecaceeesso sce ceccecuetes
LEIP RCO! 10 ae Soe ae eee
Charwoman and Occasional Assistance........
mttendants at Meetings .......ccssesecsensenes sce
BARa Ce GHUMMMICATM iy eta a sree aisle nieve os vacua aia wcleeieikctahoatalea ts

Official Expenditure :

BAO MO yaar deci a tot cache da dinate Svinte «ioiye'thenat
MinscellAMEOUSHE TING - ......)..c..ccec-seneeseve
Postages and other Expenses ....................

PAUP IS? 5 5 Gt ANE Se OR eng Se oe ae
“ALINGISTIASL 4 Ree eee ne Ee ee Sa

Publications :
Geological Map ..... BE NEE SEE lean SS
ymameberly; HOUMA 5.25, .c. acls eats cdivncsceontedee
. a Commission, Postage,
Amal AdciressinNen iss). cs sncsevaenemesnee ones
Nitsis OE CLO WIS: ib emaiss satvicqe-cass aacscnsonese renin

Abstracts, including Postage ..................
OMCTOMS LNACK: 10, ares es eaeack eee eet eene se

a5 KS OR LC Gye

TS "OM

Sela 20. 10

130% 0) 20

ao aoe O

120 70.0

Sjale 10) CO

Sate

LQ! 493150

. 10 0
IO On O

350050, 20

240 0 O

MOTs

. 40 0 0

48 0 0

2 benOea0

pin Be-r() ce)

10 10 O
8296 10 0

. 288 0 0

x, 40 :.0.40

O00 0120

oes 58, 0) 0

ule aps 160 0 O

SAW yea 5 0 0

DOR On O

1000 0 0

100 0 O

230 O

110 0 0

30 0 0

ee GR

Ney goats 36 14 8

£268) 4 8

30° PROCEEDINGS OF THE GEOLOGICAL SOCTETY.

Income and Expenditure during the

RECEIPTS.
£ & dd. 2) oe
Balance in Bankers’ hands, 1 January 1889. 232 6 0
Balance in Clerk’s hands, 1 January 1889. 16 6 5
—— 248 12 5
Compositions’: 2 2 OOP aie eee tee 189,00 0
Arrears of Admission-fees.............. 9410 0O
Admission=tees, USS) 4+. sa aie ete 20 AO A
——_——— 384 6 0
Arrears of Annual Contributions:.....4. « - ep Bee eee 1385 138 6
Annual Contributions for 1889, viz.:
Resident Fellows ........ Lbs 00
Non-Resident Fellows ... 12: 1S" a0
. _ 1587-18: 70
Annual Contributions, im advance... aesnssycusee ays eae 41 9 6
Dividends on 22 per cent. Consolidated Stock........ 245 6 11

Taylor & Francis: Advertisements in Journal, Vol.44.. 310 3
Publications :

Sale of Journal, Vols) Y=44 “Ors... eh. ceesne 89 14 3

“ Vola n ewe 73 4 0
Sale of Library Catalogue ...............08.00 bn 0
Sale of Geological Map: ......ccessenaeessooe cee 2 UG. al
Sale of Ormerond’s Index... .cc.sesscisheva-0ce t 4 Pt
Sale of Hochstetter’s New Zealand ......... Oo rae
Sale orm Era SacriOns. «wissewceeecannccenvuanece de 1 0-30
Sale of List of Fellows ...... See ee ee Oni3 iO

188) 1G

*Due from Messrs. Longmans, in addition to the
above, on Journal, Vol. 45, &.........scceseeeesee Ghd: «1

£3024 6 8

We have compared this statement
with the Books and Accounts presented
to us, and find them to agree.

(Signed) H. BAUERMAN,
HORACE W. MONCKTON,
28 January, 1890.

! Auditors.

—

FINANCIAL REPORT. 31
Year ending 31 December, 1889.
EXPENDITURE.
House Expenditure: Lees. a a 3 Soe 0s
AM Tre RE EL EP se leie eon foes saisucls ove sewsieeitaiesep'eae PANS MO) a0)
MAME OMSL ANNCE. too 4 ot an tiidea ssi vintslecies sialelewiete seed 1)
ETTIS -copodaget Cee eee ae eee eee ene 28 11 0
HU PPP Rce ee ice cieele abel hae ae «alesis acces cruclegemien A SYD)
MAUS ANG IEPAINS). ....:0.conereccceasseaeane sy ae ee)
Nese ECP AIES: 1, « ccisiae vckdawsiona dacs sions sate somes LO
EMMA MO LOA MITE”. ) far .c eee c wabecde sesso eS
PVashne and Sundries in... s.cccness-.ceesesees 34 10 3
Merona MCOLINGS. 61 fe. exaeccestececeinees Randonee kidn OO
—_——._ 204 5 8
Salaries and Wages:
PASISPAING ECEOUALY (atic de vali a cuisine cavena ruin 390 0 0
Assistants in Library, Office, and Museum... 240 O O
His MSE ROUC WANE see acts ale cee ne iclewnleinneie lew chuee of 105 0 0
PESTS SMTA io Sot. ott wia amis nlee s ccjemisnieine ofidiie's oles «3 40 0 O
ATE ATMOMS OY van sncless oisclas's fa orsasne seein naan cesses 45 12 0
RE IePECOUINENTN | 1. Se ie wane 2 fs 6 sie. a diernc'sin sie ov ole oictieiec 2411 4
Mitendants at Meetings........cessseccccecsoersoe on oO)
PrecommMiamiis: He (2. .csc.ssstneedesceenseeeseeve 0 6
———._ 827 18 10
Official Expenditure :
MIME eects ca Seer va cats tslea eh evinniea seis vores 28 13 6
MiScollancous Printings. 1... ced. csnevecceneess 83 138 0
Pestages and other Expenses ...............+4. 106 15 6
ee 219) (20
L220G)., OG SOS OE Ve cn ce rrnnee is Le Ope
OLDE ooo Sed no ee ee 146 4 0O
MOSS EDITE . oo) 2S a a Se oe eee 5 + 5
Publications :
reo CAC NAD, | is. dadeee cece cei eSecijedasnend ss Lome: of
Gourmal, Vols: 144... i. ccc scoecccctacesscaces 97 78
PP WIE AO te. Seah ois wind 880 4 8
», Commission,
Postage, and Addressing. 105 6 O
——-—_ 985 10 8
HOY OMe LOW Sis eB cetcycd Me kssseklacdsnanre cece ee 33.12 7
Abstracts, including Postage Le PB ieee 109 16 1
——_—— 1158 1 4
Investment in £200 Consolidated 22 per
PETER SEOCK, AGO! Pie sebs.. ace wild Ae lose Meee vik 5 & 198 5. 6
Balance in Bankers’ hands, 31 Dec. 1889..238 5 0 )
Balance in Clerk’s hands, 31 Dec. 1889 .. 10 19 1
—_——_ 249 4 1
£3024 6 8

THOMAS WILTSHIRE, Treasurer.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

32

OEE OR GT = ©

0 SL F9F

ag ea cg a

Ge St lg

.

' 68°81 ‘Taq uLede(T Ig ‘ stoyueg Pe QOUBT VT SC aleue coe ree

‘SINAWAV

G LI LEF

QO PL Ciiecrtr st ests tere eeeeeeeseeerees yon paqep
-I[OSuOy *4u90 ted § 8G UL poysoaut puny oy} Uo spueptatq

“gggT ‘Aivnuee | ‘Sloyuvg }B oouvypesp
pins ote ‘SLAITOaY

“ENQDOOOY IsaUy, .,,dNaq NOSanve-MOTUVG ,,

G8RT ‘req m1800( 1g ‘stoyueg ye soured
eee ee eee ves age eee Dee 809)
Lp ee Se Ola smno'T W

[epeyy WIA ‘sunpaeq pAog ‘AQ ‘Jorg 07 prray

‘SINGNWAV

9 GL GLLF

0 SL BQ CEE eee tere eees eee sgo1g aaa
aed Se uvyzrodomey Ul pejsoAut pun a 9} WO spuoprlayy

9 L TG “tt tst tte gge7 “Arenuee T ‘sroyneg 48 soneped

| De eas ‘SLAIHO GY

“INNOODY LsaAry, ¢ GNOW TVOINOTOUY) TIAA'T ,,

GRST ‘tequmoveq, TE ‘sxoyuvg 4v vourleq
Pees eee ceressssss" TUpaHAy JO 9809)
"888100 *f "Y STAUeTD “1

" [Ppa WIA “Onley “p Jorg 07 preay

‘SINGNAV

“INQOOOYW Lsauy, ,aNAT

GRgT ‘oqureseqT 1g ‘stoyuRg 4v sourreq
"i 7" paBALpoo AA UPTUIg "WY OF precy

OE OL ae ‘KT, "JOT 0} poprvae [Vpof PlOH ouryiazs jo 800

i a 5

"‘SINAIVAV

6 6 8&F

0 0 6E ttt t tT 909g emnquoqocy “yu00 tod F AVApreyy W10}s9 AY
"YON PUB WopuoTy UL poysoAu! PUNT oY} UO spuepralq

$6 6 egel ‘Arenuve [ ‘sroyuug ye souvpeg

ie Ae ie? ‘SLdIMO ayy

TVOINOTOUL) NOSIHOUNTA ,,

0 SI P93

OL, OG ELE EEE EE seen eeees 909g payep
-Ijosuog *ju00 wed £% ut poysoaur pun J 94} Uo spueplatd

ia Tore, ae Ps ans ee Pree Osa ‘Arenuve [ {Stoyueg yv oouvyped

‘D8 F ‘SLAIMO NY

‘INQOOOW ISAUy, ,,,CNOgq NOILVNO( NOLSVTIOM ,,

ise)
9)

FINANCIAL REPORT.

6 L veloy

‘OGST ‘Aimnune Ge
‘sma4T “TAUTHSLILM SVNOHL

6 L vél6s

[‘swornanqng pjosun fo
YO0ps puv ‘aungrusng “hioiguy ‘sworosyoy ay2
{0 anjva ay2 apnjour pou saop aacgn ay,— ‘A |

0 0 GOL *** ‘(00% porepisu0a) suornqiyuog [enuUY jo steer
0 GL GL °°" '°***(poos poreptsu0d) seaz-uolsstupy Jo sreeaty
0 0 898 0 0 0068 **"* 16 78 ‘S}Ue_ sed Fg poxeprosuog

VO ee —: Aqsedorg pepunyy
T 6TOL ‘''' 81 68ST 2° Te ‘spuey s3p1079 Ur eourredy
0 ¢ 8G “'"'"*"* B88T OC, TE “Spuey stoyuvg ur couereg
re ee a ee

‘JOA ‘TVuINof Jo yuUNODDR UO “ORD » URUEsUOTT MOTT oNGT
Ds F ‘KIUILOUg

“688T ‘toqums00q7 [g { ALUTAOUN S,ALAIOOG AHL AO NOMVATV A

GVO 2 6) ee ee ae DO Grol OMmMOAUT Ul oaueTeEy
DS Fx

0 1 38i¢

Le 9-"V ser seeeeresses BQQ7 “requieda, [e ‘sloyURT 4e souLT eg
GC PL SL TOL HL ‘£ ‘AW 0} poprwme [epopy ploy curyrtys Jo yo
SSS ‘ ‘SINTWAV

‘INNOODDY tsa,

Oe le

eae @ ue Soe UC Sees te ee eee OIC SIE D
-TJostoy) “yuo rod FZ UL poySoAUL pun, oy} WO spuoeprarq

OiaG. alee es POETS ele | ‘Crenuee I ‘ sto uege ye aourpeg

BOS Fog "‘SLdIMO ayy

( UNO AGSHI ,,

34 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

AWARD or tHE WoLLAston MEDAL.

In handing the Wollaston Medal to Prof. J. W. Jupp, F.R.S.,
for transmission to Prof. W. Crawrorp Wiutiramson, F.R.S., the
PresipEnt addressed him as follows :—

Professor J upp,—

The Council have awarded the Wollaston Medal for the present
year to Prof. W. C. Williamson, in recognition of his researches in
Paleontology, and especially of the series of important papers in
which he has described the structure of the plants that have contri-
buted to the formation of coal, His investigations have added
greatly to our knowledge of the Carboniferous flora, and have enabled
us to form a much clearer idea of the plant-life in those far distant
days of the Palzeozoic era than was previously possible. Although
Professor Williamson’s attention has now for many years been espe-
cially devoted to the examination of fossil plants, he had, before his
researches on ancient botany commenced, added many valuable
details to our knowledge of the fossiliferous rocks of Yorkshire and
Lancashire, and he had contributed greatly to the natural history of .
recent and fossil Foraminifera, whilst in a paper published more
than 40 years ago, on some of the microscopical objects found in the
mud of the Levant and other deposits, with remarks on the mode of
formation of calcareous and infusorial siliceous rocks, he antici-
pated many recent discoveries, both as to the part played by minute
calcareous and siliceous organisms in rock-formation, and also as
to the chemical and physical changes to which such organisms are
subject during the conversion of soft deposits into hard stone.

In asking you to transmit this Medal to Professor Williamson, may
I further beg that you will convey to him an expression of our wishes
that he may continue his important studies for many years to come,
and of our regret that his engagements have unavoidably prevented
our having the pleasure of his presence on this occasion.

Prof. Jupp, in reply, read the following communication received
by him from Prof. W1LL1amson :—

‘I need scarcely say that I feel grateful for the honour dcne me
in awarding me the Wollaston Medal; and I trust you will not deem
me presumptuous when I express a hope that it has been won by
conscientious work. Though the rich deposits of fossil plants dis-
covered in the neighbourhood of Scarborough—my native town—

ANNIVERSARY MEETING——-MURCHISON MEDAL. 35

drew my attention to paleobotany at an early age, it was only in
1851 that I commenced the study of their internal organization. I
was led to this by a specimen for which I was indebted to our
distinguished colleague Professor Prestwich, and which enabled me
to interpret the anomalous objects known as Sternbergia. ‘The
success attending this exploration whetted the appetite ; and from
that time until now the organization of the Carboniferous plants has
received my continuous attention. The difficulties impeding my
work, which have been considerable, have chiefly arisen from one
cause. Most of the Carboniferous plants belong to the Cryptogamic
division of the Vegetable kingdom, the only exceptions being some
ancestral forms of the modern Cycads and Conifers. At the present
day these Cryptogams are mainly low herbaceous plants. But forests
and forest-trees were wanted in that primeval age, which want seems
to have been inadequately supplied by the Gymnosperms just re-
ferred to. The want was met by uplifting the now lowly Cryptogams
into Forest giants, and since the stems of these required some orga-
nization additional to that which living Cryptogams possess, to enable
them to sustain their superstructures, they were strengthened for
their work by the same exogenous growth as effects that end among
modern forest-trees. But that any Cryptogams should attain so high
an organization was deemed by most botanists so improbable that
their almost universal voice rejected my views upon the subject.
But the truth has prevailed, and, happily for myself, I have been
spared long enough to witness this end of my labours.”

In conclusion, Prof. Williamson expressed his great indebtedness
to Messrs. Cash, Aitkin, Butterworth, Nield, Earnshaw, Whittaker,
Spencer, Binns, Wild, and Lomax, who have collected the valuable
materials employed by him in his researches.

AWARD oF THE Murcuison MEDAL.

In presenting the Murchison Medal to Prof. KE. Hutn, F.R.S., the
PresipEent addressed him as follows :—

Professor Hvrit,—

In handing to you, who were one of Sir R. Murchison’s colleagues
on the Geological Survey of Great Britain and Ireland, the Medal
founded by him, I shail not attempt to enumerate the many additions
that you have made to our knowledge of the geology of the British

36 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Islands and to geological literature. Your contributions to the
memoirs published by the Survey on various parts of England, and
especially on parts of Gloucestershire, Oxfordshire, Cumberland, ~
Cheshire, and Lancashire, are too well known to need recapitulation ;
and you have done good service to the cause of science by your
treatment of one of the principal geological and economical problems
presented to the Survey in your ‘Coal-fields of Great Britain,’ a
work that has deservedly passed through several editions. You have
aided greatly in the important series of investigations into the
underground distribution of the productive Coal-measurés when
concealed by later unconformable deposits, and you have applied
your extensive field-experience of British rocks to solve the difficult
question of land-distribution in past epochs, and to the elucidation
of the physical geography of the British Islands. or several years
past, whilst holding your present post at the head of the Irish Survey,
you have contributed in very many different parts of the country,
and by the investigation of many distinct rock-formations, to our
knowledge of Irish geology, and by your visit to Palestine you have
been able to throw much light on the geological structure of the
Holy Land.

Prof. Hutz, in reply, said :—

Mr. PREsIDENT,—

I appreciate very highly the honour which you and the Council
have conferred in awarding to me the Murchison Medal. The
gratification I feel is enhanced by the circumstance that this dis-
tinction is associated with the name and memory of the founder,
who was to me a wise and considerate chief as well as a personal
friend.

You have been pleased to refer to my official work on the Geolo-
gical Survey of the United Kingdom, as well as to that of a more
personal nature. It has been my lot to serve under four successive
chiefs, namely, De la Beche, Murchison, Ramsay, and Dr. Geikie,
whose names will ever be associated with the early history and pro-
gress of geological science; and I may truly say that from each
and all I received that encouragement and support which is essential
to the hearty fulfilment of the duties of a public servant ; and I am
glad to have this opportunity of saying that in bringing the Geolo-
gical Survey of Ireland to its completion I have been associated
with colleagues in this work who have combined an earnest desire

ANNIVERSARY MEELING—LYELL MEDAL. 37

to fulfil their duties to the public service with no small amount of
enthusiasm in carrying on scientific investigation. In view of my
pending retirement from this department of the public service, [ am
somewhat consoled by the hope that, in consequence, I may be
enabled, at no distant day, to take a more active part in the work
of this great Society than has hitherto been possible. In conclusion,
I have only to express my thanks to you, Mr. President, for the
kind words in which you have communicated to me the award of
the Council; these will be an incentive to further effort in the cause
of geological investigation.

AWARD OF THE LyELL MEDAL.

The Presrpent then presented the Lyell Medal to Prof. T. Ruprrt
Jonrs, F.R.S., and addressed him as follows :—

Professor Rupert JonEs,—

There is unusual pleasure in presenting one of the chief awards
in the gift of the Council to a geologist who has been so long and
so honourably associated with the Geological Society as yourself,
and the appropriateness of the award is not decreased by the cir-
cumstance that your official connexion with the Society commenced
when the great geologist who founded this medal was President.
Since that time, now forty years ago, you have written much on
various fossil organisms, but especially on Entomostraca and Fora-
minifera, and in many cases, and especially amongst the bivalve
crustaceans of the older rocks, it is largely to your researches that
we are indebted for our present knowledge of the forms. You have
also devoted much time and attention to the geology of South
Africa, and to bringing together the scattered information that we
possess concerning the geology of that interesting region.

In placing the Lyell Medal in your hands I can only add that I
think the Council have carried out the intentions of Sir Charles
Lyell, and that they are justified in believing that, in his words,
“ the Medallist has deserved well of the Science.”

Prof. T. Ruerrr Jonzs, in reply, said :—

Mr. Presipent,—
Acknowledging, with respectful thanks, the unexpected honour
with which the Council, on the part of the Society, has favoured
me, I beg to state that, in following the study of those branches of

38 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

geological science to which opportunity and other circumstances
have led me to give my best attention, I cannot claim to have been”
so successful, or so useful, or deserving of such honourable recogni-
tion as the Council, in their kindness towards an old worker, seem
to have considered me to be.

Thanks to a natural disposition to study both living and fossil
organisms, and to look with confidence for signs of the great Divine
laws governing the earth and all its belongings, my humble part
has been, as far as possible, that of a true ‘“ Minister et Interpres
Naturee.”

No great discovery, however, nor signal success in elucidating the
problems offered for our study, in the organic and the inorganic
world, has been attained by me. Persistent and, may be, an in-
dustrious search among geological facts for their causes and history,
and among fossils, especially microzoa, for evidence of their exact
relationships, to the end that our knowledge of these things should
be more perfect and more useful, has occupied much of my intel-
lectual life.

How far the Foraminifera, Ostracoda, and Phyllopoda have been
already, or willin the future be useful paleontological guides to
the geologist cannot be noticed here.

In all that I have done my work has been my pleasure, and I
can claim no reward for it; and in all that has been good I have
to acknowledge warmly the co-operative help given by W. K. Parker,
J. W. Kirkby, H. B. and G. 8. Brady, Henry Woodward, and C. D.
Sherborn; and in just now completing the Supplemental Mono-
graph of the Cretaceous Entomostraca I have had the kind aid of
G. J. Hinde.

This Medal, Sir, bequeathed by my old and revered friend Sir
Charles Lyell, and the other Awards given so graciously this day by
the Council and yourself, on behalf of the Geological Society, bear
striking and pleasant testimony to the fact that the good deeds of
great and good men live after them.

AWARD OF THE WoLtaston Donation Funp.

The PrestpEnt next presented the Balance of the Wollaston Fund
to Mr. W. A. E. Ussunr, F.G.S., and said :—

Mr. UssHer,—

In connexion with the Geological Survey of the counties of

ANNIVERSARY MEETING——-WOLLASTON DONATION FUND. © 39

Somerset, Devonshire, and Cornwall, it has been your province to
examine many of the rocks exposed, and in addition to your official
work you have contributed several useful accounts of the Paleozoic,
Triassic, and Pleistocene deposits to the Journal of this Society and
to other geological publications. In recognition of the good work
done by you the Council have authorized me to present you with
the balance of the Wollaston Donation Fund.

Mr. Ussuer, in reply, said :—

Mr. PResipENT,—

I thank the Council for the recognition of work this Award im-
plies, and you, Sir, for your allusions to it. Whatever results I
may have obtained in the discharge of my ordinary duties on the
Geological Survey are not deserving of reward. The construction
of maps may be faithfully performed without obtaining results of
moment in the furtherance of geological knowledge ; official require-
ments are so engrossing and imperative as to oblige those who, like
myself, desire to acquire as competent an acqaintance as possible
with the strata on which they are employed, to supplement, by
private work, the information acquired in public duty. The results
obtained by private investigation, whensoever they contribute to the
advancement of our common science, are in themselves rewards.

The result of my twenty years’ experience in geological mapping
is this :—the acquirement of patience ard the entire subordination
of theoretical considerations, which should be the outcome of a
careful study, collation and comparison of details, and not the
working hypothesis to weld them into system during or before the
progress of the work.

This principle I have had to keep in view in Pleistocene work,
in dealing with a variable and disturbed series of Triassic rocks,
and to a still greater extent in dealing with fossiliferous rocks such
as the Lias, Oolites, Carboniferous, and Devonian. I have learned
the extreme importance of Paleontology in investigating disturbed
paleeozoic areas, where it appears to me that the evidences of fossils
and of stratigraphy should be taken together, and without subordi-
nating the one, as a mere adjunct, to the other.

VOR. XLVI. ad

40 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

AWARD oF THE Murcuison GrEotogicaLt Funp.

In presenting the Balance of the Murchison Geological Fund to
Mr. E. Wertueren, F.G.S., the Presipent addressed him as follows:—

Mr. WEtHERED,—

The remainder of the Murchison Donation Fund has been awarded
to you by the Council of this Society on account of the researches
you have undertaken into the microscopic structure of sedimentary
rocks, and to aid you in prosecuting further inquiries. The results
of your examination of the insoluble residues obtained from the Car-
boniferous Limestone, and of the remarkable minute tubular forms
(apparently organic) from various limestones, that you have ascribed
to Girvanella, are of great interest, and have furnished an important
contribution to our knowledge of the manner in which Paleozoic and
Mesozoic limestones have been formed.

Mr. WerHeERED, in reply, said :—
Mr. PresrpEnt,—

I desire to express to the Council my thanks for the honour done
me in making me the recipient of the Murchison Fund for the year.
This kind consideration will greatly encourage me in pursuing that
branch of geological research which I have marked out as one of the
objects of my life. To have done work which merits the acknowledg-
ment of this Society—the first in the world—is one of the greatest
satisfactions a geologist can enjoy.

You have referred to my work on the microscopical examination of
limestones, and I should like to say that in this there is a most im-
portant field open for investigation. If those who have the opportunity
of examining the oldest limestones would do so through the micro-
scope, with due regard in preparing the slides to the optical properties
of the rock, my belief is that our knowledge of the life which existed
at that early period of the earth’s history would be considerably
advanced. ;

I again return my thanks for the honour done me.

ANNIVERSARY MEETING——LYELL GEOLOGICAL FUND. Al

AWARD oF THE LYELL GEOLOGICAL FuND.

The Presrpent then presented the Balance of the Lyell Geological
Fund to Mr. C. Davizs SHrrBory, F.G.S., and said :-—

Mr. Davies SHERBORN,—

There is no branch of scientific work at the present day that confers
a greater benefit on geologists in general than the recording of geolo-
gical and paleontological literature. Owing to various causes, the
mass of published matter increases yearly ; and as it is impossible for
any one to read all that appears, a heavy debt is due to those who
undertake the arrangement of a key tothe various publications. In
Palaeontology this is even of greater importance than in Geology. In
your recently published ‘ Bibliography of the Foraminifera,’ and in
the Catalogue of ‘ British Fossil Vertebrata,’ published in conjunction
with Mr. Smith Woodward, you have contributed to that important
object the establishment of a general paleontological list with full
references ; whilst in the assistance given to the ‘ Geological Record’
you have done good service to the science for the advancement of
which this Socicty exists. As a mark of the value attached by the
Council to the completion of a general index to paleontological
writings, and as an assistance in the compilation of any portion of
the work that you may undertake, I have much pleasure in pre-
senting to you the Balance of the Lyell Donation Fund.

Mr. SHERBORN, in reply, said :—

Mr. PREsIDENT,—

I must ask you, Sir, to express my thanks to the Council for the
distinction they have shown me in awarding me the Proceeds of the
Lyell Fund. I feel great diffidence in accepting such award, my
work having extended over but few years. Ihave endeavoured to
make that work as perfect as possible, and hope to devote my future
time to bibliographic research. I wish to thank Prof. Rupert Jones
and Mr. Topley for first assistance in my work, and I assure you, Sir,
I shall always labour to make my work more perfect.

a2

42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

AWARD FROM THE BARLOW-JAMESON FuND.

In presenting to Mr. W. Jerome Harrison, F.G.S., a grant from
the Proceeds of the Barlow-Jameson Fund, the Presipmnt addressed
him as follows :—

Mr. Harrison,—

In awarding to you a grant from the Barlow-Jameson Fund, the
Council recognize the value of your endeavours to spread a know-
ledge of Geology by the compilation and publication of hand-books
to the Geology of the Counties in England and Wales. ‘They also
appreciate your geological researches in the Midland Counties, and
trust that the award now made may be of use to you in the prose-
cution of future efforts to extend geological knowledge.

Mr. Harrison, in reply, said :—-

Mr. PRrestpEnt,—

In thanking the Council for the honour they have conferred upon
me, I can only say that their award was as unexpected as it was
welcome. The daily tasks of a necessarily busy life have left me
but little time for original research, and I have done—not what IL
would, but what I could. This recognition of my labours, and the
kind words with which you have accompanied it, will spur me on to
increased endeavours in those studies which the Geological Society
was established to promote.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 43

THE ANNIVERSARY ADDRESS OF THE PRESIDENT,

W. T. Buanrorp, LL.D., F.R.S.
GENTLEMEN,

In accordance with the customary practice, I shall commence
this Address with brief notices of some of the members of our
Society who have died during the past twelve months. Our
losses from the list of Ordinary Fellows have not been exceptional,
though we miss several valued and familiar names from our roll,
but some of our most distinguished Foreign Members and Corre-
spondents have gone from amongst us. Among others, we have
to deplore the decease in the same year of the father of the Society,
the Venerable Archdeacon B. Philpot, who joined our body in 1821,
five years before it was incorporated by charter, and of our senior
Foreign Member, Dr. H. v. Dechen, who was elected in 1827.
There is no reasonable doubt that Archdeacon Philpot and Dr. H. v.
Dechen were the two senior members of the Society; a few
names still remaining on the list, with earlier dates of election, are
so retained for want of information, there being no reason to
suppose that such names represent living Fellows.

The Venerable Archdeacon B. Puitpor, to whom I have already
referred as the “father” of the Society, passed away in May last,
at the advanced age of 98. He was born at Laxfield in Suffolk, on
January 9th, 1791, and took his degree at Christ’s College, Cam-
bridge in 18138. He joined this Society in 1821. By Archdeacon
Philpot’s death, Mr. John Murray, of Albemarle Street, who was
elected in 1828, becomes the senior Fellow of the Society.

Rosert Damon, of Weymouth, Dorset, who was born in 1814,
and died May 4th, 1889, became a Fellow of this Society in 1864.
As a large dealer in fossils, minerals, recent shells, and similar
objects, and as an agent for the sale of collections of natural
history, Mr. Damon must have been known to most British
geologists, by whom he was greatly respected. He was a man of
much energy; he travelled extensively; and to his exertions the
British Museum is indebted for several valuable specimens, one of
those most recently procured from him by that institution being
the skeleton of Ahytima. Mr. Damoun’s principal service to geolo-
gical science, apart from his activity in collecting, was the publi-

44 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

cation in 1860 of a work on ‘The Geology of Weymouth and the
Isle of Portland,’ to which Supplements were issued by him in
1864 and 1880, and of which a second edition appeared in 1884.

JoHN Freperick La Trost Bateman, who died on the 10th of
June, 1889, was highly distinguished as a civil engineer, and
especially known by the large works, the construction of which he
had designed or superintended, for the supply of water to towns.
He was born in Ockbrook, Derbyshire, May 30th, 1810, appren-
ticed to a surveyor and mining engineer at Oldham when 15
years of age, and commenced business as an engineer in Man-
chester in 1833. He first became known by his report on the
improvement of the River Bann, in County Down, and by the
works constructed by him in the valley of that stream ; and having
been led by his observations on the relations between the rainfall
and the amount of water drained from different districts to some
important conclusions as to the best sources for the water-supply of
towns, he was engaged for many years upon the reservoirs for the
supply of Manchester, first around Longdendale, and later at Thirl-
mere. It was at his recommendation also that the Corporation of
Glasgow were induced to? obtain a supply of water from Loch
Katrine, and to him is attributed a plan for providing a supply for
London from North Wales. Mr. Bateman’s observations on rain-
fall and outflow have been useful for geological inquiries.

In 1869 Mr. Bateman was present as the representative of the
Royal Society, of which he was elected a Fellow in 1860, at the
opening of the Suez Canal, by invitation of the Viceroy of Egypt.
He was President of the Institution of Civil Engineers for two
years from 1878.

Henry Wittram Bristow, who died on June 14th of last year,
was born May 17, 1817. He became a Fellow of this Society in
1843, and of the Royal Society in 1862. He was the only son of
Major-General H. Bristow, an officer who devoted himself to Spain;
where he died. The son, the subject of the present notice, after
receiving an education at King’s College, joined the Geological
Survey of Great Britain, as Assistant Geologist, under Sir H. De la
Beche, in 1842. Of this survey he remained an active member for
no less than forty-six years, rising gradually in rank until in 1872
he was made Director for England and Wales.

In the course of his long service, Mr. Bristow was chiefly engaged

ANNIVERSARY ADDRESS OF THE PRESIDENT. 45

in field-surveying in the southern counties of England, and it is on
his work as a field-surveyor that his principal title to remembrance
by future geologists rests; for he was one amongst the little band
who brought the geological surveying of sedimentary rocks to a
degree of exactitude and scientific accuracy previously unapproached.
Several of the beautiful longitudinal sections published by the
survey in former years were prepared by him. One of the best
known of the survey memoirs, that giving an account of the
geology of the Isle of Wight, was from his pen. He was also the
joint author, with Mr. W. Whitaker, of a‘ Memoir on the Geology of
part of Berkshire and Hampshire.’ During the last few years
Mr. Bristow was engaged in re-writing his account of the geology
of the Isle of Wight, and this at the time of his death was nearly
ready for publication.

To the Journal of this Society Mr. Bristow contributed but two
papers, one of them a short. note ‘‘ On the supposed Remains of the
Crag on the North Downs near Folkestone ” (Quart. Journ. Geol. Soe.
vol. xxil. p. 553), the other a paper “On the Lower Lias or Lias-
conglomerate of a part of Glamorganshire” (Quart. Journ. Geol.
Soc. vol. xxii. p. 199). Amongst the subjects to which his atten-
tion was particularly directed, was the question of the Rheetic beds
and their British representatives, to which he applied the name of
Penarth beds, at the suggestion of Sir R. Murchison, and of which
he communicated a description to the British Association at Bath in
1864. Apart from his labours in connexion with the Geological
Survey, Mr. Bristow’s best known work is probably his ‘ Glossary of
Mineralogy,’ published in 1861. He also translated several popular
French books by Simonin, Figuier, and others on geology and
mining.

Owing to his deafness, Mr. Bristow but rarely took part in the
meetings of this Society, and he was probably in consequence less
known than he deserved to be. He served on our Council for two
years, from 1866 to 1868. Few men have left behind them a
better record of geological work, or have more thoroughly earned
the respect and esteem of their colleagues.

Joun Prrcy was born at Nottingham on the 23rd of April 1817.
He was the son of a solicitor, and after his early education, studied
medicine in Paris, where he appears to have derived his peculiar
fondness for chemistry from the teaching of Gay-Lussac, Chevreul,
and Thenard. Subsequently he entered the University of Edin-

46 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

burgh, and took the degree of M.D. in 1839, when only 21 years
old. One of his fellow-students at Edinburgh was Edward Forbes, -
afterwards, like Percy, one of the Professors at the School of
Mines.

After leaving Edinburgh, Dr. Percy established himself in medical
practice in Birmingham, became physician to the Queen’s Hospital,
and attained to considerable eminence in his profession. His
election to the Royal Society in 1846 was due to original experi-
ments and researches in pathology. But meantime he was much
engaged in metallurgical and chemical studies, and especially in
investigations upon the properties of nickel and manganese. Some
of his discoveries at this period were the foundation of metallurgical
processes now in extensive use.

On the establishment of the Royal School of Mines in the Jermyn
Street Museum in 1851, Dr. Percy was selected as lecturer on
metallurgy, a post which he held for 28 years, until the removal of
the School to South Kensington in 1879. He gave up the practice
of medicine at the same time as he commenced his metallurgical
lectures. His position as by far the first metallurgical authority in
the country was now acknowledged on all sides, and the work to
which, in addition to his lectures, he devoted the greater part of his
time during the years that he held the Professorship in Jermyn
Street was the production of a great work on metallurgy in general,
At the time when he undertook this, there was no comprehensive
work on the subject in the English language. ‘The first volume of
his ‘ Metallurgy’ appeared in 1861, and contained general con-
siderations on metallurgical processes, a description of fuel and fire-
clay, and the metallurgy of copper, zinc, and brass. ‘The second
volume, which appeared in 1864, was devoted to iron and steel, the
third in 1870, to lead, and the fourth in 1880, to silver and gold.
Part of the first volume was reissued as a second edition in 1875.

It is difficult to over-estimate the importance of this work. A
very large portion consisted of descriptions of metallurgical pro-
cesses from the writer’s own observations, many of these processes
having never been described or only imperfectly described previously,
and all were given with great attention to details, and well illus-
trated with plans and sections of furnaces, &c. ‘The value of the
information may be inferred from the fact that translations of all
the volumes, as they appeared, were published both in French and
German. That this “ magnum opus” has never been completed is
a source of deep regret to all interested in the progress of the
metallurgical art.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 47

Besides his metallurgical works, Dr. Percy wrote several papers
on mineralogy, assaying, &c. His only contribution to the Society’s
publications consisted in a letter to Sir Charles Lyell, giving an
account of the analyses of some American coals, anthracites, &c.,
published in the ‘ Quarterly Journal’ for 1845. Before his attention
was exclusively devoted to metallurgy, Dr. Percy had published
several contributions to medical science. He was also a writer of
great force and originality on social and political questions.

But above all it is as a teacher that our late Fellow is most
warmly remembered by those who, like myself, had the advantage
of hearing the admirable course of lectures that he delivered at the
School of Mines. Rarely in any country, probably never in England,
was a more brilliant and gifted staff brought together for teaching-
purposes than those who, under Sir H. de la Beche, established a
mining school in London in 1851. Amongst the whole of them, as
I can testify from memory, in the unanimous opinion of the
students, Dr. Percy’s lectures on metallurgy, and Sir W. W. Smyth’s
on mining, were pre-eminent for clearness, command of the subject,
and the power of conveying information from the master to the
learner. It is not surprising that Dr. Percy has founded a school
of metallurgy in Britain, and that there is, at present, scarcely a
scientific metallurgist or assayer who has made himself known in
this country by his work who has not passed through Percy’s labo-
ratory and learned science from his teaching. And he was a man
not easily forgotten. Singularly tall, towering by a head over those
around him, spare, yet not weakly built, with strongly-marked
features, and a peculiar but very striking delivery, a good command
of language, and the most perfect originality of ideas, a more
thoroughly impressive and suggestive lecturer could not be found.
That there are at this day able teachers of metallurgy in Britain,
that metallurgical processes are to some extent directed by an
intelligent knowledge of the chemical reactions involved, and not
by the kind of guess-work that so long prevailed, is due to the
influence of our late Fellow and to the instruction given by him.

Dr. Percy was appointed Superintendent of the Ventilation in the
Houses of Parliament in 1865 (February 6), and held the post till his
death. In 1876 the Iron and Steel Institute recognized his services
to metallurgy by awarding to him the Bessemer Medal; and in
1885 he was elected President of the Institute, and, despite failing
health, discharged the duties of the chair with characteristic ability.
~The Howard Prize was presented to him by the Institution of Civil
Engineers in 1887, and, only two days before his death, he received

48 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the award of the Albert Medal from the Society of Arts. It
would be difficult to enumerate all the subjects, artistic, literary,
and scientific, that he studied at various periods of his life, for he
was a man of wide and versatile tastes. Mineralogy, photography,
old prints, and various branches of zoology engaged his attention in
turn, and he has left behind some extensive collections, the most
important of which, consisting of an unrivalled series of metallur-
gical products, have found a resting-place in the collections attached
to the School of Mines, with which so much of the work of his life
was connected.

Dr. Percy joined this Society in 1851, and was a member of the
Council for three years, from 1853 to 1856. He died June 19th,
1889.

The Reverend J. E. Trn1son Woops, who died at Sydney, N.S.W.,
on the 9th October, 1889, studied at Oxford, where he was an
enthusiastic participant in the Tractarian movement. He joined the
Church of Rome, and in 1857 went to Australia for the benefit of
his health. He there undertook missionary work, in which he was
engaged throughout the remainder of his life, being ultimately
appointed Vicar-General of Adelaide. He joined our Society in

1859. ,
Mr. Woods is the author of numerous papers on Australian
geology and paleontology, the greater number relating to Tertiary
fossils ; he also described organic remains from New Guinea, New
Caledonia, the Fiji Islands, and other parts of the Australasian area.
He twice contributed to our Journal, in 1860 and in 1865, both his
communications relating to the Tertiary rocks of South Australia.
He was also the author of several papers on recent mollusca, of a
work in two volumes entitled ‘A History of the Discovery and
Exploration of Australia,’ and of some other books. He was in 1880
President of the Linnean Society of New South Wales.

Tuomas Hawxrns, a native of Glastonbury, where he was born in
1810, was chiefly known by writings on Enaliosaurians, on which
he published two volumes, the best known being ‘ The Book of the
Great Sea-Dragons’ (1840). Mr. Hawkins made several large
collections of Ichthyosaurian and Plesiosaurian remains on the
Dorsetshire coast, and the finest of these collections was purchased
for the British Museum. Other collections were presented by
Mr. Hawkins to Cambridge and Oxford. He died at Ventnor,
Oct. 15th, having been a Fellow of the Society since 1832.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 49

Dantez Apamson, of The Towers, Didsbury, Manchester, who
died 13th January, 1890, was a native of Sheldon in Durham, —
where he was born in 1818. His early life as an engineer was
passed on the Stockton and Darlington Railway, on which he held
various posts until 1850. In 1851 he established himself in Man-
chester as an iron-founder, engineer, and boiler-maker, and from
that time brought out a series of improvements in iron and steel-
making, and in machinery. Some of his most remarkable inven-
tions were connected with compound engines. He patented and
brought out a triple expansion engine as long ago as 1861, and
a quadruple engine in 1872. He is, however, perhaps better known
for the support he gave to the Manchester Ship Canal, a scheme
that, in great measure by his aid, was developed into a practical
undertaking.

Mr. Adamson joined the Geological Society in 1875. He was
President of the Iron and Steel Institute from 1887 till 1889.

Hetnricu von Drecuen, the Nestor of German geologists, as he has
been aptly termed by Prof. F. v. Romer, passed away from the world
he had so long adorned on February 15th, 1889. He was born
March 25th, 1800, and had consequently nearly completed his 89th
year. As he was elected a Foreign Member of this Society in 1827,
he had been one of our body in that capacity for the unprecedented
_ period of sixty-two years. or twenty-one years after his election
no Foreign Member was brought into our list who survives him.

H. v. Dechen came of a family ennobled in 1684 and resident in
Prussia for more than two centuries. He was born in Berlin, where
his father occupied a high official post, and he passed through the
usual course of education in the gymnasium and university of that
city. At the university he attended the lectures of Prof. Weiss,
the well-known mineralogist, and here he made the acquaintance of
Leopold v. Buch, who exercised much influence on v. Dechen’s sub-
sequent career. On leaving the university in 1819 v. Dechen
entered upon the study of mining in Bochum and Essen, and was
in 1820 placed on the staff of the Mining Department of the
Prussian State. In this department he continued throughout his
service, which terminated in 1864. He was appointed “ Oberberg-
amtsassessor” in Bonn in 1828, but transferred to Berlin as *“* Ober-
bergrath ” in 1831. Shortly afterwards he received the honorary
degree of Ph.D. from the University of Bonn, and from 1834 to 1841,
in addition to his official duties, he gave lectures in the Berlin Uni-

50 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

versity as Extraordinary Professor of Geology. In 1841 he
returned to Bonn as Director of the Department of Mines (‘“ Ober-
bergamtsdirector ”), and continued a resident of that city with but
trifling exceptions for the remaining forty-eight years of his life.

In his earlier years v. Dechen made many journeys for the pur-
pose of inquiry into the mining systems of other countries, and one
of these, made in the company of his friend C. von Oeynhausen to
England and Scotland, lasted for more than a year, from September
1826 to November 1827. The object of the two travellers was
mainly official, to report to their government on the mining, and
especially the coal-mining, of England; but, both being ardent
geologists, some of their time was devoted to examining the features
of the country. One result of their visit was a paper on Ben Nevis
and some other places in Scotland, read to this Society January 19th,
1829. After their return v. Dechen and v. Oeynhausen became
connected by marriage, the former marrying a sister of the latter’s
wife, a lady named Gerhard, in 1828.

A great part of v. Dechen’s life was devoted to the official work
of mine-inspection, and to him is ascribed a foremost share in the
great progress that took place in mining and metallurgical works
throughout Rhenish Prussia during the twenty-three years that he
was director of the department. But during the whole of that time
and for many years afterwards his contributions to geological science
were numerous and important. Most of these contributions related
to the Rhineland, and his greatest undertaking was the preparation
and publication of a geological map of Rhenish Prussia and West-
phalia in thirty-five sheets, on a scale of 1: 80,000 (about 1+ inch
=1mile). This map, together with two volumes of explanatory
text, was issued at intervals between 1855 and 1882, and was the
first published geological map on a large scale that represented a
considerable part of Germany. A map of the area on a smaller
scale, 1: 500,000, was issued in 1866; a second and improved
edition appeared in 1883. . Amongst his earlier publications were
a translation of De la Beche’s ‘ Geological Manual’ into German,
published in 1832, and a general geological map of Germany, France,
England, and the neighbouring countries, which appeared in 1838.
The interest excited by v. Dechen’s Rhenish maps contributed
greatly to the establishment of a regular geological survey in Prussia
and other States of Germany.

Among y. Dechen’s services to science must be placed in a high
rank the effects of his influence on the two scientific Societies of

ANNIVERSARY ADDRESS OF THE PRESIDENT. 51

Bonn, the “ Niederrheinische Gesellschaft,” and especially the
‘¢ Naturhistorische Verein der Preussischen Rheinlande und West-
falens,” of which he was an honorary member from its commence-
ment in 1834, and president from 1845 till his death. The fact
that the number of members increased from 280 to over 1500 under
his presidency sufficiently indicates the spirit imparted to the last-
named society by his guidance.

It is unnecessary to attempt to give a list of the honours showered
upon so distinguished an official and so worthy a geologist equally by
his own and foreign governments and by learned societies in all parts
of the world. I have reason to know, however, that. he always
greatly valued the Foreign Membership of the Geological Society, one
of the first recognitions of the kind, and that he was proud of being
our senior Foreign Member. He was acorresponding member of the
French Academy and a member of the Belgian. In the year 1884,
and. consequently when upwards of 84 years old, he not only presided
over the sittings of the Geological Congress at Berlin as Honorary
President, but took a most active part in the proceedings. He pre-
served his wonderful powers of mind and body to an unusually
advanced age, and died regretted and honoured by the geologists of
other lands almost as warmly as by those of Germany.

Frieprich Aveust von QuENsTEDT was born, the son of poor
parents, at Eisleben, in Prussian Saxony, on the 9th July, 1809.
He studied at Berlin under Weiss, then Professor of Mineralogy at
the University of that city, and became Professor of Mineralogy,
Geology, and Paleontology at Tubingen, the University of Wiirt-
temberg, in 1837. This post he held for more than fifty-two years,
until his death on the 21st of last December. He became a
Foreign Correspondent of this Society in 1863, was elected a Foreign |
Member in 1885, and was awarded the balance of the Lyell Dona-
tion Fund in 1880. ‘ |

The principal work of Quenstedt’s life was the study of the
Wiirttemberg fossiliferous rocks, end especially of the Jurassic
system. ‘To this subject several of his best-known publications are
devoted, especially his ‘ Flotzgebirge Wiirttembergs’ (1843), his
‘Jura’ (1857), and his last great work ‘ Die Ammoniten der
schwabischen Jura’ (1888). But his most widely-known palson-
tological publications are his ‘Handbuch der Petrefactenkunde,’
first issued in 1852, and of which subsequent editions appeared in
1867 and 1882, and his ‘ Petrefactenkunde Deutschlands,’ com-

52 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

menced in 1846 and continued at intervals until shortly before his
death.

Whilst the great works just mentioned and many papers in trans- —
actions of societies and other serials sufficed to place Quenstedt
amongst the first paleontologists of the age, he was not less widely
known for his mineralogical and crystallographical publications.
His earlier papers were on mineralogy, and his ‘ Handbuch der
Mineralogie,’ the first edition of which appeared in 1854, has been
largely used as a text-book not only in Germany but in many other
countries. He also published at least two distinct works on erystal-
lography, ‘ Methode der Krystallographie’ (1840) and ‘ Grundriss
der bestimmenden und rechnenden Krystallographie ’ (1877).

This by no means exhausts the list of Quenstedt’s published con-
tributions to science. He brought out from time to time several
popular works on geology, especially ‘Sonst and Jetzt’ (1854),
‘Klar und Wahr’ (1872), and ‘ Die Schépfung der Erde und ihre
Bewohner ” (1882).

As a teacher Professor v. Quenstedt enjoyed a high reputation,
and his teaching was not confined to his pupils, for it is said that
he has actually made geology popular amongst the peasantry of
Wiirttemberg. In that Swabian Jurassic region to which Quenstedt
devoted so much of his life’s work almost every boy is an intelligent
collector of fossils, every quarryman acquainted not merely with
the different organisms that are found in the rocks, but with the
particular horizons at which each occurs. Owing to the impetus
given by Quenstedt to the search for fossils, an impetus the force of
which was largely due to his personal popularity, not only have
magnificent accumulations been amassed at Tubingen and Stuttgart,
but the fossils of Wurttemberg are well represented in the prin-
cipal museums of the world. It is to Quenstedt amongst others,
and perhaps more to Quenstedt than to any other, that we are
indebted for the remarkably extensive knowledge of Jurassic life
now possessed by paleontologists, a knowledge far exceeding that
of any other geological system.

Luie1 BELLaRDI was born in Genoa on the 18th May, 1818. He
studied for the law, but whilst thus engaged at the University of
Turin he devoted his leisure hours to natural history, and especially
to collecting fossils from the hills of Superga. His earliest publica-
tion, in 1838, when he was only 20 years of age, was on a fossil
Gastcropod, and throughout his life the Tertiary Gasteropoda of

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ne)

Piedmont and Liguria formed the principal subjects of his scientific
writings. For thirty years he was a professor of the ‘“ Liceo
Gioberti” at Turin and at the same time keeper of the paleonto-
logical! collection in the Royal Geological Museum of that city. The
great richness of this collection, especially in Tertiary Mollusca, is
chiefly due to Bellardi. Besides his papers on paleontology, the
majority of which were published in the ‘Memorie della Reale
Accademia delle Scienze di Torino,’ Bellardi wrote on entomological
subjects, and especially on Diptera. He was made a Foreign Corre-
spondent of our Society in 1880, and died 17th September, 1889.

By the death of Lro Lesauerrvx, which took place at Columbus,
Ohio, on the 20th, of October last, one of the principal paleo-
botanists of the world is lost to us. He was born at Fleurier, in
the canton of Neuchatel, Switzerland, in 1806, and was of French
Huguenot descent. He was educated for the church at the Neu-
chatel Academy, but, having become deaf at the age of 26, he worked
‘for twelve years as an engraver of watch-cases and a manufacturer
of watch-springs. His taste for natural history, however, gradually
made him known, and in consequence of his repute, gained by
researches on mosses and peat, he was employed by the government
of Prussia in 1845 to examine the peat-bogs of Europe. A trans-
lation of one of Lesquereux’s later papers on the formation of peat
appeared in the Society’s Journal for 1848.

Lesquereux went to the United States in 1848, and was at first
engaged there, as he had been in Europe, in the study of mosses ;
but from 1852 he became botanical paleontologist to several geolo-
gical surveys, and he published in succession a series of reports and
monographs relating to fossil plants from Pennsylvania, Arkansas,
Illinois, and Mississippi. His best-known works, and perhaps his
most-important, were a series of monographs issued between 1878
and 1883 on the Cretaceous and Tertiary floras collected by the
Geological Survey of the Territories under Dr. Hayden, and a work
in three volumes, one of them an atlas of plates, on the Coal-flora ot
Pennsylvania and the United States, published between 1880 and
1884 by the Second Geological Survey of Pennsylvania. He was a
member of the United States National Academy and of many Euro-
pean scientific bodies, also an honorary professor of the Academy of
Neuchatel. He was made a Corresponding Member of our Society
in 1880, and received the award of the Barlow-Jameson Fund in
1884.

54 PROCEEDINGS OF THE GEOLOGICAT, SOCIETY.

The last death to which I have to refer is by far the saddest
record amongst the year’s losses. The distinguished men whose —
careers have been briefly commemorated in the preceding pages
passed away, full of years and honours, at an age when their scien-
tific work might fairly be regarded as finished; but in Dr. Metcuror
Nervmayr, who died on the 29th January, 1890, at the age of 44
years, we have lost one of the best and most scientific paleeontolo-
gists who has ever lived, at an age when his talents had but recently
arrived at maturity.

Dr. Neumayr was born in Munich October 24th, 1845. He was
the son of a Bavarian Minister of State, Max v. Neumayr, and his
early life was passed in Stuttgart, where his father was the Bava-
rian Ambassador. After passing through the course of the gym-
nasium in Munich, Melchior Neumayr entered the University of
that city in the autumn of 1863 with the object of studying law,
in accordance with the traditions of his family, who had for gene-
rations furnished a series of distinguished lawyers and officials in
the service of the Bavarian government. But at the university
Neumayr’s tastes for science soon asserted themselves, and, aban-
doning the law, he devoted himself to geology and paleontology,
both at Munich and afterwards at Heidelberg, where he completed
his studies and took the degree of Ph.D. After some practice of
field-geology with Prof. Giimbel, Neumayr entered the Austrian
Geological Survey in 1868, at first as a volunteer, subsequently as
assistant geologist. In 1872 he left the Survey and returned to
Heidelberg as a tutor (Privatdocent), but was recalled the next
year to Vienna as extraordinary Professor in the newly-created
chair of Paleontology. In 1879 he was promoted to the ordinary
Professorship, a post which he held till his death. In 1878 he
married the daughter of our distinguished Foreign Member Professor
Suess. |

It would be impossible to attempt within the limits of an ordinary
obituary notice to record the various branches of geology and pale-
ontology to which Dr. Neumayr has contributed in the course of the
last twenty-five years. In addition to his scientific powers he
possessed much literary ability, and his papers are written with a
clearness which is-unfortunately not always conspicuous in German
scientific works. He was consequently a successful popular writer
on geology, one of his principal works, his ‘ Erdgeschichte,’ in two
volumes, which appeared in 1887, having had a wide circulation.
But although he wrote frequently and well on physical geology, it

ANNIVERSARY ADDRESS OF THE PRESIDENT. 55

is as a paleontologist that he will be remembered, and, moreover, as
one of the few who have not only regarded paleontology as a science
by itself, dependent on both biology and geology, but nevertheless
deserving and demanding separate recognition, but who have aided
by their work to prove that the claim of paleontology to be thus
recognized was valid.

Amongst the most important writings of Dr. Neumayr were a
series of monographs on Jurassic and Cretaceous Ammonites, and
another series of papers on the succession and relationships of recent
and Tertiary freshwater Mollusca. To the study of the latter he
was led by the peculiar facilities afforded by successive faunas in
the remarkable series of freshwater Tertiary beds that are so largely
developed in south-eastern Europe. The principal attraction to
Neumayr in both Ammonites and freshwater shells was the oppor-
tunity for tracing their descent. From his student’s days he had
been an enthusiastic supporter of Darwin’s theory of the origin of
species, and in his earlier works, as in his last and greatest book,
‘Die Stimme des Thierreichs,’ of which, unfortunately, only one
volume has been completed, he has devoted himself to the task of
tracing through the life of former times the same law of evolution
as Darwin inferred from that of the existing world. Dr. Neumayr,
I learn from Professor Judd, was in constant correspondence with
Darwin, who regarded him with the greatest esteem and attached a
high value to his observations. ,

Of Dr. Neumayr’s papers two, published in 1883 and 1885,
deserve especial notice; one of these treats of the zones of cli-
mate during Jurassic and Cretaceous times and the other of the
geographical distribution of the Jurassic formation. Both show a
wonderful knowledge of paleontological literature, and a remarkable
power of distinguishing the important facts amidst a mass of
details. ‘The first-named paper, moreover, is one of the most
important contributions to the question of climates in Mesozoic
times that has ever been written, for in it the author shows by a
mass of evidence, derived mainly from Cephalopoda, that in Jurassic
and Cretaceous times the equatorial marine fauna differed from that
of the two temperate zones, and the latter from that of the arctic
zone, much as the faunas of similar zones differ from each other in
the present day.

Within a week of his death I received from Dr. Neumayr a
packet of papers dealing with a variety of subjects and well illus-
trating the many-sidedness of his intellect. One was a popular

VOL, XLVI. é

56 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

paper on landslips, another a scientific treatise, of the highest order,
on the origin of the Unionide, a third related to Calostylis and the
perforate Hexacorallia, a fourth was a discourse on the climatic —
relations of past times, a fifth was on Belemnites from Central Asia
and South Africa, a sixth on Madagascar fossils, and a seventh on
remains of Hyopotamus from Eggenburg. All of these are of
unusual interest, and some of them, for instance that on the origin
of the Unionide and that on ancient climates, are clearly the writing
of amaster, whilst the notes on Madagascar fossils show how very
much more can be learned from Mr. Baron’s discoveries, described
in the ‘ Quarterly Journal’ of this Society, than we, who had the
fossils before us, were able to infer. To this subject further refer-
ence will be found in a subsequent part of this address.

‘Personally Dr. Neumayr was singularly quiet, modest, and
amiable, greatly beloved and respected by a wide circle of friends.
He was elected a Foreign Correspondent of this Society in 1880.

Amongst the other Fellows who have been lost to us during the
past year are THomas H. Cocxsurn-Hoop, F.R.S.E., elected in 1863,
who in 1870 contributed to our Journal a paper containing ‘‘ Geclo-
gical Observations on the Waipuru River, New Zealand;” and
James Rapvcerirre, of Dukinfield, who joined our Society in 1885,
and to whom we are indebted for an account of some very curious
grooves and quartzite boulders in the Roger Mine at Dukinfield.

As you have learned from the Council’s Report, the past year has
brought prosperity to our Society. Our Journal has been main-
tained without difficulty at its usual standard, and its contents will
not, I think, be found to show any falling off in interest. The
most important event in the history of the Society during the past
year has been the revision of the Bye-laws; and although the pro-
cess was neither pleasant nor quick, I think the Fellows may be
congratulated on the circumstance that some necessary improve-
ments have been effected without any serious alteration in those
regulations which have now, for so many years, been found to be
consistent with the Society’s well-being and progress.

It will not, I trust, be necessary to reopen, for many years to
come, the questions which were determined by the votes of those
Fellows of the Society who were‘able to attend the series of Special
Meetings held for the purpose of considering the various proposals

ANNIVERSARY ADDRESS OF THE PRESIDENT. 57

that were brought forward. Should it, however, be at a future
time thought desirable to ascertain the opinions of the Fellows
upon any question involving a great change in the constitution or
proceedings of the Society, I must express a hope that some means
will be used to ascertain the views of the Fellows as a whole, and
not merely of those who are able to attend a meeting at the So-
ciety’s rooms. I find, by going through the lists for 1888, that
only about one third of the whole number of Fellows reside in the
metropolis or in one of the metropolitan counties, two thirds live
beyond those limits. So far, too, as I am able to judge, the pro-
portion of Fellows living at a distance from London tends to
increase from year to year.

I shall not, in the present Address, attempt any review of the
geological literature of the past twelve months. ‘The various scien-
tific serials that now appear, and contain accounts of all the more
important contributions to knowledge, render the task of reviewing
the additions to our rather wide-ranging science in the Anniversary
Address less necessary than was formerly the’ case, whilst the
majority of the works and papers published can only be fairly
judged and analyzed by those who have made a special study of the
department of geology treated. There are, however, two palaon-
tological works which I ought not to pass over without mention ;
for not only are both of them of high importance, but both, I
believe and hope, are destined to serve as aids to an advance in the
science of Geology.

The first of these works is Nicholson and Lydekker’s ‘ Manual of
Paleontology,’ in which, for the first time, I believe, in the English
language, a fairly comprehensive account of the Animal Kingdom,
as represented in past times, has been afforded to students. Excel-
lent. as were Professor Nicholson’s earlier editions, they could
scarcely be said to suffice as works of reference; but the present
is a great improvement. It may be hoped, though I fear it can
scarcely be inferred, that the appearance of the present work will
coincide with the commencement of a period of increased attention
to Paleontology in these islands. Hitherto, whilst Geology and
Biology have been fairly studied in this country, and whilst trained
students in both sciences have appeared in considerable numbers,
paleontologists have been of ominous rarity. On four different
occasions When a Paleontologist was required for the Geological
Survey of India, a German was selected; and I can personally
vouch for the fact that, in one instance, and; I believe, in others,

e2

58 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

there were no qualified English students, of the proper age, available.
I cannot believe that the neglect of Paleontology in this country is |
due to apathy on the part of teachers, or to incapacity on the
part of students ; as fairly trained geologists and biologists not rarely
come from our educational institutions, I should anticipate that

equally efficient paleontologists would be forthcoming if the same
opportunities of study were offered. There are, and always have
been, a few good paleontologists in the country, but the number might
be considerably increased with advantage. It may be hoped that a
science, to which none is second in interest, none more prolific in its
additions to human knowledge, may gather fresh impetus in the
British Islands from the publication of an efficient manual, and that
the time may not be distant when British geologists, far from being

contented with the two well-filled volumes now offered for their

use by Messrs. Nicholson and Lydekker, will demand a still more

extensive work, on the scale of the superb Paleontological Compen-
dium now being published by our distinguished Foreign Member,

Prof. v. Zittel, a hook that, I fear, no English publisher at present

would feel justified in undertaking. By the work now brought out
Professor Nicholson has worthily repaid this Society for the award

to him of the Lyell Medal two years ago.

The other work to which a passing reference is due is that by
our (I deeply regret to say) late Foreign Correspondent, Dr. Mel-
chior Neumayr, “ Die Stimme des Thierreichs.” . I have already,
in a short obituary notice, endeavoured to express some sense of
the loss to geology caused by the death of this distinguished Palz-
ontologist. In this, his last and greatest work, he endeavoured to
bring together the results of many years’ labours and researches,
and to show the lines of descent that can be traced amongst ancient
forms of life. In the only volume published, he has treated of the
Protozoa, Coelenterata, Echinodermata, Annelida, and Molluscoida,
besides writing several introductory chapters full of suggestive re-
marks,

My own knowledge of the very intricate questions treated in
Neumayr’s work does not justify my expressing any view except
admiration; but I may, perhaps, quote from one of the first of
living paleontologists, Prof. v. Zittel, whose opinion is entitled to
attention. He writes thus, ‘ In the first volume of the ‘Stiimme
des Thierreichs, which appeared a few months ago, Neumayr
showed remarkable mastery of the collected data relating to his
subject; new observations, surprising applications of known facts,

ANNIVERSARY ADDRESS OF THE PRESIDENT. 59

radical improvements in classification, brilliant hypotheses on the
evolution and relationship of fossil organisms, secure for this last work
a prominent place in biological literature, and will probably occupy
followers and opponents of his views for many years to come.”

It is not my intention to attempt any survey of the geological
discoveries in the past year, though here, also, passing reference
may be made to two events of importance to Geology. Perhaps
the most striking, until within the last week, was a discovery that
could, however, scarcely be credited to 1889, that of the nature of
the Greenland ice-sheet. Though Dr. Nansen’s J ourney of 1888,
the details of which only reached us in the past year, did not do
much more than confirm the observations of Nordenskiold and
others, still the results are of the greatest importance, and the facts
now clearly ascertained of the enormous dimensions of the ice-
sheet bear witness to the accuracy of the inferences drawn by the
geologists who investigated the traces of the Glacial epoch, as to
the depth of the ice and the erosion exerted by it.

