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THE

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fnternational Science Library

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BNCIENT LIFE-HISTORY

OF

Te CEARUE

A COMPREHENSIVE OUTLINE OF THE PRINCIPLES AND LEADING
FACTS OF PALAEONTOLOGICAL SCIENCE

BY

H. ALLEYNE NICHOLSON
M.D: DoSe, i. AL, Pu D. (Gorr.); F.RoS. EBL s:
PROFESSOR OF NATURAL HISTORY IN THE

UNIVERSITY OF ST. ANDREWS

wnt jl i ie .
SN \ MsUiV/A VV

FEB 17 1982

Rew Por ioe
H. 2. fowle = = We

A enone LFattion,

Ree FA Cr.

THE study of Palzontology, or the science which is
concerned with the living beings which flourished upon
the globe during past periods of its history, may be
pursued by two parallel but essentially distinct paths.
By the one method of inquiry, we may study the
anatomical characters and structure of the innumerable
extinct forms of life which lie buried in the rocks
simply as so many organisms, with but a slight and
secondary reference to the ¢zme at which they lived.
By the other method, fossil animals are regarded prin-
cipally as so many landmarks in the ancient records of
the world, and are studied Azstorically and as regards
their relations to the chronological succession of the
strata in which they are entombed. In so doing, it is
of course impossible to wholly ignore their structural
characters, and their relationships with animais now
living upon the earth; but these points are held to
occupy a subordinate place, and to require nothing
more than a comparatively general attention.

In a former work, the Author has endeavoured to
furnish a summary of the more important facts of

V1 PREFACE.

Paleontology regarded in its strictly scientific aspect,
as a mere department of the great science of Biology.
The present work, on the other hand, is an attempt to
treat Paleontology more especially from its historical
side, and in its more intimate relations with Geology.
In accordance with this object, the introductory portion
of the work is devoted to a consideration of the general
principles of Paleontology, and the bearings of this
science upon various geological problems—such as the
mode of formation of the sedimentary rocks, the reac-
tions of living beings upon the crust of the earth, and
the sequence in time of the fossiliferous formations.
The second portion of the work deals exclusively with
Historical Paleontology, each formation being consid-
ered separately, as regards its lithological nature and
subdivisions, its relations to other formations, its geo-
graphical distribution, its mode of origin, and its char-
acteristic life-forms.

In the consideration of the characteristic fossils of
each successive period, a general account is given of
their more important zoological characters and their
relations to living forms; but the technical language of
Zoology has been avoided, and the aid of illustrations
has been freely called into use. It may therefore be
hoped that the work may be found to be available for
the purposes of both the Geological and the Zoological
student ; since it is essentially an outline of Historical
Paleontology, and the student of either of the above-
mentioned sciences must perforce possess some know-
ledge of the last. Whilst primarily intended for stu-
dents, it may be added that the method of treatment
adopted has been so far untechnical as not to render
the work useless to the general reader who may desire ~

PREFACE. vil

to acquire some knowledge of a subject of such vast
and universal interest. 3

In carrying out the object which he has held before
him, the Author can hardly expect, from the nature of
the materials with which he has had to deal, that he has
kept himself absolutely clear of errors, both of omission
and commission. The subject, however, is one to which
he has devoted the labour of many years, both in
studying the researches of others and in personal
investigations of his own; and he can only trust that
such errors as may exist will be found to belong chiefly
to the former class, and to be neither serious nor
numerous. It need only be added that the work is
necessarily very limited in its scope, and that the
necessity of not assuming a thorough previous acquaint-
ance with Natural History in the reader has inexorably
restricted its range still further. The Author does not,
therefore, profess to have given more than a merely
general outline of the subject ; and those who desire
to obtain a more minute and detailed knowledge of
Paleontology, must have recourse to other and more
elaborate treatises.

UNITED COLLEGE, ST ANDREWS,
October 2, 1876.

CON TE Ne S:

BN Roa ale
PRINCIPLES OF PALAZONTOLOGY.

INTRODUCTION.
PAGE
The general objects of geological science—The older theories of
catastrophistic and intermittent action—The more modern doc-
trines of continuous and uniform action—Bearing of these doc-
trines respectively on the origin of the existing terrestrial order—
Elements of truth in Catastrophism—General truth of the doc-

trine of Continuity—Geological time, : : : : I-10
CHAPTER:
Definition of Paleontology—Nature of Fossils—Different processes
of fossilisation, : : ; : : : : , 10-14
CHAPTER GE

Aqueous and igneous rocks—General characters of the sedimentary
rocks—Mode of formation of the sedimentary rocks—Definition
of the term ‘‘ formation ”—Chief divisions of the aqueous rocks
—Mechanically-formed rocks, their characters and mode of origin
—Chemically and organically formed rocks—Calcareous rocks—
Chalk, its microscopic structure and mode of formation—Lime-
stone, varieties, structure, and origin—Phosphate of lime —Con-
cretions—Sulphate of lime—Silica and siliceous deposits of vari-
ous kinds—Greensands— Red clays—Carbon and carbonaceous
deposits, . . : : : ; : : j : 14-36

GHAPTER Tt.