Only yesterday an announcement was made that coal has actually
been cut at Dover. Probably geologists, and especially those who
have followed the gradual accumulation of evidence as to the occur-
rence of palzeozoic rocks beneath south-eastern England, were muc
less astonished at the discovery than the public in general. A
- letter that I received yesterday from Prof. Boyd Dawkins, by whose
advice, [ believe, the boring was carried out, confirms the infor-
mation published in the newspapers, that a seam of coal has been
reached at a depth of 1180 feet, and that this seam is proved to be
of Carboniferous age by the plant-fossils in the associated clays. It
must be a source of congratulation to geologists to reflect that the
discovery is solely the result of scientific induction, and arrived at
by following the line of research first indicated, I believe, by the
late Mr. Godwin-Austen and subsequently by Prof. Prestwich.

The question of the permanence of ocean-basins, to which the
remainder of this address will be chiefly devoted, is one that has
attained great prominence in this country since the ‘ Challenger ’
Expedition. ‘The opinion that the deep parts of the ocean have
been the same from the earliest period of which we have any record
in the Harth’s strata, has received the approval of several eminent
geologists and biologists. Nevertheless there are many who feel
grave doubts on the subject, and I think the arguments on both
sides are worthy of reconsideration.

60 . PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

It will perhaps tend to render my treatment of the subject
clearer, if I point out at the outset that there are three possible ex-.
planations of the phenomena presented to us by the present and
past conditions of the land and by the distribution of terrestrial
life’; these are :—

1. That the present continental areas, including the shallow seas
around them, and the present oceanic tracts with a depth exceeding
about 1000 fathoms, have been the same since the original consoli-
dation of the earth’s crust.

2. That the continental and oceanic areas are not permanent, but
that they are from time to time interchangeable.

3. That the continental and oceanic areas are permanent as arule,
but that portions of them have at times passed from one condition
to the other.

I propose to take in order the principal physical, geological, and
biological arguments in favour of the permanence of ocean-basins,
and to inquire how far they are conclusive, and especially whether
any exceptions are probable. I wish also to call your attention to
a few facts, mainly referring to the distribution of terrestrial or-
ganisms, that I think worthy of the attention of geologists.

The permanence of the land- and sea-areas is no new idea. It
would be easy to quote from ancient and modern poets and writers
a series of extracts to show the prevalent belief in the fixed limits
of the ocean-tracts. It is only of late years, since the teaching of
Lyell and other modern geologists has become generally received,
that the old belief has been replaced by free speculation on the dis-
tribution of land and water in past periods. Under these circum-
stances, scientific men who revert to the ancient faith suffer from
the serious disadvantage of leading an euthusiastic school of fol-
lowers, who have never renounced the creed of their ancestors, and
who hail the convert to orthodoxy with the traditional joy over a
repentant sinner. ‘There is always a risk of a sound scientific
theory being accepted in a much wider sense than was intended by
its original advocates, and the risk is extreme when the theory
coincides with the popular taste.

The chief arguments brought forward in favour of the permanence
of ocean-basins or deep-sea areas are the following :—

I. The higher specific gravity of the earth’s crust beneath the
ocean, as inferred from pendulum observations, and the further in-
ference that these areas of greater density have been the same since
the original consolidation of the earth.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 61

II. The absence, with a few not very important exceptions, in
ocean tracts, of islands formed of stratified rocks such as compose
the bulk of the continents, and the fact that nearly all oceanic
islands are volcanic, and consequently such as may have been built
up from oceanic depths by the accumulation of volcanic discharges.

III. The absence of deep-sea deposits in the rocks of conti-
nental areas.

IV. The agreement between the distribution of plant- and animal-
life and the present arrangement of land-areas.

I propose to consider each of these arguments in order, though
the last is that to which it will be necessary to give the most
attention. —

I. Greater Density of Infra-oceanie Orusts.—The first argument is
one to which some importance is attached by Prof. Dana*. But it
is only founded on a few observations in India and the neighbouring
islands, and was suggested by its author, Archdeacon Pratt, as a
probable hypothesis to account for some anomalies in the results of
pendulum observations. The principal force of the contention
appears to lie in the circumstance that if the crust of the earth now
below the ocean had been exposed to denudation, and consequently
transport, its exceptional density could not have been preserved,
because the action of rivers and currents would in the course of ages
have mingled its detritus with that of the present continental areas.
It has also been urged that, owing to the contact of cold oceanic
waters, the crust beneath the ocean has become thicker and more
rigid. This view, however, depends on the hypothesis of a fluid
Jayer beneath the solid crust ; and although there is much to be said
in favour of such a view, it is impossible to accept it as a proved
theory and to use it as a basis for argument. Indeed the next
point to be noticed, the presence of volcanic islands in many parts
of the ocean, is really antagonistic to the idea of a uniformly thicker
and more rigid crust beneath the ocean-bed, because the occurrence
of volcanoes indicates areas and lines of weakness. If the infra-
oceanic crust were much more rigid and thicker than the infra-con-
tinental, volcanoes should be confined to the area occupied by the
latter; but this is not the case. That volcanoes should be most
numerous near the boundaries between continental and oceanic
areas is natural.

II. The Volcanic Origin of Oceanic Islands—This, the second
* Manual of Geology, 3rd ed. p. 815.

62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

argument, is, at present, far more important than the first. Darwin
was, I think, the first to call attention to the absence of paleozoic -
and mesozoic strata in oceanic islands, and his words* which have
already been quoted by Mr. Wallace in ‘Island Life,’ will bear re-
peating. He says :—

“‘ Looking to the existing oceans, which are thrice as extensive as
the land, we see them studded with many islands; but hardly one
truly oceanic island (with the exception of New Zealand, if this can.
be called a truly oceanic island) is as yet known to afford even
a remnant of any palwozoic or secondary formation. Hence we
may perhaps infer that during the palewozoic and secondary periods,
neither continents nor continental islands existed where our oceans
now extend; for, had they existed, paleozoic and secondary for-
mations would in all probability have been accumulated from
sediment derived from their wear and tear; and these would have
been at least partially upheaved by the oscillations of level, which
must have intervened during these enormously long periods. If,
then, we may infer anything from these facts, we may infer that,
where our oceans now extend, oceans have extended from the
remotest period of which we have any record; and on the other
hand, that where continents now exist, large tracts of land have
existed, subjected no doubt to great oscillations of level, since the
Cambrian period.”

There can be no question as to the force of this argument; but
the more fully it is admitted, the more important do any exceptions
to the volcanic character of oceanic islands become, and the fact
must not be forgotten that the number of oceanic islands in which
palzeozoic or mesozoic beds have been found has been slightly in-
creased within the last few years. The Falkland Islands, the
paleozoic fossiliferous rocks of which were described by Darwin
himself 7, were not noticed by him in the paragraph quoted, doubt-
less because he did not regard them as oceanic: although 400 miles
distant from the coast of 8. America, they are connected with it by
a bank of less than 100 fathoms deep, and they have an indigenous
land-mammal. But the Archipelago of South Georgia, 800 miles
further to the eastward and nearly 1200 miles from the American
continent, has now been shown to consist of clay-slatet. According
to the chart issued with the recently published ‘ Challenger’ narrative,

* Origin of Species, 6th ed. p. 288.
T Q.J.G.S. ii. p. 267.
¢ Geol. Mag. 1884, p. 225; ‘ Nature,’ March 27, 1884, xxix. p. 509.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 63

these islands are surrounded by ocean exceeding 1000 fathoms in
depth. Another important island also, isolated by sea exceeding
1000 fathoms in depth, is New Caledonia, where both paleeozoic and
mesozoic fossiliferous beds are met with *. This, however, is a pre-
cisely similar case to that of New Zealand. The Auckland and
Campbell Isles+ south of New Zealand are said to be separated
from it by a sea more than 1000 fathoms deep, but contain ancient
sedimentary rocks. The sedimentary deposits of the Fiji Islands,
formerly supposed to be ancient, have been shown by Mr. Brady ¢
to be of subrecent formation.

The occurrence of granitic and gneissic formations in islands
differs from that of sedimentary beds in this respect, that the former
may have consolidated at some depth below the bottom of the ocean.
But such rocks, when in place, cannot have formed parts of ordinary
submarine volcanic accumulations. A granitic or gneissic island
must be part of an ancient land tract, for the rocks could only have
been exposed after a long period of denudation. The most important
instance of granitic or gneissic rocks occurring in oceanic islands is in
the Seychelles §, and these are probably a continuation of the main
Madagascar range, which is of similar formation ; they are separated
from Madagascar and from all other land areas by sea of consider-
able depth. It should also not be forgotten that granite and schist
are said by von Buch to have been thrown out from the volcano of
Caldera (I. de Palma) in the Canary Islands |!, that similar rocks
have been ejected from the Cape Verde voleanoes 4], and that horn-
blendic granite was found by Darwin amongst the fragments thrown
out at Ascension **, Granite and gneiss are also said to occur +7 on
the Marquesas Islands in the Pacific; but there appears to be some
uncertainty about this. If confirmed, however, this occurrence
would beof the greatest importance.

* Heurteau, ‘Ann. Mines’ (7), ix. p. 232 (1876).

t Tehihatcheff, ‘ Considérations sur les Iles Océaniques,’ p. 34.

t Q.J.G.8. xliv. p. 1.

§ By some mistake, Wallace, in his recent work, ‘ Darwinism,’ p. 342, has
stated that the Seychelles are formed of coral rocks. There is, however, no
doubt about their geological conformation, as may be seen by referring to the
following writers: Velain, Bull. Soc. Géol. France, 1879, sér. 3, vii. p. 278 ;
Perceval Wright, Brit. Assoc. Reports, 1868, sect. p. 143 ; EH. Newton, Ibis, 1867,
p. 835, ‘This list of references could easily be increased considerably.

|| Von Buch, Phys. Beschr. d. Can. Inseln, p. 289.

{| Dolter, Die Vulkane der Capverden und ihre Producte (Graz, 1882), p. 159.

** Darwin, Vole. Islands, p. 40.

tt Jules Marcou, Expl. 2 éd. Carte Géol. de la terre, p. 185.

64 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

It will be seen at once that these examples do not very greatly
affect the main argument, because there is still an enormous area of.
ocean left in which the only islands are volcanic. But still the
instances mentioned are worthy of notice, because they show that
there are exceptions to the general rule that no palwozoic or meso-
zoic rocks occur on oceanic islands, and the additions made to our
knowledge in this respect of late years render it probable that other
instances remain to be discovered. Of course much depends on the
definition of an oceanic island; but the accuracy of the term can
scarcely be contested in the case of South Georgia. As it is impos-
sible for denudation to hollow out the sea-bottom beyond a few
fathoms below the surface, the isolation must in all such cases be
due to depression.

There are three other facts that should be remembered with
reference to the point under discussion. The first is that our
acquaintance with the geology of many oceanic islands is by no
means sufficiently complete to justify our being confident that no
sedimentary rocks of old date exist. The second is that the rocks
of an island may be entirely volcanic, and yet the island may be a
remnant of a continental mass. It must not be forgotten that
typically volcanic rocks in some continental areas, as in the Western
United States of North America, North-eastern Africa, and the
Peninsula of India, form vast horizontal or nearly horizontal sheets,
and completely cover the surface over areas the diameters of which
are measured by hundreds of miles. Such rocks may be of consider-
able antiquity, and they are typically continental, being all, so far as is
known, subaérial. It is, I think, far from clear that some oceanic
voleanic islands, such as St. Paul’s Rocks, Fernando Noronha, and
Kerguelen, are not composed of voleanic formations of the continental
type; and rocks of this class are well developed in some ancient
continental islands, for instance, New Caledonia. At the same time,
this only proves that such islands were formerly of considerable
extent, not that they were attached to continents.

The third fact is even more important. This, which has been
noticed by Prof. Bonney in one of his notes to the recent edition
of Darwin’s ‘ Coral Reefs’ (p. 326), is that the occurrence of vol-
canic islands does not prove that the area in which they occur is
not a sunken continent. If Africa south of the Atlas subsided 2000
fathoms, what would remain above water? So far as our present
knowledge goes, the remaining islands would consist of four voleanic
peaks, Camaroons, Kenia, Kilimanjaro, and Stanley’s last discovery,

ANNIVERSARY ADDRESS OF THE PRESIDENT. 65

Ruwenzori, together with an island, or more than one, containing
part of the Abyssinian tableland, which, like the others, would be
entirely composed of volcanic rocks, but, unlike them, would consist
of horizontal or nearly horizontal lava-flows, probably of Mesozoic
age. Ina Southern Africa, too, the peaks of the Stormberg and Dra-
kensberg, though not rising or scarcely rising above 10,000 feet, are
the highest in the country and consist of volcanic rocks. The same
is the case with the highest peaks in Madagascar, in Mexico, in the
Caucasus, in the Elburz Chain south of the Caspian, and in many
other parts of the world; though the case of Africa is perhaps the
most remarkable.

Ill. The Absence of Deep-sea Deposits in Continental Areas.—This
argument is, I think, of far greater importance than either of the
preceding. It is perfectly true that the presence or absence of deep-
sea deposits in continental areas is only indirectly connected with the
condition of the present oceanic areas in past times; because, even
if no change whatever has taken place in the former, that does not
prove that none has taken place in the latter. Even if no part of the
continental area has ever been deep sea, any oceanic area may have
been land at one time or another, the necessary compensation having
been provided by the deepening of another oceanic tract. But
there can be no question that, unless the amount of ocean water
on the earth’s surface has greatly increased in the later geological
epochs, there must have been deep sea over a considerable portion
of the earth’s surface at all times; and if the continental areas have
remained unchanged, the oceanic areas have, in all probability, pre-
served their original limits. The question for us at present is,
whether we have suflicient evidence to justify our belief that the
continental areas have remained unchanged.

In this case, even more than in that of the oceanic islands, it
appears premature to conclude that our knowledge approaches com-
pletion. Because in the extremely small area of the land surface,
assuredly not one-twentieth of the whole, that has received close
geological examination, no deep-sea deposits have been observed, we
have no right to assume that none will ever be discovered in any
part of the continental area. The recognition of the character of
deep-sea deposits is too recent for geologists in general to have
become acquainted with the peculiarities of such formations, so as
to be able to recognize them at once. On the other hand if deep-
sea deposits were not of exceptional occurrence on continental areas,
some would probably have been noticed before this. It has I believe

66 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

been suggested that the Graptolite shales of the Silurian system were
deposited in deep water, and, so far as the fauna is concerned, the
hypothesis appears plausible enough ; but the interstratification of
coarse sandstones in places seems a fatal objection. The fine slates
and interstratified volcanic tuffs of Silurian and Cambrian age are,
however, sometimes of great thickness and extent, and are worth
further examination to see if any of them are possibly of deep-
water origin *.

Throughout a large oceanic area at present it is pretty evident
that, practically, no deposits are being formed. The fact that teeth
of what are believed, on good grounds, to be extinct forms of Shark
have been dredged in a corroded state from the bottom of the ocean
shows that such objects have lain for ages where no sediment was
deposited to entomb them. ‘There is no ground for surprise there-
fore if the abyssal red clay is unknown in the older rocks. But the
absence of strata corresponding to the Globigerina- and Radiolarian
ooze of the present oceans is, so far as our knowledge extends, in
favour of the contention that the continental areas have not been
depressed beneath the deep sea.

At the same time two recent discoveries of deep-sea deposits,
each on the border of the continental area, serve to show how
cautious we should be in coming to decided conclusions. These
two instances are in the Solomon Islands, concerning which I shall
have some additional remarks to make when dealing with insular
faunas, and in Barbadoes ¢. The evidence in the latter case is very
remarkable and peculiarly complete, for the deep-sea Radiolarian
ooze rests upon sandstones and clays with coal, believed to be of
older Tertiary age, and which are evidently littoral, estuarine, or flu-
viatile in origin. It is clear that the island must have formed part
of a continent, that it must have been depressed to a depth of over
1000 fathoms, and then re-elevated ; and there is, so far as I under-
stand, no question that these changes have taken place within the
Tertiary era and probably within the Miocene and Pliocene periods.
Barbadoes is at present surrounded on all sides by seas over 1000

* There is so great a resemblance between some of these remarks and the
views on the same subject expressed by Dr. Nicholson in the last edition of his
‘Manual of Palxontology,’ i. p. 75, that it is necessary to explain that all this
part of the address was written before I had seen Prof. Nicholson’s work, and,
I believe, before it was published.

+ Guppy, ‘Solomon Islands, Geology,’ &e., pp. 77, 81, &e.

{ Feilden, Ibis, 1889, p. 478; Jukes-Browne and Harrison, ‘Nature,’ vol. xxxix.
pp. 367, 607 ; Gregory, Q. J.G. 8. xlv. p. 640.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 67

fathoms deep. Moreover Barbadoes is said not to be the only
West Indian Island in which Radiolarian deposits occur, so that
there is a probability, as might have been anticipated, that subsi-
@ences and elevations of the character mentioned affected considerable
areas.

IV. Relations between Distribution of Animals and Land-areas.—
The last argument may not be strictly geological, but all who
recognize how intimately the story of the earth is bound up with
that of its inhabitants will have little doubt that the present
distribution of animals and plants is of the highest geological
importance, and that the existence of particular forms of living
beings in continents and islands is the result and the record of the
history of those areas and of their connexions with each other.
There can be no doubt, in short, that most important testimony as
to the distribution of land and water in past epochs is afforded
by the range of living species and genera. The information on
the subject of distribution at the present day is considerable, pro-
bably more extensive and nearer completion, so far as regards
vertebrate animals and phanerogamous plants, than that relating to
the geology of the different regions. Moreover the question of
zoological distribution has been ably treated by one of the first
biologists of the day, Mr. Alfred Wallace, who has in his later
works unhesitatingly given his adhesion * to the doctrine of perm-
anent oceanic and continental areas in almost its extreme form.
Just twenty years ago the question of distribution was dealt with
by Professer Huxley in an address to this Society, and my only
excuse for referring to a subject already treated by so high an
authority, is that the aspect of the question has entirely changed
since 1870, that our knowledge has greatly increased, that the
subject has been widely discussed, that the oceans have been better
surveyed, and that we are in the presence of an entirely different
theory of the distribution of land in past ages from that which
prevailed amongst geologists when Professor Huxley’s address was
written. It is essential to add that, whereas my great predecessor
felt called upon to prove the theory of evolution before applying it,
we may now regard the doctrine as firmly established.

In all the remarks which follow I shall assume as an accepted
fact, not only that all species of a genus, all genera of a family, and
all families in an order, class, or subkingdom, are descended from

* ‘Tsland Life,’ chap. vi.; ‘ Darwinism,’ pp. 341, &e.

68 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

one stock in each case, but that similarity in organic structure is
proportional, as a general rule, to the degree of affinity, animals and —
plants that are like being more nearly related by descent than those
which are dissimilar.

As I have already said, I propose to treat the subject of distribu-
tion at some length, both because it is, I think, well worthy of the
attention of geologists, and because I believe the whole question
requires reconsideration. To understand why this is the case, it is
essential briefly to recapitulate the history of the inquiry.

Although much had been previously done, the first contribution
to which reference is necessary was a paper by Mr. P. L. Sclater,
published in 1858 *, ‘‘ On the General Geographical Distribution of
the Members of the Class Aves.” The terrestrial area of the world
was in this paper divided into the following six zoological regions :—

1. Palearctic: Europe, Northern Africa, Northern and Central
Asia.

2. Ethiopian: Africa south of the Atlas, and Madagascar.

3. Indian, renamed Oriental by Wallace: India, South-eastern
Asia, and part of the Malay Archipelago.

4, Australian: Australia, with New Guinea and adjacent islands,

_ New Zealand, and Polynesia. :
5. Nearctic: America as far south as Mexico.
6. Neotropical: Central and South America, with the West

Indies.

These regions were founded solely on birds, and mainly on
passerine birds (or on passerine and picarian). They were accepted
for snakes and Batrachia by Dr. Giinther in a paper published in
18587; but afar more extended study of the subject, and the great
additions made to our knowledge within the last thirty years, have
induced Dr. Giinther to come to a very different conclusion, as will
be shown presently.

The papers just mentioned appeared before the publication of
Darwin’s ‘ Origin of Species,’ and were, of course, written without
any reference to the idea of relationship by descent amongst different
genera of a family or different species of agenus. So soon, however,
as Darwin’s great work had produced its effect, the importance of
an inquiry into the distribution of animal- and plant-life was greatly

increased.
* Journ. Linn. Soc. Zoology, ii. p. 130.

t P.Z.S. 1858, p. 373.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 69

Various other schemes of regional subdivision have been proposed,
but it is unnecessary to notice all. I have already alluded to the
most important, that of Professor Huxley, who, on a general survey
of terrestrial vertebrates*, proposed four primary distributional
“provinces, viz. :— |

1. Novo-Zelanian (New Zealand).

2. Australian.

3. Austro-Columbian (Neotropical of Sclater, South America).

4, Arctogewan (Palearctic, Ethiopian, Oriental, and Nearctic
united).

By far the most important work on the subject yet produced is
Wallace’s ‘ Geographical Distribution of Animals’ (2 vols., 1876), in
which the author adopts Sclater’s regions in their entirety for all
terrestrial and freshwater forms of animal life. In this work lists
of the families of Mammals, Birds, Reptiles, Batrachians (or
Amphibia), Freshwater Fishes and diurnal Lepidoptera found in each
region are given, and also of the genera of mammals and some
birds (Passeres, Picariz, Psittaci, and Accipitres). Numerous details
are added relating to other terrestrial animals, but the regional
arrangement is mainly founded on the birds of the orders named, and,
as is especially stated, on Mammalia. With the question whether
the mammals quite agree with the classification proposed I shall deal
presently ; meantime it should be mentioned that Wallace, amongst
the reasons given for adopting the regions named, assigns a high
rank to the convenience of employing large subequal divisions.

There is one aspect of the whole question to which attention
must be drawn. No one doubts that the present form of the great
land-tracts extends back with but trivial modification to Pliocene
times at least, the only important changes of later date being the
opening of Behring’s Straits, and severance of America from Asia,
the separation from continents of certain continental islands, such as
Great Britain and Ireland, Sumatra, Java, and Borneo, Ceylon, &c.,
and perhaps the reunion of North and South America. The
changes since Miocene, and perhaps since Eocene, times have
probably been neither very extensive nor very numerous. If,
however, the principal divisions of the earth have remained the
same or nearly the same for a longer period than the existence of
most living genera of Vertebrata, the animals inhabiting those

* P.Z.S. 1868, p. 316; Q. J. G.S. xxvi. p. ly.
tT ‘Geogr. Distrib.’ i. p. 57.

70 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

divisions must necessarily, if we accept the ordinary teachings of
Evolution, have become materially differentiated, so that each
modern natural division has many of its generic types peculiar.

The present distribution of all terrestrial organisms, as nas been
pointed out already by Huxley, Wallace, and other writers on the
subject, is the combined result of several different factors. Of these
the original centre of dispersion in the case of each organic unity,
such as a family, genus, or species, is one; the distribution of land
and water, firstly, at the time of dispersion, secondly, since that time
are two others; whilst powers of migration and ability to live under
varied conditions are of great importance, and it is notorious that
the last two factors are as diverse in different organisms as I shall
endeavour to show that the first is.

As regards origin, there is an important point in which mammals
and birds, most reptiles and batrachians, probably all insects and
arachnida, and all land-plants differ from freshwater fishes and
crustacea, and from both freshwater and land-mollusca. The forms
in the first category are in all probability derived from terrestrial
or freshwater ancestors, differing very widely from them in structure,
so widely, indeed, that the ancestral types would have been classed in
distinct orders, or even classes. Even when there are marine
representatives, such as Cetacea, sea-snakes (Hydrophide), marine
turtles, and a few marine angiospermous plants, these are probably
descended from terrestrial or freshwater forms. On the other hand,
the fishes, crustacea, and mollusca found in rivers, and all land-
shells are in all likelihood derived from various marine stocks, and
some of them have living marine representatives belonging to the
same family. Thus freshwater Percidew, Salmonide, Clupeide, &c.,
differ sometimes generically, often merely specifically from the forms
found in the sea, and when, as in the carps and in most existing
ganoids, whole families are confined to fresh water at the present day,
there can be no reasonable doubt that marine ancestors not differing
ereatly in structure flourished at a former period. The derivation
of land-mollusca is similar, and will be dealt with presently. In the
case of terrestrial and fluviatile animals derived from marine
forms it is manifest that the geological date of origin of the
different genera of one family, or even of species of one genus, and
above all of different families was not necessarily the same, that is
their origin as land or freshwater animals may have taken place,
and in all probability did take place, not merely at different periods
of the Earth’s history, but in different parts of the land-area.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 71

It is reasonable to suppose that all mammalia and all birds have
spread from one part of the world in each case, whilst the carps
may have originated in one continent at one geological epoch, and- |
another family of freshwater fishes, for instance the Characinide or
Chromidide, at another place at a different epoch. This fact
manifestly has an important bearing on distribution; for the
original dispersal and evolution of each group must have depended
on the position and connexion of land-areas at the time.

At the same time, when the whole of a family, as in the case of
the carps or of the Cyclostomatide, is exclusively freshwater or
terrestrial, it is highly probable that all members of that family are
descended from one original marine type, and this probability is
frequently borne out by the geographical distribution of the family.
Thus carps (Cyprinids) abound throughout Huxley’s Arctogea,
the Palearctic, Ethiopian, Oriental, and Nearctic regions of Sclater
and Wallace, but are absent in Australia and South America.

As in the class Pisces, so in the subkingdom Mollusca, the fresh-
water forms belong to widely different groups. Thus the Unionide
and Paludinide, both purely freshwater families, belong to two
widely different classes, the Lamellibranchiata or Pelecypoda and the ~
Gasteropoda. Here too, as amongst the fishes, we find some families
entirely confined to fresh water, as the exampies mentioned above ;
others marine with freshwater genera, as the Rissoide or Hydrobude
with Bythima, LInttorinide with Cremmoconchus, Mytilide with
Dreassensia and Byssanodonta, and finally genera like Neritina,
with some species marine or estuarine, others fluviatile and even
inhabiting mountain-torrents.

Amongst land-mollusca, although there is by no means the same
diversity as in the freshwater members of the subkingdom, there are
nevertheless several families of very different affinities. The
families are, as a rule, entirely terrestrial, but they are frequently
allied to other families that are marine. The most important forms
belong to the order Pulmonata, including the Helicide, Limacide,
Testacelide, and several other purely terrestrial families, the
Linmneide and Physide freshwater, the Awriculide, Oncidtide, and
Amphiboliide essentially brackish water or estuarine, but with
marine representatives, and in the Auriculide with at least one truly
terrestrial genus Camptonya, and lastly the marine Stphonaride.
The estuarine and marine types are, however, without exception
littoral, and the whole order may be as thoroughly terrestrial in
origin as mammals. Very different is the case with the land-shells

VOL. XLVI. f

72 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

belonging to the order Prosobranchiata and frequently known as
Operculata, although some of these have no opercula. These
-comprise the Cyclophoride, Cyclostomatide, Aciculide, and perhaps
Truncatellide belonging, like the freshwater Paludinide, Valvatide
and Ampullaride, and many of the commonest marine univalves, to
the Tzenioglossate division of the suborder Pectinibranchiata, and the
Helicinde and Hydrocenide allied to Neritide and appertaining to
the Rhipidoglossate division of the suborder Scutibranchiata*. In
the immediate neighbourhood of the Helicinide there is another
terrestrial family, the Proserpinide, without any operculum. The
great bulk of all the divisions and orders of the Prosobranchiata, it.
is scarcely necessary to say, are marine.
There is nothing in the present distribution of the various families.
of operculated land-shells antagonistic to the idea of each family
having originated from a distinct birthplace at a different period from
any other family. The Cyclophoride, though found in all the prin-
cipal regions of the earth, are chiefly developed in the Oriental region,
and are very largely continental in their distribution. The Cyclo-
stomatide are best developed on what Wallace has termed ancient
- continental islands, which have been separated from continents.
during the later Tertiary periods, and especially on the Antilles and
Mascarene Islands; this family is represented only én the skirts of
the Oriental region. The Helicinide, also mainly insular, have a
curiously different range from the Cyclostomatida, although both are
chiefly developed in the West Indies; Helicina extending through
the islands of the Pacific to Australia, the Malay Archipelago and
even Burma, but not to India. The last western straggler is found
in the Seychelles, and the family is unknown in Madagascar or in
Africa. The Proserpinide are confined to Central America and the
West Indies. The last, judging by the small amount of differentia
tion and dispersal that they have undergone, may be of more recent.
origin than the others, whilst the abundance of the Cyclostoma-
tide on old continental islands and their poor development on
continents may show them to be of an older and less improved type
than the Cyclophoridw. Fossil forms of several kinds have been
found in Europe and elsewhere, but their affinities and even the
families to which they should be assigned are in general extremely
doubtful. !
Now this fact, that different subdivisions of an order, class or
subkingdom have in all probability originated at different periods in.

* The terms are those of Fischer's ‘Manuel de Conchyliologie.’

ANNIVERSARY ADDRESS OF THE PRESIDENT. 73

the earth’s history and at distinct points of the surface, renders it
impossible to accept the evidence of the iarger groups as a whole.
Neither the evidence of the freshwater fishes nor that of laud and
freshwater mollusca as to distribution can be viewed in the same
light as that of mammalia, birds, or reptiles. In the latter cases all
are homogeneous to that extent, at all events, that we are probably
dealing with descendants of one terrestrial form, and there can be
little doubt that all fresh groups have diverged from one centre; in
the former case there may have been several centres and several
ancestral stocks. In order to analyze the evidence afforded by
freshwater fishes and land mollusca, we must take separately each
family or other subdivision confined to land or fresh water.

Land and freshwater mollusca are probably for the most part very
ancient, and but for two circumstances would afford invaluable
evidence as to ancient distribution of land-areas. The two difficulties
are :—(1) that we are tooimperfectly acquainted with the animals of
tne majority of the species in the most important order of all, the
Pulmonata, to classify them correctly; and (2) that the mystery of
the means of migration by which some of them are transported across
the seas is unsolved. The prevalent idea that land-mollusca or their
eggs are transported by floating logs appears to me extremely
improbable in a great number of forms, because, so far as is known,
very few either hybernate in wood, or lay their eggs there; and as
the wood is carried to the sea during floods, caused by heavy rains
which would certainly make every snail leave its hiding-place, the
notion that some would remain ensconced in the clefts appears quite
opposed to the habits of the animals. A few shore-haunting forms,
such as Truncatellide or Auriculide, might very possibly be thus
transported, but not Helicnde, as arule, and still less Cyclophoride*,
the majority of which are very rarely or never seen on trees or
wood,

The smaller forms and their ova are possibly, as Wallace in
his later works has suggested, transported by wind, sometimes
attached to dried leaves. This may account for the wide distri-
bution of a small form like Deplommatina, which lives amongst
dead leaves. But both the animals and eggs of many forms are ill
suited for wind-transport; some, like Acavus, have round or oval
calcareous eges of considerable weight, not easily carried into

* The genus Leptopoma is an exception, as it is said to live on trees. But its
distribution is also exceptional, some of its species being found widely dispersed
in oceanic islands.

74 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

the air, whilst other forms, such as Ariophanta, have rather large soft
membranous eggs, quite unsuited for wind-transport to any distance.
Except with the minute forms, I suspect that transport by wind
across the sea to any distance is extremely rare, and it is in
favour of this view that the species found on oceanic islands are
almost always peculiar, testifying to a long period of isolation.
On the other hand, how rapid may be the migration of some fresh-
water forms was shown by Dreissensia polymorpha, which, in about
a century, spread over a Jarge part of Europe from the Caspian to
Scotland and the south of France.

If it be the fact, as undoubtedly it is, that different subdivisions
of the animal and vegetable kingdoms have originated at different
geological periods, the next important question is whether, inde-
pendently of evidence from fossil remains, there is any clue to
difference of age, whether any characters exist by means of which
groups of more or less ancient origin can be recognized. It is
probable that, as a general rule, the most recent groups are those in
which the fewest breaks occur, and in which the distinctions
between families and genera are most difficult to define; for these
distinctions become better marked as, in course of time, links die out
through exposure to the varying effects of change in climate and
the distribution of land, the development of enemies and the
struggle for existence. It is quite true that much depends upon the
power of each group of organisms to resist the influence of change ;
thus omnivorous animals would have greater facilities for obtaining
subsistence, should their usual food no longer be procurable, than
forms that feed invariably on fruit or vegetables, or flesh or
insects, and animals with the power of flight, as already mentioned,
may escape by migration, or those adapted for an aquatic life by
swimming, whilst creatures unable to fly or swim are overwhelmed
by floods or destroyed by change of climate, famine, or enemies.
Still, after taking all these circumstances into account, and bearing
in mind that the process of evolution appears much slower in some
groups of organisms than in others, we shall probably not be far
wrong in concluding that, as a general rule, groups of living beings
with ail the members nearly related are of more recent origin than
those in which there are broad distinctions between the different
genera and families.

Amongst the whole of the Vertebrata there is, I believe, no large
group all the members of which are so closely connected together as
the passerine* birds. They comprise more than 6000 known species,

* Not including picarians such as Pict, Coccyges, Cypseli, &c.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 75

or about half of the whole class Aves. The difficulties of classify-
ing them are so great that no two authors agree as to the number
or limits of the families into. which they can be divided. They
have undoubtedly great powers of migration, and many can adapt
themselves to changed conditions, some of the higher forms, for
instance, the crows, being omnivorous and ranging all over the
world ; but very many genera are restricted in food and range, and
appear no better adapted to survive extensive changes than mammals
or reptiles are. It may be safely inferred that the Passeres are of
more recent origin than other orders of birds, and probably than
any other order of Vertebrata. Geological evidence, so far as it is
available, coincides with this ; for no remains of the order have been
found below the Miocene. It must be remembered, however, that
remains of birds from older systems are very rare. |

It will thus be observed that Sclater’s regions, adopted by Wallace
and others, were chiefly based on what is very probably the most
recently developed group of vertebrata, perhaps the most recent in
the animal kingdom.

Huxley’s scheme of zoological distribution, to which reference
has already been made, was first proposed in a paper on the
affinities and distribution of -Alecteromorphe and Heteromorphe, or
what are commonly known as Gallinaceous birds and their allies;
but it was shown that other groups of the animal kingdom confirm
the scheme first suggested by the distribution of these birds. Now
as Huxley’s system differs widely from Sclater’s, and as beth were
suggested by different orders of the same class (birds*), it is wise
to examine a little more closely how far the distribution of other
classes or orders agrees with that of the Passeres.

I haye already noticed the great importance attached by Wallace
to the mammalia. But there are serious difficulties in the way of
accepting the Passerine regions for mammals. In the first place, the
difference between the mammals of the Australian regicn and those
of all the other regions is far greater than the distinctions between
the latter, and point, as Huxley has noticed, to the Australian
region having been divided from the rest of the world by a barrier

* Reichenow (Zool. Jahrb. iti. p. 671, 1888) has proposed the following
regions for birds :—
Arctic.
Western,—North and South America.
Eastern,—Africa, Hurope, and Asia.
Southern, —Australia, New Zealand, New Guinea, &e.
Madagascar.
Antarctic.

76 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

impassable by mammals since a very distant geological period.
Secondly, as Huxley has also pointed out, the difference be-.
tween South America and Arctogeea exceeds the difference be-
tween different parts of the latter. Thirdly, the northern part of
North America contains so large a proportion, not merely of families
and genera, but of species common to the Palearctic region, that the
mammalian fauna differs less from that of Northern Asia than the
mammals of Central Asia do from those of Europe. Fourthly, the
mammals of Madagascar differ more from those of Africa than
those of the Palearctic do from those of the Oriental region *.,

* There are about a dozen mammalian genera found in Canada and the
northern part of the Nearctic region that are wanting in northern Asia; of
these, however, several of the most important, as the Skunk (Mephitis),
Raccoon (Procyon), and Brush-tailed Porcupine (Hrethizon), are Neotropical
forms that have found their way north. On the other hand, the Lynx, Wolf,
Fox, Glutton, both Bears, Marten, Elk, Reindeer, Wapiti, Bison, Wild Sheep,
Beaver, Marmot, and some other N.-American forms, are either specifically
identical with Palearctic animals or very nearly allied to them. Hesperomys
has been shown to be congeneric with Cricetus (Thomas, P. Z. S. 1888, p. 133).
In Central Asia are found several well-marked types, like Nectogale, Uropsilus,
Alurus, Hluropus, Budorcas, Pantholops, Poéphagus, Moschus, and many others,
that distinguish the fauna from that of the western Palearctic area.

In the case of Madagascar, not only are two mammalian families, Chiromyide
and Centetide, and one subfamily, Cryptoproctineg, peculiar to the island, but
out ef about 24 genera of Primates, Carnivora, Insectivora, Rodentia, and
Ungulata found in Madagascar, and about 100 found in Africa south of the
Atlas, only two, Potamocherus and Crocidura, exist in both. The oriental
genera of the orders mentioned are about 80 in number, and the Palearctic
(omitting Seals) about the same; of these about 30 are found in both regions.
Some 25 genera belonging to these orders are common to the Oriental and
Hthiopian areas, and 2% to the Palearctic and Ethiopian, or to put the matter
more clearly, the African mammals comprise 25 per cent. of Oriental, 22 per
cent. of Palearctic, and only 2 per cent. of Madagascar genera, whilst the
Madagascar forms comprise 83 per cent. of African genera. It must be
remembered that the climates of Madagascar and Tropical Africa are similar,
that of the Palearctic region very different.

Omitting New Zealand and Polynesia, the following appears to be the
division of the earth’s surface into mammalian regions : —

A. Marsupials predominating; placental mammals few; monotremes
present,
I, Australian region, comprising, besides Australia and Tasmania, New
Guinea, and the neighbouring islands east of Wallace’s line.

B. Placental mammals predominating ; marsupials few or absent; no
monotremes.
II. South-American region.
III. Arctogean region, comprising the following major divisions :—
1. Madagascar.

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ded.

It may, however, be very fairly urged that the avifauna of Mada-
gascar differs quite as widely from that of Africa as the mammalian
fauna does, and that the question of the Nearctic region is, after all,
of secondary importance. At the same time the objections noticed
tend completely to invalidate the idea of equality in the different
regions, so far as mammalia are concerned.

Passing on to the Reptilia, we shall find a greater difference. I
have already mentioned that Dr. Giinther, who at first accepted
Sclater’s regions, has been induced by the large additions to our
knowledge in the course of the last 30 years to reconsider the whole
subject ; and he has published the result in the article on reptiles in
the ‘ Encyclopedia Britannica.’ He adopts a different set of regions
for each of the three living orders of the Reptilia, of which nume-
rous representatives are found in the world. The regions adopted
for land and freshwater Tortoises are the following :—

Chelonian Regions.
1. All Europe and Asia, Northern Africa, North and Central
America.
2. Africa.

3. a. Tropical America.
b. Madagascar.
4, Tropical Pacific (Australia, New Guinea, &c.).
5. New Zealand. |
The divisions for Lizards will be found to differ materially.

Lacertiian Regions.
1, Africa with the Western Palearctic region.
2. India with the Manchurian (Eastern Palearctic) subregion.
3. Tropical Pacific (Australia, &c. as before).
4, Madagascar.
5. South and North America.
6. New Zealand. .
Lastly, the regions adopted for Snakes show a third arrange-
ment.

2. Africa, south of the Tropic of Cancer.
3. Oriental, South-eastern Asia and Malay Islands to Wallace’s line.
4, Aquilonian, Kurope, Asia north of the Himalayas, Africa north of
the Tropic of Cancer, and America north of about 45°.
5, Medio-Columbian, America, between ahout 25° and 45° N. lat.
The last being of decidedly inferior value as a distinct division.
In some respects this rational distribution resembles that of Mr. Andrew
Murray (Geographical Distr. Mamm. 1866; maps c. ci.).

78 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Ophidian Regions.

Africa south of the Atlas.

. Western Palearctic region.

. India with the eastern Palearctic region.
. North America.

. Tropical America.

. Tropical Pacific.

. Madagascar.

New Zealand.

OIBMANEWNH HE

In the last case it is especially noticed that the relations of
Madagascar to tropical America are closer than would be supposed
from this classification.

There is, I believe, no zoologist living whose knowledge of the
Reptilia exceeds Dr. Giinther’s, and as his attention was attracted
to the question of distribution so long ago as 1858, the views now
expressed are the results of a long study of the subject under the
exceptionally favourable circumstances of being in charge of the
largest collection in the world. I may add, from a long acquaint-
ance with Dr. Giinther, to whom I am indebted for calling my
attention to the article I have quoted, that he is not in the habit of
changing views once published without strong evidence. The
following sentence from his article on Reptiles is therefore of
creat weight :—‘‘The same arrangement of the so-called primary
zoological regions is not applicable to all orders of reptiles, and the
differences in their distribution are so fundamental that they can be
accounted for only on the assumption of the various orders and
families having appeared to spread over the earth at very distant
periods when land and water were differently distributed over the
surface of the globe.”

The distribution of the Batrachia has been studied afresh by
Mr. Boulenger, who has arranged the regions thus :—

I. Northern zone: Caudata abundant; Apoda wanting.
1. Europo-Asiatic region.

2. North-American region.

II. Equatorial southern zone. Hither Caudata wanting or |
Apoda present or both Caudata wanting and Apoda
present.

A. Firmisterma division.
1. Indian region.
2. African region.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 79

B. Arcifera division.
1. Tropical American region.
2. Australian region.

The limits are the same as Wallace’s. It should be mentioned,
however, that New Zealand can scarcely be assigned to the Aus-
tralian region, for its only Batrachian belongs to a family not known
to occur in Australia. Madagascar, too, has strong claims to
separation as a distinct region.

Dr. Giinther also, in the ‘Encyclopedia Britannica’ and in his
‘Introduction to the Study of Fishes’ (1880, p. 217), proposed a
scheme of distribution for the freshwater members of the class
‘Pisces.’ The following are the divisions :—

I. Northern zone.
1. Europo-Asiatic or Palearctic region.
2. North-American or Nearctic region.

IJ. Equatorial zone.
A. Cyprinoid division.
1. Indian region.
2. African region.
B. Acyprinoid division.
1. Tropical American region.
2. Tropical Pacific region (Australia, &c.).

III. Southern Zone (Patagonia, Tasmania, and New Zea-
land).

It will not be necessary to dwell long upon the Invertebrata.
They have received less attention than Vertebrates, and except in a
very few groups, more remains to be done both in ascertaining their
distribution and in determining their structural relations. Wallace,
in his work on Geographical Distribution, states that the Lepidoptera
and the best-known families of Coleoptera have approximately the
same distribution as mammals and birds; but he admits some
ditferences—for instance, the occurrence in temperate South America
of a well-marked insect-fauna allied to that of the north temperate
zone, and not to neotropical types. |

Among the land and freshwater Mollusca, the Pulmonata, and
especially the Helicede and Lamacde, need thorough revision.
Without much additional information concerning the animals (the
shells alone having been described in a great majority of species and
even In many genera) no accurate knowledge of the affinities of

80 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

different forms is possible ; and without this knowledge the study of
geographical distribution is useless. Fischer, in his ‘Manuel de
Conchyliologie’ (p. 196), has adopted regions corresponding with |
those of Sclater and Wallace, except that a Neantarctic is sepa-
rated from the Neotropical. So far, however, as the operculated
Gasteropoda are concerned (and their affinities are far better
ascertained than those of the Pulmonata), I cannot see the least
resemblance in many cases to the distribution by regions of mam-
mals and birds. I will only notice one case. The Cyclophoride
(with one genus of Helicinide and one of Cyclostomatide) of New
Guinea and the neighbouring islands, so far as they are known,
appear to differ from those of Borneo much as the latter do from
those of Ceylon, as will be seen by the following lists of genera
represented, compiled mainly from Fischer’s :—

Operculated Land Mollusca.

New Guinea and

neighbouring islands. et Capen,

Pterocyclus. Pterocyclus, — Pterocyclus.
Cyclophorus. Opisthoporus. Aulopoma.
Leptopoma. Cyclophorus. Cyclophorus.
Cyclotus. Leptopoma. Leptopoma.
Diplommatina. Cyclotus. Cyathopoma,
Leucoptychia. Diplommatina, Diplommatina.
Pupina. Opisthostoma. Cataulus.
Pupinella. Megalomastoma.
Callia. Alyczeus.
Helicina. Pupinella,
Omphalotropis. Rhaphaulus.

Helicina.

Phaneta.

Omphalotropis.

It is true that our knowledge of the Papuan mollusca is very
inferior to that of the Bornean and Ceylonese, especially the latter ;
but sufficient is known to show that the three belong to one region
as regards operculated land-shells. The same is the case with Nor-
thern Australia. It is scarcely necessary to point out that between
the mammalia of Australia with New Guinea and those of Borneo
or Ceylon there is the greatest difference.

The distribution of land-plants into six regions of approximately
equal value has never, I believe, been accepted by any botanist.
All schemes of repartition with which I am acquainted differ widely

“ANNIVERSARY ADDRESS OF THE PRESIDENT, SI

from those of Sclater and Wallace. Thus Mr, Thiselton Dyer, in
his article on the distribution of plants in the ‘ Encyclopedia
Britannica,’ follows Bentham in recognizing “ three tolerably ancient
floras,” which he divides thus :—

I, Northern.

Whe

Arctic-alpine.

2. Intermediate or temperate (in Europe, Asia, and N.

America).

3. Mediterraneo-Caucasian (countries around the Mediter-

ranean and part of S.W. Asia, extending east to

Sind).

II. Southern.

INGE

iP
ip
3.

4,
5.
Tropical.
ile

Antarctic-alpine.

Australian.

Andine (temperate S. America, Andes, and New
Zealand).

Mexico-Californian.

South African.

Indo-Malayan (including New Guinea and North
Australia),

2. American.

3.

African.

Another classification is that of Oscar Drude *, who has divided
the land-surface of the world into the following fourteen botanical
regions or, as he terms them, floral realms (Florenreiche) :—

iL,

IO Oe

Northern (northern part of Asia and America, and nearly
all Europe).

. Central Asian (Tibet, Mongolia and Turkestan, and Caspian

region).

. Mediterranean and Orient (countries around Mediterranean,

Persia, &c., to Indian frontier).

. East Asian (China and Japan).

. Middle North American (United States chiefly).

. Tropical African (Africa 8. of the Atlas, the Cape excepted).
. East African Islands (Madagascar and Mascarene Archi-

pelago).

* Pet. Mitth. Erganzungsheft, No. 74, 1884, pp. 48, 44.

82 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

8. Indian (India and S.E. Asia, Malay Archipelago, Papuasia,
Northern Australia, and Polynesia).
9. Tropical American.
10. Cape of Good Hope (a small region near the Cape).
11. Australian (Australia south of the tropics and Tasmania).
12. Novo-Zelanian. .
13. Andian (Tropical Andes, Chili, and the Argentine Republic).
14. Antarctic (southern extremity of America and antarctic
islands).

It is sufficient to point out that, in both these systems, the
greater part of the two regions of the earth which in mammalia
exhibit the greatest diversity, the Oriental and Australian, are
combined into one region.

In many respects the distribution of plants accords very well with
that of land-mollusca.

If now we proceed to consider, as a whole, the geographical dis-
tribution of such different subdivisions of the animal kingdom as
have been noticed, it will be observed that the mammals, batrachia,
freshwater fishes, and land-mollusca appear, at all events in the
opinion of the naturalists who have paid especial attention to the
subject, to approach the passerine birds in distribution more than
the reptiles or plants do. But, as I have-pointed out, the fresh-
water fishes and land- and freshwater mollusca are heterogeneous
groups made up of families and genera of various origin, and having
very often, probably as a rule, a distribution not agreeing with each
other in the smallest degree. Under the circumstances it is easy to
see how the conflicting distribution of different families amongst
such groups as land-shells or freshwater fishes will produce a general
result, in which the only dominant feature will be trivial generic
or subgeneric distinctions, closely connected with the modern distri-
bution of land and water. The batrachians to some extent are open -
to the same remark, for they consist of three orders, Anura, Cau-
data, and Apoda, having but little affinity and almost certainly
of widely different antiquity. ‘The reason why batrachia agree
on the whole with passerine birds and mammalia better than rep-
tilia, is not improbably that anurous batrachia (frogs and toads),
the only important living order, are of comparatively recent deve-
lopment. Placental mammalia, too, may be less ancient than the
reptilian orders, at all events in the present land area. There is,
in short, a strong reason for believing that the more recently deve-

ANNIVERSARY ADDRESS OF THE PRESIDENT. 83

loped groups agree with the present distribution and connexion of
land tracts better than those of more ancient origin. The relations
between the modern range of ancient families or orders and the
ancient distribution of land tracts is a problem which it may be
hoped will not always be as difficult as 1t appears at present.

Reviewing the whole evidence, I can only come to one con-
clusion, namely, that whilst Sclater’s regions adopted by Wallace
are convenient, and whilst the recognition of them by well-
understood names has been of use and has tended to increase our
knowledge of geographical distribution, they are, so far as they are
natural, a necessary result of the present and later Tertiary distri-
bution of land and water, and that they are, to a large extent,
artificial, whilst the idea of their equality is an error. The attempt
to make all forms of life fit into the particular grooves that were
designed to accommodate passerine birds appears to me Procrustean.
_ On the whole, the evidence is far too contradictory to be re-
ceived as proof of the permanence of oceans and continents.

So far I have merely laid before you reasons for doubting
whether the distribution of animals at the present day agrees so
closely with the present arrangement of land and oceanic areas as
to lead to the inference that these have always been the same. It
is evident that if there are wide distinctions in the distribution of
different groups of living beings, all cannot be cited as witnesses
+o the permanence of continents and oceans in past times, It
is quite true, however, that within the continental limits there
have existed at various geological periods seas that, even if of no
great depth, were just as complete barriers to the migration of par-
ticular forms of life as deep oceans would be. The familiar example
of the British Islands is sufficient to illustrate this fact. As noticed
by Wallace in ‘Island Life,’ Germany possesses nearly 90 species
of land mammals and Scandinavia 60, whilst in Great Britain there
are only 40, and in Ireland only 22. Of reptiles and batrachia 22
occur in Belgium, 13 in Britain, and only 4 in Ireland. The
removal of the isthmus of Suez and the substitution of a shallow
inlet, the width of the Straits of Dover, would constitute an impass-
able barrier to many animals.

It remains to be seen whether indications exist of land-connexions
in past times across areas now occupied by deep sea. All the dis-
cussion hitherto has been to a large extent preliminary to this.

- It must be remembered that different groups of animals vary very

84 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

greatly in their power to cross the sea, thus land-mammals and
batrachians are, as a rule, unable to cross any marine barriers. -
Mammals, however, can swim further in the sea than batrachians
can, the latter and their eggs being killed by sea-water. Snakes are
very rarely found in oceanic islands, and those found belong for the
most part to particular genera. The occurrence of land-tortoises on
what appear to be evidently occanic islands, such as the Gallipagos,
although unexplained, renders the Chelonia less important as evi-
dence of land-connexion. Lizards, as a rule, have very small
migratory powers across the sea, but some scinques and geckoes
appear to form an exception. The powers of dispersal in land- and
freshwater mollusca are very limited, though some of them are oc-
casionally transported across oceanic barriers.

It must not be forgotton, too, that when we wish to inquire into
the evidence of Pretertiary land-areas, we must examine as witnesses
the descendants of the oldest inhabitants, and must turn for infor-
mation to the types that occupied the region before the invading
hordes of passerine birds and placental mammals had driven out so
many of the aborigines. If we wish to know anything about
ancient distribution of land and sea, we must scrupulously ignore
the records of a later state of things. Before we can read the old
writing on the palimpsest we must clear away all traces of the
modern inscription.

I shall proceed to examine in some little detail (except in the
first instance) the evidence of ancient land-connexion :—

1. Between New Zealand and Australia.

2. Between the Solomon Islands and New Guinea.
. Between Africa and Madagascar.

. Between Madagascar and India.

. Between South Africa and South America.

Or He CO

1. New Zealand and Australia.—The question of a former union
between New Zealand and Australia has been discussed with great
ingenuity in ‘Island Life’ by Wallace, who concludes from the
geological and biological evidence that New Zealand received its
flora and fauna from Eastern Australia at a time when the latter
was divided by sea from Western Australia, and that the charac-
teristic marsupial and monotreme fauna, with all the peculiar tem-
perate flora of Australia, must at the time have been confined to the
western island, and consequently did not pass into New Zealand.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 85

The time assigned to the union is the latter part of the Secondary
era. Here it is necessary to remark that unless the two areas
remained united in the latter half of the Cretaceous period, Dico-
tyledonous Angiospermous plants, which form the great majority of
the forms common to New Zealand and Australia, must have existed
in the Australian area before there is any evidence of their having
appeared in the northern hemisphere. The essential point is,
that Australia and New Zealand are now divided by a broad
expause of sea, between 1000 and 2000 fathoms in depth.

2. The Solomon Islands.—The next case to be mentioned is very
simple, and is a rather curious illustration of the importance
of biological evidence. I have already noticed the interesting
account of the geology of the Solomon Islands given by Dr. Guppy,
and his discovery in those islands of deep-sea deposits. He infers,
on what appears at first sight good geological evidence, that the
region has undergone upheaval of not less than 12,000 feet in Post-
tertiary times. The Solomon Islands, with New Britain and New
Ireland, are represented on the ‘Challenger’ chart as connected
with New Guinea by a bank not exceeding 500 fathoms in depth,
and they are said by Dr. Guppy to be separated from each other by
channels about 400 fathoms deep *.

Now the fauna of the Solomon Islands comprises mammals,
snakes, and batrachians in considerable numbers. As, in the seas
around New Guinea, floating wood washed down by rivers is said
te occur to an extent rarely met with in other parts of the world,
the occurrence of the Solomon Island mammals might perhaps be
accounted for, without supposing the islands to have been united to
New Guinea. The forms represented comprise, besides bats,
several species of Mus, a genus that appears occasionally, by some
means or other, to be able to traverse arms of the sea, and one kind
of Phalanger or Cuscus, an arboreal marsupial. The same species
of Phalanger is found in New Britain and New Ireland, and an
allied variety, not specifically distinguished, occurs in New Guinea,
Ceram, Bouru, and Amboyna. ‘The Phalanger also extends to San
Cristoval, the most eastern of the Solomon Islands, a matter of some
interest, as will be shown presently.

The presence of the reptiles and batrachia is not, however, to be

* T am indebted to Captain Wharton for the information that no accurate
soundings are recorded.
Tt Thomas, P. Z. 8S. 1887, p. 320, 1888, pp. 470-483.

86 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

explained without communication by land. The species have been
described by Mr. Boulenger * and comprise—1 crocodile, 17 lizards, .
10 land-snakes, and 13 species of frogs and toads belonging to 5
genera, representing 3 families, Ranide, Ceratobatrachide, and
Hylide, the second of which, so far as is known at present, is
peculiar to the islands. Our knowledge of Papuan batrachians is,
however, very imperfect.

It is a well-known fact, as I have already siemiionedl that batra-
chians and their eggs are killed by sea-water, and that snakes, as a
rule, are not found on oceanic islands. No batrachian or ophidian
fauna resembling that of the Solomon Islands has ever been observed
except in islands that have been part of a continental land. It is
impossible to come to any other conclusion than that the Solomon
Islands, with New Britain and New Ireland, once formed part of
New Guinea, and that portions of the group have never been sub-
merged since the separation.

Nor is this quite all the evidence. ‘The species of frogs and
snakes appear to be pretty generally distributed amongst the islands
in such a manner as to show that the fauna is probably nearly
uniform throughout, with the exception of the easternmost island,
San Cristoval, the fauna of which is rather well known. Whilst
from the next large island to the westward, Guadalcanar, 5 frogs
and 4 snakes have been obtained, San Cristoval has only yielded
1 frog and 3 snakes. Moreover, 2 of the 3 snakes belong to the
genus Enygrus of the family Boide, probably all good climbers and
swimmers. Both the species of Hnygrus are widely dispersed, one
ranging eastward tothe Fiji Islands, the other northwestward to the
Moluccas and Pelew Islands. The third snake, Dendrophis salomonis,
found also in Duke of York Isiand, between New Ireland and
New Britain, and in several other islands of the Solomon group, is
a climbing tree-snake, that might be transported by floating trees.
Most snakes are unable to climb trees, and would be washed off
from floating branches &c. In other respects, too, the reptilian
fauna of San Cristoval, as Mr. Boulenger has shown, is Polynesian ;
whilst Mr. Woodford has pointed out (P.Z.S8. 1888, p. 250) that
certain birds and butterflies, found in the other islands, are here
wanting. Probably San Cristoval was separated from the main-
land before the other islands, just as Ireland must have been sepa-
rated from continental Europe before Great Britain. But the poverty
in batrachians and snakes of San Cristoval serves to confirm the

* Ty. Z. 8, xii, p. 85; P.Z. 8. 1887, p.-833, 1888, p. 88.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 87

necessity for land-connexion between the remaining islands and
New Guinea; for if the snakes and frogs came over the sea to all
the other islands, why have they not reached San Cristoval ?

It is evident that the separation of the Solomon group of islands
from the mainland and from each other is due to subsidence. This
appears at first opposed to the geological evidence of elevation, and
it undoubtedly proves that the islands, none of which are 12,000
feet high, cannot as a whole have been recently elevated 12,000
feet unless, since the elevation took place, they have undergone
depression sufficient to isolate them. But the raised coral- and
rhizopod-beds described by Dr. Guppy certainly appear to bear out
his views of recent elevation, and he brings forward other evidence
of much weight. On the other hand, not only are some of the
forms of batrachia and reptilia peculiar, but the rodents, and espe-
cially the bats, show striking distinctive characters. Two new
genera of fruit-eating bats (Pterop:de@) and one of Rhinolophide
have been recently described from the Solomon Islands, and are not
known to occur elsewhere. It is therefore probable that the Solo-
mon Islands must be ancient land, and the explanation of the
apparent contradiction may be that the elevation. observed by Dr.
Guppy has been partial and local, and has not extended to the
whole area. It is also probable that the depression which has sepa-
rated the different islands, with the exception of San Cristoval,
from each other is much more recent than that which divided the
eroup as a whole from New Guinea. It is far from unlikely that
the channel separating San Cristoval from the other islands will be
found, when accurate soundings are taken, to be deeper than the
channels between the remaining islands of the group.

Another instance similar to that of the Solomon Islands is
afforded by the Liu-Kiu (Loo-choo) Islands between Japan and
Formosa. Here also the depths of the surrounding seas are not, I
believe, ascertained ; the islands are represented in the ‘Challenger’
map, like the Solomons, as within the 500-fathom line. From these
islands several lizards, land-snakes, and batrachians, including a
newt, have been obtained*. Most of the species are peculiar, but
one frog is a common oriental form, and the newt is a variety of a
Chinese and Japanese species.

3. The Mozambique Channel between Africa and Madagascar.—
Before passing on to the question of an ancient land connecting

* Boulenger, P. Z. S. 1887, p. 146.
VOL. XLVI. g

88 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

India and Madagascar, I wish briefly to call your attention to the
Mozambique Channel. This channel is 250 miles broad at its nar-
rowest part and upwards of 1000 fathoms deep throughout; the
least recorded depth (which is close to the African coast in the
narrowest part of the channel) being 1130. No one questions for
a moment that Madagascar and Africa were united during part of
the Tertiary era; the large mammalian fauna of Madagascar alone
amply proves the fact. As already mentioned, only two genera of
mammals are common to Madagascar and Africa, though a few
species of reptiles and batrachians are found in both. One of the
Mammalian genera common to both areas is Crocidura, probably an
ancient type, but also possibly introduced by man; the other is
Potamocherus, a kind of pig. Now no other ungulate, except this
pig, is found in Madagascar, and hence it is probable that all
the South African Ungulata belong to the Miocene and Pliocene
European fauna, which is believed to have migrated into South
Africa after the separation of Madagascar. As Wallace has
pointed out, all pigs swim well, and Potamocherus is said to be
more of a water-animal than most pigs, and may very probably have
crossed from the mainland after the lemurs, insectivores, and other
mammals had been isolated by sea. But how far could Potamo-
cherus swim? Surely it is not likely that it could cross the Straits
of Dover. I think we are justified in assuming about 10 miles as a
probable limit of its power of crossing the sea, but, to be safe, let us
suppose double as much *, ‘Then, in Pliocene or Pleistocene times,
quite as probably the latter as the former, when Potamocherus
reached South Africa, Madagascar was separated by a channel not
more than 20 miles broad. The conclusion is inevitable that nearly
the whole depression of upwards of 1000 fathoms is of Phocene or
Post-pliocene date. Of course it must not be understood that this
date is proved. What we may consider, however, as beyond any
doubt is that the depression cannot be older than Middle Tertiary.

4, Madagascar and India.—The question whether there was in
Secondary or Tertiary times land-connexion across the Indian
Ocean between India and Madagascar has been treated at con-
siderable length, with great. ability and literary skill, by Mr. Wal-
lace in the ‘ Geological Distribution of Animals’ and in ‘Island

* Elephants are excellent swimmers, and have been known to swim, without
a rest, for six hours, and, with a rest, for nine. But the pace is very slow,
little, if at all, more than a mile an hour.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 89

Life;’ and, although this was not his first view, he has come
in the last-named work to the decided conclusion that there is no
evidence of any former land-connexion in the direction named.
With one important exception, that of the remarks on the Upper
Paleozoic and Lower Mesozoic flora*, concerning which I think
Mr. Wallace has failed to appreciate the facts as a whole, there is
scarcely anything in his arguments with which I am inclined to
disagree. Upon the evidence noticed by him, relating chiefly to
mammals and birds, his conclusions are, I think, reasonable, and I
quite concur in his reasons for rejecting Sclater’s and Hartlaub’s
hypothesis of “ Lemuria.” But he has overlooked some of the evi-
dence and is, I think, not acquainted with certain material facts.

I have already referred to the remarkable peculiarities of the
Madagascar mammal-fauna, and its great difference from that of
Africa. Precisely the same phenomenon is presented by birds t
The most characteristic Afrcian families, such as plantain-eaters
(Musophagide), colies (Colide), and Irrisoride, barbets, hornbills,
secretary-birds, and a number of genera, such as Lamprotornis,
Buphaga, Laniarius, and Telephonus, that are the common and
familiar birds of every part of Africa south of the Sahara, are
entirely wanting in the Mascarene Islands, including the Seychelles,
Mauritius, &c., whilst no fewer than four peculiar families and
a number of genera confined to the archipelago replace them.
Amongst the Mascarene birds, too, are found several represen-
tatives of Orieutal genera, or genera closely allied to Oriental
types, and without any near Ethiopian relations. Foremost
amongst these are certain bulbuls, forming the genera Jxocinclu
and Tylas, the former compesed of species which have been usually
referred to the typically Oriental genus Hypsipetes, and the latter
nearly affined. In fact, as was shown by Geoffroy St.-Hilaire, and
as Hartlaub has since pointed out, there is in the Mascarene avi-
fauna a more marked connexion with Indian than with Ethiopian
types. In the Seychelles, especially, out of the 7 passerine genera
represented by peculiar species, three, Nectarinia, Zosterops, and
Tchitrea, are Indian and African, one, Moudia, is Ethiopian, but not
Indian, and two, Copsychus and Hypsipetes, or Ixocincla, are Indian,
but not African £. |

Another singular case of distribution that corresponds with that

* “Tsland Life,’ p. 898, footnote.
+ Hartlaub, ‘ Die Vogel Madagascars u. d. benachbarten neleynbpeny 1877.
+ KE. Newton, Ibis, 1867, p. 359.

g2

go PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

of the birds is afforded by the large fruit-eating bats (Pteropida) *.
The only African genus belonging to the family is Hpomophorus,
which is confined to the continent, whilst throughout the Mascarene —
archipelago, and even in the Comoro Islands in the Mozambique
channel, the typically Oriental genus Pteropus occurs and is repre-
sented in various islands by 5 species, one or two of them only distin-
guished by critical characters from the common “ flying-fox ” of the
Indian Peninsula.

So far as the Pteropus and birds are concerned, the explanation
afforded by Mr. Wallace seems fully to meet the case. He points
out that Madagascar was probably connected with Africa in Middle
Tertiary times, before the present mammal and bird fauna of Africa,
which in Miocene (and in Greece in Pliocene) times inhabited the
Palearctic region, had been driven south by the approach of the
colder Pliocene and Glacial epochs fT, and that the connexion with
Madagascar was severed before the southward migration of the
paleearctic fauna took place, leaving in Madagascar the old African
forms which have since undergone no great modification. He,
however, points out that the areas now occupied by the Laccadive,
Maldive and Chagos atolls, the Saya de Malha and Cargados reefs, are
clearly the remains of great islands now depressed beneath the sea,
but which must have existed in late Tertiary times, and have
afforded means of migration to bats and birds. In the case of
Pteropus, which is a powerful, flier {, though I should think cer-
tainly incapable of winging its way from India to the nearest Mas-
carene Islands, this explanation is highly probable, and it applies
to such cases as Copsychus, but as regards Hypsipetes or, rather,
Ixocincla, and Tylas, the derivation from India may be rather more
ancient. It should be remembered, however, that distinct genera

* Dobson, Cat. Chiropt. B. M. Introduction, p. xxx1i.

tT It is, however, important to notice that Mr. Wallace’s account of the wide
sea occupying the Sahara and Northern India in Miocene times is founded on
geological views once current, but now, I think, shown to have been erroneous.
There is, as Zittel has shown, no reason to believe that any part of the Sahara
has been sea since the Cretaceous period, and there is no evidence that marine
conditions prevailed at any geological epoch whatever in the plain of Northern
India from Agra to the Brahmaputra (‘ Manual Geol. India,’ i. p. 393). Another
error into which Mr. Wallace has been led by geological writers is that of sup-
posing the Pikermi and Siwalik faunas to be Miocene instead of Pliocene. The
fauna which was Pliocene in Greece may not uave reached South Africa till
Pleistocene times, as stated above.

{ The Indian flying-fox, P. medius, has been captured 200 miles from land.
Sterndale, Nat. Hist. Mamm. India, p. 39,

ANNIVERSARY ADDRESS OF THE PRESIDENT. Or

in passerine birds are founded on differences that would not be con-
sidered generic in other classes of Vertebrata, and that by no means
indicate distant relationship.

The Reptiles and Batrachians of Madagascar have been much col-
lected and described of late years, and I am indebted to Mr.
Boulenger for some additions to Dr. Bottger’s list and for other
details*. The reptiles, the snakes excepted, are on the whole more
allied to African types than the mammals or birds are, although
there is the same remarkable absence of several characteristic
Ethiopian families; for instance, there are no Trionychide, Aganude,
Lycodontide, Elapide, or Viperide. The Oriental relations are
very slight. The genus Phelswma (Geckonide) is only represented
outside of the Mascarene Islands by one species found in the Anda-
mans. This, by itself, is not of much importance, for some geckoes
are rather widely distributed on oceanic islands. The distribution
of the genus Acontias and its allies is more important. This little
group of scinques, with rudimentary limbs or none, and very peculiar
head-shields, was formerly classed as a distinct family, but has now
been placed, rightly, I believe, in the great family of Scincide.
About 12 species are known with certainty, of which 4 are found in
Ceylon, 3 in Madagascar, and 5 in Southern Africa. In the batra-
chians Oriental affinities are rather better shown, for in the Mascarene
Islands are found 16 species of Rhacophorus (Ranidz), all the other
species being Oriental, and a species of Calophrynus of which the
only other 2 species are Oriental, whilst the only member of the
family Dyscophide found outside the Mascarene archipelago is the
Burmese Caluella guttulata. The Dyscophide comprise 7 genera
and 11 species in Madagascar.

In freshwater fishes there is one very curious case of affinity.
There is a family known to ichthyologists as Chromides( Chromidide),
entirely composed of freshwater species at the present time. This
family occurs in South America and throughout Africa, being well
represented in the Nile; and species belonging to two genera,
Chromis and Hemichromis, are found in the Jordan and the Lake of
Galilee, in Palestine. Three species have been described from
Madagascar, one of these constituting a separate genus under the
name of Paretroplus, and forming a link between Hemichromis and
the only Oriental genus, Hiroplus, which is peculiar to the Indian

* The data concerning the relations and distribution of reptiles and batra-
chians in the present address are chiefly taken from Mr. Boulenger’s recently
published British Museum Catalogues.

Q2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

peninsula and Ceylon, not extending even into the Indo-Gangetie
plain. Thus we appear, in this family of fishes, to have two lines of
migration indicated from Africa into Asia; one by the Nile Valley
to Palestine, the other by the Mascarene Islands to the peninsula
of India, each branch terminating in types quite distinct from the
terminal representatives of the other, and no form of the family
being known to occur in Asia, except in the localities mentioned.

In the Seychelles, to which I have already referred as the only
thoroughly authenticated case of oceanic islands composed of grani-
toid or gneissoid rocks, two Frogs and two Cecilians are found. The
latter belong to an order entirely unknown in oceanic islands
elsewhere, and not yet recorded from Madagascar. One species
pertains to a genus found also in Africa, the other to a peculiar
generic type; but the order Apoda, consisting of the Cvecilians,
is particularly well represented in Southern India. The presence
of the Batrachia serves to prove the former union of the Seychelles.
to a continent; but this might have been Africa, or Madagascar
when forming part of the African land.

The land and freshwater Mollusca of the Mascarene Islands are
just as peculiar as the vertebrates, and exhibit the same remarkable
affinities; nothing can better show that we are dealing with a very
ancient fauna. A large proportion of the molluscan genera are
peculiar, such as felicophanta, Ampelta, and Gibbus amongst the
Pulmonata, Acroptychia, Hainesia, and Tropidophora amongst the
Prosobranchiata, but perhaps the chief claim to recognition is that
in these islands, as in the West Indies, there is a remarkable de-
velopment of the Cyclostomatide, possibly due in both cases to the
preservation, under insular conditions, of the members of a family
exposed to too many enemies for vigorous development amongst the
modern denizens of Africa and 8. America. Attention has been
directed by the late Mr. G. Nevill * to the connexion with the
Oriental fauna exhibited by the land-mollusca of the Seychelles in
particular. It would take up too much time to go into detail, and
therefore I will merely say that some Madagascar shells of Helicide
so closely resemble Indian forms that I suspect them to be con-
generic, but that without detailed knowledge of the animals it is im-
possible to speak with any certainty. A Comoro Glessula and a
Seychelles Streptavis have decided Indian affinities, however, whilst a
species of Cochlostyla, a characteristic Philippine genus, and the small
Indian Helix barakporensis have been obtained from Madagascar.

* P.Z.S, 1869, p. 62.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 93

In the operculate land-shells the evidence is clearer. Of the
Cyclostomatide, the genus Cyclotopsis is peculiar to the Mascarene
Islands and the peninsula of India, and affords a case somewhat
similar to that of Htroplus in the freshwater fishes, the only other :
members of the family found in the Oriental region being an Otopoma,
met with in Cutch, and Reala (Omphalotropis) *, another Mascarene
genus, in the Andaman and Nicobar Islands and some of the Malay
islands t. But Otopoma is also found in Southern Arabia, Socotra,
&c., and does not penetrate India further east than Cutch ; whilst
Realia is an insular type, probably possessing peculiar faculties for
migration, and ranges through various islands to Polynesia and
New Zealand. It is reasonable to suppose that, in whatever way
the transfer may have taken place, Cyclotopsis reached India from
the Mascarene Islands, where Cyclostomatide abound. On _ the
other hand, there are found on the Seychelles Cyathopoma, a
genus chiefly developed in Peninsular India, Leptopoma, a Malay
type, found also in Ceylon, and Helicina, not found in India or Ceylon,
but occurring in Burma and ranging throughout the Malay Archi-
pelago and Polynesia to America and the Antilles. These types,
belonging to two totally distinct families, Cyclophoride and Heliet-
mde, must apparently have reached the Seychelles from the east-
ward, for not one of them is found in Africa. Now if there was
not land-connexion between India and the Seychelles, these mollusks
must have been transported either by floating objects, a means of
migration concerning which I have already expressed grave scepti-
cism, or through the air. But anything floating would be transported
from the Seychelles to the Indian coasts, never the reverse, as 1s
shown by the Seychelles double cocoanut, or cocus de mer, having
been known long before its origin was discovered through being
occasionally thrown upon the Maldives and Sumatra. I have
examined the weather-charts of the Arabian Sea and neighbouring
portions of the Indian Ocean, on which the currents for different
periods of the year are shown, and I think it is evident that the
westwardly currents which prevail in parts of the sea from November

* Many of the shells referred to Omphalotropis in works on land-mollusea
really belong to Assiminea, a brackish-water form belonging to a different
family.

{+ The peculiar Madagascar shell called Acroptychia metableta is wonderfully
like Cyclophorus foliaceus from the Nicobar Islands, and C. Leai from the Anda-
mans. The Madagascar Mascaria is represented in Ceylon by Cataulus, in the
Himalayas, Burma, and Borneo by Coptochilus, and in the Neotropical region
by Megalomastoma, .

94 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

till April are too slight and irregular, especially in the neighbour-
hood of the Indian coast, to transport any objects from India to the.
Mascarene Islands. .

Wallace has suggested that in 2 stormy area like many parts of
the Indian Ocean, small organisms, such as seeds of plants and eggs
of invertebrates, may be transported by the winds across seas of
considerable breadth, and he supposes that the Azores and some other
Atlantic islands have thus been stocked with plants, insects, and
mollusca*. In the latter case he especially points out that the
efficient transport in this case is not by ordinary winds such as the
trade-winds, for otherwise the Azores would have derived their
plants, insects, and shells from America, but by violent gales and
storms, which are in the north Atlantic very capricious and irregular
in direction. With regard to storms in the Indian Ocean, I con-
sulted my brother Mr. H. F. Blanford, who called my attention to
the weather- and current-charts already mentioned, and he tells me
that no storm in the Indian Ocean ever crosses the Equator, that the
storms travel on each side, away from the equinoctial line, and that
consequently, as the Mascarene Islands lie south of the Equator, and
India to the northward, the transports of seeds or eggs from one to
the other by storms is impossible. A good steady wind blows in
the S.W. monsoon (May to October) in a somewhat circuitous
course from the Mascarene Islands up the African coast, and thence
eastward across the Arabian sea ; but this, like the trade-winds of
the Atlantic, is not likely to transport solid objects to any distance.
The N. E. monsoon in the neighbourhood of the Indian coast is
too light and irregular to be of any importance.

Of course, under exceptional circumstances, light objects might be
carried by violent upward currents, such as occur in tropical cyclones,
into the higher regions of the atmosphere, as the voleanic dust was
carried from Krakatao ; but independently of the fact that the eggs
of tropical mollusca and insects would probably be killed by the
cold, this mode of transport might explain diffusion throughout the
world, but would not account for partial dissemination of special
forms confined to certain islands in particular directions. It is true
that the difficulty of transport, either by floating objects or by the
wind, would be greatly diminished by the presence of large inter-
vening islands as already explained; but still it is doubtful whether
the presence of these islands would have any important effect on the
winds or currents, so as to obviate the difficulty of transport from
India to the Mascarene Islands.

* Island Life, pp. 247, 251, 2538, &c.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 95

Numerous cases of affinity between Mascarene and Oriental
insects have been noticed, and there are similar alliances amongst
the plants, but it is impossible to enter into these. There can be
no question that the Mascarene fauna and flora, taken as a whole,
with the exception of the land-mammalia, contains a well-marked
Oriental element. ‘This has never been questioned, but it has been
urged, with much force, that the presence of this element may be ac-
counted for without its necessarily involving land-connexion between
India and Madagascar. It is, however, admitted that the existence
at a late Tertiary epoch of large intermediate islands is essential.

If, however, any geological evidence can be produced in favour of
the view that the Indian Ocean, between India and South Africa,
was bridged by land before either country was inhabited by pla-
cental, or perhaps by any mammalia, it is, I think, clear that all
the peculiar relationships of the Mascarene Islands would be satis-
factorily explained. I think that the requisite geological evidence
does exist. In the first place, attention must be called to the
remarkable flora that extended from Australia to India and South
Africa in Upper Paleozoic times. No doubt until very recently the
principal European paleontologists refused to admit that this flora
was Paleozoic, and even now the statement is occasionally made
that the Carboniferous * flora of northern lands had a world-wide
range. But the mass of evidence now available to show that the
Newcastle flora of Australia and the Damuda-Talchir flora of India
are really Upper Paleozoic, despite the absence of European paleo-
zoic plants and the presence of what are, in Europe, Mesozoic types,
is so clear that I feel sure any geologist who will examine the question
will be convinced of its truth. In Australia the facts have long been
perfectly well known, but in India they have only recently heen fully
cleared up, chiefly by the progress of discovery in the Salt Range of
the Punjab. In South Africa the evidence is less perfect, though
some important additions to our knowledge have resulted from Dr.
Feistmantel’s examination of the fossil plants, the account of which
he has been so good as to send to me. In this account, which only
_ reached me two days since, the representation of the peculiar
Damuda flora of India in South Africa is shown to be beyond
question, and much more complete than has hitherto been supposed.

Now this flora is so strongly contrasted with the Carboniferous
flora of Europe that it is difficult to conceive that the countries in
which the two grew can have been in connexion, and the hypothesis

* In the following remarks, Carboniferous must be understood to include
Permian.

96 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

of Gondwina-land, as it is termed by Suess *, a great continent
including Australia, India, and South Africa, seems more in accord--
ance with facts than Mr. Wallace’s view that ‘“ fragmentary evidence
derived from such remote periods” is “ utterly inconclusive’’t.
For if each flora could be transported across the sea, why are no
European Carboniferous plants found in the contemporaneous de-
posits of Gondwana-land and vice verséd. Carboniferous plants of
the European type are not confined to the northern hemisphere
even, for they are found on the Zambesi in Africa and ‘in Brazil.
The accounts of their occurrence in Africa south of the Zambesi
are as yet too indefinite for any clear idea of their relations to be
formed, and it remains to be seen whether the Lepidodendron said
to be found in Natal and the Transvaal is not Lower Carboniferous
or Devonian, as in Australia.

There is some evidence, though less complete than that from
Carboniferous strata, of similar floras in Jurassic beds in Australia,
India, South Africa, and also in South America.

The evidence of the Carboniferous flora is, however, open to one
objection. It may be urged that the distinction between the
Northern and Southern floras is too great to be due solely to isola-
tion, and that some other agents, such as climate, must be the
cause of the difference. Very possibly the difference may be due to
both isolation and climate; for in the lower part of the series in
India, Africa, and Australia, the best-marked proofs, yet recorded,
of glacial action in ancient rocks have been noticed, and, despite
some curious occurrences of boulders in coal-seams, no such unequi-
vocal evidence of glacial conditions has been noticed in the Carbo-
niferous of the Northern hemisphere. But additional facts in favour
of land-connexion between India and South Africa are met with
in Cretaceous times, and in this case the evidence is derived from
marine, not from fluyiatile deposits.

The Echinoderm-fauna of the Cenomanian beds found around Big,
near the Nerbudda, in Western India, comprises 8 species ¢, only 2
of which are not found in beds of the same age in Europe. The
number of species found in the Cenomanian Utatur group of South .
India of the same age is 10 §, 4 of which, all species of Cidaris, are
referred to European species, but three of the four are doubtful. The

* Das Antlitz der Erde, Bd. i. p. 768. + Island Life, p. 398, note.

{ Duncan, Q. J. G..S. xliii. p. 154.

§ Stoliczka, ‘ Paleontologia Indica,’ ser. viii. vol. iv. p. (125). See also
Manual Geol. India, pp. 290, 297, &e.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 97

Arialur beds of Southern India (Senonian) contain 26 species, of which
4 only are known from European Cretaceous deposits, and of these 4
2 are doubtfully identified. Nota single species is common to the
Nerbudda and 8. Indian Cretaceous rocks; but this is far less impor-
tant than the fact that the former contain 75 per cent. of Kuropean
forms, and the latter a percentage certainly not exceeding 40 *, and
probably considerably less. The fauna of the 8. Indian beds generally
is widely distinct from the Cenomanian forms of Europe, that of the
Nerbudda beds, so far as known, is very similar. It is a reason-
able conclusion, as I pointed out ten years ago f, that the Nerbudda
beds were deposited in a sea in direct communication with the
Cenomanian sea of Europe, and the Trichinopoly beds in waters
that were separated by a land barrier.

But the European Cenomanian fauna is found again in Southern
Arabia and in Palestine. The Trichinopoly fauna recurs in the
Khasi hills, south of Assam, 1200 miles N.E. of Trichinopoly, and
again in Natal, more than 4000 miles to the 8.W.; and it appears
almost a necessary inference that these points were on the south
coast of a tract of land that extended across the Indian Ocean.
Since I first suggested this view in 1879, it has been strongly sup-
ported by Prof. Martin Duncan’s revision of the Nerbudda Hchino-
dermata.

Nor is this all. From a study of the Jurassic fauna of the world,
that is to say from the consideration of an entirely different group
of facts, Neumayr has come to precisely the same conclusion as to a
land union between India and 8. Africa across the Indian Ocean f,
and this view is especially founded on the Neocomian fauna of
Uitenhage §, in Cape Colony. It should, however, be noticed that
near India, very possibly to the eastward, but not, I think, precisely
in the direction indicated by Neumayr, there was probably in
uppermost Jurassic or lowest Cretaceous times, some communication
between the seas to the North and South. This would explain the
occurrence of a few identical species of Mollusca, found in very high
Jurassic or low Neocomian beds in Cutch on the one hand, and near
the mouth of the Godavari on the other. A shallow strait would

* Tt must not be forgotten that this percentage is higher in the Cenomanian
HKehinodermata than in other groups, that the total percentage of Huropean
forms in the Echinodermata of the S. Indian Cretaceous rocks is only 18 per
cent., and that of European species in the whole fauna 16.

: See Man. Geol. India, Introduction, p. xxxix, & p. 297.

{ Denkschr. k.-k. Ak. Wiss. Wien, math.-nat. Cl. Bd. 1. (1885), p. 182,
Papel. ‘ Bir Yc § Loc. cit. p. 54.

98 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

have sufficed, and if this was subsequently converted into land,
the progressive diminution of European species in the three stages
of the S. Indian Cretaceous beds would be explained by the
increasing effect of isolation.

Since the above was written another and very noteworthy piece
of evidence has been pointed out, again by Neumayr, in one of the
last papers that he wrote *. In our Quarterly Journal of last year,
as an appendix to Mr. Baron’s paper “On the Geology of parts of
Madagascar,” a list of fossils identified by Mr. R. B. Newton was
added t. Four of these fossils, all species of Belemnites, were Neo-
comian, and consequently of similar age to the Uitenhage beds of
Cape Colony, formerly supposed to be Jurassic. In the Uitenhage
beds a single Belemnite (B. africanus) occurs. Not only have none
of the species recorded from Madagascar been found in the Uiten- |
hage beds, but three of them belong to a group of Belemnites called
Notoceli, and one to the Hastatz ; whilst B. africanus is referred to
the Absoluti. Now the Notocel are typically equatorial forms,
whilst the Absolut: are as typical, in the northern hemisphere, of
boreal regions. B. prstilliformis, the Madagascar representative of
the Hastati, is also a distinctly southern form in Europe. The in-
ference that the sea to the north-west of Madagascar in Neocomian.
times was part of the warm equatorial ocean, whilst the sea of the
extreme south of Africa was part of a cold southern ocean with a
distinct fauna, is inevitable, and agrees with the other points cited
in showing that a belt of land probably extended from South Africa
across the Indian Ocean in Cretaceous times.

The evidence relating to the old land-connexion between India and
South Africa has been given at greater length than would otherwise
have been necessary because of its importance, and because this is a
crucial case. So far as I amable to judge, every circumstance as to
the distribution of life is consistent with the view that the connexion
between India and South Africa included the Archean masses of
the Seychelles and Madagascar, that it continued throughout Upper
Cretaceous times, and was broken up into islands at an early Ter-
tiary date. Great depression must have taken place, and the last
remnants of the islands are now doubtless marked by the coral atolls
of the Laccadives, Maldives, and Chagos, and by the Saya de
Malha bank. It is immaterial whether Bourbon, Mauritius, and
Rodriguez ever formed part of the Mascarene land or not.

* Neues Jahrb. f. Mineral. &. 1890, p. 1.
t Quart. Journ. Geol. Soc. xlv. p. 331,

ANNIVERSARY ADDRESS OF THE PRESIDENT. 99

It is perfectly true, however, that the charts hitherto published,
for instance, that accompanying the ‘ Challenger’ narrative, show
deep water between the various banks that support the Mascarene
Islands and the Laccadives, Maldives, Chagos, and other groups.
But the soundings in the portion of the Indian Ocean between these
islands are insufficient to enable the contours of the sea-bottom to
be laid down with any approach to acccuracy; and I anticipate
that, when the contours are better known, a bank will be found to
connect the whole series from India to Madagascar. Even should
this not be the case, the evidence of land-connexion appears so
strong that it may be a question whether the whole of the ocean-
bottom between Africa and India may not have sunk to its present
depth since Cretaceous times.

5. South Africa and South America.—The only other hypothesis
to which I shall ask your attention is that of an ancient southern
continent, and especially the possibility of ancient land-connexion
between South America and Africa on the one hand and between
South America and Australia or New Zealand on the other. The
latter, if it ever existed, must have been, I think, the later of the two,
and I will give the biological evidence in its favour first. The
most interesting relations are those of freshwater fishes, the peculiar
distribution of which has already been noticed. ‘Two families,
Haplochitonde and Galaxiade*, are found only in the southern
extremity of America, New Zealand, and Tasmania with Southern
Australia, and they form a considerable proportion of the small river-
fish-fauna of those countries.

There are some well-marked alliances between the frogs and
tortoises of Australia and those of South America. The hatrachian
family Cystegnathide and the chelonian family Chelydide are
restricted to the two areas; but on the other hand no tortoises are
found in New Zealand, and the only frog occurring there is a
member of a family otherwise confined to the Palearctic region.
Moreover fossil representatives of Chelydide have been found both
in Europe and in India, so that it is not improbable that the Cysti-
guathide, which are not very high forms, may also have once had a
more extensive range. The land- and freshwater shells, too, afford
but little evidence of connexion. If, as Wallace has suggested, the
New-Zealand, Tasmanian and Patagonian freshwater fishes or their
ova can have been transported by floating ice from the Antarctic

* A Galaxias has been described from the Indian coast, but the determina-
tion appears somewhat doubtful. .

100 PROCEEDINGS OF THE GEOLOGICAL SOCTETY,

continent, the biological evidence may be accounted for without the
necessity for land-communication. Singularly enough, so far as our
present information as to the depth of the southern oceans goes, ©
there would appear at first sight to be less difficulty in supposing a
former extension of the southern continent to Australia and South
America than to Africa, the depth as shown on the ‘ Challenger ’
chart south of the former continents nowhere exceeding 2000
fathoms, whereas to the south of Africa there is represented a con-
siderable belt of greater depth. But ou an Admiralty chart, for
which I am indebted to Captain Wharton, R.N., F.R.S., and on
which all the known deep soundings are marked, none are shown south
of the southern extremity of Africa; and it is clear that, in this
and other regions, more soundings are required before the contours
of the sea-bottom in the oceanic area can be considered as deter-
mined with accuracy. So far as our present information goes, the |
ocean south of the Cape of Good Hope may be no deeper than the
Mozambique Channel, though probably the depth is greater in the
former case.

The faunal relations between Africa and South America are very
different from those between the latter and Australia. Here, again,
there are marked cases of affinity between the freshwater fishes, the
two important families Chromidide and Characinide being (with the
exception of the few Asiatic Chromidide already mentioned) confined
to the two continental areas. Nor is this all, for in the Characi-
nide, a large and important family, three out of the eleven sub-
families into which the family is divided by Ginther are both
Ethiopian and Neotropical. The importance of this fact is so great
that it deserves particular attention, for it proves a very large
amount of communication between the two areas, it being manifest
that members of all three subfamilies were transferred from one to
the other continent after extensive differentiation had taken place
in the family.

Again in the Siluride, two subfamilies are confined to the same
two regions, and amongst the few living representatives of Dipnoans,
two closely allied genera, Lepidosiren and Protopterus, represent each
other, the former in South America, the latter in Africa.

In the reptiles the principal noteworthy cases of relationship are
the following :—The Chelonian family Pelomeduside comprises three
genera, all found in Madagascar ; two are also met with in Africa, but
not in South America, whilst one genus, Podocnemis, is also South
American, but not African. The Lacertilian family Amphisbenide

. ANNIVERSARY ADDRESS OF THE PRESIDENT. 1ol

is almost equally divided between South America and Africa, except
that one genus extends north into the Mediterranean area, and that
two are found in North America. That the original connexion was
between the southern continents is, however, indicated by two of the
genera, Amphisbena and Anops, being represented in both, whilst
the Palearctic and Nearctic genera are not nearly related to each
other. Another Lacertilian family peculiar to Africa and South
America is that of the Anelytropide ; but these are not of much
importance. Some genera of snakes, e. g. Ahetulla, Dryiophis,
Dipsadoboa, and Leptodira, have the same distribution. One genus
of apodous Batrachians (Ceciliide), Dermophis, is also African and
S. American. Amongst the Batrachia the most remarkable
instance, however, is afforded by the Aglossa, a low but peculiarly
specialized group of toads, of which one family, Pipide, is purely
Neotropical, the other, Xenopide (Dactylethride), peculiar to Africa.
It is possible that this may be a case of a group having formerly a
much wider range, and the same may be the case with the dipnoans
Lepidosiren and Protopterus; but it is difficult to account for the
distribution of the Chromidide, Characimde, and Amphisbenide on
such an hypothesis. All three are well-marked and well-developed
families in both areas. Of the Chromidide, fossil representatives,
especially Pycnosterinw, are said to have been found in the Cretaceous
rocks of the Lebanon; but the relationship of these forms is not free
from doubt, and in any case they were marine, and the marine repre-
sentatives of the Chromidide are extinct. It is also true that a
wide-spread marine family, the Labride, is closely allied to the Chro-
midide, so that although it is far from probable that the African mem-
bers of the latter have originated separatel y from the American, such a
contingency might be suggested but for the evidence afforded by the
Characinde. This family is unknown in the fossil state, and there
is nothing to indicate that it ever inhabited Europe or North America.

There is another piece of evidence. If Africa was formerly in
land communication with South America, it is probable that before
the Ethiopian fauna was profoundly modified by the incursion of
Palearctic types in the Pliocene and Pleistocene periods, several Neo-
tropical forms that are wanting there at the present day existed in
South Africa. If this was the case, and if, as has already been
pointed out, there is a remnant of the old African fauna, preserved
from contact with the improved Palearctic forms, in Madagascar,
several alliances with S. American types should be found there that
can no longer be traced in continental Africa, This is precisely

102 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

what occurs. The case of the Chelonian family Pelomeduside, in
which the American genus Podocnenvis is represented in Madagascar _
but not in Africa, has already been mentioned. Besides this, two
genera of the typically American Lacertilian family of Iguanide
occur in Madagascar. Itis true that another genus is Polynesian *,
so this may be an instance of former wide distribution ; but even in
that case, the occurrence in Madagascar of two out of the only three
genera that are not American is significant. Amongst Mascarene
snakes, four characteristically American genera of Colubride are
represented— Heterodon (2 species), Liophis (2), Dromicus (6), and
Phylodryas (2), whilst two other genera are common to America
and to other regions. In fact the ophidian fauna of Madagascar,
comprising 36 species, is very much more American than African.
Lastly, amongst the Batrachia, the family Dendrobatide consists of
one genus, Mantella, with 5 species inhabiting the Mascarene Islands,
Dendrobates, the only other genus of the family (7 sp.), being Neo-
tropical.

There is one case of affinity between the Neotropical and Ethiopian
regions, amongst freshwater shells, that deserves notice. The very
peculiar family @theriidw, consists of the genus @theria, which is
African, and two genera Mulleria and Bartlettea confined to South
America. If, however, the West Indies have the same biological
relations to the Neotropical region that the Mascarene Islands have
to the Ethiopian, and the Lower or Middle Tertiary fauna of each
region has been preserved in the corresponding insular groups
respectively, the extraordinary development of Cyclostomatide in
the Antilles and in the Mascarene Archipelago may be due to the
prevalence of the family in both Africa and South America at
the time when they possessed means of communication no longer
existing. The occurrence of a few scattered species in Africa and
South America, and the extremely poor representation of the family
elsewhere, are quite in favour of this view. Even amongst the mam-
malia there are some curious relationships ; the only family of In-
sectivora belonging to the lower section of the order with narrow

* This genus is found in the Fiji Islands, which may possibly have been the
eastern extension of the great continent which doubtless at one time included
part of Australia, New Caledonia, and New Zealand. This possibility is ad-
mitted by Wallace. The occurrence in the Fiji Islands of three species of frogs,
belonging to a genus represented also in the Solomon Islands, New Guinea, the
Philippines, &c., affords a strong confirmation of the view that the Fijis are
ancient continental islands. [Mr. Boulenger informs me that a genus of
Elapoid snakes (Ogmodon) is peculiar to the Fiji Islands. ]

ANNIVERSARY ADDRESS OF THE PRESIDENT. 103

V-shaped molars that is found out of Africa and Madagascar is
that of the Solenodontide of the West Indies. ‘These insectivores
are some of the most lowly organized of all placental mammals,
and may be more ancient than other members of the subclass.
Amongst the rodents, another placental order of low organization,
one family, Octodontide, is restricted to Africa and South America.
Of course some of the instances mentioned may be explicable by
the former existence of allied forms in Europe and North America.
_ But it is very difficult to conceive that so many cases of relationship
between the lower vertebrata of Africa and South America can be
explained in this manner. The biological evidence of a former land-
connexion between South America and Africa is much stronger
than that in favour of a belt of land between Africa, Madagascar,
and India, although the latter is supported by geological data. It
is probable that the land-barrier across the South Atlantic, if that
was the form of union, lasted to a later geological epoch than that
across the Indian Ocean. )
The direction in which the communication between South America
and Africa lay is very difficult to indicate. The relationship is
chiefly shown by tropical forms, but these may have migrated far
to the southward during warm periods. It is highly probable that
the southern extremity of South America at one time extended to
the eastward, beyond South Georgia, and land may have united
this tract with South Africa; but there is nothing known of the
sea-bottom to indicate the probability of union in this direction.
The only ancient paleontological evidence, so far as I am aware,
is that pointed out by Neumayr in the paper already referred to *.
He infers land-connexion between Africa and South America in the
Jurassic and Lower Cretaceous periods from (1) the absence of
Jurassic marine beds on the western coast of Africa and on the
eastern coast of South America; (2) the evidence of ancient land in
the Cape Verde Islands and St. Paul’s; (3) the fact that the Neoco-
mian Uitenhage fauna of the Cape of Good Hope differs entirely
from the European, whilst the Jurassic fauna of western South
America does not. The first two grounds appear insufficient, even if
the facts were fully admitted; but the third has more force and
would appear to indicate a westward or southward prolongation of
the South-African land so as to meet a corresponding south-eastward
extension of South America.
It must not be forgotten that the area around the South Pole as
far north as about, 60° of south latitude, so far as is known, is occu-

* Soc cit..p. 182.
VOL. XLVI. h

104 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

pied either by land or by sea of no great depth. If the difficulty
about the depth of the intervening ocean is overcome, there is no-
improbability in the suggestion that at some period of geological
history an important continent, having connexions with South
America, South Africa, and New Zealand, may have occupied the
Antarctic area. JI have already referred to the fact that many
biologists regard the present distribution of terrestrial life as
evidence of original dispersion from an arctic centre. But unless
we are acquainted with the distribution in past times of various
groups of animals and plants, there is always a liability to regard
the stage on the road of migration from which the present repre-
sentatives of any group diverged as the original centre of distribu-
tion. Unless we can trace the actual line of migration (and that
we may probably never succeed in doing), how are we to tell whether
placental Mammals, for instance, appeared first at an arctic centre
and diverged thence to Africa, Asia, and America, or whether the
original stock came from a southern continent, for instance, South
America, and after travelling to the northern hemisphere and mi-
grating into Asia or Europe, ramified thence again into the Oriental
and Ethiopian regions? During the period of migration and eyvo-
lution great changes would take place in the country whence the
type originally sprang; and as each fresh and improved branch ap-
peared, it would spread forward to new regions and backward to the
country of its ancestral stock, where it might either exterminate in
the struggle for existence those descendants of its own ancestors
who had not progressed in structure, or live on beside the more
favoured races that had progressed sufficiently to hold their place.

That some families of living animals may have originated in the
southern hemisphere is shown by such examples as the Amphisbe-
nide, Aglossa, and Characinide, and especially by the Galaxiide
and Haplochitonide.

In this connexion there is one series of paleontological facts of
some interest. At particular geological horizons, apparently through-
out the world, there is a sudden appearance of terrestrial animals
and plants belonging to orders or even subclasses not represented in
older strata by any probable ancestors. Amongst the most remark-
able instances is the sudden appearance in the Upper Cretaceous
epoch, almost or quite simultaneously, of Acanthopterygian fishes
and Dicotyledonous Angiospermous plants *, now the dominant and

* T have heard lately of Dicotyledonous Angiosperms in Lower Cretaceous

beds in America, but the age of the beds appears to have been determined by
the fossil plants, an unsatisfactory method which has often led to error.

ANNIVERSARY ADDRESS OF THE PRESIDENT, 105

most abundant types throughout the globe. A little later in the
geological sequence, in the Eocene, there is a similar advent of
placental Mammals, anurous Batrachia, Ophidia, and perhaps of
modern types of Lacertilia, The origin of the placental Mammalia
was discussed twenty years ago by Professor Huxley, in one of the
most interesting and suggestive addresses ever delivered from this
Chair, and the conclusion to which he came affords the only satis-
factory explanation hitherto offered. He showed that the subclass
had in all probability been developed for ages before the Kocene
period in an isolated continental area that has now apparently
disappeared, but which he suggested may have been in the Pacific.

I am inclined to believe that the origin of Dicotyledonous Angio-
sperms ls even a more remarkable case than that of placental
Mammals. There is much evidence in favour of the process of modi-
‘fication and evolution amongst plants being far slower than in the
higher animals, and many of the Cretaceous and Eocene Angio-
spermous genera are undistinguishable from those existing at the
‘presentday. This Angiospermous flora could only have originated in
a great tract of land, and unless that tract was isolated by ocean
from all countries in which the earlier Mesozoic flora of Cycads,
Conifers, Equisetacez, Ferns, &c., has been found, it is difficult to
understand why no traces of the ancestral Angiospermous forms
have been detected amongst the latter.

The Mesozoic flora itself appeared in a considerable portion of the
northern hemisphere in the Triassic period as suddenly as the
Angiospermous flora did in the Cretaceous. But in this case
we have a clue to the origin of the invaders; for we now know
that this Mesozoic flora came from the south, and had established
itself in Australia, India, and in South Africa at an Upper Paleo-
-goic epoch, whilst the well-known Palwozoic flora of gigantic
- [ycopodiacee and peculiar Lquisetacee and Ferns still flourished in
Europe, Northern Asia, and North America, There is, moreover,
some evidence in favour of the view that the transfer of the southern
plants to the northern hemisphere was caused by a period of low
temperature that drove a southern temperate flora northward to the
equator. It is known from the scanty remnants of an older Carbo-
niferous (or Upper Devonian) flora found in Australia that Lycopo-
diaceous plants, similar to northern Paleozoic forms, occurred in
the southern area at an earlier date, and it is quite possible
that the Newcastle flora of Australia and the Gondwana flora of
India, the evident precursors of the Mesozoic flora of Arctogzea,

106 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

came originally to Australia from an antarctic continent. It is
highly probable that many other forms of terrestrial life besides the
Mesozoic flora originated in the southern hemisphere; and unless a
very considerable area of what is now deep ocean was occupied by
land in Mesozoic and Paleozoic times, a change in favour of which
there appears but slight evidence, it is far from improbable that
the Antarctic continent was the original area of development.

The land-areas of the present day may differ in one important
particular from those which existed at earlier periods of the earth’s
history. With the exception of America and Australia, all the great
land-masses are joined together in the northern hemisphere, and
there cannot be a question that the division in the case of America
is of extremely recent date; for, as I have already mentioned, a con-
siderable proportion of the higher land-animals, especially carnivores
and ungulates, found in the northern parts of America, Asia, and
Kurcpe are identical, and it is evident that the duration of species
in those orders is not great, for very few, if any, were living in
Phocene times. It is far from unprobable that formerly the great
land-masses were more isolated, and consequently terrestrial orga-
nisms, such as mammals and most terrestrial reptiles, may have
had far less facilities for spreading throughout the globe. The
extraordinary diffusion of terrestrial forms in the Upper Cretaceous
und Eocene periods may perhaps have been caused by some great
breaks in the continuity of the general land-area having been then
filled up. As plants have, as a rule, greater power of diffusion
than mammals, it is not surprising that the dissemination of
angiosperms throughout the northern hemisphere preceded that of
placental mammals. There is just a possibility, if higher forms of
terrestrial life originated in the southern hemisphere in Paleozoic
and early Mesozoic times, that the origin may have been due
to a greater development of Jand in that direction, and to the
ereat land-masses being connected to the southward up to the
Cretaceous or Eocene period, much as they have been united to the
northward in the later geological epochs.

There may even, in the Mesozoic era, when South Africa was
united to India vid Madagascar on one side and to South America
on the other, especially if the Indo-Malay continent was also con-
nected with the Australian, have been a girdle of land, chiefly in
low latitudes, round nearly three quarters of the earth’s circum-
ference from Peru to New Zealand and the Fiji Islands; and this

ANNIVERSARY ADDRESS OF THE PRESIDENT. 107

arrangement of the land-areas would perhaps explain the distri-
bution of the modern flora in belts, as shown by Mr. Thistelton
Dyer, and account for the dissemination round so large a part of
the globe of a great tropical flora and of certain tropical forms of
animal life, for instance, Jgwanide, apodous Batrachians, and some
families of land-mollusca.

It will thus be seen that whilst the general permanence of ocean-
basins and continental areas cannot be said to be established on
anything like firm proof, the general evidence in favour of this view
is very strong. But there is no evidence whatever in favour of the
extreme view accepted by some physicists and geologists that every
ocean-bed now more than 1000 fathoms deep has always been ocean,
and that no part of the continental area has ever been beneath the
deep sea. Not only is there clear proof that some land-areas lying
within continental limits have at a comparatively recent date been
submerged over 1000 fathoms, whilst sea-bottoms now over 1000
fathoms deep must have been land in part of the Tertiary era, but
there are a mass of facts both geological and biological im favour
of land-connexion having formerly existed in certain cases across
what are now broad and deep oceans.

I have not hitherto adverted to the question of the origin of coral
atolls for two reasons, first that it is far better to discuss the ques-
tion of the permanence of ocean-basins on evidence which is not a
matter of dispute, secondly that I have a strong impression, almost

amounting to conviction, that a belief in the unchangeable character
of the oceanic area has been the origin of much of the opposition to
Darwin’s theory of the connexion between atolls and areas of sub-
sidence*. It will, however, be manifest that if, as I think is pro-
bable, there was a belt of land across the Indian Ocean in Cretaceous
‘times, represented during the greater part of the Tertiary era by
large islands, and if the position of those islands is now indicated
by the atolls of the Laccadives and Maldives and the great sunken
atoll-shaped banks of Chagos and Saya de Malha, it is clearly con-
sistent with this theory that atolls, asa rule, occupy areas of depres-
sion.

* T cannot but think that this is especially the case with one of the principal
writers on the subject, Mr. John Murray, and to this I attribute the circumstance
that, whilst calling attention to the submarine “elevations” which rise from
considerable depths to within a-few hundred fathoms of the surface, he has
omitted to notice that such shoal-areas may be sunken islands, and result
from subsidence, not elevation.

108 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

So far as I have been able to form an opinion, I entirely agree
with the views expressed by my friend Prof. Bonney in the Appendix
to the third edition of Darwin’s ‘Structure and Distribution of
‘Coral Reefs.’ The evidence brought forward by Mr. John Murray,
Prof. Agassiz, Dr. Guppy, and others, vertainly shows that an atoll
with a shallow lagoon may originate in an area that is stationary or
even undergoing slow elevation. At the same time I cannot concur
‘in the theory of the origin or deepening of atoll-lagoons by solution.
If sea-water were capable of dissolving corals to this extent, it is
difficult to understand how any marine limestones can haye origi-
nated, especially such as the chalk, which is’ chiefly composed of
minute Foraminifera. It has been urged by Mr. John Murray that
coral atolls may be founded on submarine banks raised to within the
limits at which reef-building corals grow (whether this be 15, 20, or
25 fathoms or more) by the deposition of shells from small floating
Mollusca, Crustacea, Foraminifera, &c. Some explanation is neces-
sary why the sea-water should be incapable of dissolving these
minute shells, but yet should have the power of forming deep lagoons
by solution of the far more solid corals. In the lagoon, it must be
remembered that the sea-water is far less quickly renewed than in
the open sea, and must be quickly saturated, and also that the
higher temperature of the lagoon-water, by diminishing the amount
of carbonic acid in solution, would lessen the quantity of calcium
carbonate that the water could dissolve. I believe, however, that
very few observers are now prepared to accept the hypothesis of the
formation of the atoll-lagoons by the solution of the coral rock * ;
and if this be not accepted, it is difficult to understand how lagoons

_40 fathoms deep and upwards, as in some of the Maldive Islands
_and on the Chagos and Saya de Malha banks, can have been formed
without subsidence.

There is another point to which Darwin especially called atten-
tion, but which has, I think, been greatly overlooked in the recent
discussions, the cumulative nature of the evidence ft. The frequent
occurrence of atolls in groups is noteworthy. The Laccadive and
Maldive atolls are together more than 30 in number, and on the
theory of subsidence, with the understanding that, as the land sank,
coral-reefs formed gradually and grew part passu with the ‘depres-
sion, it is easy to understand hew it occurs that all are now at one

* Mr. G. C. Bourne’s remarks, Proc. Roy. Soc. xliii. 1888, p. 449, are very
important.
t+ See ‘Coral Reefs,’ ed. ix. pp. ix, 125, &e.

ANNIVERSARY ADDRESS OF THE PRESIDENT. 109

level. But on the theory of elevation or of gradual building up by
volcanic outbursts, it is scarcely credible that all should have been
brought within 20, 100, or even 500 fathoms of the surface, but
that not one should have been raised above the sea. If the atolls
occupied the site of rocky islands worn down to a little below
the sea-level by marine denudation, the atoll-form remains to be
explained ; for marine denudation could not make lagoons 30 or 40
fathoms deep. Moreover the formation of the coral-reefs would
surely here and there have protected and preserved some little knoll
formed of the original foundation rock. Further, if, as has been
urged, atolls are founded on the summits of submarine elevations
formed by. volcanic eruptions or on the remains of volcanic islands
worn down to a little below the surface of the water by marine
denudation, they should be most abundant amongst groups of vol-
canic islands, where both the forms of shoal just specified would be
most likely to occur. But this is not the case: the atolls are found
by themselves over large areas of ocean, where no other island
emerges from the surface and where no trace of volcanic action is
observed, and there are either no atolls, or, so far as I can learn,
very few and small atolls, amongst the Archipelagoes that mani-
festly owe their origin to volcanic action.

Other and most important facts in favour of subsidence in the
case of the Pacific atolls and barrier-reefs have been brought to
notice so recently and so ably by Prof. Dana *, that it is unnecessary
to do more than advert to them. The proofs afforded of subsidence
in the eastern islands of the Fiji group, and in several other cases
where islands indented by deep inlets are surrounded by barrier-
reefs, must be convincing to all who have paid attention to the
evidence of elevation and subsidence along coast-lines. The curious
examples of vertical walls descending to depths of 300 and, in one
case, 600 fathoms are also easily explicable as the results of sub-
sidence, but not, so far as I can see, in any other way, unless the
very improbable hypothesis be adopted that they are due to faulting,

It is necessary to recall attention to the leading points of evi-
dence, because in the discussion of details the broad facts on which
Darwin’s theory was originally founded are liable to be over-
looked.

In concluding what has, I fear, been a somewhat dreary recapitu-
ation of details, one pleasant task remains. When I returned from

* Am. Journ, Sc. ser. 3, xxx. pp. 89, 169 (1885).

IIo PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

India, between seven and eight years ago, I never anticipated that
I should be called upon to occupy the position in which you have
done me the honour of placing me. I have, I fear, often fallen
short of my predecessors; a life passed in great measure away
from Europe has left me very imperfectly acquainted with the
details of British geology, and it is to those details that this Society,
which has done so much for the study of our science at oe and
abroad, must be mainly devoted.

I can only express my sincere thanks for the kindness with which
I have been treated, and for the ready and kindly assistance that I
have received from the Officers, Council, and Fellows of the Society,
throughout my period of office. Ido not think, too, that 1 should
retire from this Chair without expressing my great obligations to
the salaried Officers of the Society. Lastly, I have to congratulate
you in having selected as your next President a geologist in whose
hands, I feel sure, the position and reputation of this Society will
suffer no abatement, and who is peculiarly fitted to oceupy a Chair
that has been filled by all of his predecessors in the high official
position that he now occupies.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. IIl

February 26, 1890.
J. W. Huxxn, Esq., F.R.S., Vice-President, in the Chair.

Egbert B. C. Hambley, Esq., Salisbury, North Carolina, U.S.A. ;
©. Nicholson Lailey, Esq., 15 Great George Street, Westminster.
S.W.; and Donald MacDonald Douglas Stuart, Esq., Oldland,
Bristol, were elected Fellows of the Society.

The List of Donations to the Library was read.

The following communication was read :—

‘On the Relation of the Westleton Beds or ‘ Pebbly Sands’ of
Suffolk to those of Norfolk, and on their extension inland, with some
observations on the Period of the final Elevation and Denudation of
the Weald and of the Thames Valley.—Part III. On a Southern
Drift in the Valley of the Thames, with Observations on the Final
Elevation and Initial Subaerial Denudation of the Weald, and on
the Genesis of the Thames.” By Prof. Joseph Prestwich, D.C.L.,
BF R.S., &c.

The following specimens were exhibited :—

Specimens from Pebble-Beds, exhibited by Prof. J. Prestwich,
D.C.L., F.R.S., F.G.8., in illustration of his paper.

Three photographs of sections recording Glacial Action in East
Berkshire, exhibited by the Rev. Dr. A. Irving, F.G.S.

Specimens and microscopic sections of Radiolarian Chert from
the Ordovician strata (= Llandeilo-Caradoc) of the Southern Uplands
of Scotland, exhibited by Dr. G. J. Hinde, F.G.S., on behalf of the
Geological Survey of Scotland.

In explanation of the latter, Dr. Hinde said :—

‘The specimens on the table are from strata of Ordovician age
(the equivalents of the Llandeilo-Caradoc series of Wales) from the
Southern Uplands of Scotland, in the Counties of Lanarkshire and
Peebleshire. They were sent to me for examination by B. N. Peach,
Esq., F.R.S.E., F.G.8., of the Geological Survey of Scotland, with
the view of ascertaining if the Chert of this series resembles that of
the Carboniferous rocks in being of organic origin.

‘¢ Sections under the microscope show that the rock is filled with
minute spherical bodies, ranging up to one fourth of a millimetre in
diameter, in the majority of cases without structure; but in one
specimen they can be seen to consist of simple or concentric lattice-
like shells, some with relatively long radial spines, precisely similar
in character to the shells or tests of recent and fossil Radiolaria,
and itis probable that they can be included in the same genera with
recent forms. 7

VOL. XLVI. é

DEZ PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

“These Ordovician chert-beds, which are, 1 believe, of consider-

able thickness, are thus shown to be of organic origin, and to be |

composed principally of Radiolarians, sponge-remains being appa-
rently rare in them, and in this feature they differ from the Yoredale
Cherts.

“This is the first definite notice of the presence of undoubted
Radiolarians in Paleozoic strata. To Prof. Dr. H. A. Nicholson*,
F.LA., F.G.S., of Aberdeen, belongs the credit of having first noticed
these organisms in the Chert ; but in his specimens only casts without
structural characters were preserved, and they were conjectured to
be Radiolarian—a conjecture which is now shown to be correct.” |

March 12, 1890.
J. W. Hurxz, Esq., F.R.S., Vice-President, in the Chair.

George Sweet, Esq., Brunswick, Melbourne; and Mount Rat-
navélacharia, Esq., Assistant-Conservator of Forests, H.H. the
Nizam’s Service, Hyderabad, Deccan, were elected Fellows of the
Society.

The List of Donations to the Library was read.

The following communications were read :—

1. “On a Deep Channel of Drift in the Valley of the Cam,
Essex.” By W. Whitaker, Esq., B.A., F.R.S., F.G.S.

2. «On the Monian and Basal Cambrian Rocks of Shropshire.”
By Prof. J. F. Blake, M.A., F.G.S.

3. “On a Crocodilian Jaw from the Oxford Clay of Peter-
borough.” By R. Lydekker, Esq., B.A., F.G.S., &c.

4, ‘On two new Species of Labyrinthodonts.” By R. Lydekker,
Esq.) B.As, PGs...

The following specimens were exhibited :—

Rock-specimens and microscopic sections, exhibited by Prof. J.
F. Blake, F.G.8., in illustration of his paper.

Specimen and cast of Crocodilian Jaws, exhibited by R. Lydekker,
Esq., F.G.S., in illustration of his paper.

Human skull, found 27 feet below the surface in the Manchester
Ship-canal excavations in sand, exhibited on behalf of Mr. Aber-
nethy, the Consulting Engineer, by Capt. A. W. Stiffe, F.G.S.

* Trans. Edinb, Geol. Scc. vol. vi. part i. p. 56 (1890).

Te.

a

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. LES

With regard to this specimen Capt. Stiffe said that by the
courtesy of Mr. Abernethy, Consulting Engineer of the Manchester
Ship-canal, he was enabled to lay this specimen before the Meeting.
The skull appears to be that of a man, probably from 20 to 25 years
of age, and it was found at a depth of 27 feet from the surface, at a
spot indicated upon a plan exhibited to the Meeting, in a bed of
fine sharp sand, beneath a deposit of blue silt (33 feet), overlain by
red clay (6 feet). The skull is not remarkable in shape, but from
its appearance it would seem to be of considerable age.

Three specimens from Trinidad, exhibited by N. F. Robarts, Esq.,
F.GS.

March 26, 1890.
J. W. Hurxs, Esq., F.R.S., Vice-President, in the Chair.

Isaac Ashmore, Esq., Rosemont House, Chetwynd, N ewport,
Salop; David Balfour, Ksq., Mem.Inst.C.E., Myre Hall, Houghton-
le-Spring, Co. Durham ; Arthur Brown, Esq., 54 Warrington Road,
Neweastle-on-Tyne ; Edward Henry Davies, Esq., Hampden Club,
London, N.W.; Edward Greenly, Esq., of the Geological Survey of
_ Scotland, 16 Brondesbury Villas, Kilburn, N.W.; Joseph Mac-
pherson, Ksy., 4 Calle de ’Exposicion, Bario do Monasterio, Madrid ;
David Davey Rosewarne, Esq., Government Inspector of Mines for
South Australia, Adelaide, South Australia; Wilfred Ivanhoe
Thomas, Esq., 33 Chancery Lane, W.C.; and David Tyzack, Esq.,
71 Westgate Road, Newcastle-on-Tyne, were elected Fellows of the
Society.

The List of Donations to the Library was read.

The following communications were read :—

1. “On a new Species of Cyphaspis from the Carboniferous
Rocks of Yorkshire.” By Miss C. Coignou. (Communicated by
Professor I’. M°K. Hughes, M.A., F.R.S., F.G.S8.)

2. “On Composite Spherulites in Obsidian from Hot Springs near
Little Lake, California.” By Frank Rutley, Esq., F.G.S., Lecturer
on Mineralogy in the Royal School of Mines.

3. “A Monograph of the Polyzoa (Bryozoa) of the Hunstanton
Red Chalk.” By George Robert Vine, Esq. (Communicated by
Prof. P. Martin Duncan, F.R.S., F.G.S.)

114 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

4, “Evidence furnished by the Quaternary Glacial-Epoch Mo-

rainic Deposits of Pennsylvania, U.S.A., for a similar mode of

formation of the Permian Breccias of Leicestershire and South
Derbyshire.” By William 8. Gresley, Esq., F.G.S.

| Abstract. ]

In 1885 the writer communicated a paper to this Society* on |

certain fossiliferous nodules and fragments of haematite occurring in
the Permian Breccias of Leicestershire ; and, pointing to the fact that
many of these nodules &c. were more or less covered with scratches,
and occasionally exhibited polished surfaces other than slickensides,
he had reasons for supposing, with Ramsay, that such markings
were, in some way, the result of ice-action at the close of the Coal-
Period.

Since that paper was written some large subangular, grooved or
striated boulders of sandstone, about a ton in weight, have been met
with in the workings of a coal-mine in South Derbyshire, lying
immediately upon eroded Coal-measures, in Permian Breccia-beds,
at about 600 feet deep.

Spread over the denuded Coal-measures in the anthracite regions
of Pennsylvania, U.S. A., filling buried valleys and as morainic
heaps on more elevated surfaces, are large and often thick irregular
deposits of débris of rocks of various geological horizons, but chiefly
Coal-measures (conglomerates, grits, sandstones, slates, shales, coal,
fireclay, and ironstone), of all sizes up to hundreds of tons, mixed
with clay and ground-up materials. Immediately below this drift
excellent examples of glacial strie are frequently found, 2m situ,
upon the rocks; and some large ‘‘pot-holes” (one 48 ft. wide by
38 ft. deep) have been found in shallow excavations, which were
met with incidentally in the ordinary course of mining the
anthracite +. Probably no geologist questions the origin of these
surface-accumulations, namely, that they are of “the Glacial
Period.” :

The nodules of ironstone occurring in these Glacial deposits in
Pennsylvania are scratched or striated in precisely the same manner
as are those in the Permian deposits of Leicestershire and Derby-
shire ; in fact, except for colour, which goes for little or nothing,
one could not tell one specimen from the other. Furthermore, these
ironstones have been much more scratched than any other kind of
rock-fragment in both the English and American deposits. We
may satisfactorily account for this circumstance when we reflect
that, putting coal and clay on one side, the ironstone nodules would
suffer most in this respect, especially as the siliceous fragments
largely predominate, and are not often visibly affected that way.

It cannot be supposed that these ironstone nodules in North
America were scratched previous to the Quaternary Period, but
those of the English Permian were previous to that epoch. We

* Quart. Journ. Geol. Soc. vol. xli. Proceed. pp. 109, 110.
+ See ‘ Geological Survey Pennsylvania,’ Annual Report 1885.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 115

may therefore conclude that one and the same agency, namely, that
of ice, has done the work at each period.

Discussion.

Dr. Spencer referred to his own glacial experiences in America,
though in districts mostly north-west of Pennsylvania. In some
cases he had known deposits nearly 1000 feet thick. The last of
the till-deposits had been laid down before the beaches of the Great
Lakes, which might be traced for hundreds of miles. These beaches
have been much affected by subsequent terrestrial warpings, showing
that there were no highlands north of the Great Lakes affording a
breeding-ground for glaciers at the close of the Upper-Till episode.
He concluded that in studying the drift deposits, no consideration
had been taken of the deformation of the American continent due
to warping.

Dr. Hinbz said that as none of the pebbles referred to in the
paper were exhibited, it was not possible to form an opinion as to
the origin of the striations on them.

Prof. Green spoke of some striated pebbles which he had brought
from South Africa, but it had been suggested that in landslips the
action of one pebble sliding over another might have produced
these.

Mr. Monckton failed to see how the American instance given
helped the evidence, such as it was, in favour of the glacial origin
of the Permian Breccias of Leicestershire.

The Srcrerary said that no further particulars were given; he
had read the whole note.

The following specimens were exhibited :—

Specimen of Cyphaspis, exhibited by Prof. 'T. M‘Kenny Hughes,
F.R.S., F.G.8., in illustration of the paper by Miss Coignou.

Specimens and microscopic section of Spherulites in Obsidian, ex-
hibited by Frank Rutley, Esq., F.G.S., in illustration of his paper.

Bryozoa (Polyzoa) from the Red Chalk of Hunstanton, exhibited
by T. Jesson, Esq., F.G.S., in illustration of the paper by G. R.
Vine, Esq.

April 16, 1890.
J. W. Hurkn, Esq., F.R.S., Vice-President, in the Chair.

William Hew Coltman, Esq., B.A., 13 Queen’s Gate Gardens,
S.W.; and Robert 8. Wyld, Esq.. Jun., Memb.Inst.C.E., Oswestry,
Shropshire, were elected Fellows ; Dr. Dionys Stur, Vienna, a
Foreign Member ; and Magister Friedrich Schmidt, St. Petersburg,
a Foreign Correspondent of the Society.

The List of Donations to the Library was read.

116 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

The following communications were read :—

1. ‘On the Disturbed Rocks of North-western Germany.” By
Prof. A. von Konen, For.Corr.G.S. (Communicated by Sir Warington
W. Smyth, F.R.S., For.Sec.G.8.)

[ Abstract. ]

During the last eighteen years I have spent the better part of my
vacations in investigating and mapping the geology of parts of North-
western Germany. I have published, in the ‘ Jahrbuch der kéniglich
preussischen geologischen Landesanstalt,’ Berlin, for the years 1883—
1887, some of the results in a series of notes on dislocations.

I have therein stated that the Palzozoic rocks of Rhineland,
Westphalia, and Nassau, and of the greater part of the Harz, have
been plicated with a north-east strike at the beginning of Permian
times ; and that all the other Mesozoic rocks appear to be in perfect
concordance, except in cases in which discordance may be explained
by erosion or abrasion. Only in Tertiary times did dislocations
occur over a wide area, especially in Middle and later Miocene times
—first, with the strike to the north-west, afterwards to the north
or somewhat to the east. Dykes of basalt were intruded in both
directions, and cones were formed at these periods in numerous
places ; but large areas between them remained without any percep-
tible disturbance.

I have pointed out that similar dislocations occurred even in Post-
glacial times, and probably originated the valleys of North Germany
with their peculiar directions, as well as most of the lakes of
Prussia, Brandenburg, Mecklenburg, &c., and perhaps of Switzer-
land.

I also described how [ have explained for many years past, in
my geological lectures, the way in which the synclinal and anti-
clinal lines, faults, fissures, &c. were formed by lateral or tangential
pressure; but I could mention only a few of these exceedingly
variable cases which occur in that country. |

As I have tried to describe these phenomena in as few words as
possible, it will hardly be easy to follow my meaning without ex-
amining special maps; but I think I may venture to offer to English
geologists a few observations which may help to explain volcanic
action and volcanic energy.

In the synelinal as well as in the anticlinal lines the strata, for
the most part, are not simply bent, as is generally supposed ; in
many cases they are broken and interrupted, so that the fractures
converge downwards in anticlinals and diverge downwards in syn-
clinals. The hollows thus formed were, more or less, filled by the
sliding or falling down of the uppermost beds, from either one or
both sides, so thut fissures remained.

In the immediate neighbourhood of Gottingen there are very fine
sections to be seen, which explain and corroborate what is above
stated.

Now I have found that the basalts were generally erupted through

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. I17

synclinal fissures. All the beds of lignite and brown coal worked
near Cassel*, and at other places of which I have a knowledge, dip
against the slope of the mountain, if they are penetrated by a basalt-
dyke and covered by a layer of basalt ; whereas valleys between
such mountain-ridges are due to the anticlinal between the synclinal
fissures.

This may, I think, be well explained in the following way :—
During the process of folding and faulting the hard crust of the
earth was pressed downwards more particularly in the synclinal
lines, and, if in those places any molten magma existed beneath the
crust, being compressed, it escaped by the readiest way, which was
through the synclinal fissure opening downwards, like a reversed
funnel (see the section in the above-cited ‘Jahrbuch,’ 1885, pl. i.).

Now our Middle and Upper Miocene basalts are in every way
similar to many lavas of recent volcanoes, not only in petrological
composition, but also in their geological conditions, for in several
basalt cones in Hesse and in the Khon, observed by Professor Streng
and myself, the crater-form has escaped erosion by weathering, and
these craters are associated with scorie or slags, tuffs, and lapilli.

It appears to me, therefore, not unlikely that the cause of erup-
tion of recent lavas may also be similar, and that it may be the
same as that of structural earthquakes; whereas the outburst of
gas, vapours, dust, ashes, &c., may partly result from water, passing
downwards through fissures and being overheated and vaporized.
This may account for the statement of many authors that those
violent detonations &c. of volcanoes are quite independant of the
rather quiet outflowing of incandescent lava.

I would submit these observations to English geologists, as they
are specially interested in volcanic energy and in a!l that is con-
nected with volcanoes, and as we are indebted to them for a great
deal of what we know about vulcanicity.

2. “On the Origin of the Basins of the Great Lakes of America.”
By Prof. J. W. Spencer, M.A., Ph.D., F.G.S., State Geologist of
Georgia.