Chronological succession of the fossiliferous rocks—Tests of age of
strata—Value of Palzontological evidence in stratigraphical Geo-
logy—General sequence of the great formations, } P 37-44

x - CONTENTS.

NCHAPALE RAV:

The breaks in the paleontological and geological record—Use of
the term ‘‘ contemporaneous” as applied to groups of strata—
General sequence of strata and of life-forms interfered with by
more or less extensive gaps— Unconformability—Phenomena im-
plied by this—Causes of the imperfection of the palzeontological
record,)) : : : : : : . E : 44-52

CHAPTER :

Conclusions to be drawn from fossils—Age of rocks—Mode of origin
of any fossiliferous bed—Fluviatile, lacustrine,.and marine de-
posits—Conclusions as to climate—Proofs of elevation and subsi-
dence of portions of the earth’s crust derived from fossils, . 52-50

CHAPTERS VI.

The biological relations of fossils—Extinction of life-forms—Geolo-
gical range of different species—Persistent types of life—Modern
origin of existing animals and plants—Reference of fossil forms
to the existing primary divisions of the animal kingdom—Depart-
ure of the older types of life from those now in existence—Re-
semblance of the fossils of a given formation to those of the for-
mation next above and next below—Introduction of new life-
forms, ; : : : - ; : : ‘ 5 57-61

PA Robe

HISTORICAL PALAZONTOLOGY.
CHAPTER Vit:

The Laurentian and Huronian periods—General nature, divisions,
and geographical distribution of the Laurentian deposits—Lower
and Upper Laurentian— Reasons for believing that the Lauren-
tian rocks are not azoic based upon their containing limestones,
beds of oxide of iron, and graphite—The characters, chemical
composition, and minute structure of Zoz00n Canadense—Compar-
ison of Zozoéx with existing Foraminifera— Archeospherine—
Huronian formation—Nature and distribution of Huronian de-
posits—Organic remains of the Huronian—Literature, 65-76

CHAPTER VIE:

The Cambrian period—General succession of Cambrian deposits in
Wales—Lower Cambrian and Upper Cambrian—Cambrian de-
posits of the continent of Europe and North America—Life of the
Cambrian period — Fucoids— Eophyton—Oldhamia— Sponges—

_ Echinoderms—Annelides—Crustaceans—Structure of Trilobites
—Brachiopods—Pteropods, Gasteropods, and Bivalves—Cephalo-
pods— Literature, : : : : : : ; 77-90

CONTENTS, xi

CHAP Im RAI

The Lower Silurian period—The Silurian rocks generally— Limits of
Lower and Upper Silurian—General succession, subdivisions, and
characters of the Lower Silurian rocks of Wales—General succes-
sion, subdivisions, and characters of the Lower Silurian rocks
of the North American continent—Life of the period—Fucoids—
Protozoa—Graptolites—Structure of Graptolites—Corals—Gene-
ral structure of Corals—Crinoids—Cystideans— General characters
of Cystideans—Annelides—Crustaceans— Polyzoa—Brachiopods
—Bivalve and Univalve Molluscs—Chambered Cephalopods—
General characters of the Cephalopoda—Conodonts, . » 90-114

GHAR TER 2S

The Upper Silurian period—General succession of the Upper Silurian
deposits of Wales—Upper Silurian deposits of North America—
Life of the Upper Silurian— Plants — Protozoa—Graptolites—
Corals—Crinoids—General structure of Crinoids—Star-fishes—
Annelides—Crustaceans— Eurypterids— Polyzoa—Brachiopods—
Structure of Brachiopods— Bivalves and Univalves— Pteropods—
Cephalopods—Fishes—Silurian literature, : . 115-132

CHAPTER XI:

The Devonian period—Relations between the Old Red Sandstone
and the marine Devonian deposits—The Old Red Sandstone of
Scotland—The Devonian strata of Devonshire—Sequence and
subdivisions of the Devonian deposits of North America—Life of
the period—Plants—Protozoa—Corals—Crinoids—Pentremites—
Annelides— Crustaceans — Insects— Polyzoa— Brachiopods—Bi-
valves — Univalves—Pteropods—Cephalopods—Fishes—General
divisions of the Fishes—Palzontological evidence as to the inde-
pendent existence of the Devonian system as a distinct formation
—Literature, . . : 3 : 5 . : St L2 1507)

GEA PR Oe.