3. “On Ornithosaurian Remains from the Oxford Clay of North-
ampton.” By R. Lydekker, Esq., B.A., F.G.S.

4. “ Notes on a ‘ Wash-out’ found in the Pleasley and Teversall
Collieries, Derbyshire and Nottinghamshire.” By J.C. B. Hendy,
Esq. (Communicated by Dr. W. T. Blanford, F.R.S., F.G.S.)

The following specimens were exhibited :—

Specimens of remains of Lthanphorhynchus Jessoni, Lyd., from
the Oxford Clay of Northampton, exhibited by R. Lydekker, Esq.,
F.G.8., in illustration of his paper.

[* See also Quart. Journ. Geol. Soc. vol. xi. pp. 129 & 134, figs. 1 & 2.—Ep.]

118 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

April 30, 1890.
Dr. A. Grixre, F.R.S., President, in the Chair.

Edward Byron Lindon, Esq., Assoc.R.S.M., Brisbane, Queens-
land; and Edwin Melville Richards, Esq., Assoc.Memb.Inst.C.E.,
The Butts, Warwick, were elected Fellows of the Society.

The List of Donations to the Library was read.

The following name of a Fellow of the Society was read out for the
first time, in conformity with the Bye-laws, Section VI. Article 5,
in consequence of the non-payment of arrears of contributions—
J. W. Barry, Esq.

The following communications were read :—

1. “On certain Physical Peculiarities exhibited by the so-called
‘Raised Beaches’ of Hope’s Nose and the Thatcher Rock, Devon.”
By D. Pidgeon, Esq., F.G.S.

2. “The Devonian Rocks of South Devon.” By W. A. E. Ussher,
Esq., F.G.S., of H.M. Geological Survey.

The following specimens were exhibited :—

Specimens from the raised Beaches of Hope’s Nose and the
Thatcher Rock, Devon, exhibited by D. Pidgeon, Esq., F.G.S., in
illustration of his paper. .

Pebbles from the Raised Beach at Berry Head, exhibited by A. R.
Hunt, Esq., F.G.S.

Specimens exhibited by W. A. E. Ussher, Esq., F.G.S., in illus-
tration of his paper.

Specimens of Hntomis-shale (Cypridinen-Schiefer) from Thiiringia
and the Eifel, exhibited by Prof. T. Rupert Jones, F.R.S., F.G.S.

May 14, 1890.
Dr. A. Grrxin, F.R.S., President, in the Chair.

George William Lamplugh, Esq., Wellington Road, Bridlington
Quay; and Arthur Timmins, Esq., Assoc.M.Inst.C.E., Argyll Lodge,
Runcorn, were elected Fellows of the Society.

Percy H. Browne, Esq., Reigate; T. R. Maddison, Esq., Dirtcar
House, near Wakefield ; William Rogers, Esq., The Grange, Coppull,
Lancashire ; H. Rofe, Esq., Mem.Inst.C.E., 8 Victoria Street, West-
minster ; Major-General Alexander de Courcy Scott, late R.E.,
Assoc.M.Inst.C.E., 86 Cornwall Gardens, 8.W., and Thomas Sullock

—-

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. IIg

Stooke, Esq., Assoc.M.Inst.C.E., 31 St. John’s Hill, Shrewsbury,
were proposed as Fellows; Prof. H. Rosenbusch, Heidelberg, as a
Foreign Member, and Dr. Felix Karrer, Vienna, as a Foreign Cor-
respondent of the Society.

The List of Donations to the Library was read.

The following name of a Fellow of the Society was read out for the
second time, in conformity with the Bye-laws, Section VI. Article 5,
in consequence of the non-payment of arrears of contributions—

J. W. Barry, Esq.

The following communications were read :—

1. “The so-called Upper-Lias Clay of Down Cliffs.” By 8. S.
Buckman, Esq., F.G.S.

2. “On some new Mammals from the Red and Norwich Crags.”
By E. T. Newton, Esq., F.G.S.

8. “On Burrows and Tracks ef Invertebrate Animals in Paleozoic
Rocks, and other Markings.” By Sir J. William Dawson, LL.D.,
© R.0,, &.G.S.

4, “ Contact-Alteration at New Galloway.” By Miss M. I.
Gardiner. Communicated by J. J. H. Teall, Esq., M.A., F.G-S.

The following specimens were exhibited :—

Specimens of Dwmortieria radians (Reinecke), exhibited by 8. 8
Buckman, Esq., F.G.8., in illustration of his paper.

Specimens exhibited by E. T. Newton, Esq., F.G.S., in illustration
of his paper.

A series of photographs exhibited by Sir J. W. Dawson, K. C. M.G.,
LL.D., F.R.S., F.G.S., in illustration of his paper.

Specimens of Rusichnites, Arthrophycus, and other tracks and
markings from the Ordovician and Silurian strata of Canada, referred
to in the paper by Sir J. W. Dawson, K.C.M.G., exhibited by Dr.
G. J. Hinde, F.G.8.

Rock-specimens and microscopic sections exhibited by J. J. H.
Teall, Esq., M.A., F.G.S., on behalf of Miss M. I. Gardiner, in
illustration of her paper. - |

VOL. XLVI. : k

120 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

May 21, 1890.
Dr. A. Getxr1n, F.R.S., President, in the Chair.

George Fletcher, Esq., 53 Sale Street, Derby ; and Thomas Ward,

Esq., J.P., Brookfield House, Northwich, were elected Fellows of
the Society.

The List of Donations to the Library was read.

The names of certain Fellows were read out for the first time, in
conformity with the Bye-laws, Section VI. Article 5, in consequence
of the non-payment of arrears of contributions.

The following communications were read :—

1. “On some Devonian and Silurian Ostracoda from North
America, France, and the Bosphorus.” By Prof. T. Rupert Jones,
F.R.S., F.G.S.

2. ‘On the Age, Composition, and Structure of the Plateau-
gravels of East Berkshire and West Surrey.” By the Rey. A. Irving,
BA. D.Sc. 1G:8.

3. ‘Further Note on the Existence of Triassic Rocks in the
English Channel off the Coast of Cornwall.” By R. N. Worth,
Ksq., F.G.S.

[ Abstract. ]

Specimens of a Triassic breccio-conglomerate, trawled seven miles
south of the Deadman Headland, and several miles east of the pre-
viously recorded* Lizard outlier, are described. These fragments
were brought up in a small trawl used for dredging Pectens, and are
considered to have formed part of a jagged submarine reef. They
are thin slabs, both faces of which were clearly free, as they are
covered with marine growths, animal and vegetable; and im situ
they must have had an approximately horizontal projection, on ac-
count of the different extent and character of these growths. The
rock contains angular and subangular materials, with small pebbles
in the finer portions. Its constituents are—slate (apparently De-
vonian), fine grits, vein-quartz, quartz-felsites (some micaceous),
and andesitic rock, like the “ felspathic traps” found as far west as
Cawsand ; also rhyolitic rock and kaolinized felspathic matter.

4, **On a new species of Coccodus (C. Lindstremi, Davis). By
J. W. Davis, Esq., 2.G:8., Fics.

* Quart. Journ. Geol. Soe. vol. xlii. 1886, p. 313.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. I21

The following specimens were exhibited :—

Specimens of Devonian and Silurian Ostracoda, exhibited by Prof.
T. Rupert Jones, F.R.S., F.G.S8., in illustration of his paper.

Specimens and photographs exhibited by the Rev. Dr. A. Irving,
F.G.S., in illustration of his paper.

Specimens of Triassic Rocks from the English Channel, exhibited
by R. N. Worth, Esq., F.G.S., in illustration of his paper,

June 4, 1890.
Dr. A. Gurxis, F.R.S., President, in the Chair.

Percy H. Browne, Esq., Reigate; T. R. Maddison, Esq., Dirtcar
House, near Wakefield; William Rogers, Esq., The Grange, Coppull,
Lancashire ; H. Rofe, Esq., Mem.Inst.C.E., 8 Victoria Street, West-
minster; Major-General Alexander de Courcy Scott, late R.E.,
Assoc.M.Inst.C.E., 86 Cornwall Gardens, S.W., and Thomas Sullock
Stooke, Esq., Assoc.M.Inst.C.E., 31 St. John’s Hill, Shrewsbury,
were elected Fellows; Prof. H. Rosenbusch, Heidelberg, a Foreign
Member, and Dr. Felix Karrer, Vienna, a Foreign Correspondent
of the Society.

The List of Donations to the Library was read.

The following names of Fellows of the Society were read out for
the second time, in conformity with the Bye-laws, Section VI.
Article 5, in consequence of the non-payment of their arrears of
contributions :—E. Easton, Esq.; J. R. Eppy, Esq.; R. Gascoynz,
Esq.; Dr. J. M. Granvitte; Dr. H. B. Guppy; R. Henperson,
Esq.; H. Jounson, Esq.; EH. Jorpon, Esq.; H. Lzonarp, Esq. ;
Captain E. St. F. Moore; D. Rupprz, Esq.; Rev. W. Witiams;
and Dr. J. Youne.

The Prusrpenr referred to the sad loss which the Society had
sustained through the death of Mr. Dallas, and read the following
resolution, which had been passed by the Council and ordered to be
entered upon its Minutes :—

‘The Council desires to record on its Minutes an expression
of its deep regret at the death of the Assistant-Secretary,
Mr. Dallas, which took place on the 29th ultimo, and of its
sense of the loss inflicted on the Council and Society by the
removal of one who, for the long period of twenty-two years,
had done them invaluable service, and who, by his courtesy,
kindliness, and helpfulness, had endeared himself asa personal
friend to the Fellows.”

k3

122 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

It was moved by Dr. Evans, seconded by Dr. Htiypz, and carried

unanimously, that the resolution passed by the Council be commu- _

nicated to Mrs. Dallas on behalf of the Society.

The following communications were read :—

1. “ As to certain ‘ Changes of Level’ along the Shores on the
Western side of Italy.” By R. Mackley Browne, Esq., F.G.S.

[ Abstract. ]

After noticing the prevailing opinion that such changes as he
treats of were caused by earth-movements of elevation and depres-
sion, the Author suggests that the altered levels were due to altered
conditions of the Mediterranean. He brings forward objections to
the prevailing theory :—such as, that there is an improbability of
the upraising force being equally applied; and that general earth-
movements of upheaval and depression would necessarily involve
altered level and distribution of ocean-waters. He also remarks on
the possibility of periodical oscillating alterations in the tidal depth
of the ocean.

After noticing the special characteristics of the Mediterranean :—
such as, (1) non-participation in the Atlantic tides ; (2) its surface-
level not being that of Atlantic high-water; (3) terrestrial gravita-
tion chiefly regulating the condition of its waters ; (4) its inflowing
and outflowing currents,—he infers that submergence and emer-
gence on the Bay of Baiae would follow equivalent, alteration in the
level of the Atlantic waters, such as would be probably developed
by changed combinations of astronomical forces, similar to, but
greater than the actual “changes of level’? manifested in the ordi-
nary tidal phenomena. After discussing the possible dates and
periods of the changes at Pozzuoli, he makes the suggestion that
within a period of two thousand years alterations may have taken
place in the astronomical combinations, out of which a change in the
surface-level of the oceans generally may have become developed,
and wherefrom consequently a synchronous change in the Mediter-
ranean would also occur; and he observes that the amount of actual
tidal effects has never been ascertained.

Discussion.

The PresipEnt had not gathered that the paper was the result of
any personal investigation of the coast, and felt that the Author
must expect opposition to his views.

Dr. Evans thought that a small amount of travel would solve the
question more effectually than any amount of speculation. The
Temyle of Serapis was built in immediate proximity to a volcanic
centre that had been active in modern times, and he himself saw
no difficulty in supposing small earth-movements to have occurred
without any very violent disturbance. If the Mediterranean had

"t

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 123

been moved in bulk, traces of this should be found all round the
coast, and there ought to be historic records of the event, though the
reverse was actually the case. The facts that the Temple had been
depressed some 20 feet, had stood in this position some time, and had
again been raised, were established, and these were against the theory
brought forward.

Prof. Jupp felt certain that, had the Author visited the district,
he would have found so many facts opposed to his theory that he
would never have advanced it. Monte Epomeo gave evidence of
elevation to an extent of nearly 1800 feet in the most recent geo-
logical times.

The PresipEnt had recently spent some time on the borders of the
Mediterranean, and was often struck with the proof of great stability
of level, as shown by the position of Roman towns with a strip of
alluvial flat between them and the sea, but yielding no evidence of
submergence within the historic period. Had such a general rise
of the water-level taken place as the Author demanded, there would
surely have been abundant local evidence, as well as historic proof,
of it along the low coasts of the Mediterranean.

The Avrnor had visited the neighbourhood, and he believed
unquestionable evidence of changes of level would be found all round
those coasts, as they were all the world over. His argument as to
the mean surface-level of the Mediterranean being dependent upon
that of the part of the Atlantic which lies to the westward of the
Gibraltar Straits, and as to probable alteration in the state of the
Atlantic from astronomical causes, had not been met nor even
referred to in the remarks which had been made upon his paper.

2. * North-Italian Bryozoa.” By A. W. Waters, Esq., F.G.S.

[ Abstract. |

The Chilostomatous Bryozoa dealt with in the paper are, for the
most part, from known Vicentine localities, together with some from
two new localities on the Monte Baldo, in the Veronese and Tyrol.
Reuss described a number from the Vicentine, but at a time when
the chief attention was given to the shape of the zoarium, and the
oral aperture, avicularia, and ovicells did not receive the attention
now given to them. The attempt is therefore made to bring our
knowledge of these beds, which are the richest and most important
known in the Lower Tertiaries, more nearly up to present ideas, so
that more exact comparisons may be made between Tertiary and
living forms.

Several cases are mentioned in which there is great difference of
zoarial shape, and also some in which there is great range in the
zocecial characters. |

The discovery of Catenicella in these beds is of considerable im-
portance, which is enhanced by one of the species having both short
beads and longer internodes.

I24 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Porina coronata and Lepralia syringopora both have a closure,
formed by a plate with a tubule in the centre, a structure supposed
to be exclusively characteristic of the Cyclostomata. ;

The position of the beds has been established by Suess, Bayan,
Hébert, and Munier-Chalmas as of Bartonian age, and may therefore
be called Upper Eocene.

3. * Notes on the Discovery, Mode of Occurrence, and Distribution
of the Nickel-Iron Alloy ‘ Awaruite’ and the Rocks of the District
on the West Coast of the South Island of New Zealand in which it
is found.” By Professor G. H. F. Ulrich, F.G.S.

The following specimens were exhibited :—

Specimens exhibited by A. W. Waters, Esq., F.G.S., in illustra-
tion of his paper.

Specimens exhibited by Prof. J. W. Judd, F.R.S., F.G.S., for
Prof. G. H. F. Ulrich, F.G.S., in illustration of his paper.

June 18, 1890.

Dr. A. Gerxte, F.R.S., President, in the Chair.

Thomas David Williams, Esq., West Kirby, Cheshire, was elected
a Fellow of the Society.

The List of Donations to the Library was read.

The following communications were read :—

1. “The Borrowdale Plumbago, its Mode of Occurrence and pro-
bable Origin.” By J. Postlethwaite, Esq., F.G.S.

[ Abstract. |

After giving details of the mode of occurrence of the plumbago
(graphite) of Borrowdale in veins traversing diabase and diorite,
which break through the Volcanic Series of Borrowdale, and in
‘“‘sops ” or pipes, of various sizes, at a little distance from the veins, »
the Author refers to the modes of occurrence of graphite in other
regions, and contrasts these with the surroundings of the graphite
in the Lake District. He points out that many thousand feet of
volcanic rock supervened between the Borrowdale plumbago-bearing

PROCEEDINGS OF THE GEOLOGICAL SOCIETY, 125

rocks and the overlying carbonaceous shales of Silurian age. On
the other hand, he finds similarities between the containing rocks
in Borrowdale and the diamond-bearing rocks of South Africa, and
considers that the conditions under which the graphite was formed
in the Lake District approached much more closely to those which
gave rise to the Kimberley diamonds than to those which originated
the graphitic deposits in North America, though there is great dis-
similarity in the chemical composition of the intrusive rocks in the
two cases, especially with regard to the quantity of magnesia pre-
sent. He suggests that the molten magma in its upward course
passed through a deep-seated stratum of highly carbonaceous mate-
rial, and tore off numerous fragments, the bituminous matter in
which became acted upon by heat, a further alteration being subse-
quently caused by the intrusion of the diorite.

Discussion.

Prof, SEELEY was not aware of any satisfactory description of the
Kimberley diamond-mines, which contained rocks of an essentially
brecciated deposit, and therefore, as he considered, very different
from the rocks of which the Author had given a description.

The PresrpEnT believed there were two possible sources of supply
for diamonds and graphite, viz. derivation direct or indirect from
organic matter, and (as, ¢. g., in the Archean rocks and meteorites)
as an original mineral.

2. ‘“ Notes on the Valley-Gravels about Reading, with especial
reference to the Paleolithic Implements found therein.” By O. A.
Shrubsole, Esq., F.G.S. |

The following specimens were exhibited :-—

Specimens exhibited by J. Postlethwaite, Esq., F.G.S., in illustra-
tion of his paper.

Palzolithic Implements and Mammalian remains, exhibited by
O. A. Shrubsole, Esq., F.G.S., in illustration of his paper.

ADDITIONS

TO THE
LIBRARY AND, MUSEUM OF THE GEOLOGICAL SOCIETY.

Saesian 1889-90.

I, ADDITIONS TO THE LIBRARY.

1. PERIODICALS AND PUBLICATIONS oF LEARNED SOCIETIES.

Presented by the respective Societies and Editors, uf not otherwise
stated.

Acireale. Societa Italiana dei Microscopisti. Bolletino. Vol. i.
Fase. 1-3. 1889 & 1890.
H. J. Johnston-Lavis. Su una roccia contenente leucite, trovata sull’
Etna, 26.—O. Silvestri. Sopra due nuovi generi di Rizopodi (Foramini-
fere) appartenenti al Pleocene Inferiore d’Italia, 51.

Adelaide. Royal Society of South Australia. Transactions and
Proceedings and Report for 1887-88. Vol. xi. 1889.

E. H. Rennie. On some so-called South-Australian Rubies, 17.—J.G.
O. Tepper. Notes on the Surface Features and Rocks of Nuriootpa and
its neighbourhood, 25.—J. Dennant. Notes on the Muddy Creek Beds,
with brief Remarks on other Tertiary Strata of South-Western Victoria,
30.—R. Tate. The Gastropods of the Older Tertiary of Australia, 116.—
W. Howchin. On the Occurrence of Coal Detritus in the Valley of the
Murray, 215.

: - . Vol. xii. for 1888-89. 1889.

W. Howchin. The Foraminifera of the Older Tertiary of Australia, 1.
—J.J. East. On the Geological Structure and Physical Features of
Central Australia, 31.

Alnwick. Berwickshire Naturalists’ Club. Proceedings. Vol. xii.
No. 2. 1890.

Analyst. Vol. xiv. Nos. 159-163. 1889.
——. Vol. xv. Nos. 166-170. 1890.

Annals and Magazine of Natural History. Ser. 6. Vol.iv. Nos.
19-24, 1889. Purchased.

P. Martin Duncan. On the Cretaceous Species of Podoseris, Dunc.,

24.—I’, A. Bather. Pentacrini in peculiar Beds of Great-Oolite Age near

ADDITIONS TO THE LIBRARY. 127

Basle, 49.—R. Kidston. Additional Notes on some British Carboniferous
Lycopods, 60.—H. J. Carter. Ramulina parasitica, a new Species of
Fossil Foraminifera infesting Orbitulites Mantel, var. Theobaldi, with
Comparative Observations on the Process of Reproduction in the Myce-
tozoa, Freshwater Rhizopoda, and Foraminifera, 94.—C. Brongniart.
The Cockroaches of the Carboniferous Epoch, 112.—A. 8. Woodward.
Acanthodian Fishes from the Devonian of Canada, 183.—Prof. P. Martin
Duncan. A Note upon the Anatomy of the Perignathic Girdle of Dis-
coidea cylindrica, Link., sp., and of a Species of Mchinoconus, 234.—A.
Smith Woodward. On Atherstonia, a new Genus of Paleeoniscid Fishes
from the Karoo Formation of South Africa; and on a Tooth of Ceratodus
from the Stormberg Beds of the Orange Free State, 239.—C. W. De Vis.
On the Genera Nototherium and Zygomaturus, in reply to Mr. Lydekker,
257.—R. Lydekker. Note on the above, 261.—T. Rupert Jones. Notes
on the Paleeozoic Bivalved Entomostraca, No. XX VIII. On some Scan-
dinavian Species, 267.—A. Smith Woodward. On the Myriacanthide,
an Extinct Family of Chimeroid Fishes, 275.—H. J. Carter. Sketch of
the History of known Fossil Sponges in Relation to those of the Present
Day, 280.—A. Smith Woodward. On the so-called Cretaceous Lizard,
Rhaphiosaurus, 350.—G. J. Hinde. On « true Leuconid Calcisponge from
the Middle Lias of Northamptonshire, and on detached Calcisponge
Spicules in the Upper Chalk of Surrey, 352. A

Annals and Magazine of Natural History. Ser. 6. Vol. v. Nos.
25-30. 1890. Purchased.

T. Hincks. Critical Notes on the Polyzoa, 83.—R. H. Traquair. On
the Structure of Coccosteus decipiens, Agassiz, 125.—A. H. Foord and G.
©. Crick, On the Muscular Impressions of some Species of Carbonife-
rous and Jurassic Nautiloids compared with those of the recent Nautilus,
220.—A. H. Foord and G. C. Crick. Descriptions of new and imperfectly-
defined Species of Jurassic Nautili contained in the British Museum
(Natural History), 265.—J. W. Davis. On the Dentition of Pleuroplax
(Pleurodus), A. 8. Woodw., 291.—A. Smith Woodward. Evidence of a
Fossil Tunny from the Coralline Crag, 294.—F. A. Bather. British
Fossil Crinoids, 306——F. A. Bather. British Fossil Crinoids, 373.—A.
H. Foord and G. C. Crick. On some new and impertectly-defined Species
of Jurassic, Cretaceous, and Tertiary Nautili contained in the British
Museum (Natural History), 388.—A. Smith Woodward. Notes on some
Ganoid Fishes from the English Lower Lias, 430.—F. A. Bather. British
Fossil Crinoids, 485.—Stanislas Meunier. Chemical Researches on the
Fossil Tests of Foraminifera, Mollusca, and Crustacea, 487.

Atheneum (Journal). Nos. 3217-8244. 1889.
——. Nos. 3245-3269. 1890.

——. Parts 738-744. 1889.

——. Parts 745-749. 1890.

Ballarat School of Mines. Annual Report for 1886. 1887. Pre-
sented by J. Oddie, Esq., F.G.S.
F. M. Krause. The Sedimentary Rocks of the Ballarat District, 71.

for 1887. 1888.

Barnsley. Midland Institute of Mining, Civil, and Mechanical
Engineers. Transactions. Vol. xi. Part 103. 1889.

Vol. xii. Part 104, 1889,

Pt

128 ADDITIONS TO THE LIBRARY.

Basel. Schweizerische Paliontologische Gesellschaft. Abhand-
lungen. Vol. xvi. (1889). 1889. Purchased.
I. Koby. Monographie des polypiers jurassiques de la Suisse. 9° -
Per one Golliez. Nouveaux Chéloniens de la Molasse langhienne de
ausanne.—H. Haas. Beitraige zur Kenntniss der jurassischen Brachio-
podentauna. i. Theil.—P. de Loriol. Etudes sur les mollusques des
couches coralligénes inférieurs du Jura Bernois. 1° partie.

Belfast Natural History and Philosophical Society. Report and
Proceedings for the Session 1888-89. 1889.
J. Moran. Mammoth’s Tooth recently found in the Drift Gravels at
Larne Harbour, 35.

—— Naturalists’ Field Club. Annual Report and Proceedings.
1888-89. Series 2.. Vol. iii. Part 2. 1889.
W. Gray. Vestiges of Early Man in Antrim and Down, 186.

Belgrad. Annales Géologiques de la Péninsule Balkanique. Dirigées
par J. M. Zujovié. Tomei. 1889.

Partie 1e.

J. M. Zujovic. Esquisse géologique du Royaume de Serbie, 1.—F.
Toula. Revue des terrains dans le Balkan Central, 131*.—P. Ilic. Sur
quelques minéraux de Serbie, 144*.—Z. Jurisi¢é. Dr. Josif Pancié, bio-
graphie avec le portrait, 170*.—W. Zsigmondi. Das Quecksilberberg-
werk von Avala in Serbien, 196*.—EH. Pergens. Les bryozoaires du Tas-
majdan a Belgrade, 200*.—M. Petrovic. Les sources de Fruska Gora,
202*.—M. Kispatic. Die Glaucophangesteine der Fruska Gora, 204*.—
M. Petrovié. Les marais en Backa, 205*.—W. Bruno. — Beitrag zur
Kenntniss der Erzlagerstatten Bosniens, 206*.—Rutar. Die Insel St.
Andrea in Dalmatien, 224*.—E. Fuchs. L’Isthme de Corinthe, 233*.—
EK. Tietze. Ueber recente Niveauverinderungen im Attika, 240*.—
Foullon und Goldsmith. Ueber die geologische Verhialtnisse der Insel
Syra, Syphnos und Tinos, 241*.—W. Kellner. Tiirkischer Bergbau und
ag Producte, 243*.—E. Pergens. Pliociine Bryozoen von Rhodes,

64*.
Partie 2°.

S.Radovanovic. Beitriige zur Geologie und Palaeontologie Ost-Serbiens,
Die Liasablagerungen von Regotina, 1—M. Petrovic. Les sources de
Fruska Gora, 142.—J. Partsch. Die Berge der Jonischen Inseln, 146.
(Papers with * are also in Part 2.)

Berlin. Deutsche geologische Gesellschaft. Zeitschrift. Band
xl. Heft 4. 1888. 1888.

J. Lemberg. Zur Kenntniss der Bildung und Umwandlung von Sili-
caten, 625.—G. Boehm. Ueber die Fauna der Schichten mit Durea im
Département der Sarthe, 657—A. Remelé. Ueber eimge Glossophoren
aus Untersilur-Geschieben des norddeutschen Diluviums, 666.—H.
Kunisch. Ueber eine Saurierplatte aus dem oberschlesischen Muschel-
kalke, 671.—A. Osann. Ueber den Cordier fiihrenden Andesit vom
Hoyazo (Cabo de Gata), 694.—P. Oppenheim. Neue Crustaceenlarven
aus dem lithographischen Schiefer Bayerns, 709.—F. E. Geinitz. Die
Kreidegeschiebe des mecklenburgischen Diluviums, 720.—H. Trautschold.
Ueber Ldestus protopirata, Trd., 750.—E. Koken. TZhoracosaurus ma-
crorhynchus, Bl., aus der Tuffkreide von Maastricht, 754.—J. Nolting.
Ueber das Vorkommen von Kreide unter dem Diluvium der Gegend von

ADDITIONS TO THE LIBRARY. 129

Oldenburg i. Holst.,774.—Langsdorff. Ueber isolirte Zechstein-A blager-
ungen im Gebiete der Tanner-Grauwacke an den siidlichen Auslaufern
des Bruchbergs, 775.

Berlin. Deutsche geologische Gesellschaft. Zeitschrift. Band
xh. Hefte 1-3. 1889-1890.

A. Krause. Ueber Beyrichien und verwandte Ostracoden in untersilur -
ischen Geschieben, 1.—O. Feistmantel. Ueber die bis jetzt geologisch
altesten Dikotyledonen, 27.—H. Trautschold. Ueber Coccosteus mega-
lopteryx, Trd., Coccosteus obtusus und Cheliophorus Vernewl, Ag., 35.—
H. Finkelstein. Ueber ein Vorkommen der Opalinus-(und Murchisonae P-)
zone im westlichen Siid-Tirol, 49.—E. Koken. Die Hyolithen der silur-
ischen Geschiebe, 79.—K. Endriss. Geologie des Randecker Maars und
des Schopflocher Riedes, 63.—F. Frech. Ueber Mecynodon und Myo-
phoria, 127.—F. Roemer. Ueber Blattabdriicke in senonen Thonschichten
bei Bunzlau in Niederschlesien, 139.—G. Berendt. Die Lagerungsver-
haltnisse und Hebungserscheinungen in den Kreidefelsen auf Riigen, 148.
—F. Frech. Ueber das rheinische Unterdevon und die Stellung des
“ Hercyn,” 175.—H. Kayser. Ueber einige neue oder wenig gekannte
Versteinerungen des rheinischen Devon, 288.—A. Osann. Beitrage zur
Kenntniss der Eruptivgesteine des Cabo de Gata (Prov. Almeria), 297.—
E. Sickenberger. Natiirliche Camentbildung bei Cairo, Egypten, 312.—
H. Credner. Die Stezocephalen und Saurier aus dem Rothliegenden des
Plauen’schen Grundes bei Dresden. Achter Theil, 319.—F. J. P. van
Calker. Die zerquetschten Geschiebe und die nahere Bestimmung der
Groninger Morinen-Ablagerung, 343.—J. Walther. Ueber Graphitginge
in zersetztem Gneiss (Laterit) von Ceylon, 359.—H. Credner. Die La-
gerungsverhaltnisse in den Kreidefelsen auf Riigen, 365.—C. Ochsenius.
Mineralogisch-Geologisches aus Tarapacai in Chile, 371.—F. J. P. van
Calker. Beitrage zur Heimaths-Bestimmung der Groninger Geschiebe,
385.—L. Milch. Die Diabas-Schiefer des Taunus, 394.—P. Oppenheim.
Beitrage zur Geologie der Insel Capri und der Halbinsel Sorrent, 442.—
R. Brauns. Mineralien und Gesteine aus dem hessischen Hinterland,
491.—Nathorst. Ueber Goldenbere’s Onisima ornata, 545.—A. Remelé.
Ueber Hyolithus inaequistriatus, Rem., 547.—Sir W. Dawson. Ueber
einige devonische Pflanzen, 553.—Weiss. Ueber Drepanophycus, &c.,
504.—H. Trautschold. Ueber Antiodus und andere Fischreste aus dem
oberen russischen Bergkalk, 556.—Kck. Ueber die Verbreitung der
Crinoiden-Schichten im Muschelkalk Vorarlberg, 559.

——. Gesellschaft naturforschender Freunde. Sitzungsberichte.
Jahrgang 1889. 1889.

A. Nehring. Ueber Riesen und Zwerge des Bos primigenius, 5.—-A.

Krause. Ueber Beyrichien und verwandte Schalenkrebse in markischen

Silurgeschieben, 11.—A.Nehring. Ueber fossile Spermophilus-Reste von -

Curve bei Wiesbaden, 35.—A, Nehring. Ueber die gegen ihn gerichtete
Wollemonn’sche Polemik hinsichtlich der plistocaenen Steppenfauna, 37.
—A. Nehring. Ueber Spermophilus rufescens, foss., von Praunheim bei
Frankfurt a. M., 65.—A. Nehring. Ueber das Gebiss von Cervus maral,
Ogilby, sowie tiber Cervus maral, foss., 67.—A. Koken. Ueber Pleura-
canthus, Ag., oder Xenacanthus, Beyr., 77.—A. Nehring. Ueber das
fossile Vorkommen yon Canis karagan, C. corsac, Felis manul und F.
chaus im Plistocaen Mitteleuropas, 109.—Koken. Fossile Fisch-Otoli-
then, 117.—A. Nehring. Ueber Conchylien aus dem Orenburger
Gouvernment und ihre Beziehungen zu den Conchylien des mitteleuro-
paischen Losses, 166.—A. Nehring. Ueber einige den Loess und Loess-
zeit betreffende neuere Publicationen, sowie iiber Alactaga jaculus, 189,

el

a

130 ADDITIONS TO THE LIBRARY.

Berlin. K6niglich preussische Akademie der Wissenschaften-
Nitzungsberichte, 1889. Nos. 1-53. 1889.

C. Klein. Die Meteoriten-Sammlung der Koniglichen Friedrich-Wil--
helms- Universitat zu Berlin am 15 October 1889, 843.—F. Rinne. Ueber
Limburgite aus der Umgebung des Habichtswaldes, 1007.—F. Rinne.
Ueber Gismondin vom Hohenberg bei Biihne in Westfalen, 1027.

——. Koniglich preussische geologische Landesanstalt und Berg-
akademie. Jahrbuch fiir das Jahr 1888. 1889.

Mittheilungen aus der Anstalt, ix—cxlil’. M. Stapff. Ueber Niveau-
schwankungen zur Eiszeit, nebst Versuch einer Gliederung des Eulen-
gebirgischen Gebirgsdiluviums, 1.—G. Berendt. Die beiderseitige Fort-
setzung der siidlichen baltischen Endmorine, 110.—K. Keilhack. Geo-
logische Mittheilungen aus dem sudlichen Flaming, 123.—T. Ebert. Die
Raninen des Kressenbergs, 129.—K. Keilhack, Die Gastropodenfauna
eliniger kalkhaltiger Alluvialbildungen Norddeutschlands, 134—A.
Denckmann. Ueber zwei Tiefseefacies in der oberen Kreide von Han-
nover und Peine, und eine zwischen ihnen bestehende Transeression,
150.—C. E. Weiss. Fragliche Lepidodendronreste im Rothliegenden
und jimgeren Schichten, 159.—H. Schroder. Ueber Durchragungs-
Ziige und -Zonen in der Uckermark und in Ostpreussen, 166.—L.
Beushausen. Ueber einige Lamellibranchiaten des rheinischen Unter-
devon, 212.—T. Ebert. Ueber die Art des Vorkommens und die
Verbreitung von Gervilia Murchison, Geinitz, im Mittleren Buntsand-
stein, 237.—W. Frantzen. LBeitrage zur Kenntniss der Schichten des
Buntsandsteins und der tertiiren Ablagerungen am Nordrande des Spes-
sarts, 243.—G. Lattermann. Die Lautenthaler Soolquelle und ihre
Absitze, 259.—H. Loretz. Mittheilung tber einige Eruptivgesteine des
Rothhegenden im _ studoéstlchen Thitringer- Walde, 284.—E. Dathe.
Olivinfels, Amphibolit- und Biotitgneiss von Habendorf in Schlesien, 309.
—I’. Beyschlag. Die Erzlagerstatten der Umgebung von Kamsdorf in
Thuringen, 329.—A. Jentzsch; Oxford in Ostpreussen, 378.—IX. Oebbeke.
Beitrage zur Kenntniss einiger hessischer Basalte,390. ” J. G. Bornemann.
Ueber den Muschelkalk, 417.—W. Frantzen und A. von Koenen. Ueber
die Gliederung des Wellenkalks i im mittleren und nordwestlichen Deutsch-
land, 440.—W. Frantzen. Untersuchen tiber die Gliederung des Unteren
Muschelkalks im nordoéstlichen Westfalen und im sudwestlichen Hannover,
453.—C. Diitting. Geologische Aufschliisse an der Eisenbahnlinie Os-
nabriick-Brackwede (Abhandlungen 3).

——. Zeitschrift fiir das Berg-, Hiitten- und Salinenwesen im
preussischen Staate. Band xxxvil. Hefte3 &4. 1889.

Kobrich. Ueber Messungen der Erd-Temperature in den Bohrlochern
zu Schladebach und Sennewitz, 171.

—. ——. Bandxxxvil. 1und2 Statistische Lieferung. 1889.
-——,. ——. Atlas. Band xxxvii. Tafel 5-15. 1889.

-——. ——. Band xxxvii. Hefte 1-3. 1890.

—. ——. Band xxxvii. Atlas. Taf. 1-25, und 1 Kupfer-

stich. 1890.

Bern. Schweizer Alpenclub. Jahrbuch. Jahrgang 24, 1888-89.
1889. Purchased.
A. Heim. LEinige Worte zur Geologie des Clubgebietes, 247.

—_. —. ; . Beilagen, Band 24. 1889.

ADDITIONS TO THE LIBRARY. I31

Birmingham. Mason Science College. Calendar for the Session
1889-90. 1889.

— Philosophical Society. Proceedings. Vol. vi. Parts 1 & 2.
1887-88 and 1888-89. 1888 & 1889.

F. W. Martin. First Report upon the Distribution of Boulders in
South Shropshire and South Staffordshire, 93.—H. W. Crosskey. Notes
on the Glacial Geology of the Midlands, 169.—G. Deane. Note on the
Effects of a so-called Waterspout at the Wittenham Hills, Berkshire,
205.—G. Deane. The Geology and Travels of Jean André De Luc, 281.
—C. Davison. On the Secular Straining of the Earth, 307.

Bordeaux. Société Linnéenne. Actes. Vol. xli. Livr. 4-6.
(Ser. 5, Tome 1). 1887. 1889.

E. Benoist. ‘Tableau synchronique des formations tertiaires du sud-
ouest de la France, du bassin de Paris, du bassin de Mayence et du Vi-
centin, 193 (commenced 191).

Vol. xlii. (Série 5, Tomeii.) 1888. 1890.

Mémoires.

E. A. Benoist. Description des Céphalopodes, Ptéropodes et Gastro-
podes opisthobranches (Acteonide), 11.

Procés-Verbaux.

E. A. Benoist. Sur les forages artésiens exécutés a Libourne, Arveyres
et Vayres, iii. A. Benoist. Résultats stratigraphiques des sondages
artésiens exécutés entre Bordeaux et Pauillac, xxvil.Degrange-Touzin.
Couche fluvio-marine observée a Balizac, xxxi.—H. A. Benoist. Coupe
relevée entre Plassac et Roque-de-Tau, xxxiiii—l. Fallot. Observations
faites 4 Plassac, xxxv.—E. A. Benoist. Couches 8 Nummulites du Sud-
Ouest, xxxv.—l. Fallot. Quelques remarques & propos @une note de
MM. Potier et Vasseur sur les sables du Périgord, xxxix.—Deerange-
Touzin. Compte-rendu de Vexcursion faite 4 Bazas le 1* juillet 1888,
xlv.—Vasseur. Sur ]’age des sables du Périgord, lviii—Degrange-Touzin.
Note géologique sur les envirous de Bazas et sur une coupe relevée a
Cazats, lxii—Deerange-Touzin. Note géologique sur les environs de
Bazas, Ixxii, Ixxxviil, xcill, cx1.

Boston. American Academy of Arts and Sciences. Proceedings.
N.S. Vol. xv. (Whole Series, Vol. xxiii.) Part 2. 1888.

Society of Natural History. Proceedings. Vol. xxiv. Parts
Mae A883 ©1889. . 188d.

A. Hyatt. Evolution of the Faunas of the Lower Lias, 17.—C. H.
Hitchcock. Date of the publication of the Report upon the Geology of
Vermont, 33.—S. H. Scudder. An interesting Paleozoic Cockroach
Fauna at Richmond, Ohio, 45.—J. Marcou. Canadian geological classi-
fication for the Province of Quebec, 54.—J. Marcou. On some dates of
the “ Report of the Geology of Vermont,” 83.—A.C. Lane. The Geology
of Nahant, 91.—W. Upham. Marine shells and fragments of shells in
the Till near Boston, 127.—H. T. Cresson. Early Man in the Delaware
Valley, 141.—H.T. Cresson. Remarks upon a chipped implement found
in modified drift, on the east fork of the White river, Jackson county,
Indiana, 150.—G. F. Wright. The Age of the Philadelphia Red Gravel,
152.—C. C. Abbott. Remarks upon Paleolithic Implements, 157.—F. W.
Putnam. On collection of Paleolithic Implements, 157.—A. 8. Packard.
Paleontological Notes, 209.—A. R. C. Selwyn. Canadian geological
classification for the Province of Quebec, by Jules Marcon, 216.

132 ADDITIONS TO THE LIBRARY.

British Association for the Advancement of Science. Report of the
59th Meeting. Neweastle-upon-Tyne, 1889. 1890.

Everett. Eighteenth Report of the Committee appointed for the pur--
pose of investigating the Rate of Increase of Underground Temperature
downwards in various Localities of Dry Land and under Water, 35.—T.
Rupert Jones. Seventh Report of the Committee on the Fossil Phyllo-
poda of the Paleozoic Rocks, 63.—W. C. Williamson. Report of the
Committee appointed to investigate the Flora of the Carboniferous Rocks
of Lancashire and West Yorkshire, 69.—G. W. Lamplugh. Report of
the Committee appointed for the purpose of investigating an Ancient Sea-
beach near Bridlington Quay, 70.—C. E. De Rance. Fifteenth Report
of the Committee appointed for the purpose of investigating the Circula-
tion of Underground Waters in the Permeable Formations of England
and Wales, and the Quantity and Character of the Water supplied to
various Towns and Districts from these Formations, 71.—J. 8S. Gardner.
Report of the Committee appointed for the purpose of exploring the
Higher Eocene Beds of the Isle of Wight, 89.—A. Bell. Third Report
of the Committee appointed for the purpose of reporting upon the
“Manure” Gravels of Wexford, 92.—H. W. Crosskey. Seventeenth
Report of the Committee appointed for the purpose of recording the Po-
sition, Height above the Sea, Lithological Characters, Size, and Origin of
the Erratic Blocks of kngland, Wales, and Ireland, reporting other matters
of interest connected with the same, and taking measures for their preser-
vation, 115.—J. Thomson. Report of the Committee appointed to in-
vestigate the Geography and Geology of the Atlas Ranges in the Empire
of Morocco, 165.—H. J. Johnston-Lavis. Report of the Committee ap-
pointed for the investigation of the Volcanic Phenomena of Vesuvius and
its neighbourhood, 283.—J. Milne. Ninth Report of the Committee ap-
pointed for the purpose of investigating the Earthquake and Volcanic
Phenomena of Japan, 295.—J. Pattinson and H.S. Pattinson. On Chilian
Manganese Ore, 537.—J. Geikie. Address to Section C.-Geology, 551.—
C. M. Smith. The Bandai-san Eruption, Japan, July 1888, 564.—E,
Naumann. Terrestrial Magnetism as modified by the Structure of the
Earth’s Crust, and Proposals concerning a Magnetic Survey of the Globe,
565.—T. P. Barkas. Notes on the numerous newly discovered fossil
footprints on the Lower Carboniferous Sandstones of Northumberland
near Otterburn, 565.—T. Mellard Reade. The Physiography of the
Lower Trias, 566.—A. Geilkie. On the Origin and Age of some of the
Crystalline Schists of Norway, 567.—J. E. Marr. Dynamic Meta-
morphism of Skiddaw Slate, 568.—-’. H. Hatch. On the Lower Silurian
Felsites of the South-East of Iveland, 568.—A. R. Hunt. The Age of the
Granites of Dartmoor and the English Channel, 569.—R. Swan. The
Island of Paros, in the Cyclades, and its Marble Quarries, 570.—T. G.
Bonney. Preliminary Note on the alleged Occurrence of Fossils in the
Crystalline Schists of the Lepontine Alps, 571.—T. G. Bonney. The
Effects of Pressure on Crystalline Limestones, 571.—J. J. H. Teall. The
Amygdaloids of the Tynemouth Dyke, 572.—F. Nasen. Observations on
the Greenland Ice-sheet, 573.—E. Hull. On the Presence of Coral-like
Forms in the Crystalline Limestone of Inishowen, Co. Donegal, 577.—A.
C.G. Cameron. Note on the recent Hxposures of Kelloways Rock at
Bedford, 577.—W. A. E. Ussher. ‘The Devonian Rocks of Great Britain,
578.—D. Embleton. On the Spinal Column of Lozxomma Allmani,
Huxley, from the Northumberland Coal-field, 580.—R. Laing. On the
Bone Caves of Creswell, and Discovery of an Extinct Pleiocene Feline
(Felis brevirostris), new to Great Britain, 583.—R. H. Traquair. On
Fossil Fishes of the Devonian Rocks of Scaumenac Bay and Campbellton,
Canada, 584.—A. Smith Woodward. Onthe Occurrence of the Devonian

ADDITIONS TO THE LIBRARY. 133

Ganoid Onychodus in Spitzbergen, 584.—A. Smith Woodward. Notes
on some new and little-known British Jurassic Fishes, 585.—A. W.
Rucker and T. E. Thorpe. On the Relations between the Geological
Constitution and the Magnetic State of the British Isles, 586.—A. C.
Haddon. Notes on the Geology of Torres Straits, 587,—W. Whitaker.
On a Deep Channel of Drift in the Valley of the Cam, Essex, 588.—H.
H. Howorth. A Criticism of the extreme Glacial Views of Agassiz and
his Scholars, 589.—G. W. Lamplugh. Note on a New Locality for the
Arctic Shell-beds of the Basement Boulder-clay on the Yorkshire Coast,
590.—H.H.Howorth. Did the Great Rivers of Siberia flow Southwards
and not Northwards in the Mammoth Age? 591.—H. B. Dorsey. On
the Witwatersrand Goldfields, 592.—F. Clowes. On Barium Sulphate
in Water-box Deposits from the Durham Coal-mine Waters and in Not-
tingham Sandstone, 594.—A. H. Green. A word or two about the so-
called Concretionary Structures in the Magnesian Limestone of Durham,
597.—W. Topley. The Work of the Geological Survey in Northumber-
land and Durham, 597.—R. H. Tiddeman. On Concurrent Faulting and
Deposit in Carboniferous Times in Craven, Yorkshire, with a Note on
Carboniferous Reefs, 600.

British Association for the Advancement of Science. Handbook of
Manchester, 1887. 12mo. Manchester, 1887. Presented by
W. Whitaker, Esq., PBS. PGS.

Bristol Naturalists’ Society. Proceedings. N.S. Vol. vi. Part 1.
1888-89. 1889. Presented by W. Whitaker, Esq., F_RB.S.,

C. Lloyd Morgan. The Geology of Tytherington and Grovesend, 1.

Brussels. Académie Royale des Sciences, des Lettres et des Beaux-
Arts de Belgique. Annuaire 1888. 54° Année. 1888.

——e 1889. 55° Annee. . 1889.
Bulletins. Ser. 3. Tome xiv. 1887. 1887.

M. Mourlon. Sur une nouvelle interprétation de quelques dépéts ter-
tiaires, 15.—M. Mourlon. Sur les dépots rapportés par Dumont & ses sys-
téemes laekenien et tongrien, au S.E. de Bruxelles, 598.—C. de la Vallée
Poussin. Rapport sur le mémoire par MM. A. F. Renard et C. Klément.
Sur la nature minérale des silex de la craie de Nouvelles, et contribu-
tions a Vétude de leur formation, 695.—K. Van Beneden. Rapport sur
le mémoire par M. Francotte, contribution a l'étude du développement de
lépiphyse et du troisiéme ceil chez les reptiles, 699.—C. Malaise. Sur la
découverte de poissons devoniens dans le bord nord du bassin de Namur,
771.—A. F. Renard et C. Klément. Sur la nature minérale des silex de
la craie de Nouvelles, contribution a l’étude de leur formation, 773.

——, : . Ser. 3. Tome xv. 1888. 1888.

C. Malaise. Découverte de la faune de la base du silurien en Belgique,
365.—C. de la Vallée Poussin. Note sur des bancs de calcaire carbonitére
renfermant das foraminiféres et des cristaux de quartz, 368.—A. F,
Renard. Notice sur les haches en fibrolite trouvées en Espagne par MM.
H. et L. Siret, 515.—A. F. Renard. Notice sur quelques roches des iles
du Cap-Vert, 621.

ed

‘ ; . Ser. 3. Tome xvi. 1888. 1888.
M. Mourlon. Sur lexistence d’un nouvel étage de l’Eocéne moyen dans
le bassin franco-belge, 252.—G. Dewalque, A. Briart, et P. J. Van

134 ADDITIONS TO THE LIBRARY.

Beneden. Rapports sur le mémoire par Prof. J. Fraipont et Dr. F.
Tihon. Explorations scientifiques des cavernes de la Méhaigne. I. La
erotte du Docteur, 525.—C. de la Vallée Poussin. La cause générale des.

mouvements orogéniques, 718.

Brussels. Académie Royale des Sciences, des Lettres et des Beaux-
Arts de Belgique. Bulletins. Ser. 3. Tome xvii. 1889. 1889.
M. Mourlon. Sur les dépéts Eocénes et les gisements de Tortues de
Melsbroeck (au N.E. de Bruxelles), 80.—M. Mourlon. Sur la décou-
verte, a Ixelles (lez-Bruxelles) d’un ossuaire de Mammiféres, antérieur au
Diluvium, 131.—M. Mourlon. Sur le gisement des silex taillés attribués
a ’homme tertiaire, aux environs de Mons, 499.—E. Dupon. Observa-
tions sur la communication de M. Mourlon, 516.

———

; Mémoires. Tome xlvu. 1889.
A. Briart et F. L. Cornet. Description des fossiles du calcaire grossier
de Mons (4° partie), No. 7.
——. -——. Mémoires Couronnés. (Collection in 8vo.) Tome xl.
1887.

—. ——. —. (——.) Tome xl. 1888.
——. —. —. (——.) Tome xli. 1889.
(4to.) Tome xlix. 1888.

. Socicté Belge de Géologie, de Paléontologie et d’Hydrologie.
Bulletin. Tomeiii. Fase. 3-6. 1889. 1889 & 1890.

Procés-verbaux.

eee

L. Dollo. Encore un mot sur l’Aachenosaurus multidens, G. Smets,
162.—P. Choffat. Note sur un gisement pliocéne en Portugal, 168.—P.
Choffat. La géolovie et le creusement d’un tunnel sous Lisbonne, 170.—
B. Lotti. La genése des gisements cupriféres des dépéots ophiolithiques
tertiaires de l’Italie, 172.—V. Gilliéron. Note sur l’achévement de la
premiére carte géologique de la Suisse & grande échelle, 172.—F. Sacco.
Les conglomérats du Flysch, 178.—L. Dollo. Note sur les Vertébrés
fossiles récemment offerts au Musée de Bruxelles par M. A. Lemonnier,
181.—A. Houzeau. L’éruption du Bandai-San, 182.—C. Frangois. Etude
géologique et hydrologique de la région de Rebecq-Rognon faite pour
Vétablissement d’un projet @alimentations en eau potable, 194,—A,
Poskin. Les eaux minérales de Spontin, 196.—A. Poskin. Notice sur
la source thermale de Comblain-la-Tour, 200.—C. Klément. Etudes
Hydrologiques, 202.—E. Van Overloop. Les origines du bassin supérieur
de l’Escaut, 211.—L. Dollo. Notes sur les Vertébrés fossiles récemment
offerts au Musée de Bruxelles par M. A. Lemonnier, 214, 285.—R. Storms.
Sur la présence d’un poisson du genre Zhynnus dans les dépdts pliocénes
des environs d’Anvers, 215.—E. Pergens. Révision des Bryozoaires du
Crétacé figurés par d’Orbigny, 216.—L. Dollo. Premiere Note sur les
Téléostéens du Bruxellien (Hocéne moyen) de la Belgique, 218.—F.
Loeewinson-Lessing. Revue bibliographique des nouvelles publications
géologiques et paléontologiques russes, 227.—K. Van den Broeck et A.
Rutot. Projet d’alimentation de l’agglomération bruxelloise en eau
potable par M. le capitaine Verstraete, 243.—E. Van den Broeck.
Réponse au mémoire justificatif publié par MM. Leborgne et Pagnoul a
la suite des observations dont leur project de distribution d’eau potable a
été Yobjet au sein de la Société belge de Géologie, &c., 256.—B. Lotti.

ADDITIONS TO THE LIBRARY. 135

Les transgressions secondaires dans la Chaine Metallifére de la Toscane,
979.—E. Van den Broeck. Notes géologiques et paléontologiques prises
pendant le creusement des nouveaux bassins Africa et América, a Anvers
(Austruweel), 286.—J. Gosselet. Les gites de Phosphates du Nord de la
France, 287.—A. Rutot. Le puits artésien de la Place des Nations, a
Bruxelles, 311.—J. Lorié. Les deux derniers forages d’Amsterdam, 320.
—H. van Cappelle, jr. Les escarpements du ‘ Gaasterland,” sur la cdte
méridionale de la Frise, 322.—A. Rutot. Découverte dun bois de renne
dans le Quaternaire des environs de Hougaerde, 336.—T. C. Winkler.
Note sur la source ferrugineuse du Haarlemmermeer, 549.—}’. Loewinson-
Lessing. Note sur la structure des roches éruptives, 393.—H. Dupont.
Les aspects physiques et la géologie du Congo, 398.—I. Van den Broeck.
Les cailloux oolithiques des graviers tertiaires des hauts plateaux de la
Meuse, 404.—A. Rutot. Constitution géologique des collines d’ Esschene
et d’Hekelghem, entre Assche et Alost, 415.—L. Dollo. Premiére note
sur les Siréniens de Boom, 415.—G. N. Zlatarski. Analyse de ‘“ Geolo-
gische Untersuchungen im centralen Balkan,” par Franz Toula, suivie d’un
exposé général sur la eéologie de la Bulgarie centrale, 423.—F. Loewinson-
Lessing. Revue Bibliographique des nouvelles publications géologiques
et paléontologiques russes, 430.— A. F. Renard. La constitution géolo-
gique des Iles Bommel6 et Karmo et de la région voisine, 439.
Mémoires.

P. Pelseneer. Sur un nouveau Conularia du Carbonifére et sur les préten-
dus “ Pteropodes”’ primaires, 124.—C. H. T. Zboinski. L’Attique, décrite
au point de vue géologique, métallifére minier et metallurgique, 137.—
F. Sacco. Les Conglomérates du Flysch, 149.—R. Storms. Sur la pré-
sence d’un poisson du genre Thynnus dans les dépdts pliocénes des envi-
rons d’Anvers, 163.—B. Lotti. La genése des gisements cupriféres des
dépots ophiolithiques tertiaires de l’Italie, 179—A. Rucquoy. Les eaux
arsénicales de Court-Saint-Etienne, 188.—A. Rutot et EK. Van den Broeck.
Les Puits Artésiens de Vilvorde, 207.—H. van Cappelle, jr. Les escarpe-
ments du “ Gaasterland,” sur la cote méridionale de la Frise, 222.—--G. J.
Hinde. On the Nature of some fragments of Siliceous Rock from the
Boulder-clay of the “ Roode Klif”’ (Red Cliff), on the southern border of
the province of Friesland, 254.—C. Klément. Les Puits Artésiens de
Willebroeck, 259.—L. Dollo. Premiére note sur les Mosasauriens de
Mesvin, 271.—E. Pergens. Révision des Bryozoaires du Crétacé figurés
par d’Orbigny, 805.—Mayer-Eymar. Diagnoses d’huitres nouvelles des
terrains nummulitiques d’Hgypte, 401.

Traductions et Reproductions.

J. Gosselet. Lecons sur les gites de phosphate de chaux du Nord de la
France, 3.—Garrigou. Rapports entre les eaux thermo-minérales et les
terrains géologiques, 24.

Brussels. Société Royale Malacologique de Belgique. Annales.
Tome xxii. (4° Série, Tome 3.) 1888. 1889,

Meénires.
MM. Cossmann. Catalogue illustré des coquilles fossiles de l’éocéne
des environs de Paris, 3.—A. Briart. Sur le Genre Trigonia et descrip-
tion de deux Trigonies nouvelles des terrains supracrétacés de Mae-
stricht et de Ciply, 8325.—G. F. Matthew. Sur le développement. des
premiers Trilobites, 551.

Bulletin.

G. Vincent. Note sur deux Crustacés Brachyures nouveaux pour la
faune du Pays, v.—C. Malaise. A propos des schistes siluriens de Huy,

VOL. XLVI. l

136 ADDITIONS TO THE LIBRARY.

x.—D. Raeymaekers. Note sur la présence de blocs landeniens dans le
quaternaire des environs de Lovain, xiiii—M. Mourlon. Sur le ledien de
Lede, prés d’Alost, xix.—G. Vincent. Découverte de Cyrena fluminalis, —
Miill., dans les alluvions de 1’Escaut, xxxi.—D. Raeymaekers. Sur la
présence de blocs non roulés de grés tongriens fluviomarins 4 la base du
quaternaire, xxxilii—G. Vincent. Nouvelle liste de la faune conchylio-
logique de l’argile rupelienne, xxxviiiiA. Daimeries. Notes ichthyo-
logiques (Systéme landenien), xlii, xlv, ci—J. de Guerne. Description
d’un Pisidiwn nouveau des Acores, xlix.—M. Mourlon. Sur une coupe
de quaternaire a Lede, prés d’Alost, lii—M. Mourlon. Sur le ledien a
VYouest de Bruxelles, liiii—K. Vincent. Sur fossiles recueillis dans le
pliocéne d’Autruweel (Anvers), xciiii—D. Raeymaekers. Note sur un
nouveau gite diestien fossilifére prés de Teroueren, xcv.

Buckhurst Hill. Essex Field Club. Essex Naturalist. Vol. iii.
Nos. 1-12. 1889. ;

M. Christy and W. H. Dalton. Noteson an Alluvial Deposit in the
Cann Valley, with a list of the Mollusca occurring therein, 1.—J. French
and W. H. Dalton. On the Mollusca of the Shell-marl occurring at
Felstead and in other parts of Essex, 11.—W. Whitaker. Some Essex
Well-sections, Part II., 44—W. Whitaker and W. H. Dalton. List of
Works on the Geology, &c., of Essex, 61.—T. V. Holmes. Notes on the
Geology of Maldon and the Blackwater Estuary, 111—W. Whitaker.
On a Deep Channel of Drift in the Valley of the Cam, 140.—R. W.
Christy. Notes on the Geology of the District around Chelmsford, with
a List of the Mollusca from the Alluvium at Roxwell, 171.—T. V. Holmes,
On some Recent Subsidences near Stifford, Essex, 183.—W. H. Dalton.
On the Upper Clay of Walton Naze, 228.

—. —-~. —. Vol.iv. Nos. 1-3. 1890.

Budapest. Magyar Foldtani Tarsulat. Foldtani Kozlény. Kotet
xix. Fizet 7-12. 1889. Presented through the Royal Geo-
logical Institute. |

G. Szadeczky. <A tokaj-eperjesi hegység Pusztafaln koriil levo centralis
részének petrographiai es geologiai viszonyairol, 244, 320.—M. Staub.

Sabal major Ung. sp. a Marosvoleyébol, 258.—F. Schafarzik. K6sd-

kristalyok Vizaknarol, 265.—J. Szadeczky. Petrographische und geo-

logische Verhaltnisse des centralen Theiles der Tokaj-Hperjeser Gebirgs-
kette in der Umgebung von Pusztafaln, 289, 372.—M. Staub. Sabal
major Ung. sp. aus dem Marosthale, 299.—F. Schafarzik. Steinsalz-
krystalle yon Vizakna, 303.—B. Inkey. Roman foldtani kutatasok

Magyarorsza¢ hatarszélén, 513.—J. Janko. Egyptom geologiajahoz, 336.

—B. Inkey. Sur le progrés des recherches géologiques en Romanie, 365.

—J. Janko. Zur Geologie Egyptens, 383.—G. Szadeczky. Rhyolith-

nyomok Syédorsztgban, 395.—F. Schafarzik. Trachitjaink néhany

ritkabb zarvanyarol, 406.—P. Hegediis. Az Istvantelér és mellékerec-

seirol, 411.—M. Staub. Kisebb phytopolaontologiai kozlemények, 415.

—J. Szadeczky. Rhyolithspuren in Schweden, 487.—F. Schafarzik,

Ueber einige seltenere Gesteins-Einschliisse in ungarischen Trachyten,

447.—P, Hegediis. Der Stefansgang und seine Nebenkliifte, 453.—M.

Staub, Kleinere phytopalaontologische Mittheilungen, 457.

: (Ungarische geologische Gesellschaft.) Foldtani
Kozlony. Kotet xx. Fiizet 1-4. 1890.

F. Schafarzik. Adatok a Bakony geologidjahoz, 1—G. Szadeezky.

Adatok Munkées vidékének geologiajahoz, 5.—M. Staub Moricz. Adatok

ADDITIONS TO THE LIBRARY. 137

Munkacs kornyékének fosszil florajahoz, 14.—L. Cseh. A selmeczi
Ferencz-Csaszar-Altarna geologiai szelvénye, 23.—J. Janko, Ifj. A
tuniszi Dzoebel-Bu-Kornein geologiajahoz, 26.—G. Téglas. Az erdélyi
érczheeysée ovében Zamtol az Ompoly voleyéig kinyomozott barlangok
rovid attekintése, 36.—K. Faller. A vas geologiaja, 41.—F. Schafarzik.
Daten zur Geologie des Bakony, 57.—J. Szadeczky. Beitraige zur geolo-
gischen Beschaftenheit der Umgebung von Munkacs, 61.—M. Staub.
Beitraige zur fossilen Flora der Umgebung von Munkacs, 68.—L. Cseh.
Ueber das geologische Profil des Schemnitze Kaiser-Francisci Erbstol-
lens, 73.—J. Janks, jun. Zur Geologie des Djebel-Bu-Kornein in Tunis,
76.—G. Téelas. Kurze Uebersicht der in der zone des siebenbirgischen
Hrzgebirges von Zim bis zum Ompolythale erforschten Hohlen, 84.

Budapest. Magyar Kirdlyi. Foldtani Interzet. (Kon. Ungarisch
geologische Anstalt.) Jahresbericht ftir 1888. 1890.

Johann Bockh. Directions-Bericht, 5.—L. v. Loczy.—Das Kreidege-
biet zwischen der Maros und der Fehér (Weissen) Kords im Arader
Comitate, 35.—J. Petho. Erganzungs-Aufnahmen in dem rechts- und
linksufrigen Theilen des Fehér-K6rés-Thales, 47.—T. y. Szontagh. Geo-
logische Studien in der Umgebung von Nagy-Karoly, Er-Endréd, Margita
und Szalard, 62.—T. Posewitz. Das Gebiet der schwarzen Theiss, 72.—
L. R. vy. Telegd. Der Westrand des Krass6-Szorényer Gebirges in der
Umgebung von Illadia, Csiklova und Oravicza, 86.—J. Halavats. Bericht
uber die im Jahre 1888 in der Umgebung von Dognacska und Vasko
bewerkstelliote geologische Detail-Aufnahme, 110.—F. Schafarzik. Geo-
logische Notizen aus dem Mehadiaer Zuge des Krass6-Szorényer Gebirges,
122.—A. Gesell. Montangeologische Aufnahme des Kremnitzer Hrz-
bergbau-Gebietes, 133.—A. v. Kalecinszky. Mittheilungen aus dem
chemischen Laboratorium der kgl. ungar. geologischen Anstalt, 149.—
M. Staub. Zuwachs der phytopaleontologischen Sammlung, 1887-88,
173.

: : . (——.), Mittheilung aus dem Jahrbuch.
inamdyix.» Hefti l., 1890.

S. Martiny. Der Tiefbau am Dreifaltigkeits-schacht in Vihnye, 1.—
J. Botar. Geologischer Bau des Alt-antoni-stollner Eduard-hoffnungs-
schlages, 21.—F. Pelachy. Geologische Aufnahme des Kronprinz
Ferdinand-erbstollens, 29.

——. Magyar Kir. Foldtandi Intézet. Konyo-és Térképtdranak.
II. Pot-Czimjegyzéke. 1886-88. 1889.

Buenos Aires. Academia Nacional de Ciencias en Cordoba.
Boletin. 1888. Tomoix. Entrega 3. 1888.

—. ——. ——. Tomox. Entrega3a. 1889. 1889.

——. Sociedad Cientifica Argentina. Anales. Tomo xxvii.
Entregas 2-6. 1889. 1889.

L. Darapsky. La Atacamita de Chile, 175.

—. ——. ——. Tomo xxviii. Entregas1-6. 1889.

—Ss

-——. . . Tomo xxix. Entregas 1-3. 1890.
J.J. Kyle. El Platino nativo de la Tierra del Fuego, 51.

138 ADDITIONS 10 THE LIBRARY.

Caen. Société Linnéenne de Normandie. Bulletin. Série 4. Vol. ii.
1887-88. 1889.

C. Renault. Note sur une Eryonidée nouyelle trouvée 4 Ste-Honorine- -
la-Guillaume dans le grés liasique, 13.—L. Lecornu. Sur les eaux
souterraines du plateau de la Maladrerie, 22.—Lecornu. Sur la nappe
artésienne de Valognes, 84.—Moriére. Note sur quelques crustacés
fossiles, 137. Réunion extraordinaire 4 Belléme (Orne), 156.—Bizet.
Considérations géologiques et paléontologiques sur les terrains des environs
de Belléme et de Mamers, 179.—Lecornu. L’axe du Merlerault, 291.—
Letellier. Etudes eéologiques sur les deux cantons d’Alengon, 305.

Calcutta. Asiatic Society of Bengal. Journal. N.S. Vol. Iviii.
Part 2. Nos. 1-4. 1889. 1889.

. —. NAS. Vol. lviii. Part 2. Supplement.
Nos. 1 & 2. 1889. 1890.

——. ——. Proceedings. 1889. Nos. 1-10. 1889-90.

Cambridge, Mass. Museum of Comparative Zoology at Harvard
College. Annual Report for 1888-89. 1889.

Bulletin. Vol. xvi. Nos. 5-8. 1889~—90.

N.S. Shaler. On the occurrence of Fossils of the Cretaceous Age on
the Island of Martha’s Vineyard, Mass., 89.—W. M. Davis and C. L.
Whittle. The Intrusive and Ixtrusive Triassic Trap-sheets of the Con-
necticut Valley, 99.—N. 8. Shaler and A. Agassiz. The Topography of
Florida, 139.—J. E. Wolff. On some occurrences of Ottrelite- and Ime-
nite-achist j in New England, 159.

Vol. xvii. Nos. 4-6. 1889.

ee a ee ONS EVE Mae
Oe eh ee WN Qi ee) IN GSeyl ea alee
——. ——. Memoirs. Vol. xiv. Ne.l. Part II, bl.’ 1889:

=, Vol. xvi." NO. "o.? soe:
A. Hyatt. Genesis of the Arietidee, 1.

a» VOL ax NO, lew Moo On

ere Philosophical Society. Proceedings. Vol. vi. Part 6.
1889.
J. W. Clark. On the Skeleton of Rhytina gigas, lately acquired for
the Museum of Zoology and Comparative Anatomy; with some account
of the history and extinction of the animal, 340.

——-. -~——. Proceedings. Vol. vii. Part1l. 1889. 1890.
——, , =, | Pransactions. Wol. =v. Part 4. 1889.

Canterbury. East Kent Natural History Society. 25th Report

(1882). 1883. Presented by W. Whitaker, Esq., F.BS., PGS.
32nd Report (1889). 1890. Presented by W.
W hitaker, Esq., LBS, L.GS.

——. ——. Transactions. Nos.3 & 4. New series. 1889.
Presented by W. Whitaker, Esq., F.BRS., F.GS.
G. Dowker. The Probability of finding Coal in Kent, 130.—J. G.

ADDITIONS TO THE LIBRARY. 139

McDakin. On the Occurrence of Manganese near Canterbury, 183.—
J.G. McDakin. On the Origin of Glauconite in the Lower Greensand,
135.—W. P. Marshall. Recent Fall of Rock at Niagara Falls, 139.—
A. 8S. Reid. On Time, as a Geological Factor, 145.

Cardiff. South Wales Institute of Engineers. Proceedings.
Vol. xvi. No. 4. 1889.

Carlisle. Cumberland and Westmoreland Association for the Ad-
vancement of Literature and Science. Transactions. No. 14.

1888-89. 1889. |
J.G. Goodchild. The History of the Eden and of some Rivers adjacent,

73.

Chemical News. Nos. 1543-1570. 1889.

—. Nos. 1571-1595. 1890.

Chemical Society. Journal. Nos. 320-326. 1889-90.
—-. -——. Supplementary number, Dec. 18389,

: . Nos. 327-330. 1890.
J. W. Judd. The evidence afforded by Petrographical Research of
the occurrence of Chemical Change under great Pressure, 404.

——__—__

Cincinnati. Society of Natural History. Journal. Vol.xi. No.4.
1889.

3 Vol. xy. Nos. 1-2. 1389.
J. F. James. Remarks upon sedimentation in the Cincinnati Group,
34.—J.8. Newberry. Devonian Plants from Ohio, 48.

=

——. Index to the Journal. Vols. i.—x. inclusive, by J. F. Jamzs.
1889.

City of London College. Calendar for 1889-90. 1889.

Colliery Guardian. Vol. lvii. Nos. 1488-1513. 1889.

J. H. Collins. A practical Dictionary of English and Foreign Mining,
Metallurgical, and Mineralogical Terms, 63, 98, 131, 170, 206, 274, 315,
350, 420, 457, 494, 580, 559, 602, 637, 670, 709, 750, 785, 858, 931.—
The Coalfields of Madagascar, 94.—K. Gilpin, jun. The Geological
Relations of the Principal Nova-Scotia Minerals, 818.

—. Vol. lvini. Nos. 1514-1538. 1890.

J. H. Collins. A practical Dictionary of English and Foreign Mining,
Metallurgical, and Mineralogical Terms, 30, 145, 182, 223, 262, 301, 378,
A00, 454, 495, 559, 648, 685, 728, 803, 841, 879, 921.—W. Whitaker.
Coal in the South of England, 60.—Discovery of a Coalfield in Kent, 296,
335, 449, 557, 643, 682, 906.

Copenhagen. Kongelige Danske Videnskabernes Selskab. Natur-
videnskabelige og Mathematiske Afhandlinger. Rekke vi.
Band v.- ‘Nos. 1&2. 1889.

ee ee nike wie) amore Nol aml soe

I40 ADDITIONS TO THE LIBRARY.

Copenhagen. Kongelige Danske Videnskabernes Selskab. Over-

sigt. 1889. Nos. 2-3. 1889-90.

A. G.Nathorst. Sur la présence du genre Dictyozamites, Oldham, dans
les couches jurassiques de Bornholm, 96,

—. 1890. No.1. 1890.

Cracow. Académie des Sciences. Bulletin International. Comptes
Rendus des Séances de Vannée 1889. Octobre—Decembre.
LEs8o,

J. Siemiradzki. Faune de l’étage jurassique moyen de Popielany,

XVill., XXVi. :

: : ; Oct._Décembre. 1889.

A. Rehman. Dolne dorzecze Sanu, xvii.—W.Szajnocha. Ozetknieciu
sie porfiru zwapieniem weglowym kolo Dubia, xxi.i—W. Szajnocha.
Olosiu kopalnym z jaskini pod Jaszczurowka, xxii. .

é , . -——. Janvier-Mai. 1890.

F. Kreutz. Grafit w granitowej skale z Jézefowki i z Samezyka na
Wolyniu, 22.—M. Raciborski. Flora kopalna_ krakowskich glin ognio-
trwalych Czesce I. Paprocie i skrzypy, 31—T. Wisniowski. Mikvofauna
il6w ornatowych okolicy Krakowa; Otwornice z Grojca, 63.—H. Zapalo-
wicz. Rosglinna szata zor Pokucko Marmaroskich, &c., 88.—F. Tondera.
Uebersicht der in den Steinkohlen-Lagern von Dabrowa und Gotonég, im
Konigreich Polen, gesammelten fossilen Pflanzen, 141.

—

Darmstadt. Vereins fur Erdkunde zu Darmstadt und mittel-
rheinische geologische Verein. Notizblatt. 4 Folge, 9 Heft.
1888.

C. Chelius. Granit und Minette an der Hirschburg bei Leutershausen
sudlich Weinheim a. d. Bergstrasse, 1—G. Greim. Der Granatgneiss
(Kinzigit) und Graphitschiefer bei Gadernheim im Odenwald, 6.—
E. Eger. Chemische Analyse yon tertiiren und diluvialen Gesteinsarten
aus den Bruchen von Weisenau und Laubenheim bei Mainz, 25.—C.
Chelius. Notizen aus den Aufnahmegebieten, 380.

—. ——. —. —. 10 Heft. 1889.

Davenport, Iowa. Davenport Academy of Natural Sciences. Pro-
ceedings. Vol. v. Parti. 1884-89. 1889.

R. E. Call. On Certain Recent, Quaternary, and New Freshwater
Mollusca, 1.—W. H. Barris. A Defence of our Local Geology, 15,—
C. 8. Watkins. Volcanoes of the Sandwich Islands, 23.—C.L. Webster.
A Description of the Rockford Shales of Iowa, 100.

Demerara. Royal Agricultural and Commercial Society of British
Guiana. 'Timehri, being the Journal. N.S. vol. iii. Part.1.
1889.

Dijon. Académie des Sciences, Arts et Belles-Lettres. Mémoires.
Sér. 4. Tome i. 1888-89. 1889.

Dresden. Naturwissenschaftliche Gesellschaft Isis. Sitzungsbe-
richte und Abhandlungen, 1889. Juli-December. 1890.

ADDITIONS TO THE LIBRARY. I4l

Dublin. Royal Irish Academy. ‘ Cunningham Memoirs.’ No. 5.
1890.

; Proceedings. Series 3. Vol.i. No.2. 1889.

W. J. Knowles. Report on the Prehistoric Remains from the Sand-
hills of the Coast of Ireland, 173.—W. J. Knowles. Report on Flint
Implements of the North-east of Ireland, 188.—J. P. O’Reilly. On the
Directions of the Lines of Jointing observable in the Rocks in the Neigh-
bourhood of the Bay of Dublin and their Relations with Adjacent Coast
Lines, 229.

—-, ieeameaehion: Vol. xxix. Parts 6-13. 1889-

1890.
East-India Association. Journal. Vol. xxi. Nos. 2-5. 1889.
ee) Vol. xx, Nos. 1 & 2. 1890.

Edinburgh. Royal Physical Society. Proceedings. Session 1887—
Son NOS8s.

R. H. Traquair. Notes on Carboniferous Selachit, 412, 421.—G. Ram-
age. Notes on a Visit to Fernando Noronha, 426.—B. N. Peach. Ona
New Eurypterid from the Upper Coal-measures of Radstock, Somerset-
shire, 458.—J. Bennie. On the Prevalence of Eurypterid Remains in the
Carboniferous Shales of Scotland, 499.—R. Kidston. On the Fructifica-
tion of two Coal-measure Ferns, 510.—R. Kidston. On the Fructification
and Affinities of Archeopteris hibernica, Forbes, sp., 516.

‘ , 1888-89. 1889.

R. H. Traquair. On the Structure and Classification of the Astero-
lepide, 23.—R. H. Traquair. Homosteus, Asmuss, compared with Cocco-
steus, Agassiz, 47.—R. Kidston. Additional Notes on some British
Carboniferous Lycopods, 88.—J. G. Goodchild. On some of the Modes
of Formation of Coal-seams, 97.—J. Bennie and T. Scott. The Ancient
Lakes of Edinburgh, 126.

Ekaterinburg. Société Ouralienne d’Amateurs des Sciences Natu-
relles. Bulletin. Tome x. Livr. 3. 1887.

: , . Tome xi. Livr.1 & 2. 1887-88.
V. Malakhoff. QCéuvres Posthumes, 9.

Falmouth. Royal Cornwall Polytechnic Society. 56th Annual
Report. 183838. 1889.
J. Garland. On Certain Tin-deposits in Galicia, Spain, 54.
, . O/th Annual Report for 1889. 1890.
F. J. Stephens. The Perranzabuloe Mining District, 105.
Frankfurt am Main. Senckenbergische naturforschende Gesell-
schaft. Bericht, 1889. 1889.
Ester Theil.
F. C. Noll. Die Veranderungen in der Vogelwelt im Laufe der Zeit, 77.

Lweiter Theil.

F. Kinkelin. Der Plocinsee des Rhein- und Mainthales und die
ehemaligen Mainlaufe, 59—F. Kinkeln. Erlauterungen zu den geolo-
gischen Uebersichtskarten der Gegend zwischen Taunus und Spessart, 323.

——___

142 ADDITIONS TO THE LIBRARY.

Freiburg i. B. Naturforschende Gesellschaft. Berichte. Band iv.
Hefte4u 5. 1889.

G. Bohm. Ein Beitrag zur Kenntniss fossiler Ophiuren, 232.

Geneva. Société de Physique et d’Histoire Naturelle. Mémoires.
Tome xxx. Partie 2. 1889-90. 1890.

J. Brun et J. Tempére. Diatomées fossiles du Japon, No. 9.

Geological Magazine. Dec. iii. Vol. vi. Nos. 7-12. 1889.

J. C. Russell. Subaérial Deposits of the Arid Region of North
America, 289, 342.—E. Wilson and W. D. Crick. The Lias-marlstone
of Tilton, Leicestershire, 296, 537.—H. Howorth. Was there an Arctic
Ocean in the Mammoth Period ?, 305.—J. G. Goodchild. On some
Modes of Formation of Coal-seams, 308.—T.G. Bonney. Note on some
Pebbles in the Basal Conglomerate of the Cambrian at St. David’s, 315.
—C. Callaway. The Present State of the Archzan Controversy in
Britain, 319.—R. Lydekker. Note on some Points in the Nomenclature
of Fossil Reptiles and Amphibians, with Preliminary Notices of two new
Species, 8325.—G. M. Dawson. Glaciation of High Points in the Southern
Interior of British Columbia, 350.—R. Lydekker. Notes on New and
other Dinosaurian Remains, 353.—A. J. Jukes-Browne. The Occurrence of
Granite in a Boring at Bletchley, 356.--A. Smith Woodward. Paleonto-
Jogy in the Malton Museum, 361.—T. Rupert Jones and H. Woodward.
On some new Devonian Fossils, 385.—R. Lydekker. On an Ichthyo-
saurian Paddle showing the contour of the integuments, 388.—C. Davi-
son. On the origin of the Stone-Rivers of the Falkland Islands, 390.—
A. Smith Woodward. Note on Rhinobatus bugesiacus, 395.—A. Harker.
On “ Eyes” of Pyrites and other Minerals in Slate, 396.—-R. Schafer.
On Phillipsastrea, d’Orb., with especial reference to Philhipsastrea radiata,
S. Woodward, sp., and Phillipsastrea tuberosa, McCoy, sp., 398.—C.
Davison. Note on the Mean rate of Subaérial Denudation, 409.—J. E.
Marr. Notes on the Lower Paleozoic Rocks of the Fichtelgebirge,
Frankenwald, and Thiiringerwald, 411.—G. H. Stone. On the Scratched
and. Facetted Stones of the Salt Range of India, 415.—H. A. Nicholson.
On the relations between the genera Syringolites, Hinde, and Remeria,
Edwards and Haime, and on the genus Caliopora, Schluter, 433.—E. D.
Cope. On the Proboscidea, 438.—A. Smith Woodward. Preliminary
notes on some new and little-known British Jurassic Fishes, 448.—P. G.
Sanford. An Analysis of the Fuller’s Earth of Nuttield, 455.—P. G.
Sanford. Analysis of the Gault and Greensand, 456.—J. J. H. Teall.
On the Amygdaloids of the Tynemcuth Dyke, 482.—T.G. Bonney. The
Effects of Pressure on Crystalline Limestones, 483.—E. Naumann. Ter-
restrial Magnetism as modified by the structure of the Earth’s Crust, and
proposals concerning a Magnetic Survey of the Globe, 486, 535.—R. H.
Traquair. On the Systematic Position of the “ Dendront Fishes,” 490,—
J.S. Hyland. On Zonal Structure in Olivine, 492——A. H. Foord and
G. C. Crick. On the Muscular Impressions of Celonautilus cariniferus,
J. de C. Sowerby, sp., compared with those of the Recent Nautilus, 494.
—F. Chapman and C.D.Sherborn. Foraminifera from the London Clay
of Sheppey, 498.—A. Smith Woodward. On the Occurrence of the
Devonian Ganoid Onychodus in Spitzbergen, 499.—H. J. Johnston-Lavis.
Notes on the Ponza Islands, 529.—F. H. Hatch. On the Lower-Silurian
Felsites of the South-east of Ireland, 545.—T. M. Reade. Physiography
of the Lower Trias, 549. ;

—. —. ——. (2ndcopy.) Purchased.

ADDITIONS TO THE LIBRARY. 143

Geological Magazine. Dec. iii. Vol. vu. Nos. 1-6. 1890.

O. C. Marsh. The Skull of the Gigantic Ceratopside, 1.—H. H. Ho-
worth. Did the Great Rivers of Siberia flow Southwards and not North-
ward in the Mammoth Age?, 5.—H. H. Howell. Note on the Classifi-
cation of the Red Rocks in South-east Durham, 8.—W. Whitaker.
Coal in the South-east of England, 13.—R. H. Traquair. Notes on the
Devonian Fishes of Scaumenac Bay and Campbelltown in Canada, 15.—
G. F. Harris. Notes on the Geology of the Gironde, with especial refe-
rence to the Miocene Beds, 22.—W. M. Hutchings. Note on an occur-
rence of Willemite in a Slag, 31.—T. G. Bonney. Mr. Mellard Reade’s
Interpretation of the Lower-Trias Physiography, 52.—R. H. Traquair.
On Phlyctenius,anew Genus of Coccosteide, 55.—G. W. Lamplugh.
On a New Locality for the Arctic Fauna of the ‘‘ Basement ” Boulder-
clay in Yorkshire, 61.—T. F. Jamieson. On the Climate of the Loess
Period in Central Europe and the Cause which produced it, 70.—J. G.
Goodchild. The Paste of Limestones, 73.—F. Chapman. On a method
of producing Perlitic and Pumiceous Structures in Canada Balsam, 79.—
H. Woodward. Notes on the Paleontology of Western Australia, 97.—
A. H. Foord. Description of Fossils from the Kimberley District,
Western Australia, 98, 145.—C. A. McMahon. Notes on the Culm-
measures at Bude, North Cornwall, 106, 222.—J. Saunders. Notes on
the Geology of South Bedfordshire, 117.—T. M. Reade. Physiography
of the Trias, 155, 260.—A. Smith Woodward. On a new Species of
Pyenodont Fish (Mesodon Damoni) from the Portland Oolite, 158.—
J. W. Davis. On Celacanthus Phillips, Agassiz, 159.—A. Somervail.
On the Schists of Lizard District, 161.—H. A. Nicholson and G. J. Hinde.
Notes on the Paleontology of Western Australia, 193.—J.8. Hyland.
On some Epi-diorites of N.W. Ireland, 205.—J. W. Spencer. The High
Continental Elevation preceding the Pleistocene Period in America, 208.
--A. C. Seward. Woodwardian Laboratory Notes, 213.—A. J. Jukes-
Browne. The Physiography of the Lower Trias, 220.—W. H. Hudleston.
Further Notes on some Mollusca from South Australia, 241.—H. J.
Johnston-Lavis. The Extension of the Mellard Reade and C. Davison
Theory of Secular Straining of the Earth to the Explanation of the Deep
Phenomena of Volcanic Action, 246.—R. H. Traquair. Notice of new
and little-known Fish-Remains from the Blackband Ironstone of Borough
Lee, near Edinburgh, 249.— A. Irving. Note on the Airolo-Schists
Controversy, 252.—H. T. Newton. Note on the Occurrence of the Tunny
(Thynnus thynnus) in the Cromer “ Forest Bed,” 264.—W. M. Hutchings.
Notes on the Probable Origin of some Slates, 264.

—. 1 ——. ——. (2nd copy.) Purchased.

Geological Record for 1880-84 (inclusive). Vol. ii. Edited by
W. Topley and C. D. Sherborn. 1889. Four copies. Pur-
chased. }

Geological Society [of London]. Regulationsof the. 12mo. Lon-
don. 1808. Presented by J. H. Marr, Esq., See. G.S.

——. Two circulars dated 1824. 8vo. Presented by C. D. Sher-
born, Esg., L.G.S., and another.

——. Petition for Charter. 1824. 8vo. Presented by C. D.
Sherborn, Esq., £.GS., and another. |

——. List of Fellows 1824 and 1828. 8vo. Presented by C. D.
Sherborn, Esq., 2.G.S., and another.

144 ADDITIONS TO THE LIBRARY.

Geologists’ Association. Proceedings. Vol. x. No9. 1888.

H. Woodward. Visit to the British Museum (Natural-History De-
partment of Geology), 457.—G. 8. Boulger. Visit to the British Museum
Botanical Department, 468.—W. Topley. Excursion to Wimbledon and
Putney, 471.—J. D. Paul. Excursion to Charnwood Forest, 472.—
C. A. McMahon. Notes on the Microscopic Character of some Specimens
of Rocks collected during the Excursion to Charnwood Forest, 476.—
T. V. Holmes. Excursion to Laindon (or Langdon) Hills, Essex, 489.—
J. H. Blake. Excursion to Reading, 493.—G. 8. Boulger. Excursion
to Godstone, Tilburstow, and Nutfield, 496.—J. Hopkinson. Excursion
to Rickmansworth, 499.—T. V. Holmes. Excursion to Loampit Hill,
Lewisham, and West Combe Park, Greenwich, 501.—A. C. G. Cameron.
Excursion to Bedford and Clapham, 504.—E. Wethered. On the Lower
Divisions of the Carboniferous Rocks of the Forest of Dean, 510.—W. F.
Gwinnell. Sketch of the Geology of the Forest of Dean, with special
reference to the Long Hxcursion, 522.—H. B. Woodward. Notes on the
Rhetic Beds and Lias of Glamorganshire, 529.—F. W. Rudler. Note
on the South-Wales Coal-field, 538.—F. W. Rudler, &c. Exeursion to
the Forest of Dean, Wye Valley, and South Wales, 542.

: . Vol. xi. Nos. 2-6. 1889. | 1889-90:

A. Smith Woodward. On the Paleontology of Sturgeons, 33.—J. G.
Goodchild. Some Observations upon the Mode of Occurrence and the
Genesis of Metalliferous Deposits, 45.—F. W. Rudler. Experimental
Geology, 69.—W. H. Hudleston. On the Geological History of Iron
Ores, 104.—J. F. Blake. A Visit.to the Volcanoes of Italy, 145.—
R. Lydekker. Note on a Chelonian Humerus from the Middle Eocene
of Bracklesham, 177.—Marshall Hall. On Rocks from the Saas-Thal
and Geneva, 179.—E. Litchfield. Notes on Early References to Geology,
mostly before 1800, 187.—T. H. Wilson. Notes on the Artificial Un-
making of Flints, 194.—A. J. Jukes-Browne. The Geology of Upton
and Chilton in Berks, 198.—C. J. Spurrell. On the Estuary of the
Thames and its Alluvium, 210.—T. V. Holmes. The Geology of North-
west Cumberland, 231.—J. G. Goodchild. An Outline of the Geological
History of the Eden Valley or Edenside, 258.—A. Smith Woodward. A
Synopsis of the Fossil Fishes of the English Lower Oolites, 285.—R. 8.
Herries. Excursion to Newbury, xii.—R. S. Herries. Excursion to
Southampton, xvi.—G. 5S. Boulger. Visit to the Natural-History Museum,
Cromwell Road, Department of Botany, xxi—J. Foulerton. Visit to the
Museum of the Royal College of Surgeons, xxiiii—H. B. Woodward.
Preliminary Excursion to Lyme Regis, xxvii—W. H. Hudleston. Ex-
cursion to Weymouth, xlix.—J. Hopkinson. Excursion to Boxmoor and
Nash Mills, lviiii—R. 8. Herries, H. W. Monckton, and H. B. Wood-
ward. Excursion to Brentwood, lxii—J. Prestwich and W. Topley.
Excursion to Ightham (Kent), lxvi—W. Whitaker. Whitsuntide Ex-
cursion to the Crag District, lxviii.—l’. C. J. Spurrell. Excursion to
Higham, Ixxiii—J. Hopkinson. Excursion to Totternhoe and Ivinghoe,
Ixxiv.—W. Topley. Excursion to Limpsfield (Surrey), lxxxili—W.
Whitaker.—Excursion to Upton and Chilton, Ixxxiiii—T. V. Holmes
and J. G. Goedchild. Excursion to North-west Cumberland and Eden-
side, Ixxxv.

Gotha. Petermann’s Mittheilungen aus Justus Perthes’ geograph-
ischer Anstalt. Band i—xxxiv. 1855-88. Purchased.

: Band xxxv. 1889. Purchased.
G. Schweinfurth. Ueber die Kreideregion bei den Pyramiden von
Gizeh, 1.—V. Hilber. Die Bildung der Durchgangsthaler, 10.—O. Bau-

ADDITIONS TO THE LIBRARY. 145

mann. Usambara, 41.—O. Kriimmell. Ueber Erosion durch Gezeiten-
strome, 128.—N. Latkin. Die Goldwascherei des Amurlandes, 172.—
G. Rohlfs. Gold in Afrika, 187.—A. Rothpletz. Das Thal von Orotava
auf Tenerife, 237.—A. Philippson. Ueber die jiingsten Erdbeben in
Griechenland, 251.—T. Thoroddsen. Reise im siidlichen Island, 1889.

Gotha. Petermann’s Mittheilungen aus Justus Perthes’ geograph-

ischer Anstalt. Band xxxvi. Nos. 1-7. 1890. Purchased.

P. Langhans. Dr. K. W. Schmidt’s Reisen auf den westlichen Komo-

ren, 11.—H. Meyer. Die Besteigung des Kilimandscharo, 15.—W.

Kiukenthal. Bericht tiber die von der geographischen Gesellschaft in
Bremen im Jahre 1889 veranstaltete Reise nach Ostspitzbergen, 61.

—. ——. Erginzungshett. Nos. 1-97. 1860-90. Purchased.

Gratz. Naturwissenschaftliche Vereine fur Steiermark. Mittheil-
ungen. Jahrgang 1888. 1889.

R. Hoernes. Die geologische und palaeontologische Literatur der
Steiermark, lxxix.—R. Hoernes. Die mineralogische und petrographische
Literatur der Steiermark, Ixxxviii.—F. Standfest. Die vermeintlichen
Fucoiden der Grazer Devon-Ablagerungen, lxxxix.—V. Hilber. Zur
Fossilliste des Miocin-Fundortes Hirzenbihel zu Pols, Wildon, O. Steier-
mark, xci.—H. Hussak. Ueber ein neues Mineralvorkommen (Uwarowit)
von Gulsen bei Kraubat in Steiermark, 3.—H. Hussak. Ueber kiinstliche
Spharolithe, 7.—H. Hatle. Beitrage zur mineralogischen Topographie
der Steiermark, 74.

Halifax. Yorkshire Geological and Polytechnic Society. _ Pro-
eccamecs NLS. Vol. xi. “Part 2.) 1890.

G. R. Vine. Notes on British Eocene Polyzoa, 154.—E. M. Cole.
Notes on the Driffield and Market-Weighton Railway, 170.—W. Cheet-
ham. On a Boulder with Cup-and-Ring Markings at Horsforth, 175.—
T. Carter Mitchell. On the Drift-deposits of the Vale of Mowbray, 177.
—J. 5S. Tute. Notes on some Singular Cavities in the Magnesian Lime-
stone, 182.—G. R. Vine. A Monograph of Yorkshire Carboniferous and
Permian Polyzoa, Part 2, 184.—C. EH. De Rance. Notes on Underground
Water-supply and River-floods, 200.—G. W. Lamplugh. On the larger
Boulders of Flamborough Head, Parts 2 and 3, 231.—A. Lupton. Some
notes on Gold-, Slate-, and Salt-mines in Great Britain, 239.—G. R.
Vine. Further notes on the Polyzoa of the Lower Greensand and the Upper
Greensand of Cambridge, Part 2, 250.—G. W. Lamplugh. Glacial
Sections near Bridlington, Part 4, 275.—A. Harker. Petrological notes
on some Boulders from the Boulder-clays of East Yorkshire, 300.—
T. Tate. Yorkshire Petrology. Part 2. The Lamprophyres, 311.—
T. Hicks and W. Cash. On the Structure and Affinities of Lepidoden-
dron, 316.—J. W. Davis. Fossil Fish-remains from Carboniferous Shales
at Cultra, co, Down, Ireland, 332.—J. W. Davis. Summary of Geo-
logical Literature relating to Yorkshire published during 1889, 344.

Halifax, N.S. Nova-Scotian Institute of Natural Science. Pro-
ceedings and ‘Transactions. Vol. vii. Part 3. 1888-89,
1889.

D. Honeyman. A Geological Recreation in Massachusetts Centre, 197.
—H.8. Poole. Ice in the Carboniferous Period, 202.—D. Honeyman.
Glacial Boulders of our Fisheries and Invertebrates Attached and De-
tached, 205.—E, Gilpin. The Geology of Cape Breton, 214.—G. Patter-
son. The Stone Age in Nova Scotia, 231.

146 ADDITIONS TO THE LIBRARY.

Halle. Kaiserliche Leopoldinisch-Carolinische Deutsche Akademie
der Naturforscher. Verhandlungen (Nova Acta). Band liii..
1889. .

H. Pohlig. Dentition und Kranologie des Elephas antiquus, Fale.,
au Beitrigen tiber Elephas primigenius, Blum., und Elephas meridionalis,
esti, 1.

—. ~——. Katalog der Bibliothek. Lief.2. 8vo. 1889.

——. “Zeitschrift fiir Naturwissenschaften. Band lxi. (Folge 4.
Band vii.) Heft5&6. 1888.

D. von Schlechtendal. Mittheilungen tiber die in der Sammlung auf-
bewahrten Originale zu Germar’s “ Insekten in Bernstein eingeschlossen”
mit Rucksicht auf Giebels “Fauna der Vorwelt,’ 475.—F. Dreyer,
Beitrige zur Kenntniss der Foraminiferen des mittleren Lias vom grossen
Seeberg bei Gotha, 492.

-, . Bandlxi. (Folge 4. Band vii.) Heft 1-6, 1889.
O. Luedecke. Mittheilungen iiber einheimische Mineralien, 1.—O.
Luedecke. Ueber grosse Glauberit-Krystalle (Brongniart) von Leopolds-
hall, 325.—A. Sauer. Ueber die aeolische Entstehung des Loss am
Rande der norddeutschen Tiefebene, 326.—D. von Schlechtendal. Bemerk-
ungen und Beitrige zu den Braunkohlenfloren von Rott am Siebenge-
birge und Schlossnitz in Schlesien, 383.

Hanau. Wetterauische Gesellschaft fiir die gesammte Naturkunde

za Hanau. Bericht. 1887-89. 1889.

F. vy. Sandberger. Notizen zur Flora des Hanauer Oberlandes, 14.—
R. Temple. Ueber den Diamant, 19.—K. Flach. Ueber die tertidren
Arten des Genus Acme, Hartmann, 69.—F. Kinkelin. Beitrage zur
Geologie der Umgebung von Hanau, 77.

Harlem. Société Hollandaise des Sciences. Archives Néer-
landaises. Tome xxill. Livr. 3-5, 1889.

Hazell’s Annual for 1890, edited by E. D. Price. 1889.

Helsingfors. Société de Géographie Finlandaise. Bulletins. (Fen-
nia;) 1, 1889,

ERS 2 eee ee!

: : ort us SSO:
W. Ramsay. Geologische Beobachtung auf der Halbinsel Kola.
No. 7.—B. Frosterus. Einige Beobachtungen tber geschichtete Morane
und “ Asar.” ” No. 8.

Hermannstadt. Siebenbirgische Verein fiir Naturwissenschatten.
Jahrgang 39. 1889.
E. A. Bielz. Die in Siebenburgen vorkommenden Mineralien und
Gesteine, 1.

Hertford. Hertfordshire Natural-History Society and Field-Club.
Transactions. Vol.u. Parts 7&8. 1883 & 1884.

é 3 Vol. v. Parts 5-8. 1889-90.
H. Hicks. Pre-historic Man in Britain, 147.—J. Morison. Notes on
the Chalk-rock, 199.

ADDITIONS TO THE LIBRARY. 147
Hobart. Royal Society of Tasmania. Papers and Proceedings for
1888, 1889.

Ingeniero y Ferretero Espanol y Sud Americano. Vol. iv. Nos.
1-25. 1889.

Vol. v. Nos. 1-9, 11-12. 1890.

Institution of Civil Engineers. Minutes of Proceedings. Vol. xevi.
1889.

——. Vol. xcvii. 1889.

—. Vol. xevii. 1889.

——. Vol. xcix. 1890.

: . Brief Subject-Index. Vols. lix.-xecvill. 1879-89.

bec

. Charter, Supplemental Charter, Bye-Laws, and List of
Members. 1889.

Tron. Nos. 907-910. 1890.

Iron and Steel Trades Journal. Nos. 1567-1594. 1889.
. . Nos. 1595-1619. 1890.

Jena (late Berlin). Paliontologische Abhandlungen. N.F. Bandi.
Heft 1-2. 1889. Purchased.

E. Holzapfel. Die Cephalopoden-fuhrenden Kalke des unteren Car-
bon von Erdbach-Breitscheid bei Herborn, 1.—L. Crié. Beitrage zur
Kenntniss der fossilen Flora einigen Inseln des stidpacifischen und ind-
ischen Oceans (77) or 1.

Jobannesburg. The Witwatersrand Mining and Metallurgical
ikeview. No. I.. 13890.
C. J. Alford. The Geology of Witwatersrand District, 1—C. J.
Alford. Geological Features of the De Kaap Gold-fields.

‘ Nom2a ALSO 0:

C. Vautin. The Occurrence of Gold in Banket above and below Water-
level, 7.—C. Henrich. Some Forms of Ore-deposits in Limestone
Formation, 14.

—, ==, No. 3. 1890.

; ONG. Od.) LEW,
C. J. Alford. The Geology of the Sheba Mine, 7.

Kieff. Société des Naturalistes. Mémoires. Tome x. Livr. 2.
1889.

Kiel. Mineralogische Institut der Universitit. Muittheilungen.
Band i. .Heft 2. 1889. Purchased. ,

K. Danzig. Bemerkungen tber die Gneisse im Granulit des siichsischen
Mitteleebirees, 99.-—J. Petersen. Ueber den Wiesenkalk des Farbe-
berges bei Nindorf, 104, 149.—H. Haas. Betrachtungen iiber die Art
und Weise wie die Geschiebemergel Norddeutschlands zur Ablagerune
gelangt sind, 111—E. Stolley. Ueber ein Neocomgeschiebe aus dem
Diluvium Schleswig-Holsteins, 137.

148 ADDITIONS TO THE LIBRARY.

Lausanne. Musées d’Histovre Naturelle. Rapports Annuels des
Conservateurs 4 la Commission des Musées pour l’année 1883.
1889. Presented by Prof. E. Renevier, F.C.GS.

——. Société Géologique Suisse. LEcloge. 1889. No.5. 1890.

C. Schmit. Excursion de 1889, 385.—F. Miuhlberg. Grenzgebiet
zwischen Ketten- und Tafel-Jura, 397. See rendu de la réunion de
Lugano, 437.

—. Société Vaudoise des Sciences Naturelles. Bulletin. Ser. 3.
Vol. xxiv. No.99. 1889.

. » per. 3. .. Vole xxy? No, 100 aissce
H. Schardt. Etude de quelques dépéts quaternaires fossiliféres, 79.

ee
.

Leeds. Philosophical and Literary Society. Annual Report for
1888-89. 1889.

Leicester. Literary and Philosophical Society. Transactions. New
Quarterly Series. Vol.i. Parts 11 &12. 1889.

H. E. Quilter. The Rheetics of Leicestershire, 14.—A. Smith Wood-
ward. On some remains of Fossil Fishes from the Rhetic Beds of the
Spinney Hills, Leicestershire, 18.—A. Smith Woodward. Note on a
Species of Pholidophorus from the Rheetic Paper-shales of Wigston, 22.
—J. J. W. Knowles. The Theories as to the Variations of Race in
Mankind, 6.

Nol. © Partie (S897. esas

Montagu Browne. Ona Fossil Fish ( Chondrosteus) from Barrow-on-
Soar, hitherto recorded only from Lyme Regis, 17.

ee ee Vole) aris nO oUe

Leiden. Geologische Reichsmuseums. Sammlungen. Ser. l.
No. 18-20. 1889-90. Purchased.
K. Martin und A. Wichmann. Beitrage zur Geologie Ost-Asiens und
Australiens. Band 4. Heft 5-7, von K. Martin.

Ser. 2. No.4. 1889. Purchased.
Beitriige zur r Geologie yon Niederlandisch West-Indien und angren-
zender Gebiete. Band 1. Heft 3, von J. H.. Kloos.

Leipzig. Zeitschrift fiir Krystallographie und Mineralogie. Band
xy. Heft 6. 1889. Purchased.

H. Biicking. Glaserit, Blodit, Krainit und Boracit von Douglashall
bei Westeregeln, 561. e2q illeaitiae Ueber Baryt aus dem Kronthal im
Klsass, 576._N. V. Ussing. Untersuchungen der Mineralien von Fisk-
ernis in Gronland, 596.—K. Busz. Mittheilungen aus dem mineralo-
gischen Museum der Universitit Bonn, 616.

Band xvi. 1890. Purchased.
Ww. C. Brégger. Die Mineralien der Syenitpegmatitgange der sud-
norwegischen “‘Augit- und N ephelinsyenite, 1.

. Band xvii. Hefte 1-6. 1889-90. Purchased.

A. Cathrein. Neue Flachen am Quarz, 19.—V. Goldschmidt. Chem-
isch-mineralogische Betrachtungen.—G. A. Konig. Neue nordameri-
kanische Mineral-vorkommen, 85.—W. Muthmann. Messelit, ein neues

ADDITIONS TO THE LIBRARY. I49

Mineral, 93.—R. Prendel. Ueber den Wiluit, 94.—A. Belar. Ueber
Aurichaleit und Kiinstliches Zinkearbonat (ZnCO,+H,O), 113.—A.
Becker. Zwei Glimmeranalysen, 128.—A. Cederstrom. Pseudobrookit
in grossen Krystallen von Havredal, Bamle, Norwegen, 133.—G. A. F.
Molengraaff. Studien am Quartz, 137.—A. Hamberg. Ueber Krystal-
lisertes Blei von der Grube Harstigen bei Pajsberg in Wermland nebst
Bemerkungen tiber die Paragenesis der begleitenden Mineralien, 253.—
O. Lehmann. Ueber Zwillingsbildung bei Chlorbaryum, 268.—A. von
Elterlem. Hin neues Tiroler Kalkspath-vorkommen, 280.—J. Becken-
kamp. Zur Symmetrie der Krystalle, 521.—W. Muthmann. Unter-
suchungen wtber den Schwefel und das Salen, 336.—K. Oebbeke.
Arsenkies aus dem kornigen Kalke von Wunsiedel, 384.—H. 8. Dana.
Ueber das Baryumsulfat von Perkin’s Mill, Templeton, Prov. Quebec,
393.—G. Seyfriedsberger. Ueber Quecksilbersulfate aus dem Mauer-
werke eines Idrianer Ofens, 433.—W. Miller. Ein neuer Orthoklas-
zwilling aus dem Fichtelgebirge, 484.—K. Weinschenk. Beitrage zur
Mineralsynthese, 486.—L. Brugnatelli. JBeitrage zur Kenntniss des
Epidot, 529.—H. Laspeyres. Die Grundformen der Glimmer und des
Klinochlor, 541.—K. Busz. Schwefel von Bassick, Ver. Staaten N.-
Amerika: Beryll von San Piero, Elba: Flussspath von Cornwall: Gothit
von St. Just, Cornwall: und Hypersthen vom Rocher du Capucin, Mont
Dore, 549.—W. Bruhns. Korund vom Laacher See, 554.—W. Bruhns
und K. Busz. Phosphosiderit, ein neues Mineral von der Grube Kalterborn
bei Eiserfeld im Siegenschen, 555.—F. A. Genth und 8. L. Penfield.
Ueber Lansfordit, Nesquehonit (ein neues Mineral) und Pseudomorphosen
von Nesquehonit nach Lansfordit, 561.

Liége. Societe Géologique de Belgique. Annales. Tome xiv.
Livraison 2. 1886-87. 1889.

Bulletin.
Laurent-Guillaume de Koninck, clxxxix.

Mémotres.
X.Stainier. Jue Diabase de Malmédy, 213.
Bibhiographie.
H. Forir. Les dépots glaciaires du plaines basses de l’Allemagne du
Nord, par W. Dames, 3.—H. Forir. De la formation des vallées de la
rive gauche du Rhin, et particuliérement de la vallée de la Nahe, 17.—
H. Forir. Sur les plissements interrompus, par Eduard Suess, 27.—
H. Forir. Les plus récentes variations dans les vues modernes sur la
formation des montagnes, par A. Bittner, 32.

Sauer lome'=xv.) | See.@ 7 JGaS. volocdyirn. 13/4)

—_. ——. ——. Tome xvi. Livraison 1. 1888-89, 1889.

Bulletin.

C. de la Vallée Poussin. Etude sur les dépéts gypseux et gypso-
salifériens, xxii.—Piedboeuf. Sur quelques fossiles devoniens des environs
de Dusseldorf, xxvii—V. Dormal. Sur quelques dépdts sableux de la
Heshaye, xxxix.—C. Cesaro. Le procédé Solvay inventé cinquante ans
auparavant par Fresnel, lii.

‘ Mémorres.

X. Stainier. Etude géologique des gisements de phosphate de chaux
du Cambrésis, 4.—J. Fraipont. Sur les affinités des genres Favosites,
Emmonsia, Pleurodictyum, et Michelinia & Voccasion de la description
d’une forme nouyelle de Favositide du calcaire carbonifére supérieur, 20.—
R, Malherbe. Etude sur la stratigraphie souterraine de la partie Nord-

150 ADDITIONS TO THE LIBRARY,

ouest de la province de Liége, 33.—A. Briart. Etude sur les Dépéts
Gypseux et Gypso-salifériens, 62.—G. Cesaro. Reproduction de la
Nadorite, 189.—Max Lohest. De Vorigine des Anthracites du Calcaire °
Carbonifere de Visé, 151.—L. Bayet. Note sur un faciés local du Pou-
dingue de Burnot, 158.—G. Cesaro. Les formes cristallines dela Calcite
de Rhisnes, 165.—A. Hrens. Note sur les roches cristallines recueillies
dans les Dépots de Transport situés dans la partie méridionale du Lim-
bourg Hollandais, 395.—H. Forir. Contributions 4 l’étude du systéme
crétacé de la Belgique, 445.

Libliographie.
C. Malaise. L’Ardenne par J. Gosselet, 3.

Liége. Socicté Géolegique de Belgique. Annales. Tome xvii.
layne 251890;
Bulletin.

C. Malaise. Sur un nouveau gisement d’octraédrite, xv.—Carte @éo-
logique de la Belgique, xix.—G. Schmitz. Sur un gisement de calcite
lamellaire et d’un trone de sigillaire, xxvi—W. Spring. Sur la vitesse
de dissolution de quelques minéraux carbonatés dans les acides, xxxi.—
A. de Vaux. Sur les fossiles houillers de Ghlin, xxxvii.—A,. Firket.
Fossiles des gites de phosphorite de la Hesbaye, xliv.—A. Firket. Sur
Yage et Vorigine d’un limon récent de la vallée de l’Ourthe, xlvi.—xX.
Stainier. Compte-rendu de la Réunion Extraordinaire de la Société
Géologique de Belgique dans le Brabant Méridional du7 au 10 Septembre
1889, 30.

Mémoires.

X. Stainier. La Diabase de Grand Pré, Mozet, 3.—R. Malherbe.
Géogénie de la Houille, 25.—X. Stainier. Mélanges pétrographiques, 41.
—J. Fraipont. Huryptérides nouveaux du dévonien supérieur de Belgique,
53.—G. Schmitz. Note sur les sablonniéres de Rocour, 65.—G. Cesaro.
Lamelles de calcite dans la houille des environs de Liége, 85, 99.—
G. Cesaro. Figures produites par la rayure sur les clivages du sel gemme
et sur les faces m du prisme primitif de l’aragonite, 93.—M. Lohest. Sur
le mouvement d’une couche de houille entre son toit et sur mur, 124.—
A. Briart. Note sur les mouvements paralléles des roches stratifiées, 129.
—M. Lohest. Des gisements de Phosphate de Chaux de la Hesbaye
137.—M. Lohest. De Vage relatif des failles du Bassin Houiller de
Liége, 149.

——. Société Royale des Sciences. Mémoires. Sér. 2. Tome xvi.
1890.

Lille. Société Géologique du Nord. Annales xvi. 1888-89,
Livr. 5-6. 1889.

L. Cayeux. Compte-rendu de l’Excursion géologique du Nord dans
les environs de Mons, 254.—J. Ortlieb. Note sur la Ciplyte, 270.—L.
Cayeux. Description géologique du canton d’Avesnes-Nord, 280.—
Levaux. Coupe de la carriére Bertrand 4 Louvroil, 841.—L. Cayeux.
Un cas de stratification entrecroisée des limons, & Cysoing, 343,—
L. Cayeux. Structure de la bande de calcaire carbonifére de 'Taisniéres-
sur-Helpe, 344.—Malaquin. [Excursion générale annuelle a Mons-en-
Bareeul, 353.—L. Cayeux. Forages de Roubaix, Tourcoing, Wattrelos
et Roncq, 358.

ADDITIONS TO THE LIBRARY. I51

Lille. Société Géologique du Nord. Annales. Tome xvii. Livr.
1-3. 1889-90. 1890.
L. Boutan. Quelques remarques sur la classification des ongulés, 2

C. Barrois. Notice explicative de la feuille de Redon, 16. ai) Ure
Sur les diabases du Menez-Hom (Finistére), 28. —-J. Gosselet. Les
Demoiselles de Lihus, 35.—Jannel. Etudes sur les lignes de ’ Hst, 45.——
Gronnier. Excursions géologiques dans les environs de, Vichy, 47.—
L. Cayeux. Ondulations de la craie de la feuille de Cambrai et rapports
de la structure ondulée avec le systéme hydrographique de cette carte,
71.—C. Barrois. Feuille de Pontivy, 90.—L. Cayeux. Mémoire sur la
craie grise du Nord de la France, 105.—H. Lasne. Sur la composition
des phosphates des environs de Mons, 142.—Ladriére. Resultats de deux
sondages exécutés a4 Marquette et a la Madelaine, 149.—L. Cayeux.
Découverte de silex taillés & Quiévy (Nord), 151.—J. Ortlieb. A propos
de la Ciplyte, 155.

Linnean Society. Journal. Vol. xx. Zoology. Nos. 122-123.
1889.

——. ——. Vol. xxi. Zoology. Nos. 133-135. 1889.
Vol. xxii. Zoology. Nos. 141-144. 1889.

Py Martin Duncan. A Revision of the Genera and great groups of the
Echinoidea, 1.

—-, ——. Vol. xxv. Botany. Nos.171-172. 1889 & 1890.
——. ——. Vol. xxvi. Botany. No. 174. 1890.
—. ——. Vol. xxviu. Botany. Nos. 181-182. 1890.

—-—. Proceedings. May 1890.
——. Transactions. Ser. 2. Zoology. Vol. v. Part 3. 1889.

Lisbon. Sociedade de Geographia. Boletim. Serie 8. Nos. 3,
6-8. 1888-89. 1889.

Liverpool Geological Association. Journal. Vol. ix. 1888-89.
1890.

P. F. Kendall. The Geology of Mull, 9. —C. Ricketts. On a Probable
Cause of Contortion in Strata, 17.—W. OD, He Wengen Meteor rites, 22.—
Jowaldine.. The Building-stones used in Liverpool, 25.—J. E. George.
Notes on some Manx Lavas, 41.—W. Hewitt. The Evolution of the
Grand Cafion of the Colorado, 49.—H. T. Mannington. Note on a Cal-
careous Deposit near Flint, 57,—J. Wilding. The Sandstones used in
Birkenhead Priory, 59.—J. Hornell. The Hand-footed Labyrinthodont,
65.

Liverpool Geological Society. Proceedings. Session 13. 1888-9.

fol vi. Partl.” 1389.

Sir J. A. Picton. Notes on the Local Historical Changes in the Sur-
face of the Land in and about Liverpool, 31.—J. J. Fitzpatrick. The
Permian Conglomerate and other Palaeozoic Rocks to the North of
Morecambe Bay, 42.—G. H. Morton. Further Notes on the Stanlow,
Ince, and Frodsham Marshes, 50.—A. Timmins. Notes on u few Borings
and the Base of the New Red Sandstone in the neighbourhood of Liver-
pool, 56.—J. Lomas. Notes on some Basaltic Dykes occurring near Aros,

VOL, XLVI. 1)

152 ADDITIONS TO THE LIBRARY.

Mull, 69.—Sir J. A. Picton. The Vyrnwy Valley, its Geological and
Glacial History, 74—G. F. Deacon. Note on the Glacial Geology of the.
Vyrnwy Valley, 86.—T. Mellard Reade. Slickensides and Normal
Faults, 92.—G. H. Morton. Some Faults Exposed in Shafts and Borings
in the neighbourhood of Liverpool, 115.—E. Dickson and P. Holland.
Some Volcanic Rocks in the Isle of Man, 123.

Liverpool. Literary and Philosophical Society. Proceedings.
Vol. xli. 1886-87. 1887.

5 5 Vol. xlii. 1887-88. 1888.

H. H. Higgins. On the Remains of Temperate and Subtropical Plants
found in Arctic Rocks, 103.—R.McLintock. Lake Lahontan, an Extinct
Quaternary Lake of North-west Nevada, U.S.A., 339.

—. ——. ——. Vol. xlii. 1588-89. 1889.

London, Edinburgh, and Dublin Philosophical Magazine and Journal
of Science. Ser. 5. Vol. xxvii. Nos. 170-177. 1889. Pre-
sented by Dr. W. Francis, F.G.S.

E. Hull. Ona possible Geological Origin of Terrestrial Magnetism,

: ae Karsten. The Geological Age of the Mountains of Santa Marta,

a, W———, AVol, xxix.» Wos: b76—16le le o0 see by
Dr. W. Francis, F.GS.

London. Society of Amateur Geologists. Proceedings. Vol. i.
No. 4. 1889.

W. Smart. Kent’s Cavern, and Cave Deposits, 41.—J. Slade. Me-
teorites, 44.—J. T. Day. Notes on papers on “ The Action of Water in
Seismic and Volcanic Phenomena, by Stanislas Meunier,” and “The
Variations of Level on the Coast of Sweden, by L. Holstrém,” 47.—G.S.
Boulger. The Evidence of Paleontology as to Evolution, 50.—W. J.
Atkinson. On the Relative Changes of Level of Land and Water, 55.—
H. Fleck. On the Classification of Igneous Rocks, 58.

Madison. Wisconsin Academy of Sciences, Arts, and Letters.
Transactions. Vol. vii. 1883-87. 1889.
F, Leverett. Raised Beaches of Lake Michigan, 177.

Madrid. Real Academia de Ciencias Exactas, Fisicas y Naturales.
Memorias. Tomo xiii. Parte 2-3. 1889.

M. P. Graells. Las Ballenas en las Costas Ocednicas de Espaiia, 7.
(Fossil, at p. 102.)

=, -- =, Revista, ‘Tomo xan Nos. 5-7. 188e2s0

Manchester. Geological Society. Transactions. Vol. xx. Parts 9—
17. 1889-90.

W. Clifford. Additional notes on Richmond Coal-field, Virginia, in
reply to Criticisms, 247.—W. J. Bird. Note on the Seaton-Carew
Boring, 263.—W. Watts. Erratic Boulders and Boulder-Clay in Castle-
shaw Valley, 265.—H. Hall. On the Duration of our Coal-supply, 379.
—Mark Stirrup. Report on the meeting of the British Association at
Newcastle-upon-Tyne, 394.—M. Stirrup. On an alleged recent Dis-
covery of a Fossil Forest in Scotland, 412—E. Hull. On the probable

ADDITIONS TO THE LIBRARY. 153

average depth at which Coal is now being worked in the British Isies,
417.—H. W. Williams. On Pembrokeshire as a field for the Study of
Geology, 426.—Mark Stirrup. On the Hydrology of the Causses of
Languedoc; the Gorges of the Tarn, its Caverns and Subterranean
Streams, 446.—R. Walkden. On the ‘ Stigmaria ficordes”’ found in a
mine at Over Darwen, Lancashire, 461.—T. Ward. On the Salt-deposits
of the United States of America and Canada, 471.

Manchester. Literary and Philosophical Society. Memoirs and
Proceedings. Series 4. Vol. 1. 1889.

W.C. Williamson. The Permanence of Oceanic Basins, 33.—W. Boyd
Dawkins. The Permanence of Oceanic Basins, 36.—W. Thomson. On
Leaves found-in the cutting for the Manchester Ship-caiial, 21 feet under
the surface, and on Green Colouring-matter contained therein, 216.—E.
Schunck. On the Green Colouring-matter from Leaves found in one of
the Cuttings for the Manchester Ship-canal, 231.

. Public Free Libraries. 37th Annual Report to the Council
of the City of Manchester. 1888-89. 1889.

Melbourne. Geological Society of Australasia. Transactions. Vol. i.
Part 4. 1890.

F. W. Hutton. On the Granites and Associated Rocks of the Upper
Buller River, New Zealand, 99.—F. W. Hutton. Description of some
Eruptive Rocks from the neighbourhood of Westport, New Zealand, 106.
—F. D. Power. Notes on the Brighton Coast, 112.—F. McKnight. A
new Protaster from Australia, 116.—T. P. Moody. On the occurrence
of Amberite, Ambrite, or Fossil Gum, in a Coal-seam at Kawakawa
Colliery, Bay of Islands, New Zealand, 117.

——. Royal Society of Victoria. Proceedings. N.S. Vol. i.
1889.

T. 8S. Hall. On two new Fossil Sponges from Sandhurst, 60.—F. A.
Campbell. The Active Volcano on Tana, New Hebrides, with some
remarks on the Cause of Volcanic Action, 71.—J. Stirling. Notes on
the Physiography of the Western portion of the County of Croajengo-
long, 84.

——. Working Men’s College. Report for 1888. 1889.

Meriden, Conn. Meriden Scientific Association. Proceedings and
Transactions. Vol. ii. 1887-88. 1889.

W. M. Davis. The Ash-Bed at Meriden and its Structural Relations,
23.

Middlesex Natural-History and Science Society. Transactions.
Session 1888-89.
W. H. Flower. The Natural-History Museum, Cromwell Road, 3.—
J. A. Brown. Working-sites and inhabited land-surfaces of the Paleo-
lithic Period in the Thames Valley, 40.

Mineralogical Society. Mineralogical Magazine and Journal. Vol.
vill. Nos. 39-40, 1889.

L. Fletcher. On Crystals of Percylite, Caracolite, and an Oxychloride
of Lead (Dayiesite), from Mina Beatriz, Sierra Gorda, Atacama, South
America, 171.—A. H. Church. Note on Colorado Hydrophane, 181.—
G.T. Prior. Note on Connellite from a New Locality, 182. R.H. Solly.
Pseudomorphs of Hematite after Iron-pyrites, 183.—J. W. Judd. On

m2

154 ADDITIONS TO THE LIBRARY.

the Processes by which a Plagioclase Felspar is converted into a Scapo-
lite, 186.—M. Forster Heddle. On the occurrence of Gyrolite in India,
199.—M. Forster Heddle. On Dudgeonite, Hydroplumbite, Plumbona-
crite, and Plattnerite, 200.—H. A. Miers. Mineralogical Notes, 204.—
L. Fletcher. On the Meteorites which have been found in the Desert of
Atacama and its neighbourhood, 223,—T. McK. Hughes. On the manner
of occurrence of Beekite and its bearing upon the origin of Siliceous Beds
of Paleozoic Age, 265.—M. F. Heddle. On the Crystalline Form of
Gyrolite, 272.—M. F. Heddle. On the Identity of Bruiachite and Fluor,
274.—M. F. Heddle. On New Localities for Linarite, Caledonite, and
Hpistilbite, 278.

Mineralogical Society. Mineralogical Magazine and Journal. Vol.

ix. No. 41. 7 1390.

H. A. Miers. The Hemimorphism of Stephanite: the crystalline form
of Kaolinite, 1.—J. T. Cundall. On Zine Oxide from a Blast-furnace,
5.—G. T. Prior. On Zinc Sulphide replacing Stibnite and Orpiment :
Analyses of Stephanite and Polybasite, 9.—L. Fletcher. The ,Meteoric
Tron of Tucson, 16.

Minneapolis. American Geologist. Vol. iv. Nos. 1-6. 1889.

Purchased. |

F, Leverett. Studies in the Indiana Natural Gas-field, 6.—E. O.
Ulrich. On Lingulasma, a new Genus, and eight new Species of Lingula
and Trematis, 21.—J. C. White. The Age of the Tipton-Run Coal of
Blair County, Pennsylvania, 25.—J. Hensoldt. Meteorites and what
they teach us, 28, 73.—J. Le Conte. The general interior condition of
the Earth, 38.—P. Frazer. The late Session of the International Congress
of Geologists at London, 44.—G. M. Dawson. Notes on the Ore Deposits
of the Treadwell Mine, Alaska, 84.—F. D. Adams. On the Microscopic
character of the Ore of the Treadwell Mine, Alaska, 88.—W. H. Sherzer.
New characters of Diphyphyllum semcoénse (Bill.), Rom., 93.—S. Calvin.
Tron Butte, Montana—Some preliminary notes, 95.—J. F. Kemp and
V. F. Marsters. On certain Camptonite Dikes near Whitehall, N.Y.,
97.—C. S. Beachler. Notice of some new and remarkable forms of
Crinoidea from the Niagara Limestone at St. Paul, Indiana, 102.—G. F.
Matthew. How is the Cambrian divided ? 139.—G. C. Broadhead. The
Missouri River, 148.—J. Marcou. The Mesozoic series of New Mexico,
155.—W. Upham. Glaciation of Mountains in New England and New
York, 165.—R. T. Hill. Foraminiferal origin of certain Cretaceous
Limestones, and the sequence of Sediments in North American Cretaceous,
174.—C. R. Keyes. The subgeneric groups of Naticopsis, 193.—A.
Winchell. Views on Prenebular conditions, 196—W. Upham. Glacia-
tion of Mountains in New England and New York, 205.—J. Marcou.
The Mesozoic series in New Mexico, 216.—A. F. Foerste. Note-taking
and the use of Maps in Geological Field-work, 229.—C. H. Gordon.
Notes on the Geology of South-eastern Iowa, 257.—R. 8. Woodward.
Mathematical theories of the Earth, 268.—V. C. Alderson. Geology in
High Schools, 284.—M. Fischer. The photographic survey of a State,
289.—N. H. Winchell and H. V. Winchell. On a possible chemical
origin of the Iron Ores of the Keewatin in Minnesota, 291.—N. W. Perry.
The Cincinnati rocks : What has been their Physical History ?, 326.—T.
Rupert Jones. On some Paleozoic Ostracoda from Pennsylvania, U.S.,
337.—N. H. Winchell. Methods of Stratigraphy in studying the Huro-
nian, 342.—Jules Marcou. Jura, Neocomian, and Chalk of Arkansas,
357.—A., F. Foerste. Fence-wall Geology, 367.—Some recent specula-
tions on the Origin of Petroleum, 371.

ADDITIONS TO THE LIBRARY. 155

Montreal. Natural-History Society. Canadian Record of Science.

Voli, Nos. 7-8. , 1389.

G. F. Matthew. On the Cambrian Organisms in Acadia, 383.—E. T.
Chambers. Notes on the Lake-St.-John Country, 388.—G. J. Hinde.
On a new Genus of Siliceous Sponges from the Trenton Formation at
Ottawa, 395.—H. M. Ami. On a Species of Goniograptus from Lévis
Formation, 422.—Sir J. W. Dawson. On Fossil Sponges at Little Metis,
429.—Sir J. W. Dawson. New Fossil Plants from the North-west, 430.
—D. G. Penhallow. Notes on Erian (Devonian) Plants, 430.—G. F.
Matthew. How is the Cambrian divided ? a plea for the classification
of Salter and Hicks, 475.—G. F. Matthew. On the occurrence of Lepto-
plastus in the Acadian Cambrian Rocks, 485.—H. M. Ami. Additional
Notes on Gontograptus Thureant, M‘Coy, from the Lévis Formation,
Canada, 502.

—., : Vol.iv.,, Nos. 1-2. 13890,

J. W. Dawson. On new Plants from the Erian and Carboniferous,
and on the Characters and Affinities of Paleozoic Gymnosperms, 1.—
R. MacFarlane. On an [Expedition down the Beghula or Anderson
River, with Introduction by G. M. Dawson, 28.—Sir J. W. Dawson.
Note on a Fossil Fish and Marine Worm found in the Pleistocene
Nodules of Green’s Creek, on the Ottawa, 86.—B. J. Harrington. Notes
on Gothite, Serpentine, Garnet, and other Canadian Minerals, 93.—J. T.
Donald. Scolecite from a Canadian Locality, 99.—J.T. Donald. Notes
on Asbestus and some Associated Minerals, 100.—W. Deeks. The Lower
Helderberg Formation of St. Helen’s Island, 104.

——. Royal Society of Canada. Proceedings and Transactions
for the year 1888. Vol. vi. 1889.

Section III.

T. Sterry Hunt. The Classification and Nomenclature of Metalline
Minerals, 61.

Section LV,

R. Bell. The Huronian System of Canada, 3—L’Abbé Laflamme.
Le Gaz naturel dans la province de Quebec, 15.—D. P. Penhallow. On
Nematophyton and allied forms from the Devonian (Erian) of Gaspé and
Bay des Chaleurs; with Notes by Sir W. Dawson, 27.—G. F. Matthew.
On some Remarkable Organisms of the Silurian and Devonian Rocks in
Southern New Brunswick, 49.—E. Gilpin, jun. Notes onthe Nova-Scotia
Gold Veins, 63.—Sir W. Dawson and G. M. Dawson. On Cretaceous
Plants from Port McNeill, Vancouver Island, 71.—J. F. Whiteaves.
Tllustrations of the Fossil Fishes of the Devonian Rocks of Canada,
Patt Uli 17.

Moscow. Société Impériale des Naturalistes. Bulletin. 1889.
Ser. 2. Tomei. Nos. 1-8. 1889-90.

A. Paylow. Etudes sur les couches jurassiques et crétacées de la
Russie. I. Jurassique supérieur et crétacé inférieur de la Russie et de
PAngleterre, 61.—Stanislas Meunier. Sur un procédé naturel qui permet
aux eaux superficielles de pénétrer dans les régions chaudes des profon-
deurs terrestres, 161.—A. Pavlow. Communication supplémentaire sur
les couches néocomiennes et jurassiques supérieures de la Russie et de
co 176.—W. Tzebrikow. Note sur le néocomien de la Crimée,

156 ADDITIONS TO THE LIBRARY.

Moscow. Sociceté Impériale des Naturalistes. Beilage zum Bulletin.

Ser. 2. Tome ii. Meteorologische Beobachtungen. 1889. .
Hefte 1-2. 1889.

——. ——. Nouveaux Mémoires. Tome xv. Livr. 6. 1889.

Munich (Cassel). K6niglich-bayerische Oberbergamt, Geognostische
Abtheilung. Geognostische Jahreshefte. Zweiter Jahrgang,
L889. Les9;

H. Thiirach. Uebersicht tiber die Gliederung des Keupers im nérd-
lichen Franken in Vergleiche zu den benachbarten Gegenden, 1.—O. M.
Reis. Die Korallen der Reiter Schichten, 91—C. W. v. Gumbel. Die
geologische Stellung der Tertiarschichten von Reit im Winkel, 163.—
A. Leppla. Zur Lossfrage, 176.

Munich. Koniglich-bayerische Akademie der Wissenschaften.
Abhandlungen der mathematisch-physikalischen Classe. Band
xvi. Abth.3. 1888.

; . Sitzungsberichte der mathematisch-physikalischen
Classe. 1888. Heft 3. 1889.
F. y. Sandberger. Ueber Lithionit-Granite, mit besonderer Riicksicht

auf jene des Fichtelgebirges, Erzgebirges und des nordlichen Bohmens,
423,

5 : . 1889. Hefte 1-3. 1889-90.

C. W. v. Giimbel. Ueber das Erdbeben vom 22 Februar 1889 in der
Umgegend von Neuburg a. D., 79.—O. E. Meyer. Ueber Gebirgs-
magnetismus, 167.—W. v. Giimbel. Geologische Bemerkungen iiber die
warmen Quellen von Gastein und ihre Umgebung, 341.

Nancy. Académie de Stanislas. Mémoires, 1888. 139e Année.
5e Série. Tome vi. 1889.

——, Socicté des Sciences. Bulletin. Série2. Tomeix. Fase.
99. Yie Année. L888. 1889.
A. Liétard. Note sur le trias dans la région méridionale des Vosges,
44,—Bleicher. Note sur la découverte d’un atelier de taille de silex aux
environs de Commercy, 94.

Nature. Vol. xl. Nos. 1025-1044. 1889.

R. Abercromby. Nitrate of Soda and the Nitrate Country, 186, 308.—
A. S. Woodward. The Paleontology of Sturgeons, 186.—A. Geikie.
Recent researches into the Origin and Age of the Highlands of Scotland
and the West of Ireland, 299, 320.—L. Lydekker. The entire Skeleton
of an English Dinosaur, 324.—A. G. Nathorst. On the Geological
History of the Prehistoric Flora of Sweden, 453.—J. Geikie. Opening
Address to Section C, Geology, British Association, 486.—American
Association for the Advancement of Science, 556.—J. Milne. Seismo-
logical work in Japan, 656.

——, Vol. xl. Nos. 1045-1069. 1890.

L. Fletcher. On the supposed enormous Showers of Meteorites in the
Desert of Atacama, 108.—Geological Excursion to the Active and Ex-
tinct Volcanoes of Southern Italy, 133.—H. F. Osborn. The Paleonto-
logical Evidence for the Transmission of Acquired Characters, 227.—
J. D. Dana. Sedgwick and Murchison: Cambrian and Silurian, 421.—
The Primitive Types of Mammalian Molars, 465,

ADDITIONS TO THE LIBRARY. 157

Wature. Vol. xiii. Nos. 1070-1077. 1890.

W. J. L. Warton. Eva Island, Tonga Group, 85.—J. W. Judd.
Chemical Changes in Rocks under Mechanical Stresses, 101—M. Neu-
mayr. The Climates of Past Ages, 148, 175.—J. Murray and R. Irvine.
oe Reefs and other Carbonate-of-Lime Formations in Modern Seas,
162.

Neweastle-upon-Iyne. Natural-History Society of Northumber-
land, Durham, and Newcastle-upon-Tyne and Tyneside Natu-
ralists’ Field-Club. Natural-History Transactions. Vol. viii.
Part 3. 1889.

D. Embleton. On a Spinal Column of Lovomma Alimani, Huxley,
349.

——. North of England Institute of Mining and Mechanical
Engineers. Transactions. Vol. xxxviii. Parts 3-5. 1889-
1890.

T.O. Robson. Notes on the variations in the Faulting of Coal, observed
in the action of the same series of faults in three seams at Redheugh
Colliery, 49.—C. Z. Bunning. Coal-Mining at Warora, Central Provinces,
East India, 77.—J. M. Liddell. The Gold-fields of the Valley of De
Kaap, Transvaal, South Africa, 171.

New Haven. American Journal of Science. Ser. 3. Vol. xxxviil.
Nos. 223-228. 1889.

Sir W. Dawson. A new Erian (Devonian) Plant allied to Cordaites,
1.—C. D. Walcott. Stratigraphic Position of the Olenellus Fauna in
North America and Europe, 29.—A. Hague. Notes on the occurrence of
a Leucite Rock in the Absaroka Range, Wyoming Territory, 43.—J. C.
Branner and R. N. Brackett. The Peridotite of Pike County, Arkansas,
50.—R. N. Brackett. A Microscopic Study of the Peridotite of Pike
County, Arkansas, 56.—T. M. Chatard. On Urao, 59.—J. Croll. On
prevailing misconceptions regarding the evidence which we ought to
expect of former Glacial Periods, 66.—G. F. Kunz. Mineralogical Notes
on Fluorite, Opal, Amber, and Diamond, 72.—O. C. Marsh. Discovery of
Cretaceous Mammalia, 81, 177.—G. H. Williams. On the possibility of
Hemihedrism in the Monoclinic Crystal System, with especial reference
to Hemihedrism of Pyroxene, 115.—G. M. Dawson. On the Earlier
Cretaceous Rocks of the North-western portion of the Dominion of Canada,
120.—F. W. Clarke. A new Occurrence of Gyrolite, 128.—J. F. Kemp.
On certain Porphyrite Bosses in North-western New Jersey, 130.—N. H.
Darton. On the great Lava-flows andintrusive Trap-sheets of the Newark
system in New Jersey, 134.—W. B. Dwight. Recent Explorations in the
Wappinger-Valley Limestones and other formations of Dutchess Co.,
N.Y., 189.—O. C. Marsh. Notice of Gigantic Horned Dinosauria from
the Cretaceous, 173.—C. R. Keyes. The Carboniferous Echinodermata
of the Mississippi Basin, 186.—F. A. Genth.—Contributions to Minera-
logy, No. 44, 198.—L. C. Johnson. The “ Grand-Gulf” Formation of
the Gulf States, 213.—C. E. Beecher. Note on the fossil Spider, Arthro-
lycosa antiqua of Harger, 219.—W. H. Hobbs. On the Paragenesis of
Allanite and Kpidote as Rock-forming Minerals, 223.—F. L. Nason. New
locality of the Camptonite of Hawes and Rosenbusch, 229.—J. B. Mack-
intosh. Notes on some Native Iron Sulphates from Chili, 242.—J. Le
Conte. On the Origin of Normal Faults and of the Structure of the
Basin Region, 257.—G. H. Eldridge. Some suggestions upon the method
of Grouping the Formations of the Middle Cretaceous and the employment
of an additional term in its nomenclature, 313.—D. W. Langdon, Jr.

158 ADDITIONS TO THE LIBRARY.

Some Florida Miocene, 322.—R. 8S. Woodward. The Mathematical
Theories of the Earth, 8357.—E. O. Hovey. Observations on some of the

Trap Ridges of the Kast Haven-Branford Region, with a map, 361.—F.

W. Clarke. A Theory of the Mica Group, 384.—W. 58. Yeates. Pseu-
domorphs of Native Copper after Azurite, from Grant County, New
Mexico, 405.—C. A. White. The Lower Cretaceous of the South-west,
and its relation to the underlying and overlying formations, 440.— W. H.
Dall. On the Hinge of Pelecypods and its Development, with an attempt
toward a better subdivision of the group, 445.—R. T. Hill. Relation of
the Uppermost Cretaceous Beds of the Eastern and Southern United
States ; and the Tertiary-Cretaceous Parting of Arkansas and Texas, 468.
—W. E. Hidden and J. B. Mackintosh. A description of several Yttria
and Thoria Minerals from Llano County, Texas, 474.—O. C. Marsh. The
Skull of the Gigantic Ceratopside, 501.

New Haven. American Journal of Science. Ser. 3. Vol. xxxix.
Nos. 229-234. 1890.

H. 8. Williams. The Devonian System of North and South Devon-
shire, 31—W.H.Seamon. The Zinciferous Clays of South-west Missouri,
and a Theory as to the growth of the Calamine of that section, 38.—J. D.
Hawkins. On Minium from Leadville, 42.—W. P. Blake. Mineralo-
eical Notes, 45.—F. A. Genth. Contributions to Mineralogy, 47.—T.
Mellard Reade. Origin of Normal Faults, 51—L.G. Hakins. A new
Stone Meteorite, 59.—E. 8. Dana. On the Barium Sulphate from Per-
kins’ Mill, Templeton, Province of Quebec, 61.—O. C. Marsh. Descrip-
tion of New Dinosaurian Reptiles, 81—D. White. On Cretaceous Plants
from Martha’s Vineyard, 93.—C. D. Walcott. A Review of Dr. R. W.
Ells’s Second Report on the Additional Notes on the “ Quebec Group,”
101.—F. A. Genth and S. L. Penfield. On Lansfordite, Nesquehonite,
a new Mineral and Pseudomorphs of Nesquehonite after Lansfordite, 121.
—A. R. C. Selwyn and G. F. Matthew. Tracks of organic origin in rocks
of the Animikie Group, 145.—J. D. Dana. Sedgwick and Murchison:
Cambrian and Silurian, 167.—G. M. Dawson. Notes on the Cretaceous
of the British-Columbian Region, 180.—G. H. Williams. Celestite from
Mineral County, West Virginia, 183.—G. J. Brush and E.S. Dana. On
the Mineral Locality at Branchville, Connecticut, with analyses by H. L.
Wells, 201.—F. Cramer. On a recent Rock-flexure, 220.—E. Orton.
On the Origin of the Rock-pressure of the Natural Gas of the Trenton
Limestone of Ohio and Indiana, 225.—_J. C. Branner. The A¢olian Sand-
stones of Fernando de Noronha, 247.—N. H. Darton and J. 8. Diller.
On the occurrence of Basalt Dikes in the Upper Paleozoic series in Central
Appalachian Virginia, 269.—W. F. Hillebrand and KE. S. Dana. Ad-
ditional Notes on the Tyrolite from Utah, 271.—W. 8. Bayley. The
Origin of the Soda-granite and Quartz-keratophyre of Pigeon Point, 275.
—W. E. Hidden and J. B. Mackintosh. On the occurrence of Polycrase,
or of an allied species, in both North and South Carolina, 302.—R. 8.
Tarr. Origin of some Topographical Features of Central Texas, 506.—
G. F. Becker. A elementary proof of the Earth’s Rigidity—G. H.
Williams. On the Hornblende of St.-Lawrence County, N.Y., and its
Gliding Planes, 352.—W. Cross. Note on some secondary minerals of
the Amphibole and Pyroxene groups, 359.—S. L. Penfield. On Spango-
lite, a new Copper Mineral, 370.—J.D. Dana. Archzean axes of Kastern
North America, 378.—F. J. H. Merrill. On the Metamorphic Strata of
South-eastern New York, 383.—L. G. Eakins. Meteoric Iron from North
Carolina, 395.—O. C. Marsh. Distinctive Characters of the order Hal-
lopoda, 415.—O. C. Marsh. Additional Characters of the Ceratopside,
with notice of New Cretaceous Dinosaurs, 418.—W. EH. Hidden and 8. L.

ADDITIONS TO THE LIBRARY. 159

Penfield. Hamlinite, a new rhombohedral mineral from the Herderite
locality at Stoneham, Me., 511.—O. C. Marsh. Notice of New Tertiary
Mammals, 525.

New York. Academy of Sciences. Annals. Vol.iv. Nos. 10-12.
1889.
E.N.S. Ringueberg. The Calceocrinide, 588.

: ee Volley. lesuy Nose lo.) VSee,
A. W. Vogdes. A Catalogue of North-American Paleeozoic Crustacea,
confined to the non-trilobitic genera and species, 1.

——. ——. Transactions. Vol. vili. Nos. 1-38. 1888-89.
ote) 3

G. F. Kunz. Beryls from North Carolina, 2—A. A. Julien and H.
Carrington Bolton. The true cause of Sonorousness in Sand, 9.—G. F.
Kunz. Bertrandite from Maine and Colorado and other minerals, 11.—
G. F. Kunz. New Minerals from the trap of Bergen Hill, 16.—J. 8.
Newberry. The new Oil-field of Colorado, and its bearing on the ques-
tion of the genesis of Petroleum, 25.—T. D. Rand. Comparison of the
Rocks of Philadelphia and New York, 47.—J. J. Friedrich. The Litho-
logy of Manhattan Island, 53.—J. Eyerman. The Mineralogy of the
French-Creek Mines, Pennsylvania, 56.—D. G. Eaton. Volcanoes, their
distribution and phenomena, 82.—A. Hyatt. Modes of evolution in Fossil
Shells, 114.—J.S. Newberry. The Man of Spy, discovery of Paleolithic
Human Skeletons near Liége, Belgium, 132.—J. H. Furman. The Tin-
deposits of North Carolina, 186.—J.S. Newberry. Amber, its History,
Occurrence, and Use, 156.—G. F. Kunz. American Ambers, with other
Mineralogical Notes, 158.—G. F. Kunz. The Precious and Ornamental
Stones of North America, 160.—N. L. Britton. Remarks on recent Dis-
coveries in local Cretaceous and Quaternary Geology, 177.—H. C. Bolton.
Jebel Nagous and a New ‘“ Mountain of the Bell,” 182.—W. E. Hidden.
Yttrium Minerals from Llano Co., Texas, 185.—A. R. Ledoux. The Pipe-
Creek (Texas) Meteorite, 186.

: . -———. Vol.ix. Nos.1 &2. 1889-90. 1890.

D.S8. Martin. The origin of Diagonal Trends in the Earth’s Crust, with
application to the production of normal and reversed faults and the fold-
ing of strata, 15—H.C. Bolton. Researches on Sonorous Sand in the
Peninsula of Sinai, 21.—J. 8. Newberry. The Laramie Group, its geo-
logical relations, its economic importance, and its fauna and flora, 27.—
J. J. Friedrich. On some new species of Protozodtites, Quaternary and
Tertiary, from California, and on the importance of Protozoa as rock-
building agents, 52.—J. S. Newberry. The Rock-salt Deposits of the
Salina Group in Western New York, 39.—F. J. H. Merrill and D. 8.
Martin. A note on the Coloured Clays recently exposed in railroad cut-
tings near Morrisania, N.Y., 45.

—_——-

|

. American Museum of Natural History. Annual Report of
the Trustees, for the year 1888-89. 1889.

—— Bulletin. Vol. i. “Now. 1888.

: . —. Vol.u. No.2. 1889.

KR. P. Whitfield. Observations on some imperfectly known Fossils from
the Calciferous Sand-rock of Lake Champlain, and descriptions of several
new forms, 41.—R. P. Whitfield. Additional notes on Asaphus canalis,
Conrad, 64.—R. P. Whitfield. Description of a new form of fossil Bala-

160 ADDITIONS TO THE LIBRARY,

noid Cirripede, from the Marcellus Shale of New York, 66.—R. P. Whit-
field. Note on the Faunal Resemblance between the Cretaceous formations
of New Jersey and those of the Gulf States, 113.

New York. Cooper Union for the Advancement of Science and Art.
13th Annual Report of the Trustees, May 29th, 1889.
SSO.

Northampton. Northamptonshire Natural-History Society and Field
Club... Journal.: Volniv-yuNe. 27. 1886.
T. Rupert Jones and J. W. Kirkby. On Carboniferous Ostracoda from
the Gayton Boring, Northamptonshire, 98.

Padua. R. Accademia di Scienze, Lettere, ed Arti. Atti e Memorie.
1888-89. Nuova Serie. Vol. v. 1889.

Palermo. Annales de Géologie et de Paléontologie. See Booxs.
Gregorio, Marquis A. de.

——. Societa di Scienze Naturali ed Economiche. Giornale.
Vol. xviii. 1887.
G. Di Stefano. Sul lias inferiore di Taormina e dei suoi dintorni, 46.
—G. Di Stefano. L’eta delle rocce credute triassiche del territorio di
Taormina, 589.

; : Volvxixe NSGe:
G. G. Gemmellaro. La fauna dei calcari con Fusulina nella valle del
fiume Sosio, 1.

Paleontographical Society. Monographs. Vol. xl. 1889.
1890. (Two copies.)

T. Rupert Jones and G. J. Hinde. A supplementary monograph of
the Cretaceous Entomostraca of England and Ireland.—W. H. Hudleston.
A monograph of the British Jurassic Gasteropoda, Part 1, No. 4.—S. 8.
Buckman. A monograph of the Inferior-Oolite Ammonites of the British
Islands. Part 4——G. F. Whidborne. A monograph of the Devonian
Fauna of the South of England, Part 2.

Paris. Académie des Sciences. Comptes Rendus. Tome cviii.
No. 25. 1889.
A. Gaudry. MRestauration du squelette du Dinoceras, 1292.—A.
Gaudry. Sur les Mastodontes trouvés a Tournan, dans le Gers, par M.
Marty, 1293.

a ablesaomeieyin. tase:
Tome cix. Nos. 1-27. 1889.

U. le Verrier. Sur une venue de granulite a riebeckite de Corse, 38.—
A. Lacroix. Sur une roche a amphibole sodique (riebeckite), astrophyl-
lite, pyrochlore et zircon du Colorado, 59.—B. Renault. Sur les feuilles
de Lepidodendron, 41.—H. Wild. 'Tremblement de terre a Werny, 164.
—Stanislas Meunier. Détermination lithologique de la météorite de San
Emigdio Range, California, 206.—O. Silvestri, Sur l’éruption récente
de Vile de Vulcano, 241.—H. Faye. Note sur la période glaciaire, 287.—
René Nicklés. Sur le gault et le cénomanien du sud-est de l’Espagne,
386.—Stanislas Meunier. Sur la Spongeliomorphia Saportat, espéce nou-
velle parisienne, 536.—Seunes et Beaugey. Roches éruptives récentes
des Pyrénées occidentales, 509.—W. Kilian, Nouvelles contributions 4
l'étude géologique des Basses-Alpes, 651.—A. Lacroix. Sur lexistence

ADDITIONS TO THE LIBRARY. 161

de nombreuses zéolithes dans les roches gneissiques de la haute Ariége,
719.—P. Fliche. Sur les bois silicifiés d’Alyérie, 873.—A. Gaudry. Ob-
servations & propos de la communication de M. Fliche, 874.—Stanislas
Meunier. Analyse de la météorite de Phu-Hong, 875.—A. Gaudry. Sur
la découverte d’un Singe fossile par M. le Dr. Donnezan, 955.—Stanislas
Meunier. Analyse de la météorite de Mighei (Russia), 976.—Y. Wada.
Tremblement de terre de l’ile Kioushou au Japon, 978.—C. Depéret. Sur
le Dolichopithecus ruscinensis, nouveau Singe fossile du pliocéne du Rous-
sillon, 982.

Paris. Académie des Sciences. Comptes Rendus. Tables. Tome
Ci, 1889.

—, : » Pome vex. Nosy lion teo0:

A. Daubrée. Analogies de gisement du diamant, d’une part, dans les
gites de l’Afrique australe; d’autre part les météorites, 18.—A. Lacroix.
Sur les cipolins & minéraux et les roches 4 wernérite de l’Ariége, 54.—
Thoulet. Le relief et la géologie sous-lacustres du lac de Longemer, 56.
—S8. Reinach. Sur les prétendues éruptions volcaniques qui auraient eu
lieu en France au V° siecle aprés J.-C., 97.—L. de Launay. La géologie
de Vile Mételin, 158.—A. de Schulten. Sur la reproduction artificielle
de la malachite, 202.—A. de Grossouvre. Sur la présence de fossiles
alpins dans le callovien de l’ouest de la France, 204.—E. Mallard. Sur
la iussatite, nouvelle variété minérale cristallisée de silice, 245.—Beaugey.
Formation du quartz par la source de Mauhourat, a Cauterets, 300.—A.
Lacroix. Sur l’existence de roches 4 leucite dans l’Asie Mineure, et sur
quelques roches a hypersthéne du Caucase, 302.—L. Cayeux. De la
composition de quelques craies pseudo-dolomitiques du nord de la France,
304.—A. Gaudry. Le Dryopithecus, 373.—A. Issel. Radiolaires fossiles
contenus dans les cristaux d’albite, 420.—S. Meunier. Contribution 4
Vhistoire du fer chromé, 424.—V. Lemoine. Sur les rapports qui parais-
sent exister entre les mammiféres cretacés d’ Amérique et les mammiféres
de la faune cernaysienne des environs de Reims, 480.—A. Gaudry. Ap-
parences d’ inégalité dans le développement des étres de ancien et du
nouveau continent, 482.—Venukoff. De la formation du delta de la Néva,
484,—Stanislas Meunier. Recherches chimiques sur les tests fossiles de
Foraminiféres, de Mollusques et de Crustacés, 597.—J. Caralp. Sur un
kersanton pyrénéen, son age, ses aflinités avec l’ophite, 599.—G. Cotteau.
Sur les Hchinides crétacés du Mexique, 621.—Michel-Lévy et Munier-
Chalmas. Sur de nouvelles formes de silice cristallisée, 649.—J. Thoulet.
De la solubilité de quelques substances dans l’eau de mer, 652.—G. Rol-
land. Sur les grandes dunes de sable du Sahara, 659.—Munier-Chalmas.
I. Sur les formations gypseuses du bassin de Paris. II. Sur les dépdts
silicieux qui ont remplacé le gypse, 663.—Chevalier. Sur un tremble-
ment de terre a Chang-Hai et les mouvements des boussoles 4 Zi-Ka- Wei
durant ce tremblement de terre, 670.—P. Termier. I. Sur les séries
d’éruptions du Mézenc et du Meygal (Velay). II. Sur l’existence de
Veegyrine dans les phonolithes du Velay, 730.—H. Boursault. Compo-
sition de quelques roches du nord de la France, 733.—A. Julien. Ré-
sultats généraux d’une étude d’ensemble du carbonifére marin du plateau
central, 756.

; . ——. Tome cx. Nos. 17-23. 13890.

A. F. Marion. Sur le Gomphostrobus heterophylla, Conifére prototy-
pique du Permien de Lodéve, 892.—C. Depéret. Sur la découverte d’une
Tortue de terre géante au mont Léberon, 915.—E. Mallard. Sur la tri-
dymite et la christobalite, 964.—A. Lacroix. Sur les zéolithes des gneiss
de Cambo (Basses-Pyrénées), 967.—A. Michel-Lévy. Existence du

162 ADDITIONS TO THE LIBRARY.

péridot microlithique dans les andésites et les labradorites de la chaine des
Puys, 1007.—A. Lacroix. Sur les phénoménes de contact de la syénite
éléolithique de Pouzac (Hautes-Pyrénées), et sur la transformation en
dipyre de la roche ophitique du méme gisement, 1011.—C. L. Frossard.
Sur les roches métamorphiques de Pouzac (Hautes-Pyrénées), 1013.—A.
F, Marion. Sur la flore turonienne des Martigues (Bouches-du-Rhéne),
1052.—Bourgeat. Observations sur la structure de quelques dépéts fer-
rugineux des terrains secondaires, 1085.—G. Vasseur. Découverte d’une
flore turonienne dans les environs des Martigues (Bouches-du-Rhone),
1086.—A. Pomel. Sur les Hippopotames fossiles de Algérie, 1112.—A.
Lacroix. Sur la syénite éléolithique de Montreal (Canada) et sur les
modifications de contact endomorphes et exomorphes de cette roche, 1152.
—G. Vogt. De la composition des argiles et kaolins, 1199. —M. Bleicher.
Sur la nature des phosphates du massif du Dekma (Département de Con-
stantine), 1226.—G. Vasseur. Sur existence de dépdots marins pliocénes
en Vendée, 1228.

Paris. Annales des Mines. Série8. Tome xv. 138° livraisons

de 1889." 13889:
L. Aguillon. L’Ecole des Mines de Paris, 433.

———, ‘Tome xvi. 4°—6° livraisons. dewieso:

1889.

L. de Launay. Mémoire sur l’industrie du cuivre dans la région .
d’ Huelva, 427.

——. Annales des Sciences Géologiques. Tome xxi. 1889.

Purchased.
J. Bergeron. Etude géologique du massif ancien situé au sud du
Plateau Central, 1.

——. Annales des Sciences Naturelles. Zoologie et Paléontologie.
Série 7. Tome vii. Nos. 3-6. 1889. Purchased.

: : Tome vil. Nos. 1-6. 1889. Purchased.
G. Cotteau. Hchinides recueillis dans la province d’Aragon (Espagne)
par M. M. Gourdon, 1.
——. Annuaire Géologique Universel. Tome y. 1889. (Annual
Résumé of Geology.)

——. Annales Hydrographiques. Série 2. 1 et 24 volume de
13895, 1889:

——. Association Francaise pour l’Avancement des Sciences.
Compte Rendu de la 18™e Session. 1° et 2° Partie. 1889.
Purchased. —

Ramon de Luna. Sur les apatites de Jumilla (Espagne), 276.—Car-
riére. Notes sur la géologie du département d’Oran, 289 (390).—G. Leu-
nier. TF ossiles siluriens recueillis a la Hague dans la baie d’Esculgrain,
289.—Wohlgemuth. Sur la cause du changement de lit de la Moselle,
ancien affluent de la Meuse, 289 (403).—Bleicher. Formations glaciaires
des Vosges, 290.—G. Cotteau. Note sur VHemipneustes ocellatus,
Drapier, 290.—Ficheur. Sur la présence de la Terebratula diphya dans
Voxtordien de l’Ouarsenis (Algérie), 291 (409).—H. Nicolas. Les insectes
fossiles d’Aix en Provence du muséum Requien, & Avignon, 291 (424).—
Gauthier. Supplément aux “ Echinides de l’Algérie,”’ 292 (433).—G.
Cotteau. Considérations sur les Echinides éocénes de la France, 292

ADDITIONS TO THE LIBRARY. 163

(449).—Szabo. Les mines d’opale en Hongrie, 292 (436).—Danton.
Sur une preuve scientifique de Porigine ignée de la terre 2983 (455),—
Danton. Notes sur la géologie de louest de la France, 293 (456).—
Collot. Sur la présence du Planorbis erassus au sommet de la pre-
miére série lacustre des Bouches-du-Rhone, 294.—Malaise. Sur les
Oldhamia de Belgique, 294.—J. Bergeron. Sur la présence du genre
Oldhamia dans la Montagne-Noire, 295.—H. Riviere. Faune de la
grotte de la Combe dans les Alpes-Maritimes, 295 (459).—E. F. Hon-
norat-Bastide. Sur une forme nouvelle des Basses-Alpes (Ammonites
Bastide), &c., 295 (462).—Caraven-Cachin. La caverne de Roset (Tarn),
296 (467).—Caraven-Cachin. -Découverte du poudingue de Palassou sur
le versant sud-ouest du Plateau Central, 296 (476).

[Numbers in( __) indicate pages in Part II., Memoirs. |

Paris. Institut de France. Lois, Statuts et Réglements con-
cernant les anciennes Académies et l'Institut de 1635 4 1889.
Par L. Aucoc. 8vo. Paris, 1889.

——. JournaldeConchyliologie. Série 3. Tome xxix. Nos. 2-4,
1889. Purchased.
C. Mayer-Eymar. Description de Coquilles fossiles des Terrains ter-
tiaires supérieurs, 200, 229.

—. ——. ——. Tome xxx. No.1. 1890. Purchased.
—. Journal des Mines. 36° Anné, Nos. 1-52. 1889.
—. —. 37° Année, Nos. 1-25. 1890.

——. Muséum d’Histoire Naturelle. Nouvelles Archives. Série 2.
Tome x. Fase. 2. 1888.

ee Scrie 3.. Tome i. Fase, 1.2... 1889:
——. Revue Scientifique. Tome xliii. Nos. 25-26. 1889.

—. -——. Tomexliv. Nos. 1-26. 1889.
A. Gaudry. Le creusement des Vallées, 359.

——. ——. Tomexlv. Nos. 1-24. 1890.
A. Gaudry. Les enchainements du monde animal dans les temps
secondaires, 257,

——. Société Francaise de Minéralogie. Bulletin. Tome xii.
Nos. 5-9. 1889. Purchased.

G. Kunz. Minéraux intéressants des Etats-Unis, 865.—G. Wyrouboff.
Sur quelques sulfates de la série magnésienne, 866.—H. Dufet. Comptes
rendus des publications étrangéres, 378.—P. Termier. Sur un gisement
de staurotide aux environs de Saint-Htienne (Loire), 395.—Beaugey.
Inclusions d’anhydrite, 396.—G. Wyrouboff. Quelques observations sur
un mémoire de M. Vernadsky, 398.—G. Cesaro. Sur les plans qui peu-
vent, dans les cristaux uniaxes, donner deux rayons réfractés en coinci-
dence, 401.—G. Cesaro. Sur une face de la topaze de Saxe, 419.—E.
Mallard. Sur un siliciure cristallisé de fer et de manganése, 421.—E.
Mallard. Sur les alliages de fer et de chréme, 425,—A. Lacroix. Comptes
rendus des publications étrangéres, 427.—Des Cloizeaux. Note sur le
Mazapilite de Konig, 441.—KH. Jannettaz. Note sur une wernérite

164 ADDITIONS TO THE LIBRARY.

(dipyre) du Chili, 445.—W. Vernadsky. Note sur l’influence de la haute
température sur le disthéne, 447.—L. Bourgeois. Compte rendu de la
visite faite par la Société de Minéralogie a l’Exposition Universelle de
1889, 458.—L. Bourgeois. Essai de reproduction de la barytocalcite,
464.—F. Gonnard. Sur des cristallisations produites autour d’ossements
humains provenant de Solutré, prés de Macon (Sadne-et-Loire), 464.—
H. Dufet. Notices cristallographiques, 466.—A. Lacroix. Nouveau
gisement francais de bertrandite, 514.—A. Lacroix. Gypse artificiel
maclé suivant a 3, 515.—A. Lacroix. Matériaux pour la minéralogie de
la France, 517.—A. Lacroix et C. Baret. Bertrandite, apatite, &c., de
la Loire-Inférieure, 527.—G. Wyrouboff. Nouveaux composés du thal-
lium, 5386.—A. de Schulten. Reproduction de la molybdénite, 545.—J.
Morel. Sur un nouvel hydrate de carbonate de sodium, 546.

Paris. Société Francaise "de Minéralogie. Bulletin. Tome xiii.
Nos. 1-5. 1890. Presented. “

A. Lacroix. Sur l’existence d’une roche a diaspore dans la Haute-
Loire, 7.—A. Lacroix. Sur la forme cristalline de la carphosidérite, 8.
—A. Lacroix. Sur les propriétés optiques de la crocidolite et la diffusion
de ce minéral, 10.—A. Lacroix. Sur les propriétés optiques du titano-
livine, 15.—A. Gorgen. Sur les oxydes de manganése naturels, 21.—
H. Dutet. Extraits de minéralogie, 52.—L. Michel. Recherches sur la
cristallisation du minium et du peroxyde de plomb (plattnérite), 56.—
Beaugey. Calcaire albilifére de Bedous (Basses-Pyrénées), 57.—
Beaugey. Calcaires a cristaux de quartz de Villefranque et de
Biarritz, 59.—E. Mallard. Sur les clivages du quartz, 61.—H. Mallard.
Sur la lussatite, nouvelle variété minérale cristallisée de silice, 63.—
L. Bourgeois. Sur la préparation du nitrate basique de cuivre cristallisé
et sur son identification avec la gerhardtite, 66.—F. Gonnard. Sur les
zéolites du mont Simiouse (Loire), 70.—A. Lacroix. Sur Vorigine du
zircon et du corindon de la Haute-Loire, et sur les enclaves de gneiss et
de granulites des roches voleaniques du Plateau Central, 100.—E. Jan-
nettaz. Sur la turquoise dite de nouvelle roche, 106.—H. Le Chatelier.
Sur la dilation du quartz, 112.—H. Le Chatelier. Sur la polarisation
rotatoire du quartz, 119.—E. Mallard et H. Le Chatelier. Sur la varia-
tion qu éprouvent, avec la température, les biréfringences du quartz, de
la barytine et du disthéne, 125.—C. et G. Friedel. Action des alcalis
sur le mica: production de la néphéline, de l’orthose, de Vamphigéne,
129.—L. Michel. Sur la production artificielle de l’azurite et de la
gerhardtite, 139.—EH. Jannettaz. Note sur une dioptase du Congo fran-
- cais, 159.—E. Mallard. Sur la tridymite et la christobalite, 161.—E.
Mallard. Note sur la mélanophlogite, 180.—C. L. Frossard. Sur le
dipyre et la couseranite des Pyrénées, 187.

—. Société Géologiquede France. Bulletin. Sér.3. Tome xyi.
Less... No. 10; 31389,

De Rouville. Note sur la région paléozoique orientale de ’Hérault au
point de vue de la faune primiére, 848.—Jacquot. Sur le gisement et
la composition du systéme triasique, dans la région pyrénéenne, 850.—
Welsch. Sur des éboulis quaternaires a Hélix des environs d’Alger, 877.
—Welsch. Le terrain pliocene de la Vallée de l’oued-Nador, 881.—
A. Toucas. Note sur le Jurassique supérieur et le Crétacé inférieur de
la vallée du Rhone, 903.—F. Wallerant. Des sphérolites des roches
siliceuses et de leur mode de formation, 927.—J. Bergeron. Réponse au
Dr. Frech de Halle, 935.—V. Raulin. Note pour l’Histoire des Cartes
géologiques, 947.

ADDITIONS TO THE LIBRARY. 165

Paris. Société Géologique de France. Bulletin. Sér. 3. Tome
xvil. 1889. Nos. 1-9. 1889.

Larrazet. Le Steneosaurus de Parmilieu, 8.—L. Landesque. Cal-
caire & Paleotherium de lAgenais et du miocéne supérieur, 24.—H. H.
Sauvage. Note sur les Bryozaires jurassiques de Boulogne, 38.—E.
Fallot. Limite entre l’Oligocéne et le Miocéne dans la Gironde, 53.—
J. Bergeron. Roches éruptives de la Montagne Noire, 54.—Le Mesle.
Jurassique du Zaghouan, 63.—Stanislas Meunier. Réponse a des obser-
vations de M. Augé et de M. A. de Grossouvre sur Vhistoire de la bauxite
et des minerais sidérolithiques, 64.—P. Gourret. Etude géologique du
tertiaire marin de Carry et de Sausset, 68.—Welsch. Sur les différents
pliocénes des environs d’Alger, 125.—P. de Loriol. Note sur deux Echi-
nodermes nouveaux, 150.—G. Cotteau. Note sur un exemplaire du
Coraster Vilanove provenant de Tersakhan (Turkestan), 155.—Stuart-
Menteath. Sur certaines Relations entre la géologie et l’art des mines,
157.—A. Bigot. Le précambrien et le cambrien dans le Pays de Galles
et leurs équivalents dans le massif Breton, 161.—H. E. Sauvage. Note
sur les Ganoides du terrain houiller de Commentry (Aller), 184.—
Rolland. Carte géologique du littoral nord de la Tunisie, 192.—P. de
Rouville et A. Delage. Pétrographie de |’Hérault——Les Porphyrites de
Gabian, 197.—F. Sacco. Le Ligurien, 212.—J. Seunes. Gault coral-
ligéne des Pyrénées, 250.—Bertrand. Plis couchés de la région de
Draguignan, 234.—K. Ficheur. Crétacé moyen et supérieur de la région
d’Ain-Bessem (Alger), 247.—Michel-Lévy et Munier-Chalmas. Etude
sur les environs d’Issoire, 267.—M. Boule. Géologie des environs du
Puy, 270.—A. de Lapparent. Note sur le réle des. agents minérali-
sateurs dans la formation des roches éruptives, 282.—H. Arnaud. Argiles
gypsiferes des Charentes, 290.—Beaugey. Note sur les gites de manga-
nese des Hautes-Pyrénées, 297.—Landesque. Recherches sur le quater-
naire ancien des bassins de la Dordogne et de la Garonne, 301.—C. L.
Frossard. Note sur les terrains éruptifs de Pouzac (Hautes-Pyrénées),
518.—M. Boule. Le Canis megamastoides du pliocéne moyen de Perrier
(Puy-de-Dome), 321.—G. Fabre. Coupe de la montagne de la Tessonne
prés le Vigan (Gard), 331.—E. Ficheur. Note sur les Nummulites de
VP Algérie, 845.—Welsch. Sur un ilot de terrain cristallophyllien au
Nord du Chenoua (Département d’Alger), 361.—Landesque. Quelques
renseignements nouveaux sur les terrains tertiaires des environs de
Beaumont, 364.—L. Carez. Notes sur ‘les couches dites triasiques des
environs de Sougraigne (Aude), 372.—Viguier. Etude sur le pliocéne
de Montpellier, 379.—C. Gorceix. Note sur les fossiles urgo-aptiens des
environs de Bayonne, 424.—D. P. Gthlert. Notes sur les terrains paléo-
zoiques des environs d’Haux-Bonnes, 425.—A. de Grossouvre. Observa-
tions sur la théorie des “ Horst,” 485.—R. Zeiller. Notes sur quelques
empreintes végétales des couches de charbon de la Nouvelle-Calédonie,
443,—K. Ficheur. Deuxiéme note sur les Nummulites de l’ Algérie, 447.
L. Carez. Note sur le crétacé inférieur des environs de Mouriés
(Bouches-du-Rhéne), 466.—Tardy. Dernier diluvium quaternaire en
Aleérie, 470.—De Grossouvre. Sur le terrain crétacé dans le Sud-Ouest
du bassin de Paris, 475.—V. Gauthier. Note sur les Echinides crétacés
recueillis par M. de Grossouvre, 525.—E. Fallot. Note sur la constitu-
tion du terrain crétacé aux environs de Crest (Dréme), 541.—De Lacoivier.
Réponse @ M. Roussel, 549.—H. E. Sauvage. Note sur quelques pois-
sons fossiles de Tunisie, 560.—M. Mieg. Note sur le gypse de Zimmers-
heim (prés Mulhouse), 562.—Bleicher et Fliche. Recherches relatives
a quelques tufs quaternaires du Nord-Est de la France, 566.—R. Zeiller.
Sur les variations de formes du Sigillaria Brardi, Brongniart, 603.—
Marte]. Les eaux souterraines des Causses et la formation des Caiions,

166 ADDITIONS TO THE LIBRARY.

610.—P. Lebesconte. ‘Sur les assises siluriennes les plus anciennes de
Bretagne, 621.—H. Douvillé. Sur quelques Rudistes du terrain crétacé.
inférieur des Pyrénées, 627.—A. de Lapparent. Rapport de la Commis-
sion du Prix Fontannes, 661.—Sayn. Note sur quelques Ammonites
nouvelles ou peu connues du néocomien inférieur, 679.—Beaugey.
Note sur une porphyrite augitique de la Selva de Sallent (Pyrénées
espagnoles), 688.—D. Hollande. Etude stratigraphique des montagnes
jurassiques de Sulens et des Almes, situées au milieu des Alpes calcaires,
690.—Bourgeat. Observations sommaires sur les principales formations
oéologiques du Jura méridional, 718.—Bourgeat. Premiére contribution
a l’étude du calcaire coralligéne de Belledalle dans le Boulonnais, 721.
—J. Welsch. Découverte du jurassique moyen (dogger) sur les hauts
plateaux d’Oran, 723.—A. Toucas. Nouvelles observations sur le juras-
sique supérieur de l’Ardéche, 729.—D. P. Gthlert. Sur le dévonien des |
environs d’Angers, 742.—A. Bigot. Note sur quelques pélécypodes des
erés siluriens de l’Ouest de la France, 791—J. Seunes. Observations sur
le erétacé supérieur des Pyrénées occidentales, 8302.—J. Seunes. HEchi-
nides crétacés des Pyrénées occidentales, 804.—R. Nicklés. Note sur
quelques gisements sénoniens et daniens du Sud-Est de ? Espagne, 824.

Paris. Société Géologique de France. Mémoires. Paléontologie.
Tomei. Fasc. 1. 1890. Purchased.
A. Gaudry. Le Dryopithéque, No. 1.—J. Seunes. Contributions a
Yétude des Céphalopodes du crétacé supérieur de France, No. 2.—C.
Depéret. Les animaux pliocénes du Roussillon, No. 3.

Philadelphia. Academy of Natural Sciences. Proceedings, 1889.
Parts 1-38. 1889-90.

G. A. Koenig. On Anhydrite, 11.—J. Leidy. The Sabre-tooth Tiger
of Florida, 29.—J. Eyerman. Notes on Geology and Mineralogy, 32.—
G. A. Koenig. On Mazapilite, a new mineral species, 45.—F. A. Genth.
On two Minerals from Delaware County, Pa., 50.—J. Leidy. Fossil
Vertebrates from Florida, 96.—J. T. Rothrock. The Sand-Dunes of
Lewes, Del., 184.—E. Goldsmith. Gadolinite from Llano Co., Texas,
164.—J. M. Safford and A. W. Vogdes. Description of new species of
Fossil Crustacea from the Lower Silurian of Tennessee, with remarks on
others not well known, 166.—G. A. Koenig. Chloanthite, Nicolite, De-
Saulesite, Annabergite, Tephrowillemite, Fluorite, and Aquatite from
Franklin, N.J., 184.—W. B. Scott. Notes on the osteology and syste-
matic position of Dinictis felina, Leidy, 211.—C, R. Keyes. Lower-Car-
bonic Gasteropoda from Burlingtcn, Iowa, 284.—C. R. Keyes. The
American Species of Polyphemopsis, 299.—C. R. Keyes. Sphzerodoma:
a genus of fossil gasteropods, 308.—A. Meyer. Notes on the presence of
Umbral or Mountain-limestone in Lycoming Co., Penn., 310.—T. D.
Rand. Notes on the drift on Block Island, 408.

—. American Philosophical Society. Proceedings. Vol. xvi.
No.-08, | 1377-

—. —. ——. Vol. xvii. No. 100. 1877.
—_—. ——. —. Vol. xviti, No. 104. 1879.

= Vol. xxvi. Nos. 129 & 130. 1889.
KE. D. Cope. A review of the North-American Species of Hippothe-
rium, 439,

—

ADDITIONS TO THE LIBRARY. 167

Philadelphia. American Philosophical Society. Transactions. N.S.
Nolhxins (Parts 1&2. 1370.
E. D. Cope. Synopsis of the Extinct Batrachia and Reptilia of North
America, 1.

._ —. ~-——. ——. Vol. xv. Parts 1-3. 1873-1875
& 1881.

B.S. Lyman. Topography of the Punjab Oil Region, 1.—J. J. Ste-
venson. Note on the Geology of West Virginia, 15.—B. S. Lyman.
The Staley’s Creek and Nick’s Creek Iron Ore Region, 33.—W. M. Gabb.
On the Topography and Geology of Santo Domingo, 49.—E. D. Cope.
Supplement to the Extinct Batrachia and Reptilia of North America,
261.—-S. 8. Haldeman. On the Contents of a Rock Retreat in South-
eastern Pennsylvania, 351.

_——. : Vol. xvis,) Bart, 33, 1690.

J.C. Brunner. The Cretaceous and Tertiary Geology of the Sergipe-
Alagéas Basin of Brazil, 369.—G. B. Simpson. Descriptions of New
Species of Fossils from the Clinton, Lower Helderberg, Chemung, and
Waverly Groups, found in the Collections of the Geological Survey of
Pennsylvania, 435.—W. B. Scott and H. F. Osborn. The Mammalia of
the Uinta Formation, 461.

Subject Register of Papers Published in the Trans-
actions ~and Proceedings, compiled by Henry Phillips, Jun.
8vo. 1889.

—_ OO

Supplement, 1881-89. 1889.

: Report of the Committee appointed to assist the
Commission on Amended Orthography, created by virtue of a
Resolution of the Legislature of Pennsylvania. 8vo. 1889.

——. Wagner Free Institute of Science. Transactions. Vol. ii.
1889.

J. Leidy. Notice of some Fossil Human Bones, 9.—J. Leidy. De-
scription of Mammalian Remains from a Rock Crevice in Florida, 18.—
J. Leidy. On Platygonus, an extinct genus allied to the Peccaries, 41.—
J. Leidy. Remarks on the Nature of Organic Species, 51.

Photographic Society of Great Britain. Journal and Transactions.
N.S. Vol. xiii. No.9. 1889.

—. ——. ——. Vol. xiv. Nos. 1-8. 1889-90.

Physical Society of London. Proceedings. Vol. x. Parts 2 & 3.
1889 and 1890.

Pisa. Societa Toscana diScienze Naturali. Atti. Processi Verbali.
Wolavin (1889. Pp. 211-302. 1889;
L. Busatti. Sulla sabbia silicea di Tripalle, presso Fauglia, in pro-
vincia di Pisa, 220.—G. A. De Amicis. Altri calcari ad Ellipsactinie
nella provincia di Salerno, 238.

—_——_

: 5 ; Vol. vii. Pp. 1-80. 1890.

G. Ristori. Un nuovo Crostaceo fossile del Giappone, 4.—G. Ristori.

Ancora sui depositi quaternari del Casentino, 6.—A. De Gregorio. In-

torno all’opuscolo del sig. dott. Gioli sui fossili di 8. Vigilio, 54.—G.
VOL. XLVI. n

168 ADDITIONS TO THE LIBRARY.

Gioli. Sopra alcuni resti di Rhinoceros etruscus, Falc., rinvenuti a Prata,
presso Massa Marittima, 56.—C. J. Forsyth Major. L’Ossario di Olivola
in Val di Magra (Provincia di Massa Carrara), 57.

Pisa. Societa Toscana di Scienze Naturali. Atti. Memorie.
Volix. 1889:

G. Gioli. Fossile della oolite inferiore di 8S. Vigilio e di monte
Grappa &c., 8.—L. Busatti. Sulla lherzolite di Rocca di Sillano (Monte
Castelli) e Rosignano (Monti livornesi), 110.—G. Gioli. Briozoi neo-
genici dell’ isola di Pianosa, nel mar Tirreno, 251.

Plymouth. Devonshire Association for the Advancement of Science,
Literature, and Art. Report and Transactions. Vol. xxi.
1889.

W.H. Hudleston. Presidential Address, 25.—A. R. Hunt. On the
Age of the Granites of Dartmoor and the English Channel, 238.—R. N.
Worth. Geological Notes on the South-western line between Lydford
and Devonport, 261.—W. A. E. Ussher. The Devonian of the Western
Region, and Geology of Tavistock, 437.—A. R. Hunt. Notes on the
oe Geology of the English Channel off the Coast of South Devon,

61.

—. —. —. The Devonshire Domesday. Part vi. 1889.

Plymouth Institution. Annual Report and Transactions.
Vol. x. Part 2 (1888-89). 1889.
R. N. Worth. The Dartmoor Volcano, 146.

Vol. x. Part 3 (1889-90). 1890.

Quekett Microscopical Club. Journal. Ser. 2. Vol. iv. Nos. 25-
26. 1889-90.

Red Hill. Holmesdale Natural-History Club, Reigate. Proceed-
ings for 1879 and1880. 1881? Presented by W. Whitaker,
Esq., FBS.

W. Gilford. The Geology of this district, especially in reference to
the question of the Water-supply, 17.—R. C. Baxter. The Sub-Wealden
Gypsum Company’s works at Mountfield, Sussex, 19—W. H. Tyndall.
The Rivers of Surrey, 56.

Research. Vol. ii. Nos. 13-24. 1889-90.

J.S. Hyland. Granite from a Geological and Economic Standpoint,
2, 26.—O. W. Jeffs. Geological Photography, 7.—W. Hewitt. The
Evolution of the Grand Cation of the Colorado, 11, 37, 50.—Geological
Photography, 27,—Earthquake in Manila, 65.—S, A. Adamson. Scien-
tific Aspects of Health Resorts—Scarborough and District, 52; Brid-
lineton and District, 80; Whitby and District, 102; Saltburn and Dis-
trict, 148.—C. Carus-Wilson. Scientific Aspects of Health Resorts —
Bournemouth, 122.—H. E. Quilter. The Life-zones of the British Lias,
97.—W.Semmons. The Recent-additions Case at the British Museum,
126.—O. W. Jeffs. Provisional List of Geological Photographs, 139.—
A. G. Nathorst. Do the Poles Change their Position P 172.—C. Carus-
Wilson. The Rounding and Isolation of Rock-masses, 185.—Coal in
Cheshire, 217.—McPherson. Fossils and Evolution, 221.—O. W. Jeffs.
A Relic of an old Eruption, 224.—E, M. Cole. Coast Erosion in York-
shire, 225.—Geological Sections on the Manchester Ship-canal, 232.—
T. Ward. Notes on the Salt Districts of North America, 241, 272.—
W.Semmons. Minerals at the Paris Exhibition of 1889, 244.

ADDITIONS TO THE LIBRARY. 169

Rome. Reale Accademia dei Lincei. Atti. Serie 4. Rendiconti.
Vol.v. Fasc. 5-13. 1° Semestre. 1889.
P. Tacchini. Sulle attuali eruzioni di Vulcano e Stromboli, 327.—F.
Keller. Contributo allo studio delle rocce magnetiche dei dintorni di
Roma, 519.

—. . —. ——. ——. Vol.v. Fase. 1-13. 2° Se-
mestre. 1889.

G. Struever. Contribuzioni alla mineralogia della Valle Vigezza, 183.
—G. Capellini. Gli antichi confini del Golfo di Spezia, 185.

—. _ —. ——. —. Vol. vi. Fasc. 1-12. 1° Se-
mestre. 1890. ;

G. Struever. Sulla brookite di Beura nell’ Ossola, 77.—G. Capellini.
Di un Ittiosaure e di altri importanti fossili cretacei nelle argille sca-
gliose dell’ Emilia, 79.—G. Agamennone. Registratore di terremoti a
doppia velocita, 788.

: ; : Memorie. Vol. ii. 1886.

T. Taramelli e G. Mercalli. I terremoti Andalusi, cominciati il 25
dicembre 1884, 116.—G. Ponzie R. Meli. Molluschi fossili del Monte
Mario, presso Roma, 672.

—-. 5 , : . -Vol.iv. 1887.

E. Artini. Natrolite della Regione Veneta, 76.—H. Artini. Contri-
buzioni alla Mineralogia del Vicentino, 90.—G. Struever. Ulteriori os-
servazioni sui giacimenti minerali di Val d’Ala in Piemonte, 101.—E.
Artini. Epidoto dell’ Elba, 880.—A. Sella. Sulla Sellaite e sui minerali
che ’accompagnano, 455.

——. R. Comitato Geologico d’ Italia. Bollettino. 1889. Vol.

xx. 1839.

VY. Simonelli. Appunti geologici sull’ isola di Giannutri (Arcipelago
toscano), 10.—P. Moderni. la trachite e il tufo di Rispampani, presso
Toscanella, 19.—G. Steinmann. Sulla eta del calcare appenninico di
Capri, 25.—C. Klein. Analisi petrografica di.una serie di roccie dei
dintorni del lago di Bolsena, 32.—G. Di Stefano. I Pliocene ed il Post-
pliocene di Sciacca, 69.—R. Travaglia. Contributo agli studj sulla genesi
dei giacimenti di solfo, 11O—HEH. Niccoli. la frana di Casola Valsenio,
nel circondario di Faenza, 118.—A. Portis. Nuove localita fossilifere in
Val di Susa, 141.—D. Pantanelli. Tufi serpentinosi eocenice nell’ Emilia,
184.—V. Simonelli. Terreni e fossili dell’ isola di Pianosa, nel Mar
Tirreno, 193.—F. Sacco. La conca terziaria di Varzi-S. Sebastiano, 257.
—C. De Stefani. Il lago pliocenico e le ligniti di Barga nella valle del
Serchio, 278, 329.—A. Piatti. La sorgente termo-solforosa di Sermione,
sul lago di Garda, 288.—A. Portis. Studio sopra alcuni gimnodonti
fossili italiani, 352.

——. Societa Geologica Italiana. Bollettino. Vol. viii. 1889.
Base. 1. 1889,
F. Sacco. I colli Monregalesi, 59.—G. Tuccimei. I] Villafranchiano
nelle valli Sabine ei suoi fossili caratteristici, 95.—A. Neviani. Contvri-
buzioni alla geologia del Catanzarese, 133. Mey

‘ : Vol. ya. US8so. J hasc..3, “1890!

G, Capellini. Sul giacimento di vertebrati fossili a Olivola, nelle Alpi
apuane, 271.—G. Capellini. Sulla scoperta di una caverna ossifera a
nm 2

17o ADDITIONS TO THE LIBRARY.

monte Cucco, 274.—L. Mazzuoli. Rettifica di una citazione fatta dal
Sig. C. De Stefani, 279.—F. Sacco. Catalogo paleontologico del bacino
terziario del Piemonte, 281.—A. Verri. Note a scritti sul pliocene um--
brosabina e sul vulcanismo tirreno, 357.—A. Neviani. Coutribuzioni
alla geologia del Catanzarese, 489.—G. Ristori. I] bacino pliocenico del
Mugello, 455.—R. Meli. Sopra i resti fossili di un grande avvoltoio
(gyps) racchiuso nei peperini laziali, 490.—Adunanza generale della
Societa geologica italiana tenuta in Catanzaro, 545.

Royal Agricultural Society of England. Journal. Series 2. Vol. xxv.
Part: 2:. No..o0. 1839:

——, : . Seriesyd..¢, Vol. 1. Patt 1. so;

W.H. Flower. The Evolution of the Horse, 110.

Royal College of Physicians. List of Fellows, Members, Extra-
Licentiates, Licentiates, &c. 1890.

Royal College of Surgeons of England. Calendar, 1889.

Royal Colonial Institute. Proceedings. Vol.xviii. 1886-7. 1887.
Presented by Prof. T. Rupert Jones, F.BRS., F.GS,
T. Rupert Jones. The Mineral Wealth of South Africa, 217.

Royal Geographical Society. Proceedings. Vol. xi. Nos. 7-12.
1889.

: Vol. xu. Nos: 1-6. 1890.

M.S. Bell. The Great Central Asian Trade Route from Peking to
Kashgaria, 57.—J. J. Lister. A Visit to the newly emerged Falcon
Island, Tonga Group, South Pacific, 157.—D. W. Freshfield. Search
and travel in the Caucasus, 257.—Dr. H. Meyer. Ascent to the summit
of Kilma-njaro, 331.

Royal Institution of Great Britain. Proceedings. Vol. xii. Part3.
No, 83. , 1889.
A. Geikie. Recent Researches into the Origin and Age of the High-
lands of Scotland and the West of Ireland, 528.

Royal Meteorological Society. Quarterly Journal. Vol. xv. Nos. 71-
Aes, LOOe:

ES ce STB OOM iT Moliexvien Nos. (arg 740.1890:

Royal Microscopical Society. Journal. 1889. Parts4-6a. 1889.

C. Davies Sherborn and F. Chapman. Additional Note on the Fora-
minifera of the London Clay exposed in the Drainage Works, Piccadilly,
London, in 1885, 483.

——, — ——, 1690,) Pagel oe leon:

Royal Society. Proceedings. Vol. xlvi. Nos. 280-285. 1889-90.

HK. Hull. On a possible Geological Origin of Terrestrial Magnetism,
92.—S. Allport and T.G. Bonney. Report on the Effect of Contact
Metamorphism exhibited by the Silurian Rocks near the Town of New
Galloway, in the Southern Uplands of Scotland, 193.—F. Clowes.
Barium Sulphate as a Cement in Sandstone, 863.—F. Clowes. Deposits
of Barium Sulphate from Mine-water, 368.

ae, § Hs, Nolxlvii./) Nosa2ep-2ss... 1890:

ADDITIONS TO THE LIBRARY. EFL

Royal Society, see Booxs. Lendenfeld, R. v.

Rugby School Natural-History Society. Report for 1889. 1890.
W.H. Draper. The Eruption of Krakatoa, in Aug, 1883, 39.

St. Petersburg. Académie Impériale des Sciences. Mémoires.
Sér. 7. Tome xxxvi. Nos. 14-17. 1889.

J. V. Rohon. Die Dendrodonten des devonischen Systems in Russ-

land, No. 14.F. Brauer, J. Redtenbacher und L. Ganglbauer. Fossil
Insekten aus der Juraformation Ost-Sibiriens, No. 15.

—-. é 5 . Tomexxxvii. Nos. 1-7. 1889-90.
A. Karpinsky. Ueber die Ammoneen der Artinskstufe und einige mit
denselben verwandte Carbonische Formen, 1.—Baron E. vy. Toll. Die
palaozoischen Versteinerungen der Neusibirischen Insel Kotelny, No. 3.
—J.Schmalhausen. Tertiare Pflanzen der Insel Neusibirien, mit einer
Einleitung von Baron E. von Toll, No. 5. |

Saint John, N.B. Natural-History Society of New Brunswick.
Bulletin. No. 8. 1889.

San Francisco. California Academy of Sciences. Proceedings.
Series 2. Vol.1. Parts1&2. 1888 & 1889.
W. Lindgren. Contributions to the Mineralogy of the Pacific Coast,
1—J. G. Cooper. West-Coast Pulmonata; Fossil and Living, 11.—
W. Lindgren. Geology of Baja California, 173.

Santiago. Deutsche wissenschaftliche Verein. Verhandlungen.
Bandu. Heftl. 1889.

K. Stolp. Meteorischer Staub, gesammelt auf den Cordilleren Chiles,
und Beobachtung einer Feuerkugel im Lichtscheine des westlichen Him-
mels im Jahre 1883, 42.—H. Schulze. Mineralogisches aus Tarapacé,
49.

Shanghai. China Branch of the Royal Asiatic Society. Journal.
N.S. Vol. xxii. Nos. 2-3. 1888-89,

Society of Amateur Geologists. Proceedings. Vol. i. No.5. 1890.

T. Leighton. On some Polymorphic Species of Mollusea and their
bearing upon geological inquiry, 69.—R. McAllan. A Geological Trip to
Dublin, 72.—G. 8. Boulger. The Methods of Geological Study and In-
struction, and the educational value of geology, 75.

Society of Arts. Journal, Nos. 1886-1936. 1889.

: . Nos. 1937-1961. 1890.
W. Whitaker. Coal in the South-east of England, 548.

Society of Biblical Archeology. Proceedings. Vol. xi. 1889.
——. ——. Vol. xi. Parts 1-4. 1889-90.

Society of Public Analysts, see Anatysr.

Stettin. Vereins fiir Erdkunde. Jahresbericht. 1888-89. 1889.
E. Wisotski. Hauptfluss und Nebenfluss, 1. ;

172 ADDITIONS TO THE LIBRARY.

Stockholm. Geologiska Foreningens i Stockholm. Forhandlingar.
Bandet xi. Hifte 5-7. 1889. ro
O. Gumeelius. Meddelanden fran Kantorp, 248.—A.G. Hégbom. Om
relationen mellan kalcium- och magnesiumkarbonat i de qvartiira afla-
eringarna, 263.—H. Munthe. Jakttagelser Ofver qvartira aflagringar pa
Bornholm, 274.—S. L. Tornqvist. Nagra anmarkningar om vestra Huro-
pas kambriska och siluriska korologi, 299.—P. W. Strandmark. Ytter-
ligare om jiikelelfvar och rullstensasar, 340.—M. Stolpe. Om orsakerna
till rullstensésars uppkomst, 369.—C. W. Blomstrand. Om nagra
svenska monaziter, 3/9.—L. J. Igelstr6m. Mineralogiska meddelanden,
x., 889.—A. af Schultén. Om framstallning af konstgjord molybden-
glans, 401.—A. G. Nathorst. Naturfenomen iakttaget den 15 augusti
1889 i Loftahammars socken, Kalmar lin, 405.—E. Svedmark. Bergs-
handteringen i Sverige ar 1888, 407.—E. Svedmark. Meddelanden om
jordstotar i Sverige, 417.—C. A. Hansson. Om nagra “hacklor” eller
“lerhorn” fran norra Bohuslan, 425.

: : Bandet xii. Hafte 1-4. 1890.

O. Widman. Mineralanalytiska meddelanden fran Upsala kemiska
laboratorium, 20.—A. G. Nathorst. Linnés iakttagelser 6fver strand-
linier vid gransen mellan Sverige och Norge, 80.—G. De Geer. Om
Skandinaviens nivaéforandringar und qvartarperiod, 61.—E. Svedmark.
Meteorer iakttagna inom Sverige ar 1889, 111.—L. J. Igelstrém. Mine-
ralogiska meddelanden, 1i., 157.—E. Svedmark. Meteoren den 23 No-
vember, 1889, 140.—A.G. Nathorst. Nagra reffelobservationer i trakten
af Omberg, 141.—G. Lofstrand. Om apatitens forekomstsatt i Norr-
bottens lan jemfordt med dess upptridande i Norge, 145.—G. Lofstrand.
Um apatitens forekomstsitt i Norrbottens lan jemfordt med dess upptra-
dande i Norge, 207.—H. Backstrom. Om “kvartskakelagrena” vid
Gud&, Norge, 209.—T. Thoroddsen. Nogle Bemzrkninger om de is-
landske Findesteder for Dobbelspath, 247.—E. Mortsell. Resenotiser
fran det fossilforande kambrisk-siluriska omradet af Vesterbottens Lapp-
mark, 255.—G. Holm. Forsteningar fran Lappland, 259.—G. Holm.
Om forekomsten af en Caryocrinus i Sverige, 268.—T. Hedlund. Me-
teoren den 29 November, 1889, 270.—V. Petersson. Studier 6fver gado-
linit, 275.—G. Nordenskidld. Om mineral frin drushél vid Taberg i
Vermland, 348.

: . ——. Generalregister till Bandet vix. 1882-88.
(Svo.) 1890.

——. Kong]. Svenska Vetenskaps-Akademien. Bihang till Hand-
lingar. Bandet 9. Hifte1]&2. 1884.

J. H. Vogt. Studier over Slagger, No. 1.—A. G. Nathorst. Redo-
gérelse for den tillsammans med G. De Geer ar 1882 fretagna geologiska
expedition till Spetsbergen, No. 2.—A. G. Nathorst. Bemerkungen tiber
Herrn y. Ettingshausen aufsatz “Zur Tertiarflora Japans,” No. 18.

d ; Bandet 10. Hifte1&2. 1885.
F. Hichstadt. Ueber die kristallographischen Constanten des Gado-
linits, No. 18.

: , Bandet 11. Hiafte1 & 2. 1886-87.

B. Lundgren. On an Inoceramus from Queensland, No. 5—G. Holm.
Om Vettern och Visingsé-formationen, No. 7.—F. Hichstidt. Pyroxen
och amfibolforande bergarter fran mellersta och dstra Smaland, No. 14.

—. —. —. Bandet 12. Afdelningi. 1886.

ADDITIONS TO THE LIBRARY. 173

Stockholm. Kongl. Svenska Vetenskaps-Akademien. Bihang till
Handlingar. Bandet 12. Afdelning ii. 1887.

W. Ramsay. Om turmalinens hanforande till den romboédrisktetar-
toédriska formgruppen af det hexagonala systemet, No. 1.—G. Flink.
Mineralogiska notiser, I., No. 2.—W. Ramsay. Methode zur Bestim-
mung der Brechungsexponenten in Prismen mit grossen Winkeln, No. 4.
—C. W. Blomstrand. Om de zirconiumhattiga silikatens kemiska byge-
nad, No. 9.—C. W. Blomstrand. Om dens. k. Cyrtolithen fran Ytterby,
No. 10.

—. —. ——. Bandet 12. Afdelning ii. 1887.

: : .. Bandet 12. Afdelning iv. 1887.

J.C. Moberg. Iakttagelser fran en med understéd af allmanna medel
sommaren 1885 foretagen geoliska resa till Irland, Norra Frankrike,
Holland och Westphalen, No. 2.

——. —~-. ——. Bandet 13. Afdelningi. 1888.

5 : Bandet 18. Afdelning ii. 1888.
A. Hamberg. Natiirliche Corrosionserscheinungen und neue Krystall-
flachen am Adular vom Schwarzenstein, No. 4.—H. Backstrom. Krystal-
lografisk nndersékning af tvé nya Kolvaten, No. 5.—W. Ramsay. Om
tetartoedri hos turmalin, No. 6.—G. Flink. Mineralogiska notiser, IL.,
No. 7.—G. Flink. Ueber die Krystallform und Zwillingsbildung des
Skolecit von Island, No. 8.

—. . ——. Bandet 13. Afdelning ii. 1888.
A.G. Nathorst. Om de fruktformer af Trapa natans, L., som fordom
fumits 1 Sverige, No. 10.

ee eee

—_- ——

Bandet 13. Afdelning iv. 1888.

B. Lundgren. Anmiarkningar om permfossil fran Spetsbergen, No. 1.

: . Handlingar. Ny Foljd. Bandet20. Hafte 1 & 2.
1882-83. 1882-84.
A. G. Nathorst. Contributions 4 la flore fossile du Japon, No, 2.—E.

Ray Lankester. Report on fragments of Fossil Fishes from the Palszo-
zoic strata of Spitzbergen, No. 9.

—EEEE

85. 1884-87.
H. y. Dunikowski. Ueber Permo-Carbon Schwamme von Spitzbergen,
No. 1.—T. Torell and G. Lindstrém. On a Silurian Scorpion from Got-
land, No. 9.—A. G. Nathorst. Nouvelles observations sur les traces

d’animaux et autres phénoménes d'origine purement mécanique décrits
comme ‘ Aloues fossiles,” No. 14.

—. Bandet 21. Haftel & 2. 1884-

eee

1887,

SS . Oversigt. Bandet 41. 1884. 1885.

W.C. Brogger och G. Flink. Om Kristaller af Beryllum och Vanadium,
No. 2, 65.—C. Morton. Stephanit fran Kongsberg, 99.—J. Lorenzen.
Undersgelse af nogle Mineralier fra Kangerdluarsuk, No. 2, 105.—A. Sj6-
gren. Allaktit ett nytt mineral fran Nordmarks grufvor, No. 3, 29.—K.
Fristedt. Om en fossil spongia, No. 4,55.—L. I. Igelstrém. Aimatolit
och Aimafibrit, tvenne nya mineral fran Nordmarks jerngrufyor i Verm-

—. —. Fol. Atlas to Bandet 21. No. 8.

174 ADDITIONS TO THE LIBRARY,

land, No. 4, 85.—L. I. Igelstrom. Manganostibiit, ett nytt mineral fran
Nordmarks grufvor i Vermland, No, 4, 89.—J. Lorenzen. Rodtarsenik-.
minera (Aimatolit) fra Nordmarken, No. 4,95.—J. Lorenzen. To petro-
orafiske notitser, No. 5, 187.—L. I. Igelstrom. Xanthoarsenit, ett nytt
mineral fran Sjogrufvan i Grythytte socken, Orebro lin, No. 7, 99.—A.
Sjogren. Nya Arseniater fran Mossgrufvan 4 Nordmarksfiltet, No. 8, 3.
—C. Morton. Nagra goniometriska bestamningar 4 Kalkspat frin Aren-
dal, Kongsberg, Utd och Bamle, No. 8, 65.—M. Weibull. Mineralfore-
komsten vid Vestra Silfberg, No. 9, 11.

Stockholm. Kongl. Svenska Vetenskaps-Akademien. Oversigt.
Bandet xli. 1885. 1886.

M. Weibull. Om Olivingruppens mineral, No. 2, 3.—G. Holm. | For-
teckning pa Meteoriter i Upsala Universitets mineralogiska samlingar,
No. 2, 23.—G. Lindstrom. Forteckning pa Gotlands Siluriska Crustaceer,
No. 6, 387.—L. I. Igelstrom. Polyarsenit, ett. nytt mineral fran Sjogruf-
van, Grythytte socken, Orebro lin, No. 7, 257.—P. E. W. Oberg. Bidrag
till kannedom af nagra mineraliers specifia varme, No. 8, 43.—A. G.
Nathorst. Om kambriska pyramidalstenar, No. 10, 5.

Bandet xlii. 1886. 1887.

A. E. Tornebohm. Nagra ord om den geologiska dfversigtskarstan
éfver Sverige, 79.—A. G. Nathorst. Om de sandslipade stenarnes fore-
komst i de kambriska lagren vid Lugnas, 185.—A.G. Nathorst. Om
lemmingar af Dryas octopetala, L., 1 kalktuff vid Rangiltorp nara Vad-
stena, 229.

; : Bandet xliv. 1887. 1888. |
A. Sjogren. Allaktit frin Langbans grufvor, 107.—G. Kriiss och L. F.
Nilson. Om jordarterna och niobsyran i Fergusonit, 267.—G. Kriss och
L. F. Nilson. Studier 6fver sallsynta jordarters absorptionsspektra och
komponenter, 361.--O. Torell. Undersékningar ofver istiden, 429.—A.
E. Nordenskiéld. Ytterligare iakttagelser om Gadolinitjordens atomviet,
463.—A. Sjogren. Periklas vid Nordmarks grufvor, 479.—G. Lindstrom.
Om hyalotepit fran Langban, 589.—E. Svedmark. Till fragan om be-
stamningen af plagioklasens natur i gabbro fran Radmanso, 621.—H.
Munthe. Om postglaciala aflagringar med Ancylus fluviatilis pa Got-

land, 719.

; : Bandet xlv. 1888. 1889.

A. G. Nathorst. Sur de nouvelles remarques de M. Lebesconte con-
cernant les Cruziana, 3.—A. Sjogren och C, H. Lundstrom. -Om Barysil,
ett ej forr uppmirksammadt blysilikat fran Harstigsgrufvan, 7H}.
Sjégren. Om aralokaspiska hafvet och nordeuropiska glaciationen, 155,
—W. Petersson. Analyser af gadolinit och homilit, 179.—B. Lundgren.
Om Sveriges Kritfauna. Nagra anteckningar, 225.—A. G. Nathorst,
Om Kristalliseradt bly fran Harstigsgrufvan vid Pajsberg i Varmland,
. 483.—W. C., Brogger und Helge Backstrom. Ueber den “ Dahllit,” ein
neues Mineral von Odegarden, Bamle, Norwegen, 493.—A. HE. Norden-
skidld. Om ett den 5 och 6 Februari, 1886, 1 Schlesien, Mahren och
Ungern med sn6 nedfallet stoft, 497.—A. Sjogren. Om ett nytt mineral
frin Mossgrufvan i Nordmarken, 561.—G. Flink. Mineralogische No-
tizen, 571.

Forteckning 6fver innehallet . . .. Skrifter 1826-83.
8vo. 1884.

——, ——. lLefnadsteckningar. Bandet 2. Hafte 3. 1885.

ADDITIONS TO THE LIBRARY. 175

Stuttgart. Neues Jahrbuch fiir Mineralogie, Geologie und Palion-
tologie. 1889. Bandu. Hefte]1 &2. 1889.

L. Darapsky. Der Atacamit in Chile, 1—O. Jakel. Ueber einen
Ceratiten aus dem Schaumkalk von Riidersdorf und ueber gewisse als
Haftring gedeutete Hindriicke bei Cephalopoden, 19.—L. J. Igelstrom.
Gediegen Blei in der Mangan- und Eisenerzgrube “Sjégrufvan” in den
Kirchspiele Grythyttan, Gouvernement Orebro, Schweden, 32.—L. J.
Igelstrom. Anthochroit, ein neues Mineral von der Braunitgrube bei
Jakobsberg, Gouvernement Wermland, Schweden, 36.—L. J. Igelstrom.
Pleonektit, ein neue Mineral von der Hausmannit- und Braunitgrube
“ Sjogrufvan,” Kirchspiele Grythyttan, Gouvernement Orebro, Schweden,
40.—M. Neumayr. Calostylis und,die perforaten Hexacorallier, 44.—P.
und F. Sarasin. Ueber die Anatomie der Echinothuriden und die Phylo-
genie der Echinodermen, 54.—H. Trautschold. Ueber den russischen
Jura, 60.—W. Bruhns. Beitrage zur Mineralsynthese, 62.—J. Petersen.
Darstellung der Geisererscheinungen, 65.—B. Lundgren. Wirbelthier-
Funde im Saltholmskalk, 73.—Gurich. Beziehungen des Tafelbergsand-
steins zu den Homalonotus-fuhrenden Bockeveldschichten der Capcolonie,
Sudafrika, 73.—H. Rosenbusch. Zur Auffassung des Grundgebirges, 81.
—QO. Mugge. Ueber durch Druck entstandene Zwillinge von Titanit nach
den Kanten [110] und [110], 98.—S. Nikitin. Einige Bemerkungen tber
die Jura-Ablagerungen des Himalaya und Mittelasiens, 116.—A. Roth-
pletz. Nachtragliches zu der geologisch-palaeontologischen Monographie
der Vilser Alpen, 146.—A. B. Meyer. Nephrit in Schlesien schon zu
Linné’s Zeit bekannt, 147.—F. Maurer. Palaeontologische Studien im
Gebiet des rheinischen Devon, 149.—F. v. Sandberger. Ein neuer Mete-
orit aus Chile,173.—R. Fuess. Ueber eine Orientirungsvorrichtung zum
Schneiden und Schleifen yon Mineralien nach bestimmten Richtungen,
181.—J. W. Retgers. Ueber schwere Flissigkeiten zur Trennung von
Mineralien, 185.—H. Traube. Bemerkungen zu der Mittheilung des
Herrn A. B. Meyer, 193.—H. B. Geinitz. Petrefactenfunde im Rothlie-
genden, 193.—H. Credner, EK. Geinitz, und F. Wahnschaffe. Ueber das
Alter des Torflagers von Lauenburg an der Elbe, 194.

1890. Bandi. Hefte 1-3. 1890.

M. Neumayr. Ueber neuere Versteinerungsfunde auf Madagascar, 1.
—M. Bauer. Beitriige zur Mineralogie. VI. Reihe, 10.—L. Darapsky.
Ueber einige Mineralien aus Atacama, 49.—A. Cathrein. Zur Diinn-
schliffsammlung der Tyroler Eruptivgesteine, 71.--G. Greim. Die plei-
stocanen Schichten bei Raunheim in Hessen, 82.—M. Neumayr. Ueber
Palaechinus, Typhlechinus, und die Echinothuriden, 84.—A. Kenngott.
Ueber Pyrophysalith vom Fimbo, Augit von Risoe, und Martit von
Ypanema, 87.—A. Rothpletz. Ueber Gerdlle mit Kindriicken, 92.—A.
Agassiz. Ueber einen neuen Tiefsee-Crinoiden aus der Familie der
Apiocriniden, 94.—P. Oppenheim. Ueber die Jurafauna von Visciano
bei Nola in Campanien, 95.—R. Brauns. Ueber die Entstehung der sog.
Rutschflachen im bunten Sandstein der Umgebung von Marburg, 97.—F
Klockmann. E.8. Padmore’s Bilder aus den Oberharzer Gruben, 98.—
F. vy. Sandberger. Arsenikkies und andere Mineralien von Goldkronach
....Neusorg bei Markt Redwitz .... Winnweiler (Pfalz).... Fulda
...+ Coburg, 99.—H. Eck. Zur Gliederung des unteren Muschelkalks
am Odenwalde, 102.—G. Giirich. Geologisch-mineralogische Mittheil-
ungen aus Sudwest-Afrika, 103.—G. Doelter. Ueber die kiinstliche
Darstellung und die chemische Constitution einiger Zeolithe, 118.—M.
Neumayr. Kritische Bemerkung tiber die Verbreitung des Jura, 140.—
R. Fuess. Ein neuer Erhitzungsapparat fiir das Reflexionsgoniometer,
161.—A. Penck. Ueber Durchbruchthaler, 165.—E. Hussak. Ueber

a ae

OO OTL eC TC OOOO

176 ADDITIONS TO THE LIBRARY.

Leucit-Pseudokrystalle im Phonolit (Tinguait) der Serra der Tingua,
Estado Rio de Janeiro, Brazil, 166.—J. vy. Siemiradzki. Kritische Be-.
merkungen iiber neue oder wenigbekannte Ammoniten aus dem Braunen
Jura von Popielany in Lithauen, 169.—F. vy. Sandberger. Synonymie
einiger devonischen Versteinerungen, 183.—A. G. Nathorst. Ueber die
Entdeckung des alteren baltischen Hisstroms, 184.—H. Traube. Ueber
pleochroitische Hofe im Turmalin, 186.—S. Nikitin. Ueber Parabelknoten
bei den Ammoniten, 188.—F. Kinkelin. Das Alluvium (Altalluvium)
oder Pliocin in der Raunheimer Schlusse, 190.—J. E. Wolff. Ueber
Theralit, 192.—F. Rinne. Ueber optische Eigenschaften des Eisenglim-
mer, 193.—H. Traube. Untersuchungen an den Syeniten und Hornblende-
schiefern zwischen Glatz und Reichenstein in Niederschlesien, 195.—E.
Fedorow. Gonoedrische demonstrative Apparate in Anwendung auf die
Krystallographie, 234.—L. J. Igelstr6m. Mineralogische Mittheilungen
aus Schweden, 249.—F. Toula. Zur Kenntniss der Krystallinischen
Gesteine des centralen Balkan, 263.—F. v. Sandberger. Ein merkwur-
diges Gerdll aus dem pleistocanen Sande von Mosbach bei Wiesbaden,
273.—F. Toula. Geologische Untersuchungen im 6stlichen Balkan, 273.
—G. Gurich.—Zur Altersbestimmung der unteren Grenze der Karoo-
formation, 283.—H. Traube. Pyrargyrit von Kajinel in Siebenburgen,
286.—A. von Koenen. Ueber die sogenannten Rutschflachen in Buntsand-
stein der Umgebung von Marburg, 289.

Stuttgart. Neues Jahrbuch fiir Mineralogie, Geologie und Palion-

tologie. Beilage-Band vi. Heft 2&3. 1889.

L. Teisseyre. Ueber Proplanulites, nov. gen., 148.—W. Deecke. Be-
merkungen zur Entstehungsgeschichte und Gesteinskunde der Monti
Cimini, 205.—E. Koken. Ueber die Entwickelung der Gastropoden von
Cambrium [ste] bis zur Trias, 805.—E. Goller. Die Lamprophyrgange
des siidlichen Vorspessart, 485.—L. Teisseyre. Ueber die systematische
Bedeutung der sog. Parabeln der Perisphincten, 570.

: Beilage-Band vi. Heft 1. 1890.

J. Martin. Beitraige zur Kenntniss der optischen Anomalien einaxiger
Krystalle, 1.—R. Fuess. Ueber Mikroskope fur krystailographische und
petrographische Untersuchungen, 55.—P. Dahms. Ueber einige Eruptiv-
gesteine aus Transvaal in Stid-Afrika, 90.

Paleontographica. Band xxxvi. Lief. 1-6. 1889. Pur-
chased.

E. Fraas. Die Labyrinthodonten der schwabischen Trias, 1.—M. Yo-
koyama. Versteinerungen aus der japanischen Kreide, 159,.—B. Sturtz.
Neuer Beitrag zur Kenntniss palaeozoischer Seesterne, 203.

—

——., Verein fiir vaterlindische Naturkunde in Wiirttemberg.
Jahreshefte. Jahrgang xlvi. 1890.

O. Fraas. Ueber den Basalt des Eisenriittels,82.—Engel]. Palaeonto-
logische Funde aus dem Lias 6 des Filsbetts bei Hislingen, 84.—Nies.
Zur Erdbebenfrage, 74.—O. Spohn. Der Stiftsberg bei Heilbronn, 106.
—F. Knickenberg. Die Nordgrenze des ehemaligen Rheingletschers, 109,
—A.Leuze. Beitrige zur Mineralogie Wiurttembergs, 181.—A. Schmidt.
Untersuchungen iiber zwei neuere Erdbeben, das schweizerische vom
7 Januar 1889 und das nordamerikanische vom 51 August 1886, 200.

Swansea. South Wales Institute of Engineers. Bye-Laws and
Regulations, revised March 1889. 1889.

———,}. —— +. || Proceadings.is jVol avin tiNes.'3=5. 61889.

ADDITIONS TO THE LIBRARY. 177

Sydney. Australian Association for the Advancement of Science.
Report of the First Meeting, 1888. 1890.

J.C. H. Mingaye. On the occurrence of Tellurium in New South
Wales Ores, 116.—W. A. Dixon. Some considerations in regard. to the
formation of Coal and Carbonaceous Minerals, 125.—G. 8S. Mackenzie.
Notes on the composition of Fahlerz and Embolite, from New South
Wales, 153.—W. Skey. On Gold: its formation in our Reefs, and notes
on some newly-discovered reactions, 155.—R. L. Jack. On some salient
points in the Geology of Queensland, 196.—A. W. Howitt. Notes on the
Metamorphic Rocks in the Omeo District, Gippsland, 206.—S. H. Cox.
The development of Mining in Australasia, 225.—R. Tate. On the Age
of the Mesozoic Rocks of the Lake Eyre Basin, 228.—R. Tate. Glacial
phenomena in South Australia, 231.—T. W. E. David. Origin of the
Laterite in the New-Eneland district of New South Wales, 233.—H. Y.
L. Brown. The Mesozoic plains of South Australia, 241.—F. W. Hutton.
On the Rocks of the Hauraki Gold-fields, 245.—T. W. E. David. Cupri-
ferous Tufts of the Passage-beds between the Triassic Hawkesbury series
and the Permo-Carboniferous Coal-measures of New South Wales, 275.
—T. W. E. David. Micropetrographical notes on some of the Hydro-
thermal Rocks of New South Wales, 290.—J. Mitchell. The Geological
sequence of the Bowning Beds, 291.—W. H. Rands. Notes on certain
Boulders met with in the beds and reefs of the Gympie Gold-field,
Queensland, 297.—W. J. C. Ross. On Metamorphism and the Rocks of
the Bathurst District, 300.—J. Smith. On the discovery of Fossils at
Rockhampton, 300.—R. M. Johnston. How far can Australian geologists
safely rely upon the Order of Succession of the characteristic Genera of
Fossil Plants of a far distant region, in the determination of the order and
relationship of Australian Terrestrial Formations ?, 502.

——. Australian Museum. See Booxs, New South Wales.

—— linnean Society of New South Wales. Proceedings. Ser. 2.
Wolhiv. Parts] & 2. 1889:

R. Etheridge, Jun. Remarks on Fossils of Permo-Carboniferous age,
from North-western Australia, in the Macleay Museum, 199.—W. Ste-
phens. An attempt to Synchronise the Australian, South-African, and
Indian Coal-Measures. Part I., 381—T, W. Edgeworth David. Note
on the Origin of Kerosene Shale, 483.

Royal Geographical Society of Australasia, New South Wales
Branch. ‘Transactions and Proceedings. Vols. iii. & iv.
1885-86. 1888.

C. 8. Wilkinson. Report on the Geological Specimens from New
Guinea collected by the Exploring Expedition of the Geographical Society
of Australasia, 203.

——

' First Report on New Guinea. By John F. Mann.
8vo. 1889.

—. Royal Society of New South Wales. Journal and Pro-
Geedines: Vol) xxin.” Part 2) 18388)
‘RR. Tate. Census of the Fauna of the Older Tertiary of Australia, 240,
—J. E. Tenison-Woods. The Desert Sandstone, 290.—A. Liversidge.
Notes on some New South Wales Minerals, 362.

. ‘ Volj xxi. Partda 1889.
W. A. Dixon. Note on the Composition of two Sugar-plantation soils,

178 ADDITIONS TO THE LIBRARY.

32.—H. C. Russell. The Source of the Underground Water in the
Western Districts, 57—F. W. Hutton. The Eruptive Rocks of New.
Zealand, 102.

Sydney. Royal Society of New South Wales. Catalogue of the
Scientific Books in the Library. Part 1. 8vo. 1889.

Topeka. Kansas Academy of Science. Transactions. Vol. vill.

1881-82. 1883.

E. Haworth. The Coal-fields of Cherokee County, 7.—S. C. Mason.
A preliminary List of Fossils found in Riley County, 12.—R. Hay. The
Igneous Rocks of Kansas, 14.—E. Haworth. Are there Igneous Rocks
in Cherokee County ?, 18.—R. Hay. Fossil Wood, 20.—E. Haworth.
Notes on Kansas Minerals, 25.—G. E. Patrick. Protozoan Remains in
Kansas Chalk, 26.

: : Vol. ix. 1883-84. 1885.

R. Hay. Preliminary Report on the Geology of Norton County, Kan-
sas, 17.—R. J. Brown. Is a Geological Survey of the State a necessity P
49,—K. H. 8. Bailey and E. W. Walter. The Water of the Fort Scott
Artesian Well, 96.—R. Hay. Notes on the Fossil Jaw of Bison, from
the Pliocene of Norton County, 98.—E. P. West. The last Submersion
and Emergence of South-eastern Kansas from the Carboniferous seas or
those affecting the Carboniferous formation in Kansas, 106.—J. Savage.
Notes on the Geology of the Spanish Peaks, 113.—G. H. Failyer. Notes
on some Kansas Mineral-waters, 114—B. B. Smyth. The Age of
Kansas, 129.

—_——

: 3 . Vol. x. 1885-86. 1887.

F. H. Snow. On the discovery of a Fossil Bird-track in the Dakota
Sandstone, 3.—R. Hay. A Geological Section in Wilson County, Kansas,
6.—A. H. Thompson. The relation of a State Geological Survey to the
work of the National Survey, 9.—R. Hay. Report on Geology, 21.—D.
S. Kelly. Coal-measures of Lyon County, 45.—R. Hay and A. H.
Thompson. Historical sketch of Geological work in the State of Kansas,
45.—R. Hay.—Natural Gas in Eastern Kansas, 57.—E. H. Bailey. Mis-
cellaneous Chemical Notes, 62.—G. H. Failyer and J. T. Willard. On
some Kansas Mineral-waters, 63.—R. Hay. Note on a remarkable
Fossil, 128.

: : Vol. xi. 1887-88.

R. Hay. Horizon of the Dakota Lignite, 5.—E. H. 8. Bailey. On
the newly-discovered Salt-beds in Ellsworth County, 8.—J. Savage. The
Pink-and-white Terraces of New Zealand, 26.—F. H. Snow. On the
discovery and significance of Stipules in certain Dicotyledonous Leaves of
the Dakota Rocks, 33.—R. Hay. The Geology of Kansas, 35.—E. Jame-
son. Geology of the Leavenworth Prospect Well, 87.—R. Hay. The
Triassic Rocks of Kansas, 38.—F. H. Snow. The Logan County Nickel-
mines, 39,—E. H. S. Bailey. The composition of Kansas Coals, 46.—G.
H. Failyer and C. W. Breese. Mineral Waters, 109.

Tokyo. College of Science, Imperial University, Japan. Journal.
Vol. iii. Parts 1-38. 1889.
Matajiro Yokoyama. Jurassic Plants from Kaga, Hida, and Echizen,
1.—Yasushi Kikuchi. On Pyroxenic components in certain Volcanic
2ocks from Bonin, 67.—S8. Sekiya. The Eruption of Bandai-san, 91.

ADDITIONS TO THE LIBRARY. 179

Tokyo. Seismological Society of Japan. Transactions. Vol. xiii.
Part 1. 1889.

H. Hoefer. Peculiar Phenomena in the Propagation of Karthquakes, 1.
—J. Milne. Earth-Tremors in Central Japan, 7.—E. Odlum. How
were the Cone-shaped Holes on Bandai-san formed ?, 21.—J. Milne. On
the Distribution of Harthquake-motion within a small area, 41.—J. Milne.
Report on Harthquake Observations made in Japan during the year 1886,
91.—Stanislas Meunier. Abstract of a Theory as to the cause of Karth-
quakes, 133.

=: : Mol, xiv.) [i1690,)|
J. Milne, J. Lescasse, and T. Bertelli. Construction in Earthquake
Countries, 1.

Toronto. Canadian Institute. Annual Report. 1889. 1889.

——, . Proceedings. Series 3. Vol. vii. No.1. 1889.
W. Kennedy. The Central Basin of Tennessee, 64.

Toulouse. Société d’Histoire Naturelle. Bulletin. 23° année.
1889. January—December. 1889.

Mémoires.
J. Laromiguiére. Note sur les phosphates de la Somme, 5.

Truro. Royal Institution of Cornwall. Annual Reports. 21st, for
the year 1839. 1840.

—. ——. ——. 23rd—26th, for the years 1841-44. 1842-45.
—, ——~, ——. 33rdand 34th, for the years 1851 and 1852.

1852-53.
——, —. ——.. 36th—40th, for the years 1854-58. 1855-59.
—. ——. ——. 42nd. Pt. 2, for the year 1860. 1861.
—. ——. ——. 44th. Pt. 1, for the year 1861. 1862.

2, 45th, for the year 1862, 1863.

: . —. 47th and 48th, for the years 1864 and 1865,
1865 and 1866.
| ——. d0th—-6lst, forthe years 1867-77. 1868-78.

—— —. Journal. Vol.ii. (Nos. 5-8). 1866-67. 1866-67.
—, ——. ——. Vol.in. (Nos. 9-12). 1868-70. 1868-71.
—. —. ——. Vol.iv.(Nos.13-15). 1871-73. 1872-74,

ae Ok va Nosy 16219. 7 Parts V& Oy) 87a"
78. 1875-78. (Wants titlepage and table of contents.)

Vol. vi. (Nos. 21-23). 1879-81. 1879-81.

—_——_—=—

(No. 20 wanting.)
Vol. vii. 1881-83. 1881-83.

ee

180 ADDITIONS TO THE LIBRARY.

Truro. Royal Institution of Cornwall. Journal. Vol. viii.
1883-85. 1884-85. |

Vol, 1m.) Part, 1.) 1886) 1 8eGe

R.N. Worth. Notes on the Igneous Rocks of South-east Cornwall
and their Stratigraphical value, 19.—F, Brent. On the occurrence of
Flint Flakes and small Stone Implements in Cornwall, 58.—J. H. Collins.
Notes on the Great Mother Lode of California, 62.

Part 4. 1889. 1889.

TL Clark, The Bacal Wrecks and ewer of Extinct Volcanoes in
South-west Cornwall, 449.—J. H. Collins. Notes on some oxidized
Copper-ores from the Torreon mines in the Province of Chihuahua,
Mexico, 471.—E. A. Wiinsch. The problem of the Lizard Rocks, 489.

———

—_-_,

List of Antiquities in the Hundreds of Kirrier and
Penwith, West Cornwall. By J.T. Blight. 8vo. 1862.

The Cornish Fauna. Part I. The Vertebrate
Animals and Crustaceans. By J. Couch. Second edition.
8vo. 1878.

. The Keclesiastical Seals of Cornwall. By W. Jago.
Reprint, with additions. 8vo. 1884.

—_—__,

See
e

Museum Catalogues. No.1. Non-metallic Minerals.
Syvo. 187s:

—, ——. —. No.2. Metallic Minerals. 8vo. 1881.

Turin. R. Accademia delle Scienze. Atti. Vol. xxiv. Disp. 11-15.
1888-89. 1889.

Sacco. I] seno terziario di Moncalvo, 562.—Piolti. Gneiss tormalini-
fero di Villar Focchiardo (Val di Susa), 661.

. Vol. xxv. Disp. 1-10. 1889-90.
C. Montemartini. Composizione chimica e mineralogica di una roccia
serpentinosa di Borzanasca (Riviera Ligure), 209.

Memorie. Serie 2. Tomo xxxix. 1889.
Classe di Scienze Fisiche, Matematiche e Naturalii—F. Sacco. I
Cheloni astiani del Piemonte, 427.

. Osservazioni Meteorologiche fatte nell’ anno 1888,
all’ Osservatorio delle R. Universit. By G. B. Rizzo. 8y0.
1890.

University College. Calendar. Session 1889-90. 1889.

——,

Victoria Institute. Journal of the Transactions. Vol. xxiii. Nos.
89-91. 1889.

H. B. Guppy. Coral Islands and Savage Myths, 46.—H. B. Guppy.
Preliminary note on the Keeling Atoll or ‘Cocos Isl ands, 72.—T. Mc.K.
Hughes. On Cuts on Bone as evidence of Man’s Existence i in Remote
Ages, 209.

ADDITIONS TO THE LIBRARY. 181

Vienna. Kaiserliche Akademie der Wissenschaften. Anzeiger,
1890. Nos. 1-27. 1890.

F. Toula. Geologischen Untersuchungen im éstlichen Balkan und in
den angrenzenden Gebieten, 17.—N. Karakasch. Ueber einige Neocom-
ablagerungen in der Krim, 110.—F. Toula. Pyrgulifera Pichlert, Horn,
in Bulgarien, 140.—E. Naumann und M. Neumayr. Zur Geologie und
Palaontologie Japans, 162.—A. Rosiwal. Zur Kenntniss der Krystalli-
nischen Gesteine des centralen Balkan, 168.—P. Oppenheim. Die Land-
und Siisswasserschnecken der Vicentiner Eocanbildungen, 197.—K. A.
Weithofer. Ueber Jura und Kreide aus dem nordwestlichen Per-
sien, 247.

foe, | 1890. Nos. 6-11, 1890.

L. v. Hohnel, von F. Toula und E. Suess. Grundziige des Baues des
dstlichen Africa, 93.—C. Délter. Versuche iiber die Loslichkeit der
Minerale, 101.

. Denkschriften. Mathematisch-naturwissenschaftliche
Classe. Band lv. 1889.
i. Abtherlung.

C. v. Ettingshausen und F. KraSan. Beitrige zur Erforschung der
atavistischen Formen an lebenden Pflanzen und ihrer Beziehungen zu
den Arten ihrer Gattung, ii. Folge, 1.

ul. Abthedlung.

F. Toula. Geologische Untersuchungen im centralen Balkan, 1.—K.
A. Weithofer. Die fossilen Hyanen des Arnothales, 337.

oe

: Sitzungsberichte. Mathematisch-naturwissenschaft-
liche Classe. Band xcvii. Hefte 6-10. 1888. 1888-89.
L. Szajnocha. Ueber fossile Pflanzenreste aus Cacheuta in der Argen-
tinischen Republik, 219.—F. Katzer. Spongienschichten im mittelbdhm-
- ischen Devon (Hercyn), 300.—C. Diener. Geologische Studien im siid-
westlichen Graubiinden, 606.

—. «——. ——. ——. Band xcviii. Hefte]1& 2. 1889.
1889.
M. Neumayr. Ueber die Herkunft der Unioniden, 5.—A. Rodler.
Bericht iiber eine geologische Reise im westlichen Persien, 28.—C. Die-
ner. Zum Gebirgsbau der “‘ Centralmasse des Wallis,” 78.

——. K.-k. Bergakademie zu lLeoben und Piibram und der
kéniglich-ungarische Bergakademie zu Schemnitz. Berg- und
Hiittenminnisches Jahrbuch. Band xxxvii. Hefte 1-4. 1889.

A. Pallausch. Die Graphitbergbaue im siidlichen Bohmen, 94.—E.

Sedlaczek. Ueber beschleunigten Stollenbetrieb im Zusammenhange mit

der Ausftthrung der Localbahn Hisenerz-Vordernberg, 185.—Max vy.

Wolfskron. Die Goldvorkommen Mahrens, 229,

; : . Band xxxvii. Heft 1. 1890.
FE. L. von Ebengreuth. Asbest, 87.

——. K.-k. geologische Reichsanstalt. Abhandlungen, Band xiii.
ett Tov 1889.6 1889.

G. Stache. Die liburnische Stufe und deren Grenz-Horizonte. i. Heft
i, Abtheilung, 1.

182 ADDITIONS TO THE LIBRARY.

Vienna. K.-k. geologische Reichsanstalt. Abhandlungen. Band xv.

Hefte 1&2. 1889-90. |

G. Geyer. Ueber die liasischen Brachiopoden des Heerlatz bei Hall-

statt, 1.—L. Tausch vy. Gloeckelsthurn. Zur Kenntniss der Fauna der
“ Grauenkalke ” der Suid-Alpen, 1.

——. ——. Jahrbuch. Jahrgang 1889. Band xxxix. Hefte
1-4. 1889. ‘

D. Stur. Momentaner Standpunkt meiner Kenntniss tiber die Stein-
kohlenformation Englands, 1.—D.Stur. Zur Frage der Erweiterung des
Heilbades ‘‘ Wies-Baden” bei Ried, 21.—D. Stur. Zur Frage der Ver-
sorgung der Stadt Ried mit Trinkwasser, 29.—D. Stur. Der Trink-
wasserversorgung der Stadt Hainburg, 35.—J. v. Siemiradzki. Ueber die
Gliederung und Verbreitung des Jura in Polen, 45.—A. Weithofer.
Ueber die tertiiren Landsdugethiere Italiens, 55.—G. Stache. Die
Wasserversorgung von Pola, 83.—S. Fr. v. Wohrmann. Die Fauna der
sogenannten Cardita-und Raibler-Schichten in den nordtiroler und bayer-
ischen Alpen, 181.—D. Stur. Zur Trinkwasserfrage von Neunkirchen, 259.
—C. Angermann. Die Naptafelder in Wietrzno, 281.—K. Tietze. Beitraige
zur Geologie von Galizien, 289.—L. v. Tausch. Bericht tiber die geo-
logische Aufnahme der Umgebung von Mahrisch-Weisskirchen, 405.—H.
Sjogren. Uebersicht der Geologie Daghestans und des Terek-Gebietes,
417.—D. Stur. Eine fliichtige, die Inoceramen-Schichten des Wiener
Sandsteins betreffende Studienreise nach Italien, 439.—J. v. Siemiradzki.
Beitrag zur Kenntniss des nordischen Diluviums auf der polnisch-lithau-
ischen Ebene, 451.—D. Stur. Geologisches Gutachten in Angelegenheit
der Entziehung des Wassers aus den Brunnen der Ortschaft Brunn am
Erlaf bei Pochlarn, 463.—C. v. John. Ueber den Moldavit oder Bouteil-
lenstein von Radomilic in Bohmen, 475.—J. Blaas. Ueber sogenannte
interglaciale Profile, 477.—A. Bittner. Die Trias von Eberstein und
Polling in Karnten, 483.—F. Frech. Ueber die Korallenfaunen der nord-
alpinen Trias, 489.—G. Geyer. Beitrige zur Geologie der Miirzthaler
Kalkalpen und des Wiener Schneeberges, 497.

: Verhandlungen, 1889. Nos. 7-18. 1889.

F. Bartonec. Galmevorkommen auf secundarer Lagerstatte bei Nowa
Gora in Galizien, 140.—A, Bittner. Hin neuer Fundort von Brachiopoden
des Hallstatter Kalkes auf dem Nasskor bei Neuberg an der Miirz and
die Hallstitter Brachiopoden von Miihlthal bei Piesting, 145.—Clar. Zur
Hydrologie von Gleichenberg, 147.—M. Vacek. Ueber die geologischen
Verhiltnisse des Wechselgebietes, 151.—L. v. Tausch. Ueber einige
nichtmarine Conchylien der Kreide und des steirischen Miocans und ihre
geographische Verbreitung, 157.—A. Bittner. Revision der Brachiopoden
von Sct. Cassian, 159.—A. Cathrein. Petrographische Notizen aus den
Salzburger und Tiroler Alpen, 171K. A. Weithofer. Yapir und Nau-
tilus aus oberosterreichische Tertiarablagerungen, 179.—R. Hoernes.
Bemerkungen zur Zinnwalder Frage, 180.—R. Hoernes. Zur Geologie
von Untersteiermark, 181.—D. Stur. Eine Sammlung fossiler Pflanzen
aus der Kreideformation Béhmens, 183.—R. Hoernes. Zur Geologie
Untersteiermark, IT., 19].—T. Wisniowski. Kinige Bemerkungen tiber
die Technik der mikroskopischen Untersuchungsmethode der Hornsteine,
195.—H. B. v. Foullon. Ueber den Prehnit aus dem Floitenthale, 197.—
J. Prochizka, Die Fauna des miocinen Sandes von Poisdorf, 201.—C.
W. v. Giimbel. Ueber einen aufrechtstehenden Kohlenstamm der Pil-
sener Mulde, 203.—J. E. Hibsch. Der Doleritstock und das Vorkommen
yon Blei- und Silbererzen bei Rougstock im béhmischen Mittelgebirge,
204.—F, Teller. Daonella Lommel: in den Pseudo Gailthalerschiefern

——_—

ADDITIONS TO THE LIBRARY, 183

von Cilli, 210.—C. M. Paul. Aufnahmsbericht aus dem dstlichen Mah-
ren, 211.—D. Stur. Zur Kenntniss der Verhiltnisse im Steinbruche bei
Mietniow im Siidosten bei Wieliczka, 212.—C. W. v. Giimbel. Ueber
einen Nummulitenfund bei Radstadt, 231.—J. Blaas. Ein Profil durch
die Achensee-Dammschotter, 232.—F. Teller. Zur Kenntniss der Tertiar-
ablagerungen des Gebietes von Neuhaus bei Cilli in Siidsteiermark,
234.—R. Hoernes. Zur Geologie Untersteiermarks, 254.—C. v. Camer-
lander. Reisehericht aus dem Gebiete des mihrischen Hohe Haide-
Hirschkamrnzuges, 258.—G. Bukowski. Reisebericht aus der Gegend von
Romerstadt in Mahren, 261.—A. Bittner. Zur Altersbestimmung des
Miocans yon Tiiffer in Siidsteiermark, 270.—L. v. Tausch.—Miocan bei
Leipnik, 275.—L. v. Tausch. Reisebericht des Sectionsgeologen der
Section 111, 276.—E. v. Mojsisovics. Nachweis der Zone des Tvropites
subbullatus in den Hallstatter Kalken bei Hallein, 277.—A. Bittner. Die
Trias von Eberstein und Polling, 280.—C. v. Voedt. Ueber die Ober-
eocan- und Oligocan-Schichten der Halbinsel Krim, 289.—H. Bergmann.
Bohrung nach artesischem Wasser in der Niederung von Neubydzovy,
nordlich von Chlumac in Bohmen, 313.—C. M. Paul. Geologische Auf-
nahmen im mahrischungarischen Grenzgebirge, 314.—F. Teller. Fusu-
linenkalk und Ugeowitzer Breccie innerhalb der Weitensteiner Eisenerz-
formation und die Lagerungsbeziehungen dieser paliozoischen Gebilde zu
den triadischen und tertiaren Sedimenten des Weitensteiner Gebirges,
514.—-R. Hoernes. Diabas von Lebring bei Wildon und von Kaindorf
bei Leibnitz, 339.

Vienna. K.-k. geologische Reichsanstalt. Verhandlungen, 1890.
Nos. 1-5. 1890.

A. Cathrein. Ueber den sogenannten Augit-porphyr von Ehrwald, 1.
—M. Vacek. Ueber die Krystallinische Umrandung des Grazer Beckens,
9.—D. Stur. Jahresbericht, 29.—v. Giimbel. Lrthiotis problematica, G.,
eine Muschel, 64.—R. Hoernes. Zur Geologie Untersteiermarks, 67, 81.
—E, Doll. Der Meteorfall im Jeliza-Gebiree in Serbien, 70.—H. Tietze.
Die Gegend von Olmiitz, 77.—V. L. Szajnocha. Ueber eine cenomane
Fauna aus den Karpathen der Bukowina, 87.—A. Pichler. Zur Geologie
von Tirol, 90.—L.v. Tansch. Ueber eine tertiire Stisswasserablagerung
bei Wolfsberg in Karnten, 95.—A. Rzehak. Die Conchylienfauna des
diluvialen Kalktuffes von Tutschin in Mahren, 107.—J. Prochazka. Rfi-
noceros tichorhinus von Herotic in Mahren, 107.—E. Doll. Ueber den
Meteoriten von Ochansk, 109.—H. v. Foullon. Ueber Krystallinische
Gestein aus Kleinasien, 110.—C. y. Camerlander.—Zur Geologie des
niederen Gesenkes, 113,

Mineralogische und petrographische Mittheilungen. N. F.
Band x. Heft 6. 1889. Purchased.

Pedro Augusto von Sachsen-Coburg. Beitriége zur Mineralogie und
Petrographie Brasiliens, 451.—K, A. Reiser. Ueber die Eruptivgesteine
des Algau, 500.

: ‘ Band xi. Heft 1. 1889. Purchased.

W. H. Hobbs. Ueber die Verwachsung von Allanit (Orthit) und Epi-
dot in Gesteinen, 1.—R. Prendel. Ueber den Senarmontit, 7.—B. Doss.
Die Lamprophyre und Melaphyre des Plauen’schen Grundes bei Dresden,
17.—A. Frenzel. Whewellit von Zwickau, 83.

——. K.-k. naturhistorische Hofmuseums. Annalen. Band iii.
No. 3. 1888.
_A. Rzehak. Das Foraminiferen des kieseligen Kalkes von Nieder
Hollabrunn und des Melettamergels der Umgebung von Bruderndorf in
Niederésterreich, 557,
VOL, XLVI. 0

184 ADDITIONS TO THE LIBRARY.

Vienna. K.-k. naturhistorische Hofmuseums. Annalen. Band iy.
Nos. 3&4. 1889-90.

. Band v. No.1. 1890.
A. W. Stelzner. Ueber die Isolirung von Foraminiferen aus dem
Badener Tegel mit Hilfe von J odidlésung, i,

——

—. Kaiserlich-kénigliche zoologisch-botanische Gesellschaft.
Verhandlungen. Band xxxix. Quartal 1-4. 1889. 1889.
F. Krasser. Ueber die fossilen Pflanzenreste der Kreideformation in
Mahren, Sitzb., 31.

——. Tschermak’s Mineralogische und Petrographische Mittheil-
ungen. Neue Folge. Band xi. Hefte2&3. 1890. Pur-
chased.

J. von Siemaschko. Hinige Beobachtungen an dem Meteorsteine von
Ochansk, 87.—F. Eigel. Ueber einige Eruptivg gesteine de Capverden,
91.—E. Ludwig. Die Mineralquellen Bosniens, 105.—H. Rosenbusch.
Ueber die chemischen Beziehungen der Eruptivgesteine, 144.—A. Frenzel.
Mineralogisches, 214.—F. Becke. Ueber Dolomit und Magnesit und uber
die Ursache der Tetartoédrie des ersteren, 224.—A. Kiebel. Berechnung
von H. Niedmann’s Biegungsversuchen an Kreisplatten von Baryt, 261.

——. ——. Register zu Bandi-ix. 1800. Purchased.

Warwick. Warwickshire Naturalists’ and Archeologists’ Field-
Club. Proceedings and 33rd Annual Report, 1888. 1889.
Rey. P. B. Brodie. On the predominance and importance of the
Blattidee in the Old World, 12.

Washington. Smithsonian Institution. Annual Report for the
year ending June 30, 1886. Part1l. 1889.

. Bureau of Ethnology. Annual Report. 1883-84.
8vo. Washington. 1887.

—. —. 1884-85. 8vo. Washington.

1888,

Bibliography of the Iroquoian. Languages,
By J. C. Pilling. 8vo. Washington. 1888.

. Textile Fabrics of Ancient Peru. By W.
H. Holmes. 8vo. Washington. 1889.

EE

—. ——. —. Bibliography of the Muskhogean Languages.
By J.C. Piling. 8vo. Washington. 1889.

; . The Problem of the Ohio Mounds. By C.
Thomas. Svo. Washington. 1889.

: . The Circular, Square, and Octagonal Earth-
works of Ohio. By C. Thomas. 8vo. Washington. 1889,

ADDITIONS TO THE LIBRARY. 185

Washington. Smithsonian Institution. United States National
Museum. Bulletins, Nos. 33-37. 8yvo. Washington. 1889.

No. 33. Catalogue of Minerals and Synonyms alphabetically
arranged for the use of Museums. by T. Egleston.

No. 34. The Batrachia of North America. By E. D. Cope.

No. 35. Bibliographical Catalogue of the Described Transforma-
tions of North-American Lepidoptera. By Henry Edwards.

No. 36. Contributions to the Natural History of the Cetaceans:
a review of the Family Delphinide. By F. W. True.

No. 37. A Preliminary Catalogue of the Shell-bearing Marine
Mollusks and Brachiopods of the South-eastern coast of the

United States, with illustrations of many of the Species.
By W. H. Dali.

Wellington. New Zealand Institute. Transactions and Proceed-
mec toes. Vol. xxi. 1889.

Hutton. The Earthquake in the Amuri, 269.—H. A. de Lantour. On
the Fossil Marine Diatomaceous Deposit near Oamaru, 293.—A. Hamilton.
Notes on a deposit of Moa-bones in the Te Aute Swamp, Hawke’s Bay,
311.—H. Hill. Discovery of Fossil Moa-feathers in Rocks of Pliocene
age, 318.—H. Hill. The Oil prospects of Poverty Bay and District, 320.
—J. Park. On the Extent and Duration of Workable Coal in New Zea-
land, 325.—L. O. Beal. The Alluvial Deposits of Otago, 332.—T. G.
Bonney. Note on Rock collected by the Rev. W.S. Green from near the
summit of Mount Cook, 334.—G. J. Binns. Ona Striated Rock-surface
from Boatman’s, near Reefton, 335.—J. Harding. On the Neighbourhood
of Te Aoroa, Northern Wairoa, 336.—A. P. W. Thomas. Notes on the
Geology of Tongariro and the Taupo District, 338.

Wiesbaden. Nassauische Vereins fur Naturkunde. Jahrbiicher.
Jahrgang xlii, 1889.

II. Abhandlungen.

F. vy. Sandberger. Ueber die Entwickelung der unteren Abtheilung
des devonischen Systems in Nassau, verglichen mit jener in anderen
Liandern, 1.—F. Kinkelin. Der Basalt in der Senke Louisa-Florsheim
bei Frankfurt a, Main, 109.—A. Reuss. Die Bohrungen bei Kiedrich,
121.

York. Yorkshire Philosophical Society. Annual Report for 1889.
ee S90.

Anon. Platycherops Richardson, 35.—A. Smith Woodward. On the
Tooth of a Carboniferous Dipnoan Fish, Ctenodus interruptus, 87.—A.

Smith Woodward. On two groups of teeth of the Cretaceous Selachian
Fish, Ptychodus, 88.

Zoological Record. Vol. xxv. 1888. 1890. Purchased.

Zoological Society. Proceedings. 1889. Parts 2-4. 1889-90,
E, T. Newton.—A Contribution to the History of Eocene Siluroid
Fishes, 201.—A. Smith Woodward. Note on Bucklandium diluvu, Konig,
a Siluroid Fish from the London Clay of Sheppey, 208.—A. G. Butler.
Description of a New Genus of Fossil Moths belonging to the Geometrid

94

186 ADDITIONS TO THE LIBRARY.

Family Euschemide, 292.—R. Lydekker. On associated Remains of a
Theriodont Reptile from the Karoo System of the Cape, 572.—A. 8,
Woodward. Remarks upon an extinct Saw-fish (Sclerorhynchus atavus),

449,
Zoological Society. Proceedings. 1890. Part 1. .1890.
R, Lydekker. On a new Species of Otter from the Lower Pliocene of
Eppelsheim, 3.
——. Report of the Council for the Year 1889. 1890.

——, Transactions. Vol. Xi, warts: 9. Ge lO; .< PSae-

2. Booxs,
Names of Donors in Italics.
Adams, F. D. See Dawson, G. M.

Adamson, S. A. The Yorkshire Boulder Committee and its third
year’s work. S8yvo. Leeds, 1889.

Alford, C.J. Witwatersrand Gold Fields: Their Geological Fea-
tures. 8vo. London, 1889. Presented by Messrs. T. J. Bewick,
F.GS., C. A. Moremg, F.GS., and C. J. Alford, F.GS.

Alsace-Lorraine. Geologische Specialkarte von Elsass-Lothringen.
Abhandlungen. Bandin. Hefte 3 und 4. 8vo. Strassburg,
1889, Purchased.

Anon. Coal in the South of England. Slip (‘ Engineer,’ Feb. 28,
1890). Presented by W. Whitaker, Esq., F.RS., F.GS.

Discovery of a Coal Field in Kent. Slip (‘ Daily News,’
Feb. 20, 1890). Presented by W. Whitaker, Esq., F.RS., FAS.

Army Medical Department. Report for the year 1887. Vol. xxix.
8vo. London, 1889.

Aucoc, L. See Sertats, Paris. Institut de France.
Australian Museum. See New South Wales.
Ayres, HE. F. See Chatard, T. M.

Barrois, C. Mémoire sur les éruptions diabasiques siluriennes du
Menez-Hom, Finistére. 8yo. Paris, 1890,

. Note sur l’existence du terrain déyonien supérieur 4 Ros-
tellec (Finistére). S8yvo. Lille, 1889.

Bauerman, H. A treatise on the Metallurgy of Iron. 6th edition.
8vo. London, 1890, ‘

——

ADDITIONS TO THE LIBRARY. 187

Baumhauer, H. Das Reich der Krystalle fiir jeden Freund de
Natur, insbesondere fur Mineraliensammler. 8vo. Leipzig, 1889.
Purchased.

Bauernfeind, C. Max von. Das Bayerische Praecisions-Nivellement.
7° Mittheilung. 4to. Munich, 1888. Presented by the K. 6b.
Akademie der Wissenschaften zu Munchen.

Bayley, W.S. The origin of the Soda-Granite and Quartz-Kera-
tophyre of Pigeon Point. 8vo. New Haven. 1890.

Bellardi, L., ¢ F. Sacco. I Molluschi dei Terreni Terziarii del Pie-
monte e della Liguria. Parte 6. 8vo. Turin, 1890.

Bird, C. Underground Water. 4to. Rochester, 1887.
——. Rochester Rainfall. 1884-7. 4to. Rochester, 1888.

Blake, W. P. Uintaite, Albertite, Grahamite, and Asphaltum de-
scribed and compared, with observations on Bitumen and its
compounds. S8vo. 1890.

—. Wurtzilite from the Uintah Mountains, Utah. 8vo. ——
1880.

Blytt, A. On Variations of Climate in the course of time. 8vo.
Christiania, 1886. Presented by W. 7’. Blanford, Esq., F.RS.

3

Bonaparte, Prince Roland. Le Glacier de l’Aletsch et le Lac de
Marjelen. 4to. Paris, 1889.

——. la Laponie et la Corse. 8vo. Geneva, 1889.

Le premier établissement des Néerlandais 4 Maurice. 4to.
Paris, 1890. .

Bonney, T. G. Notes on two Traverses of the Crystalline Rocks of
the Alps. 8vo. London, 1889.

Bornemann, J.G. Ueber den Buntsandstein in Deutschland und
seine Bedeutung fur die Trias, nebst Untersuchungen uber Sand-
und Sandsteinbildungen im Allgemeinen. 4to. Jena, 1889.
Purchased.

Boué, Ami. Die Europiische Turkei. Bande 1 und 2 (Deutsch |
herausgegeben von der Boué-Stiftungs-Commission der Kais.
Akademie der Wissenschaften in Wien). 8vo. Vienna, 1889.

Brazil. See 8. Paul.
Briart, M. La Formation Houillére. 8yo. Brussels, 1889.

British Museum. Catalogue of the Fossil Reptilia and Amphibia
in the British Museum (Natural History). Parts 2 and 3, by R.
Lydekker. 8vo. London, 1889. Presented by the Trustees of
the British Museum.

188 ADDITIONS TO THE LIBRARY.

Brodie, P. B. On the predominance and importance of the Blattide
in the Old World. 8vo. Warwick, 1889. |

On the character, variety, and distribution of the Fossil
Insects in the Paleozoic (Primary), Mesozoic (Secondary), and
Cainozoic (Tertiary) Periods. 8vo. Warwick, 1890.

Brogger, W.C. Die Mineralien der Syenitpegmatitgainge der siid-
norwegischen Augit- und Nephelinsyenite. 8vo. Leipzig, 1890.

Brongniart, C., H. Fayol, L. de Launay, 8. Meunier, B. Renault,
H. E. Sauvage, et R. Zeiller. Etudes sur le terrain houtller de
Commentry. 2° Livre. Flore Fossile par B. Renault et R.
Zeiller. 1° Partie, par R. Zeiller. Text. 8vo. Saint-Etienne,
1888; Atlas. Fol. 1888. (Presented by M. Fayol, 76 Bd.
Malesherbes, Paris.)

Brough, B. H. Outbursts of Gas in Metalliferous Mines. 8vo.
Neweastle-upon-Tyne, 1889.

Brown, H. ¥. L. See South Australia.

——,J.A. On the Discovery of Hlephas primigenius associated
with Flint Implements, at Southall. 8vo. London, 1888.

——. On some small highly specialized forms of Stone Implements
found in Asia, North Africa, and Europe. 8vo. London, 1888.

——. Working-Sites and Inhabited Land-Surfaces of the Palzo-
lithic Period in the Thames Valley, etc. 8vo. London, 1889.

Browne, Montagu. On a Fossil Fish (Chondrosteus) from Barrow-
on-Soar, hitherto recorded only from Lyme Regis. 8yvo. Lei-
cester, 1889.

Bucquoy, Dautzenberg et G. Dollfus. Les Mollusques marins du
Roussillon. Tome nu. Peélécypodes. Fasc. 1-8. dvo. Paris,
1887, ’88 & ’89.

Bukowski, G. Der geologische Bau der Insel Kasos. 8vo, Vienna,
1889,

Grundziige des geologischen Baues der Insel Rhodus. 8vo.
Vienna, 1889.

Burmeister, Hermann. Los caballos fosiles de la Pampa Argentina.
Suplemento. Fol. Buenos Aires, 1889.

California State Mining Bureau. W. Irelan, Jr., State Mineralo-
gist. 8th Annual Report of the State Mineralogist for the year
ending October 1, 1888. 8vo. Sacramento, 1888. |

Cambresy, A. Le Laurium, 8vo. Paris, 1889. Presented by H.
Bauerman, Esq., F.GS.

ADDITIONS ‘IO THE LIBRARY. 189

Canada. Geological and Natural History Survey. Annual Report.
(New Series.) Vol. iii. Part ii. 1887-88. 1889. 8vo. Mont-
real, 1889, and Maps &e.

: Contributions to Canadian Paleontology. Vol. 1.
J. F. Whiteaves. Part 2. 1889.

> Contributions to the Micro-Palzontology of the
Cambro-Silurian Rocks of Canada. Part ii. By E. O. Ulrich.
8vo. Montreal, 1889.

Cantami, A. Acireale considered as a climatic station and a bath-
ing town. 8vo. Naples, 1880.

Capellini, G. Commemorazione di Giuseppe Meneghini. 8vo.
Bologna, 1889.

Sul primo uovo di Aepyornis maximus arrivato in Ltalia.
Ato. Bologna, 1889.

. Ichthyosaurus campylodon e Tronchi di Cicadee nelle Argille
Scagliose dell’ Emilia. 4to. Bologna, 1890.

Oarez, L. Géologie—Iles Britanniques. [Annuaire Géologique
Universel.} 8vo. Paris, 1889.

——. Geéologie—France. [——]. 8vo. Paris, 1889.

Note sur les couches dites Triasiques des environs de Sou-
eraigne (Aude). 8vo. Paris, 1889.

. Note sur le Crétacé inférieur des environs de Maurice
(Bouches-du-Rhéne). 8vo. Paris, 1889.

. Sur lexistence de phénoménes de recouvrement dans les
Petites Pyrénées de ?Aude. 4to. Paris, 1889.

=, wee Vasseur, G.

Castillo, Antonio del. Catalogue descriptif des Météorites (Fers et
Pierres Météoriques) du Mexique. 8vo. Paris, 1889.

Cassino, 8. E. The Naturalists’ Directory. 8vo. Boston, 1890
Purchased.

Challenger. Report of the Scientific Results of the Voyage of
H.M.S. ‘Challenger’ during the years 1873-76. Physics and
Chemistry. Vol. 11. 4to. London, 1889. Presented by H.M.
Treasury.

. —. Zoology. Vol. xxxii. 4to. London, 1889. Pre-
sented by HM. Treasury.

Chapman, HE. J. Some remarks on the classification of the Trilo-
bites, as influenced by Stratigraphical Relations: with outline of
a new grouping of these Forms, 4to. Montreal, 1889.

Igo ADDITIONS TO THE LIBRARY.

Chatard, T. M. Analyses of the Waters of some ares: Alkali
Lakes. 8vo. New Haven, 1888. :

. The determination of Water and Carbonic Acid in Natural
and Artificial Salts. 8vo. New Haven, 1889.

——. Urao; with notes on the crystallization of Trona (Urao).
By E. F. Ayres. .8vo. New Haven, 1889.

Clarke, F. W. An Address before the permanent Subsection of
Chemistry of the American Association for the Advancement of
Science at the St. Louis Meeting, Aug. 1878. 8vo. Salem,
1878.

—. Mica. 8vo. Washington, 1885.

——-. The Meteorite Collection in the U.S. National Museum: A
Catalogue of Meteorites represented November 1, 1886. 8vo.
Washington, 1889.

. The Relations of the Government to Chemistry. Address
to the Chemical Society of Washington. 1885. 8vo. Wash-
ington, 1886.

Work done in the Division of Chemistry and Physics mainly
during the fiscal years 1884-86. 5vo. Washington, 1886 &
1887.

——. Studies in the Mica Group. 8vo. New Haven, 1887.
—. Some Nickel Ores from Oregon. 8vo. New Haven, 1888.

—. The Chemical Structure of the Natural Silicates. 8vo.
Amer. Chem. Journ. 18&8.

——. The Present Status of Mineralogy. 8vo. New York, 1888.

——. A New Occurrence of Gyrolite. 8vo. New Haven, 1889.
——. <A Theory of the Mica Group. 8vo. New Haven, 1889.

—. The Relative Abundance of the Chemical Elements. 8vo.
Washington, 1889.

and C. Catlett. A Platiniferous Nickel Ore from Canada,
8vo. New Haven, 1889.

and G. P. Merrill. On Nephrite and Jadeite. 8vo. Wash-
ington, 1888.

— and G. P. Merrill. On Nephrite and Jadeite. 8vo. Wash-
ington, 1888.

Coode, Sir John, Address to the Institution of Civil Engineers, 12th
November, 1889. 8vo. London, 1889.

ADDITIONS TO THE LIBRARY. Igt

Cope, E. D. Synopsis of the Vertebrate Fauna of the Puerco Series.
4to. Philadelphia, 1888.

——. The Pineal Eye in Extinct Vertebrates. 8vo. Philadelphia,
1888.

The Mechanical Causes of the Origin of the Dentition of
the Rodentia. 8vo. Philadelphia? 1889 or ’88.

. A Review of the North-American Species of Hippotherium.
8vo. Philadelphia, 1889.

——, The Horned Dinosauria of the Laramie. S8vo. Philadel-
phia, 1889.

Riitimeyer on the Classification of Mammalia and on Ame-
rican Types recently found in Switzerland. 8vo. Philadelphia,
1888.

The Vertebrate Fauna of the Equus Beds. 8vo. Phila-
delphia, 1889.

-——. The Mechanical Origin of the Hard Parts of the Mammalia.
Svo. Philadelphia, 1889.

——. [Extracts regarding the Paleontological Department of the
U.S. Geological Survey.| 8vo. Philadelphia, 1890,

——. See Serrats. Washington. Smithsonian Institution.

Costa Kica and Nicaragua. Argument on the question of the vali-
dity of the treaty of limits between Costa Rica and Nicaragua
and other supplementary points connected with it, submitted to
the arbitration of the President.of the United States of America,
filed on behalf of the Government of Costa Rica by P. P. Zeledon.
8vo. Washington, 1887.

Reply to the Argument of Nicaragua on the question of the
validity or nullity of the treaty of limits of April 15, 1858, to be
decided by the President of the United States of America as Ar-
bitrator. Filed on behalf of the Government of Costa Rica by
P. P. Zeledon. 8vo. Washington, 1887.

—. The Case of the Republic of Nicaragua submitted to His
Excellency Hon. Grover Cleveland, President of the United States,
Arbitrator, under the treaty of Guatemala of December 24th,
1886. 8vo. Washington, 1888. Presented by the Oficina de
Deposito y Canje de Publicaciones, Republica de Costa Rica, San
José.

Cotteau, G. Catalogue des Echinides recueillis par M. Roussel dans
le terrain Crétacé des Petites Pyrénées et des Corbiéres. 8vo.
Paris, 1887.

Echinides nouveaux ou peu connus, 6° et 7° articles. 8yo.
Paris, 1887 and 1888,

— ——_ Se —a7~s

—_ SS

==

[g2 “ADDITIONS TO THE LIBRARY.

Cotteau, G. Note sur la famille des Brissidées. 8vo. Paris, 1887.

Sur les genres éocéne de la famille des Brissidées (Echinides
irréguliers). 4to. Paris, 1887.

Terrains Tertiaires, Eocéne, Echinides. Tome i. Text,
feuilles 27-42, Planches 121-200 (Paléontologie Francaise). 8yvo.
Paris, 1887-1889.

Echinides éocénes de la province d’Alicante (Espagne). 4to.
Paris, 1888.

La Géologie au Congrés Scientifique de Toulouse en 1887
et Compte-rendu du Congres. 8vo. Auxerre, 1888.

——. Echinides crétacés de Madagascar, S8vo. Paris, 1889.

Note sur un exemplaire du Coraster Vilanove provenant de
Tersakhan (Turkestan). 8vo. Paris, 1889. (This accompanies
a paper by P. de Loriol.) 8vo. Paris, 1889.

Réunion de la Société Helvétique a Soleure (Suisse). 8vo.
Auxerre, 1889.

. Sur deux Echinodermes fossiles provenant de Thersakhan
(Turkestan). 4to. Paris, 1889.

Credner, H. Die Stegocephalen und Saurier aus dem Rothliegenden
des Plauen’schen Grundes bei Dresden. VIII. Theil. 8vo. Berlin,
1889.

Oredner, H., EK. Geinitz, & F. Wahnschaffe. Ueber das Alter des
Torflagers von Launburg an der Elbe. 8vo. Stuttgart, 1889.

Curie, J., et G. Flamand. Etude succincte sur les roches éruptives
de ’Algérie. 8vo. Algers? 1889.

Dall, W. H. See Snrtats. Washington. Smithsonian Institute.
Dana, E. 8. See Dana, J. D.

Dana, J. D. On the Volcanoes and Volcanic Phenomena of the
Hawaiian Islands. With a paper on the Petrography of the
Islands by E. 8. Dana. 8vo. New Haven, 1887-89.

Areas of continental progress in North America, and the
influence of the conditions of these areas on the work carried
forward within them. S8vo. 1890.

——, Archean Axes of Eastern North America. 8vo. New
Haven, 1890.

Characteristics of Volcanoes, with contributions of facts and
principles from the Hawaiian Islands. 8vo. London, 1890.

—. Corals and Coral Islands. 3rd edition. 8vo. New York,
1890.

ADDITIONS TO THE LIBRARY. 193

Dana, J. D. Sedgwick and Murchison; Cambrian and Silurian.
8vo. New Haven, 1890.

Danube, European Commission of the. Mémoire sur les travaux
d’amélioration du cours du Bas-Danube exécutés pendant la
période 1873-1886 par la Commission Européenne instituée en
vertu de Varticle 16 du traité de Paris du 30 Mars 1856. Text.
Ato. Galatz, 1888. Atlas. Fol. Leipzig, 1887. Presented
through the Foreign Office by direction of the Marquis of Salisbury.

Darton, N. H. On the occurrence of Basalt Dikes in the Upper
Paleozoic series in Central Appalachian Virginia ; with notes on
the Petrography by J. S. Diller. 8vo. New Haven, Conn.,
1890.

Dautzenberg. See Dollfus, G.
David, T. W. E. See New South Wales. Australian Museum.

Davis, W. M. The Physical Features of New England. 4to.
Cambridge, Mass. 1888. Presented by W. Whitaker, Esq.,
He Sa, SC.

Geographic Methods in Geologic Investigation. 8vo. Wash-
ington, 1888.

The Rivers and Valleys of Pennsylvania. 8yvo. Washing-
ton, 1889.

Davis, W. M. The structure of the Triassic Formation of the Con-
necticut Valley. 8vo. Washington, 1889.

. Topographic Development of the Triassic Formation of the
Connecticut Valley. 8vo. New Haven, 1889.

Structure and origin of Glacial Sand Plains. 8vo. Wash-.
ington, 1890.

and J. W. Wood, Jr. The geographic development of Northern
New Jersey. 8vo. Boston, 1889.

Dawson, G. M. Glaciation of High Points in the Southern Interior
of British Columbia. 8vo. London, 1889.

On the Earlier Cretaceous Rocks of the North-western
portion of the Dominion of Canada. 8vo. New Haven, 1889.

——. On some of the larger unexplored regions of Canada. S8vo
Ottawa, 1890.

and F. D. Adams. Notes on the Ore-Deposit of the Treadwell
Mine, Alaska, by G. M. Dawson ; On the Microscopical Character
of the Ore of the Treadwell Mine, Alaska, by F. D. Adams. 8vyo.
Minneapolis, 1889,

194 ADDITIONS TO THE LIBRARY.

Dawson, Sir J. W. The Geological History of Plants. 8vo.
London, 1888. Purchased.

ia isbas Sir J. W. New species of Fossil Sponges from the Siluro-
Cambrian at Little Metis, on the Lower St. Lawrence, with Notes
by Dr. G. J. Hinde. Ato. Montreal, 1889.

On Fossil Plants from the Mackenzie and Bow Rivers. 4to.
Montreal, 1889.

Note on the Fossil Fish and Marine Worm found in the
Pleistocene nodules of Green’s Creek, on the Ottawa. §8vo.
Montreal, 1890.

On new plants from the Erian and Carboniferous, and on
the characters and affinities of Palzozoic Gymnosperms, $8yo.
Montreal, 1890.

and D. P. Penhallow. On the Pleistocene Flora of Canada.
8vo. Washington, 1890.

Deane, G. The Geology and Travels of Jean André de Luc. 8vo.
Birmingham, 1889. |

Delafond. See France.

Delgado, J. F. N. FRelatorio acerca da decima sessio do Congresso
Internacional de Anthropologia e Archeologia Prehistoricas. 4to.
Lisbon, 1890.

Derby, O. A. Os picos altos do Brazil. 8vo. Rio de Janeiro,
1889.

==) S96 a0 Pawo,

Dewalque, G. Compte-rendu de la Session Extraordinaire de la
Société Géologique de Belgique a Spa en 1886. 8vo. Liége,
1888.

Préparations microscopiques de calcaires oolithiques des
systémes dévonien et carbonifére de la Belgique. 8vo. Liége,

1888.

——. Rapport sur le travail des MM. J. Fraipont et F. Tihon.
Explorations scientifiques des cavernes de la Méhaigne. I. La
grotte du Docteur. 8vo. Brussels, 1888.

——. Sur quelques dépdts tertiaires des environs de Spa. 8vo.
Liége, 1888.

Diller, J. S. Geology of the Lassen Peak District. 8vo. Wash-
ington, 1889.

Mineralogical Notes. 8vo. New Haven, Conn., 1889.
——. Sandstone Dikes. 8vo. Washington, 1890.
=, See Darton, Nooo.

ADDITIONS TO THE LIBRARY. I95

Dollfus, G. Observations critiques sur la classification des Polypiers
paléozoiques. 4to. Paris, 1875.

Note sur une nouvelle coupe observée a Rilly-la~-Montagne,
prés Reims. 8vo. Lille, 1876.

Description et classification des dépots tertiaires des environs
de Dieppe. 8vo. Lille, 1876.

Bryozoaire nouveau du terrain dévonien du Cotentin. Tere-
bripora capillaris. 8vo, Caen, 1877.

Contributions 4 la Faune des Marnes blanches supérieures
au Gypse. 8vo. Paris, 1877.

Valvatu disjuncta. Espéce nouvelle des Meuliéres supé-
rieures des environs de Paris. 8vo. . Brussels, 1877.

——. les suables de Sinceny. 8vo. Paris, 1878,

. Observations sur le sondage de Monsoult (Seine-et-Oise).
8vo. Paris, 1878.

——. Les dépéts quaternaires du Bussin de la Seine. 8vo. Paris,

A

Contribution a la stratigraphie parisienne; Les sables
moyen parisiens dits de Beauchamp. 8vo. Paris, 1879.

Essai sur l’extension des terrains tertiaires dans le bassin
anglo-parisien. 8vo. Le Havre, 1880.

Notes géologiques sur le nouveau chemin de fer de Beau-
mont-sur-Oise 4 Hermes. 8vo. Paris, 1880.

Essai sur la détermination de lage du soulévement du pays
eo bray. Svo. Paris, 1881.

. Découverte de la dolomie dans les sables parisiens moyens.
Svo. Paris, 1881.

——. Kssai sur la Nomenclature des Ktres organisés. 8vo. Paris,
1882.

——. Liste des coquilles marines recueillies 4 Palavas, 4to. Paris,
1883.

——. Nomenclature critique du Trophon antiquus. 8vo. Brussels,

1883.

. Lo terrain quaternaire d’Ostende et le Corbicula fluminalis.
8vo. Brussels, 1884.

——. Quelques nouveaux gisements de terrain tertiaire dans le
Jura, pres de Pontarlier. 8vo. Paris, 1887.

Coquilles nouvelles ou mal connues du Sud-Ouest. Fasc. 1
eb 2. 8yo, Dax, 1887 & 1889,

196 ADDITIONS TO THE LIBRARY.

Dollfus, G. Revue du terrain quaternaire (Annuaire géologique
universel, Tome iii.). S8vo. Paris, 1888.
( Tome iv.) 8vo. Paris, 1889.

Notice sur une nouvelle carte géologique des environs de
Paris. 4to. Berlin, 1888.

Revue des animaux inférieurs, Bryozoaires Anthozoaires,
Foraminiféres, Spongiaires, Radiolaires, pour 1887. (Annuaire
géologique universel, Tome iv.) 8vo. Paris, 1889.

—— et Dautzenberg, P. Etude préliminaire des coquilles fossiles
des faluns dela Touraine. 4to. Paris, 1886.

Description de coquilles nouvelles des faluns de la
Touraine. 8vo. Paris, 1888.

et Ramond. Bibliographie de la Conchyliologie du terrain
tertiaire parisien. 8yo. Paris, 1886.

et G. Vasseur. Coupe Géologique de chemin de fer de Mery-
sur-Oise, entre Bessancourt et Valmondais. §vo. Paris, 1878.

—. See Bucquoy and Ortlieb, J.

Duncan, P. Martin, and W. Percy Sladen. A Note upon the Ana-
tomy of the Perignathic Girdle of Discordea cylindrica, Link., sp.,
and of a Species of Hchinoconus. 8vo. London, 1889.

Dujardin-Beaumetz, F. Histoire graphique de 1 Industrie Houillére
en Belgique depuis 1865. Fol. Paris, 1888. Presented by Dr.
C. Le Neve Foster, F.GS.

Histoire graphique de l’Industrie Houillére en France de-
puis 1865. Fol. Paris, 1888. Presented by Dr. C. Le Neve
Foster, F.GS.

Dunker, W. Ueber den norddeutschen sogenannten Walderthon
und dessen Versteinerungen. (Programme der hoheren Gewerb-
schule in Cassel 1843-1844.) 4to. Cassel, 1843. Presented
by C. Davies Sherborn, Esq., P.GS. }

Dunsford, H. A. H. The opening of the Arctic Sea. 8vo. London,
1890.
Edwards, H. See Sertats. Washington. Smithsonian Institute.

Egleston, T. See Sertats. Washington. Smithsonian Institute.
Etheridge, Jun., R. See Australian Museum.

England and Wales. Geological Survey. Memoirs. The Geology
of the Isle of Wight, by H. W. Bristow. Second edition, revised
and enlarged by C. Reid and A. Strahan. 8vo. London, 1889.

. The Geology of the Cheviot Hills (English
side), by oO. T. Clough. 8vo. London, 1888.

ADDITIONS TO THE LIBRARY. 197

England and Wales. Geological Survey. Memoirs. The Geology
of Plashetts and Kielder, by C. T. Clough. 8vo. London, 1889.

——. The Geology of the country around Kast
Dereham, by J. H. Blake. 8vo. London, 1888.

——. Guide to the Geology of London and the
neighbourhood, by W. Whitaker. 5th edition. 8vo. London,
1889.

——. The Geology of the country near Yarmouth
and Lowestoft (Explanation of Sheet 67), by J. H. Blake. 8vo.
London, 1890.

——_,,

——. Geology of London poe of part of the
Thames Valley (Explanation of Sheets 1, 2, and 7), by W.
Whitaker. 2 vols. 8vo. London, 1889.

Exhibition of 1851. Seventh Report of the Commissioners for the
Exhibition of 1851 to the Right Hon. Henry Matthews. 8vo.
London, 1889. Presented by Her Majesty’s Commissioners for the
Exhibition of 1851.

, 1888. Melbourne Centennial International Exhibition, 1888.
New South Wales Mineral Court. Descriptive Catalogue of
Exhibits of Metals, Minerals, Fossils, and Timbers (Government
aud Private). 8vo. Sydney, 1889. Presented by the Hon. The
Minister for Mines, New South Wales.

, 1889. Republica Argentina (Comisién Central de Minas).
Catalogo Oficial de las Muestras de Minerales exhibidas en la
Seccién Argentina, anexa 4 la Exposicion de Paris, 1889. 4to.
Buenos Aires, 1889. Presented by H. D. Hoskold, Esq., F.GS.

Exposition de Paris de 1889. République Argentine. See
Hoskold, H. D.

Eyerman, J. Notes on Geology and Mineralogy. 8vo. Phila-
delphia, 1889.

——. The Mineralogy of Pennsylvania. Part 1. S8vo. Easton,
1889.

Feilden, Colonel H. W. On the Birds of Barbados. 8vo. London,
1889.

Feistmantel, O. Uebersichtliche Darstellung der geologisch-palzon-
tologischen Verhaltnisse Stud-Afrikas. Theil I. Die Karoo-
Formation und die dieselbe unterlagernden Schichten. 4to.
Prague, 1889.

Felix, J., und H. Lenk. Beitriige zur Geologie und Paliontologie
der Republik Mexico. TheilI. 4to. Leipzig, 1890.

Purchased.

198 ADDITIONS TO THE LIBRARY.

Finland. Finlands Geologiska Undersékning. Beskrifning till
Kartbladen Nos. 12-15. 8vo. Helsingfors, 1888. 3

Fisher, O. Physics of the Earth’s Crust. 2nd edition. 8vo,
London, 1889. Purchased.

Foord, A. H., & G. C. Crick. On the Muscular Impressions of

Celonautilus cariniferus, J. de C. Sowerby, sp., compared with
those of the Recent Nautilus. 8vo. London, 1889.

Fornasim, Carlo. Foraminiferi Miocenici di San Rufillo. 4to.
Bologna, 1889.

Minute forme di Rizopodi reticolari nella marna pliocenica

del Ponticello di Savena, presso Bologna. 8vo. Bologna, 1889.

Contributo alla conoscenza della Microfauna Terziaria
Italiana. Lagenidi Pliocenica del Catanzarese. 4to. Bologna,

1890.
Foraminiferi di Roccantica in Sabina. 8yvo. Rome, 1890.

Fortwr, H. Contributions a l'étude dusysteme crétacé de la Belgique.
8vo. Liége, 1889.

Foster, C. Le Neve. See Great Britain and Ireland.

France. Ministére des Travaux Publics. Carte Géologique de la
France et des Topographies Souterraines. Bulletin. 8vo. Paris,
1889. Purchased.

. No. 1. Etude sur le massif cristallin du
Mont- Pilat, par M. Termier. 8vo. Paris, 1839.

; . No. 2. Note sur les terrains d’alluvions
des environs de Lyon, par M. Delafond. 8vo. Paris, 1889.

: No. 3. Note sur )Existence de Phénoménes
des Recouvrement dans les Pyrénées de Aude. 8yvo. Paris,
1889.

: ‘ . No. 4. Note sur les Roches Primitives de
la feuille de Brives. S8vo. Paris, 1889.

No. 5. Notes stratigraphiques sur le bassin
tertiaire de Marseille, par C. Depéret. 8vo. Paris, 1889.

No. 6. Note sur la géologie des environs
d’Annecy, ike Roche, Bonneville, &c., par G. “Maillard. 8v0.
Paris, 1889. Purchased.

; No. 7. Mémoire sur les éruptions dia-
basiques siluriennes du Menez-Hom, Finistére, par C. Barrois.
8vo. Paris, 1890. Purchased.

Ministere des Travaux Publics. Etudes des Gites Minéraux
de la France. Bassin Houiller et Permien d’Autain et d’Epinac.
pee he 1, Stratigraphie, par Delafond, avec une carte géologique
au zyhpy par Michel-Lévy, Delafond et Renault, to. Paris,

Z000
89.

—
.

——, _— — —. ———_ ——_... Purchased,

ADDITIONS TO THE LIBRARY. 199

Franchi, S. Anomalie della declinazione magnetica in rapporto con
erandi masse serpentinose. 8vo. Rome, 1889.

Francke, H. H. A. Ueber die mineralogische Nomenclatur. 8vo.
Berlin, 1890. Purchased.

Frantzen, W.,und A. v. Koenen. Ueber die Gliederung des Wellen-
kalks in mittleren und nordwestlichen Deutschland. 8vo. Ber-
lin, 1889,

Fritel, P. See Lapparent, A. de.

Fritsch, A. Fauna der Gaskohle und der Kalksteine der Permfor-
mation Bohmens. Band ii. Heft 4. 4to. Prague, 1889.

Galloway, W. Report upon the Coal-deposits in the Indwe Basin
and Stormberg Range of Mountains, Cape of Good Hope. 4to.
Cape Town, 1889.

Gaudry, A. Restauration du squelette du Dinoceras 4to. Paris,
1889.

——. Le Dryopithéque. 4to. Paris, 1890.

Geikie, A. Outlines of Field Geology. 8vo. London, 1889.
Purchased.

Geinitz, H. B. XIV Kupfertafeln zu Darstellung der Flora des
Hainichen-Ebersdorfer und des Flohaer Kohlenbassins. Fol.
Leipzig, 1854. Presented by the Royal Astronomical Society.

Ueber die rothen und bunten Mergel der oberen Dyas bei
Manchester. 8vo. Dresden, 1889.

Gilliéron, V. Note sur ’achévement de la premiére carte géologique
de la Suisse 4 grande échelle. 8vo. Brussels, 1889.

Gilpin, E., Jun. Coal Mining in Nova Scotia. 8vo. Montreal,
1889.

The geological relations of the principal Nova Scotia
Minerals. &vo. , 1890 ?

Goldschmidt, V. Index der Krystallformen der Mineralien. Band 2.
Hefte 6 & 7. 8vo. Berlin, 1890. Purchased.

Gordon, H. A. A Miners’ Guide. 8vo. Wellington, N.Z. 1889.

' Gossclet, J. Considérations sur le Bief 4 silex de lArtois. 8vo.
Lille, 1890.

——. Les Demoiselles de Lihus. 8vo. Lille, 1890.

Relations entre les sables de l’éocéne inférieur dans le nord
de la France et dans le Bassin de Paris. 8vo. Paris, 1890.

Great Britain and Ireland. Mineral Statistics of the United King-
dom of Great Britain’ and Ireland, with the Isle of Man, tor the
year 1888. 4to. London, 1889. Presented by the Secretary of
State for the Home Department. ;

VOL. XLVI. p

200 ADDITIONS TO THE LIBRARY.

Great Britain and Ireland. List of Mines worked in the year
1888. 4to. ° London, 1889.

—. ——. ——. Presented by Dr. C. Le Neve Foster, F.GNS.

List of the Plans of Abandoned Mines deposited in the
Home Office, under the Coal and Metalliferous Mines Regulation
Acts. Corrected to the 30th June, 1889. 4to. London, 1889.

—-, -——. ——. Presented by Dr. C. Le Neve Foster, F.GN.

Report of C. Le Neve Foster, H.M. Inspector of Mines for
the North Wales, &c., and Isle-of-Man District (No. 9), to Her
Majesty’s Secretary of State, for the year 1888. 4to. London,
1889.

Greenland. Meddelelser om Gronland, udgivne af Commissionen
for Ledelsen af de geologiske og geographiske Underségelser i
Gronland. 3 Hefte. Fortscettelse II. 8vo. Copenhagen, 1888.
Purchased.

——. ——. 8 Hefte. 8vo. Copenhagen, 1889. Purchased.
——-, ——. 13 Hefte. 8vo. Copenhagen, 1890. Purchased.

Gregorio, Marquis Antoine de. Annales de Géologie et de Paléon-
tologie. 6° Livraison. 4to. Palermo, 1889.

Groth. Ueber die Molekularbeschaffenheit der Krystalle. 4to.
Munich. 1888. Presented by the K.b. Akademie der W assenschif -

ten zu Minchen.

Gimbel, C. W. von. Die mineralogisch-geologische Beschaffenheit
der auf der’ Forschungsreise S.M.S. “ Gazelle”? gesammelten
Meeresgrund-Ablagerungen. 4to. Berlin, 1890.

Geologische Bemerkungen tber die warmen Quellen yon
Gastein und ihre Umgebung. 8vo. Munich, 1890.

Hackel, E. Natiirliche Schopfungs-Geschichte. 8vo. Berlin,
1889. Purchased.

Harker, A. The Bala Voleanic Series of Caernarvonshire and
associated rocks. - 8vo. Cambridge, 1889.

Harris, G. F. Notes on the Geology of the Gironde, with especial
reference to the Miocene Beds. 8yvo. London, 1890.

Harrison, J. The Geology of London. 8vo. 1889.

Harrison, J. Thornhill, On the Creation and Physical Structure of
the Earth. 8vo. London, 1889.

Harrison, W. J. Notes upon a proposed Photographic Survey of
Warwickshire. 8vo. Birmingham, 1890.

ADDITIONS TO THE LIBRARY. 201
Hébert, E. Le Terrain Crétacé Supérieur (suite). 8vo. Paris,
1888. Presented by his Executors.

——. Remarques sur la zone a Belemnitella plena. S8vo. Faris,

1888.

Remarques sur la découverte, faite par M. Bergeron, de la
faune primordiale en France. 4to. Paris, 1888.

Hector, Sir James. Phormium tenax as a Fibrous Plant. Second
edition. 8vo. Wellington, N.Z., 1889.

Heilprin, A. The Bermuda Islands. 8vo. Philadelphia, 1839.
Purchased.

Henry, James. Aeneidea, or critical, exegetical, and aesthetical

remarks on the Aeneis. Vol. 8. 8vo. Dublin, 1881, 1882,
1889. Presented by his Executors.

oo, Vol. 4. 8vo. Dublin, 1889.

Hill, R. T. Check-list of the Invertebrate Fossils from the Cre-
- taceous Formations of Texas. S8vo. Austin, Texas, 1889.

Paleontology of the Cretaceous Formations of Texas. Part 1.
S8vo. Austin, Texas, 1889.

. Relation of the Uppermost Cretaceous Beds of the Eastern
and Southern United States. 8vo. New Haven, 1889.

The Foraminiferal Origin of certain Cretaceous Limestones,
and the sequence of Sediments in North-American Cretaceous.
8vo. Minneapolis, 1889.

. The Neozoic Geology of South-western Arkansas. [Notice
of.| S8vo. Minneapolis, 1889.

Hinde, G. J. On a new Genus of Siliceous Sponges from the
Lower Calcareous Grit of Yorkshire. S8vo. London, 1890.

On a true Leuconid Calcisponge from the Middle Lias of
Northamptonshire, and on detached Calcisponge Spicules in the
Upper Chalk of Surrey. 8vo. London, 1889.

See H. Van Cappelle, Jr.
Holmes, W. H. See Purtopicats. Washington.

Hoskold, H. D. Mémoire Général et Spécial sur les Mines, la
métallurgie, les lois sur les mines, les ressources, les avantages,
ete., de l’exploitation des Mines dans la République Argentine,
8vo. Buenos Aires, 1889. (Exposition de Paris de 1889.)

Hull, H, A sketch of Geological History, being the Natural History
of the Earth and of its Pre-Human Inhabitants. Syvo. London
1887.

——. Memoir on the Geology and Geography of Arabia Petrea,
Palestine, and adjoining districts. 4to. London, 1889.

p2

’

202 ADDITIONS TO THE LIBRARY.

Hutton, F. W. On the Rocks of the Hauraki Gold-Fields. Sydney,
1888. a :

India. Geological Survey. Memoirs. Palewontologia Indica. Ser.
XII. Salt-range Fossils. Vol.iv. Part 1. Geological Results,
by W. Waagen. 4to. Calcutta, 1889.

———, = Records Volley Part 2) alissee.
Vio ea ee eine lee
SS Vol eoan eee ache ool:

Issel, A. Dei noduli a radiolarie di Cassagna e delle roccie silicee e
manganesifere che vi si connettono. 8vo. Genoa, 1890.

——. II calcifero fossilifero di Rovegno. S8vo. Genoa, 1890.

Italy. Ministero di Agricoltura, Industria e Commercio. Direzione
Generale dell’ Agricoltura. Annali di Agricoltura, 1888. Ri-
vista del Servizio Minerario nel 1886. 8vo. Rome, 1888. Pre-
sented by H. Bauerman, Esq., P.G.S.

——__—_

: Rivista del Servizio Minerario nel
1se8. “Svox lh lorence, 1899. Presented by H. Bauerman, Esq.,
EGS.

: ; : . 1889. Rivista del Servizio Mine-
rario nel 1887. 8vo. Florence, 1889. Presented by H. Bauer-
man, Esq., L.GS.

- ———,- 1889. Sui combustinili tessa
importati in Italia, di L. Mazzuoli. 8vo. Rome, 1889. Pre-
sented by H. Bawa Esq., £.GS.

Jack, R.L. On some Salient Points in the Geology of Queensland,
8vo. Sydney, 1888.

—-. See Queensland.

———-, —_—-,.

James,J. #,. Remarks upon Sedimentation in the Cincinnati Group.
8vo. Cincinnati, 1889.

Jeffs, O. W. Geological Photography. 8vo. Liverpool, 1889.
Presented by W. Whitaker, Esq., F.RS., F.GS.

Jentzsch, A. Oxford in Ostpreussen. 8vo. Berlin, 1889,

Jones, T. Iiupert. Notes on the Paleozoic Bivalved Entomostraca.
No, xxviii. On some Scandinavian Species. 8vo. London, 1889.

---—. On some Paleozoic Ostracoda from Pennsylvania, U.S. 8vo.
Minneapolis, 1839.

Seventh Report of the Committee, consisting of Mr. R.
Etheridge, Dr. H. Woodward, and Professor T. Rupert Jones
(Secretary), on the Fossil Phyllopoda of the Paleozoic Rocks,
1889. 8vo. London, 1889.

ADDITIONS TO THE LIBRARY. 203

Jones, T. Rupert. On some Paleozoic Ostracoda from North
America, Wales, and Ireland. 8vo. London, 1890.

,and G. J. Hinde. A supplementary monograph of the Cre-
taceous Entomostraca of England and Ireland. 4to. London,
1890.

,and J. W. Kirkby. On some Ostracoda from the Mabou
Coal-field, Inverness Co., Cape Breton (Nova Scotia). 8vo.
London, 1889.

, and H. Woodward. On some new Devonian Fossils. S8vo.
London, 1889.

Klement, C. Les Puits Artésiens de Willebroeck. 8vo. Brussels,
1889.

imioos, J. H., und Max Miiller. Die Hermannshdhle bei Riibeland.
Text und Tafeln. 4to. Weimar, 1889. Purchased.

Koenen, A. von. Sur une faune paléocéne de Copenhague. 8vo.
Liege, 1888. Presented by Prof. G. Dewalque, P.M.GS.

Ueber die Ergebnisse der geologischen Aufnahme der Um-
gegend von Gottingen. 8vo. Gottingen, 1889.

——. Ueber Dislokationen auf Riigen. 8vo. Berlin, 1889.

Das Norddeutsche Unter-Oligocin und seine | Mollusken-
Fauna. Lief. 2. S8vo. Berlin, 1890.

—-. See Frantzen, W.

Kokscharow, N. von. Materialien zur Mineralogie Russlands.
Band 10, pp. 97-224. 1889.

Lapparent, A.de. Note sur le role des agents minéralisateurs dans
la formation des roches éruptives. 8vo. Paris, 1889.

——. Cours de Minéralogie. 2° édition. 8vo. Paris, 1890.

La nature des mouvements de l’écorce terrestre. Svo.
Brussels, 1890.

, et P. Fritel. Fossiles Charactéristiques des Terrains Sédi-
mentaires. Fossiles Primaires. 4to. Paris, 1886.

—— ——_, ——.. Fossiles Secondaires. 4to. Paris, 1888.
— ——. ——. Fossiles Tertiaires. 4to. Paris, 1886.

Laspeyres, H. Heinrich von Dechen. Ein Lebensbild. 8vo. Bonn,
1889.

Lefevre, Th. A propos de la nouvelle organisation des services de
la Carte Géologique. 8vo. Brussels, 1890.

Note préliminaire sur les restes de Siréniens recueillis en
Belgique. 8vo, 1889.

204 ADDITIONS TO THE LIBRARY.

Lendenfeld, Robert von. A monograph of the Horny Spence 4to.
London, 1889. Pr esented by the Royal Society.

Lévy, A. Michel, et A. Lacroix. Tableau des Minéraux des Roches.
Ato. Paris, 1889. Purchased.

Lindstrom, G. The Ascoceratide and the Lituitide of the Upper
Silurian Formation of Gotland. 4to. Stockholm, 1890.

List, J. A new measure for Old Time. 8vo. Newport, I.W.
1889,

Lobley, J. Logan. Mount Vesuvius. A descriptive, historical, and
geological account of the Volcano and its surroundings. vo.
London, 1889. Purchased.

Loewinson-Lessing, F. Die Olenezer Diabasformation. 8yvo. St.
Petersburg, 1888.

Loriol, P. de. Note sur deux Echinodermes nouveaux. S8vo. Paris,
1889. .

Lory, Charles. Description géologique du Dauphiné (Isére, Drome,
Hautes-Alpes) pour servir 4 l’explication de la Carte Géologique
de cette province. 8vo. Paris, 1864. Purchased.

M'Gee, W. J. Classification of geographic forms by Genesis. 8vo.
Washington, 1888. Presented by W. Whitaker, Esq., F.AS.,
GS:

Paleolithic Man in America; his antiquity and environ-

ment. 8vo. New York, 1888. Presented by W. Whitaker,

sq., F.RS., GS.

Marcou, J. Les géologues et la géologie du Jura jusqu’ en 1870.
S8vo. Lons-le-Saunier, 1889.

Zarsh, O. C. Discovery of Cretaceous Mammalia. Parts 1 & 2.
8vo. New Haven, 1889.

——. The Skull of the Gigantic Ceratopside. S8vo. New Haven,
1889.

Notice of gigantic Horned Dinosauria from the Cretaceous.
8vo. New Haven, 1889,

——. Additional characters of the Ceratopside, with notice of
new Cretaceous Dinosaurs. 8vo. New Haven, 1890.

Description of new WDinosaurian Reptiles. 8vo. New
Haven, 1890.

Distinctive characters of the order Hallopoda. S8vo. New
Haven, 1390.

Mayer-Eymar, C. Tableau des terrains de sédiment. 8vo. Agram,
1889. Presented by W. Whitaker, Esq., F.BRS., PGS.

—. Ueber das Tongrian von Cairo (Egypten). 8vo. Zurich,
1889. Presented by W. Whitaker, Esq., F.RS., PGS.

ADDITIONS TO THE LIBRARY. 205

Mazzuoli, L. See Italy.

Mei, R. Castor fiber, Lin.,, Ursus spelaeus, Blum., Canis lupus,
Lin., fossili nelle ghiaie quaternarie della valle del Tevere. 8vo.
Rome, 1889.

Sul rinvenimento dei resti fossili di un grande avvoltoio
racchiuso nel peperino Laziale. Svo. Rome, 1889.

Mello, J. Magens. The Dawn of Metallurgy. 8vo. London, 1889.

Miller, S. A. North-American Geology and Paleontology. 8vo.
Cincinnati, Ohio, 1889. (Dulau.) Purchased.

Minnesota. Geological and Natural History Survey. N. H.
Winchell, State Geologist. 16th Annual Report, for the year
1887. 8vo. Minneapolis, 1888.

; 17th Annual Report. NW. A. Winchell, State
Geologist. 8vo. St. Paul, Minn., 15389,

Bulletin, Nos. 1 and 3. 8vo. St. Paul, Minn.,

—— oe

1889.

Morgan, C. Lloyd. The Geology of Tytherington and Grovesend.
8vo. Bristol, 1889. :

Moro, G. Dal Lido di Venezia al tempio di Serapide in Pozzuolli.
8vo. Venice, 1889.

Musée Teyler. See Winkler, T. C.

Nathorst, A. G. Sur la présence du genre Dictyozamites, Oldham,

dans les couches jurassiques de Bornholm. 8vo. Copenhagen,
1889.

—. bBeitrige zur mesozoischen Flora Japans. 4to. Vienna,
1890.

Jordens Historia efter M. Neumayrs Erdgeschichte utar-
betad med siirskild hinsyn till Nordens Urverld. Hatt 4-5.
8yo. Stockholm, 1890.

Linnés iakttagelser dfver strandlinier vid gransen mellan
Sverige och Norge. 8vo. Stockholm, 1890.

—. Melchior Neumayr. 8vo. Stockholm, 1890.

Nagra reffelobservationer itrakten af Omberg. 8vo. Stock-
holm, 1890.

—. Ueber die Reste eines Brotfruchtbaums, Artocarpus Dicksoni,
n. sp., aus den Cenomanen Kreideablagerungen Gronlands. 4to.
Stockholm, 1890.

Newmayr, M. Ketten- und Massengebirge. Svo. Munich 1888,

——. Calostylis und die perforaten Hexacorallier. €vo, Vienna,
889.

206 ADDITIONS TO THE LIBRARY.

Newmayr, M. Die klimatischen Verhiltnisse der Vorzeit.
Vienna, 1889.

——. Hyopotamusreste von Eggenburg. 8vo. Vienna, 1888.
——. Ueber Bergstiirze. S8vo. Vienna, 1889.
-——. Ueber die Herkunft der Unioniden. 8vo. Vienna, 1889.

Ueber einige Belemniten aus Centralasien und Sidafrika
und tiber den Canal der Belemniten. 8vo. Vienna, 1889.

New Jersey. Geological Survey. Annual Report of the State
Geologist for the year 1888. 8vo. Camden, N.J., 1889.

Final Report of the State Geologist. Vol. 1. Topo-
eraphy , Magnetism, Climate. 8vo. ‘Trenton, N.J., 1888.

New South Wales. Australian Museum. Memoirs, No. 2. Lord-
Howe Island, its Zoology, Geology, and Physical Characters, by
R. Etheridge, jun., A. J. North, J. D. Ogilby, A. 8. Olliff, and
T. W. E. David. 8vo. Sydney, 1889. Presented by A. J. Jukes-
Browne, Esq., L.GS.

———, =, Records. Volt." No, 1. S590)

—. ——. Report of Trustees for the year 1888. 4to. Sydney,
1889.

. Department of Mines. Annual Report for the year 1888.
Ato. Sydney, 18389.

Geological Survey of New South Wales. Memoirs.
Paleontology. No. 2. Contributions to the Tertiary Flora of
Australia, by Constantin Baron von Ettingshausen. 4to, Syd-
ney, 1888.

i ~ ——,. Records.« Vol. 1. Parts 1 & 22 dese
8vo. Sydney, 1889.

Newton, EH. T. A contribution to the History of Eocene Siluroid
Fishes. 8vo. London, 1889.

New York. Geological Survey. Natural History of New York.
Paleontology. Vol. vii. ‘Trilobites and other Crustacea, by
James Hall, assisted by G. B. Simpson. With Supplement to
Vol. v. Part 2. Pteropoda, Cephalopoda, and Annelida. By
James Hall. 4to. Albany, 1888. Presented by the Regents of
the University of the State of New York,

—. State Library. 70th and 71st Annual Reports of the
Trustees for the years 1887 and 1888. 8yo. Albany, 1888-89.

State Museum of Natural History. 40th and 41st Annual
Reports of the Trustees for the years 1886 and 1887. 8vo.
Albany, 1887 and 1888,

ADDITIONS TO THE LIBRARY. 207

New York. State Museum of Natural History. 42nd Annual
Report of the Trustees, for the year 1888. 8vo. Albany, 1889.

. Bulletin. Vol.i. Nos. 2-6. 8vo. Albany, 1887-
88. Presented by the Trustees.

New Zealand. Colonial Museum and Geological Survey. (Sir James
Hector, K.C.M.G., Director.) Reports of Geological Explorations
during 1887-88. 8vo. Wellington, N.Z., 1838.

: . 2drd Annual Report on the Colonial Museum and
Laboratory. 1887-88. 8vo. Wellington, N.Z., 1889.

See Hector, Sir James.

Department of Mines. Report on the Mining Industry.
Ato. Wellington, 1889.

: Reports on Mining Machinery and Treatment of
- Ores in Australian Colonies and America. 4to. Wellington,
1889.

Nicaragua. Sce Costa Rica.

Nicholson, Henry Alleyne, and Richard Lydekker. A Manual of
_ Paleontology for the use of Students. 3rdedition. Vols.1.&u.
Svo. London, 1889.

Noé, Franz. Erlauterungen zu der geologischen Uebersichtskarte der
Alpen. 8vo. Vienna, 1890. Purchased. (See Maps.)

North, A. J. See New South Wales. Australian Museum.

Norwegian North-Atlantic Expedition. Norske Nordhavs-Expedi-
tion, 1876-78. Presented by the Meteorologiske Institut, Christi-
ania. XIX. Zoologi. Actinida ved D. C. Danielssen. Ato,
Christiania, 1890.

Nova Scotia. Department of Mines. Report for the year 1889.
Syo. Halifax, 1890. Presented by EL. Gilpin, Esq., F.GS.

@hlert, D. P. Molluscoides-Brachiopodes. [Annuaire Géologique
Universel, 1888.] S8vo. Paris, 1889.

Notes sur les terrains paléozoiques des environs d’EKaux-
Bonnes. 8vo. Paris, 1889.

. Sur la constitution du silurien dans la partie orientale du
départment de la Mayenne. Ato. Paris, 1889,

——. Sur le Dévonien des environs d’Angers. 8vo. Paris, 1890.
Ogilby, J. D. See New South Wales, Australian Museum.
Olliff, A. 8. . See New South Wales, Australian Museum.

Ormerod, G. W. Annals of the Teignbridge Cricket Cub, 1823-83,
tto. Teignmouth], 1889,

208 ADDITIONS TO THE LIBRARY.

Ortlieb, J., et Dollfus, G. Compte-rendu de l’excursion de la Société
Malacologique de Belgique dans le Limbourg belge, Mai 1873.
8vo. Brussels, 1873.

Paléontologie Frangaise. Série 1. Animaux Invertébrés. Ter-
rains Tertiaires. lLivr.18. Eocene, Echinides. Tome ii., par G.
Cotteau. S8vo. Paris, 1889. Purchased.

-- Animaux Fossiles. Terrains Tertiaires. Livr. 19.
Eocéne, Echinides. ‘Tome ii., par G. Cotteau. 8vo. Paris,
1890. Purchased.

: : Livr. 20. Eocéne, Echinides.
Tome ii., par G. Cotteau. 8vo. Paris, 1890. Purchased.

. Terrain Jurassique. Livr. 89, Crinoides,
par de Loriol. 8vo. Paris, 1889. Purchased.

Série 2. Végétaux. Terrain Jurassique. Livr.41. Ephé-
drées; Spirangi¢es et Types proangiospermiques, par le Marquis
G. de Saporta. S8vo. Paris, 1889. Purchased.

Livr. 42. Ephédrées ; Spirangiées
et Types proangiospermiques, par le MarquisG. deSaporta. 8vo.
Paris, 1890. Purchased.

Pennsylvania. Geological Survey. Annual Report for 1887.
8vo. Harrisburg, 1889.

. ——. D Reports. South Mountain Map, Sheets, C
and D,, ,,,.;, ovo. Harrisburg, 1839 ?

P, Report. A Directory of the Fossils of Pennsyl-
vania and neighbouring States named in the Reports and Cata-
logues of the Survey. 8vo. Harrisburg, 1889.

. AA. Atlas. astern Middle Anthracite Field.
Part iii. 8vo. Harrisburg, 1889.

, f Northern Anthracite Field. Parts
iil.—y. Syo. Harrisbure, 1889.

1? 27 39 4?

———_—_—-

——. Southern Anthracite Field. Partii.
Svo. Harrisburg, 1889.

. ——. HHand HHH. Atlas to Reports. 8vo. Harris-
burg, 1889.

} OOO. Catalogue of the Geological Museum. Part
iii. 8vo. Harrisburg, 1889,

Percy, John. Lecture reports, newspaper paragraphs, and tracts on
Chemical Geology, &c. 4to. 1863, &e. Presented by H. Bauer-
man, Esq., F.GS.

Pilling, J.C. See Pertopicats, Washington.

ADDITIONS TO THE LIBRARY. 209

Poole, H. 8. Ice inthe Carboniferous Period. S8vo. Halifax, N.S.
1889,

Portugal. Commissdo dos Trabalhos G'eologicos de Portugal. Com-
municagoes. Tom... Fasc. 1. 1888-89. 1889.

Etude Géologique du Tunnel du Rocio. Contribu-
tion a la connaissance de sous-sol de Lisbonne. Par Paul Choffat.
Avec un article paléontologique par J. C. Berkeley Cotter, et un
article zoologique par A. Girard. 4to. Lisbon, 1889.

Postlethwaite, John. Mines and Mining in the Lake District.
Svo. Leeds, 188Y.

Prestwich, J. On the relation of the Westleton Beds, or Pebbly
Sands, of Suffolk to those of Norfolk, and on their extension
inland. Parts 1-3. 8vo. London, 1890.

Queensland. Albert and Lodan District. Report by W. H. Rands,
Assistant Government Geologist. 4to. Brisbane, 1889.

——. Geological Features and Mineral Resources of the Mackay
District. Report by A. G. Maitland. 4to. Brisbane, 1889.

——. Geological observations at the Heads of the Isaacs, the
Suttor, and the Bowen Rivers. Report by A. G. Maitland. 4to.
Brisbane, 1889.

. Gympie Gold-field. Report by W. H. Rands, Assistant
Government Geologist. 4to. Brisbane, 1889.

Limestone District, Part of the Palmer Gold-field. (Preli-
minary Report by &. L. Jack, Government Geologist, on). to.
Brisbane, 1888.

Report on the Sellheim Silver-mines and surrounding dis-
trict, by &. L. Jack, Government Geologist. 4to. Brisbane,
HSs9.

Report by #. LZ. Jack, Government Geologist, on the Taran-
ganba Gold-mine. 4to. Brisbane, 1889. ;

Quiroga, F. Observaciones geoldgicas hechas en el Sahara occi-
dental. 8vo. Madrid. 1889.

Ramond. See Dolifuss, G.

Reade, T. Mellard. On the advantage to the Civil Engineer of a
study of Geology. 8vo. Liverpool, 1889.

—. Origin of Normal Faults. 8vo. New Haven, Conn.,
1890.

——. Physiography of the Lower Trias. 8vo. London, 1889.

Slickensides and Normal Faults; their characteristics and
cause. Svo. Liverpool, 1839.

210 ADDITIONS TO THE LIBRARY.
Reade, T. Mellard. The New Red Sandstone and the Physio-
graphy of the Triassic Period. 8vo. Birmingham, 1889, |

Cause of the Coloration of Red Sandstone. S8vo. Birm-
ingham, 1890,

Physics of the Earth’s Crust. [Review.] 8vo. Liverpool,

1890.

Reichenbach, O. On some properties of the Earth. 8vo. London,
1880. Presented by A. J. Jukes-Brown, Esq., F.G.S.

Renevier, H. Philippe de la Harpe. Sa vie et ses travaux scien-
tifiques. 8vo. Lausanne, 1889.

Restrepo, Vicente. A study of the Gold- and Silver-mines of
Colombia, March 1884. Translated by C. W. Fisher. 8vo. New
York, 1886. . Presented by H. Bauerman, Esq., F.G.S. Se.

Reusch, Hans. Fjeld- og jordarter i de skandinaviske lande og
Finland. 8vo. Christiania, 1890. (See Mars.)

Reyer, E. Die Skaptar-Eruption, Island, 1783. 4to. Berlin,
1889.

Reynolds’s Geological Atlas of Great Britain. 2nd edition. 8vo.
London, 1889. Presented by Messrs. J. Reynolds & Sons.

Ricciardi, I. Genesi e composizione chimica dei Terreni vuleanici
Italiani. 8vo. Florence, 1889.

Roumania. Biuroulu Geologict. Anuarulu. Anulti 1882-83.
No. 4. 8vo. Bucharest, 1&89.

Russia. Comité Géologique. Bulletin. 1888. Tome vii. Nos.
7-10. 8vo. St. Petersburg, 1888-89.

. . —. 1889. Tome viii. Nos. 1-6. 8vo. St.
Petersburg, 1889.

‘ ‘ Supplément au Tome viii. Bibliothéque
Géologique de la Russie, 1888, composée sous la rédaction de §.
Nikitin. 8vo. St. Petersburg, 1889.

; . Mémoires. Vol. iti, No, 4. 1889. Allgemeine
Geologische Karte von Russland. Blatt 189. Beschreibung des
Central-Urals und des Westabhanges, von T. Tscheryschew.
Ato. St. Petersburg, 1889.

; d Vol. vii. No.1. 1888. Ueber die russ-
ischen Aucellen, von J. Lahausen. 4to. St, Petersburg, 1888.

Sacco, F. Le Ligurien. 8vo. Paris, 1889.

—-—. Un coin intéressant du Tertiaire d’Italie. Svo. Brussels,
1889.

——. See Bellardi, L.

ADDITIONS TO THE LIBRARY. 2.0

S. Paulo. Commissio geographica e geologica da Provincia de S.
Paulo [Brazil]. Orville A. Derby, Chefe. Exploracéo dos rios
Tlapetininga e Paranapanema, pelo T. F. Sampaio. Obl. 4to.
Rio de Janeiro, 1889.

. Boletim. Nos. 1-3. 8vo. 8. Paulo (Brazil),
1889. Presented by O. A. Derby, Esq., F.GS.

Sampaio, T. F. See 8. Paulo.

Sandberger, F.v. Bemerkungen iiber die fossile Flora des Infralias-
Sandsteins von Burgpreppach bei Hassfurt. 8vo. Wurzburg,
1839.

Ueber die Entwickelung der unteren Abtheilung des devon-
ischen Systems in Nassau, verglichen mit jener in anderen
Liindern. 8vo. Wiesbaden, 1889.

. Ein merkwiirdiges Geroll aus dem pleistocinen Sande von
Mosbach bei Wiesbaden. 8yvo. Stuttgart, 1890.

. Synonymie einiger devonischen Versteinerungen. 8vo.
Stuttgart, 1890.

Ueber Steinkohlenformation und Rothliegendes im Schwarz-
wald und deren Floren. 8vo. Vienna, 1890.

Uebersicht der Versteinerungen der Trias-formation Unter-
frankens. 8vo. Wiirzburg, 1890.

Saporta, Le Marquis G. de. Derniéres adjonctions 4 la Flore
Fossile d’Aix-en-Provence. 8vo. Paris, 1889. Purchased.

Sawyer, A. R. Diamonds in South Africa. Mining at Kimberley.
Svo. Newcastle-under-Lyme, 1889.

The Witwatersrand Gold-field. Mining at Johannesburg.
Syo. Newcastle-under-Lyme. 1889.

——. Ooal-mining in South Africa. Svo. Newcastle, Staff., 1890.

Saxony. Greologische Landesuntersuchung des Kénigreichs Sachsen.
Erlauterungen zur geologische Specialkarte. Blatt. 16,17, 32, 48,
102, 103, und 130. 8vo. Leipzig, 1889. |

Schenck, A. Ueber Glacialerscheinungen in Siidafrika. 8vo, Berlin,
1889.

Schmidi, A. Geologie des Miinsterthals im badischen Schwarzwald.
Theil 3. 8vo. Heidelberg, 1889.

Scudder, S. H. The Fossil Butterflies of Florissant. 8vo. Wash-
ington, 1889.

——. Pysche. The work of a decade upon Fossil Insects, 1880-
89. 8vo. Cambridge, Mass. 1890.

by,
Ye

2712 ADDITIONS TO THE LIBRARY,

Seeley, H. G. Researches on the structure, organization, and clas-
sification of the Fossil Reptilia—VI. On the Anomodont Reptilia
and their allies. 4to. London, 1889.

Sherborn, CO. D., and F. Chapman. Additional Notes on the Fora-
minifera of the London Clay exposed in the Drainage Works,
Piccadilly, London, in 1885. 8vo. London, 1889.

Smith, J. P. Paper on Dunald Mill Hole. S8vo. Barrow-in-
Furness. 1890.

Smith, P. Bosworth. Report on the Kolar Gold-field and its Southern
extension, in which the Auriferous Rocks are traced from the
Mysore State into the Madras Presidency. 4to. Madras, 1889.

Somervail, A. On the metamorphic and associated Rocks of the
extreme south of Devonshire. Part 3. 8vo. Plymouth, 1889.

South Australia. Geological Map of the Tertiary Deposits of the
Hundred of Barossa, with Explanatory Notes by H. Y. LZ. Brown,
Government Geologist. 4to. Adelaide, 1889.

Government Geologist’s Report on a Journey from Adelaide
to Hale River. (H. Y. L. Brown, Government Geologist.) 4to.
Adelaide, 1889. Presented by the Agent-General for South
Australia.

—. Report on Journey from Warrina to Musgrave Ranges, by
H. Y.L. Brown. Ato. Adelaide, 1890.

Spain. Comision del Mapa Geoldgico de Espana. Boletin. Tomo xy.
8vo. Madrid, 1888.

Spencer, J. W. ‘Terraces and Beaches about Lake Ontario, 8vo.
New Haven, 1882.

A Landslide at Brantford, Ontario, illustrating the Effects
of Thrusts upon Yielding Strata. 8vo. Philadelphia, 1887.

Notes upon Warping of the Earth’s Crust in its relation to
the origin of the Basins of the Great Lakes. 8vo. Philadelphia,
1887.

Sand-boulders in the Drift, or subaqueous origin of the
Drift, in Central Missouri. 8vo. ‘ Philadelphia. 1887.

Economic Geological Survey in Georgia and Alabama,
throughout the belt traversed by the Macon and Birmingham
Railway. 8vo. Athens, 1889.

——. “Southern Drift” and its Agricultural Relations. 8vo.
——. 1890.

——. The High Continental Elevation preceding the Pleistocene
Period. Also Ancient Shores, Boulder-Pavements, and High-
level Gravel Deposits in the region of the Great Lakes. 8vo.
1889.

9

ADDITIONS TO THE LIBRARY. 213

Spencer, J. W. The Iroquois Beach: a Chapter in the Geological
History of Lake Ontario. 4to. Montreal, 1889.

Stefani, C. de. Le pieghe delle Alpi Apuane. 8yo. Florence,
1889. Presented by the R. Istituto di Stud) Superiort Pratichi é
di Perfezionamento, Florence.

Steinmann, G., und L. Doderlein. Elemente der Pali&ontologie.
2° Halfte. 8vo. Leipzig, 1890. Presented by Herr W. Engel-

mann.

Struckmann,C. Die Grenzschichten zwischen Hilsthon und Wealden
bei Barsinghausen am Deister. 8vo. Berlin, 1890.

Thomas, ©. See Pertopicats, Washington.

True, F. W. See Pertopicats, Washington. Smithsonian Institution.
Ulrich, E.O. See Canada.

United States. Geological Survey. Seventh Annual Report, 1835-—
86. S8vo. Washington, 1888.

; Monographs. Vol. xiii. Geology of the Quicksilver
Deposits of the Pacific Slope, by G. F. Becker. 4to. Washing-
ton, 1888.

——, ——. ——. Atlas. Fol. Washington, 1887.

: Monographs. Vol. xiv. Fossil Fishes and Fossil
Plants of the Triassic Rocks of New Jersey and the Connecticut
Valley, by J.S8. Newberry. 4to. Washington, 1888.

. —. Bulletin. Nos. 48-53. 8yvo. Washington, 1888
and 1889.

Upham, Warren. Glaciation of Mountains in New England and
New York. 8vo. Boston, 1889.

——. Marine Shells and Fragments of Shells in the Till near
Boston. 8vo. Boston, 1889.

Prof. Henry Carvill Lewis and his work in Glacial Geology.
Svo. Minneapolis, 1888.

——. The Structure of Drumlins. 8vo. Boston, 1889.

Ussher, W. A. E. The Devonian of the Western Region, and
Geology of Tavistock. 8vo. Plymouth, 1&89.

Von Cappelle, J. H. Les Escarpements du “Gaasterland” sur la
cote méridionale de la Frise; suivie dune étude sur les roches

siliceuses 4 spicules de spongiaires du Boulder-clay du Roode-
~Kiif, par G. J. Hinde. 8vo. Brussels, 1889.

Vasseur, G., et L. Carez. Sur une nouvelle Carte géologique de
France au szy5y5- 4to. Paris, 1889.

—. See Dollfuss, G.

214 ADDITIONS TO THE LIBRARY.

Victoria. Annual Report of the Secretary for Mines to the Honour-
able Duncan Gillies, M.P., Minister of Mines for Victoria, on the
working of the Regulation and Inspection of the Mines and Mining
Machinery Act during the year 1888, 4to. Melbourne, 1889.

——. Gold-Fields. Reports of the Mining Registrars for the
quarter ended 30th March, 1889. 4to. Melbourne, 1889. Pre-
sented by the Department of Mines and Water Supply, Melbourne.

——. Reports of the Mining Registrars for the quarter
ended 30th June, 1889. 4to. Melbourne, 1888. Lane by
the Department of Mines and Water Supply.

——. ——. Reports of the Mining Registrars for the quarter
ended 30th September, 1889. 4to. “Melbourne, 1889.

. Reports of the Mining Registrars for the quarter
nuded 31st December, 1889. 4to. Melhor 1890. Presented
by the Mining Department.

Mineral Statistics of Victoria for the year 1888. Report of
the Secretary for Mines to the Honourable Duncan Gillies. Ato.
Melbourne, 1889. Presented by the Mining Department.

. Natural History of Victoria. Prodromus of the Zoology of
Victoria. By F. M°Coy. Decades xviii. and xix. 8vo. Mel-
bourne, 1889. Presented by the Department of the Public
Labrary, Museums, and National Gallery of Victoria, by direction
of the Premier of Victoria.

Walcott, C. D. Descriptive notes of new Genera and Species from
the Lower Cambrian or Olenellus Zone of North America. 8vo.
Washington, 1889.

Description of a new Genus and Species of Inarticulate
Brachiopod from the Trenton Limestone. 8vo. Washington,
1890.

Walford, E. A. On some Terraced Hill-slopes of the Midlands.
Svo. ? Northampton, 1890.

Wallace, A. R. Darwinism; an exposition of the Theory of
Natural Selection, with some of its applications. 8yo. London,
1889. Purchased.

Ward, John. The Geological Features of the North-Staffordshire
Coal-Fields ; their Organic Remains, their range and distribu-
tion. 8vo. Newcastle, Staffordshire, 1890.

Watts, W. W. Geology of Powys-Land. 8vo. London, 1890.

Westlake, FE. Outlines of the Geology of Fordingbridge and neigh-
bourhood, including the valley of the Avon. 8vo. Fordingbridge,
1889.

ADDITIONS TO THE LIBRARY, 215

Whitehouse, E. Cope. The Raiyan Moeris. 8vo. New York,
— 1890.

Winkler, T.C. Musée Teyler. Catalogue des collections géogno-
stico-minéralogiques du Musée Teyler. 8vo. Haarlem, 1889.

Wmwood, H. H. Notes on a Geological Section between Tyther-
ington and Thornbury. 8vo. Gloucester, 1889.

Woodward, A. Smith, and C. Davies Sherborn. A Catalogue of
British Fossil Vertebrata. 8vo. London, 1890.

Purchased.

Woodward, H. B. Henry W. Bristow, F.R.S., F.G.8, 8vo.
London, 1889.

Notes on the Rheetic Beds and Lias of Glamorganshire.
Svo. London, 1889.

——. The Geology of Lyme Regis. 8vo. London, 1889.

Worth, R. N. The Dartmoor Volcano. 8vo. Plymouth, 1889.

Wright, G. F. The Ice Age in North America, and its Bearings
upon the Antiquity of Man. 8vo. New York and London,
1889. Purchased.

Zeller, R. Note sur quelques empreintes végétales des couches de
charbon de la Nouvelle Calédonie. 8vo. Paris, 1889.

Sur les Variations de formes du Szgillaria Brardi, Brong-
Mice ove. Paris, 1889.

Zeledon, P. P. See Costa Rica.

Zigno, Baron A. de. Chelonii scoperti nei terreni Cenozoici delle
- Prealpi Venete. 4to. Venice, 1889.

Zittel, K. A. Handbuch der Paleontologie. 1 Abtheilung. Paleo-
zoologie. Band iii. Lieferung 3. 8vo. Munich, 1889. Lur-
chased.

é . 2Abtheilung. Paleophytologie. Lieferungen 7 & 8.
Von A. Schenk. 8vo. Munich, 1889. Purchased.

Zujovié, J. M. Le Docteur Josif Panéié. 8vo. Belgrade, 1889.

VOL. XLVI. qg

216 ADDITIONS TO THE LIBRARY.

3. Maps, &c.

Names of Donors in Italics.

Dunn, LH. J. Geological Sketch Map of South Africa. Melbourne,
1887.

England and Wales. Geological Survey.
One-inch Drift Map. Sheet 10.
Vertical Sections. Sheets 77, 78.
Presented by H. M. Government.
Finland. Finlands Geologisku Undersikning. Kartbladen 12-15.
; ,
200000°

France. Carte géologique détaillée de la France. Nos. 159, 167,
N97, 234, 255, — +. Purchased.

1
50000"
Ireland. Geological Survey.
One-inch Map. Nos. 3, 6, 17, 23, 31.
Horizontal Section. Nos. 27, 28.
Plan and Sections of the Ovoca Mines. (New Edition.)
Presented by H. M. Government.

Japan. Imperial Geological Survey (Noshomusho). Zone 8. Col. 10.
Zone 12, Cols. 12 & 13. Scale sygyqz- 1889.

Mining Map of Japan (showing only principal
Mines). Presented by Y Tto, Director of the Mining Bureau,
Noshomusho, Tokyo, through Prof. John Milne, F.RS., F.GS.

Maidment, C. Geological Map of Zoutpansberg, Northern Trans-
vaal Territory. Johannesburg, 1889.

Mexico. Bosquejo de una carta geologica de la Reptblica Mexicana,
formada por disposicion del Secretario de Fomento, Gral. Carlos
Pacheco, por una Comision especial, bajo la direction del Professor
Antonio del Castillo, Director de la Escuela Nacional de Ingeni-
eros. Scale szgtpgz- 1889.

Carta Minera de la Republica, formada por disposicion del
Secretario de Fomento, Gral. Carlos Pacheco, por el Ingeniero de
Minas Antonio del Castillo, Director de la Escuela Nacional de
Ingenieros, Scale syghpq9- 1889.

Noé, Franz. Geologische Uebersichtskarte der Alpen. Scale
1: 1,000,000, Vienna, 1889. Purchased. (See Booxs.)

ADDITIONS TO THE LIBRARY. 2h 7

Ordnance Survey.

One-inch General Maps. England and Wales, N.S. 23 Quarter-
sheets.

——. Ireland. 3 Quarter-sheets.
——. Scotland. 6 Sheets.
Six-inch County Maps. 29 Sheets; 318 Quarter-sheets.
Indexes (large).
Presented by H. M. Government.

Reusch, Hans. Geologisk Kart over de skandinaviske lande og
Finland. Christiania, 1890.

Roumania. Biuroulu Geologict. Harta geologica generala a Ro-
maniel. (Gr. Stefanescu, Director.) Sheets 20-24.

Saxony. Geologische Landesuntersuchung des Konigreichs Sachsens.
Geologische Specialkarte. Blatt. 16, 17, 32, 48, 102, 103, and
130. Seale 5-4,>5.

73 Cartes, being Portraits of Fellows of the Society. Presented by
the photographers, Messrs. Maull & Fox.

II. ADDITIONS TO THE MUSEUM.

A Series of Specimens from the Main Reef, Witwatersrand Gold-
field, east and west of Johannesburg and neighbourhood. Pre-
sented by Dr. H. Hxuton, F.G.S.

OOF al FE ida Baia) oes ae
, hyd ; hey oF vv] a ; ;

, Kapaiyadtis aetesuty 44

ary

9 pe

a5 sh Ce % =
ht ehtup a
"i re if A L. ier

ra)
a

oi Wa) 4 eee
; y re jie aah
{ Ay jE PST AS att Varheh. ‘ ¥ * Jp 7,

,
z i

|
B

<

a

oo se ee. = el

————— ll Cw

ee eee

“nae =
« 3 =
ig a= ea

“Aa AE

a
aie
LPT aye
SAIS ht

1
i
nally Dee
‘
f

ca
uh

a

ce
*
L

sel

“MOOI

3 9088 0