The Carboniferous period—Relations of Carboniferous rocks to De-
vonian — The Carboniferous Limestone or Sub - Carboniferous
series—The Millstone-grit and the Coal-measures—Life of the
period—Structure and mode of formation of Coal—Plants of the
Coal, : 5 ; 5 ; ; E ; A . 157-170

CHAPTER XU:

Animal life of the Carboniferous period—Protozoa—Corals—Crinoids
—Pentremites—Structure of Pentremites—Echinoids— Structure
of Echinoidea — Annelides — Crustacea — Insects—Arachnids— -
Myriapods— Polyzoa—Brachiopods—Bivalves and Univalves—
Cephalopods — Fishes — Labyrinthodont Amphibians — Litera-
ture, ; . : Aaah : é 5 170-192

Xil CONTENTS.

CHAPTER XIV.

The Permian period—General succession, characters, and mode of
formation of the Permian deposits—Life of the period—Plants—
Protozoa — Corals — Echinoderms — Annelides — Crustaceans—
Polyzoa — Brachiopods — Bivalves — Univalves — Pteropods —

Cephalopods—Fishes—Amphibians—Reptiles—Literature, 492-203

CHAPTER XV.

The Triassic period—General characters and subdivisions of the Trias
of the Continent of Europe and Britain—Trias of North America
—Life of the period—Plants—Echinoderms—Crustaceans—Poly-
zoa—Brachiopods — Bivalves— Univalves— Cephalopods—Inter-
mixture of Paleozoic with Mesozoic types of Molluscs—Fishes—
mea TPG eye Ae ene of Birds— Mammals

—Literature, . . « 203-225

CHAPTER XV 1:

The Jurassic perlod—General sequence and subdivisions of the Juras-
sic deposits in Britain—Jurassic rocks of North America—Life
of the period— Plants—Corals —Echinoderms—Crustaceans— in-
sects— Brachiopods— Bivalves — Univalves — Pteropods— Tetra-
branchiate Cephalopods—Dibranchiate sae es Cane

Reptiles —Birds—Mammals— Literature, . 226-256 —

CHARTER VET:

The Cretaceous period—General succession and subdivisions of the
Cretaceous rocks in Britain—Cretaceous rocks of North America
—Life of the period—Plants—Protozoa—Corals—Echinoderms
—Crustaceans — Polyzoa — Brachiopods— Bivalves— Univalves—
Tetrabranchiate and Dibranchiate ads

tiles—Birds—Literature, . : . 256-284

CHAPTER xviii.

The Eocene period—Relations between the Kainozoic and Mesozoic
rocks in Europe and in North America—Classification of the
Tertiary deposits—The sequence and subdivisions of the Eocene
rocks of Britain and France—Eocene strata of the United States
—Life of the period—Plants—Foraminifera—Corals—Echino-

derms— Mollusca—Fishes—Reptiles—Birds—Mammals, . 284-305

GHAPTER. XIX.

The Miocene period—Miocene strata of Britain—Of France—Of
Belgium—Of Austria—Of Switzerland—Of Germany—Of Greece
— Of India—Of North America—Of the Arctic regions—Life of
the period—Vegetation of the Miocene period —Foraminifera—
Corals — Echinoderms—Articulates— Mollusca— Fishes—Amphi-

bians—Reptiles—Mammals, . : ° . - 305-323

CONTENTS. Xill

CHAPTER XxX.

The Pliocene period—Pliocene deposits of Britam—Of Europe—Of
North America—Life of the period—Climate of the period as
indicated by the Invertebrate animals—The Pliocene Mammalia
—Literature relating to the Tertiary deposits and their fossils, 323-333

CHAPTER COW:

The Post-Pliocene period—Division of the Quaternary deposits into
Post-Pliocene and Recent—Relations of the Post-Pliocene de-
posits of the northern hemisphere to the ‘‘ Glacial period ”—
Pre-Glacial deposits—Glacial deposits—Arctic Mollusca in Gla-
cial beds—Post-Glacial deposits—Nature and mode of formation
of high-level and low-level gravels—Nature and mode of forma-
tion of cavern-deposits—Kent’s Cavern—Post-Pliocene deposits
of the southern hemisphere, : ; : ; : - 334-344

GHAP TE Reet:

Life of the Post-Pliocene period—Effect of the coming on and de-
parture of the Glacial period upon the animals inhabiting the
northern hemisphere—Birds of the Post-Pliocene—Mammalia of
the Post-Pliocene— Climate of the Post-Glacial period as deduced
from the Post-Glacial Mammals—Occurrence of the bones and
implements of Man in Post-Pliocene deposits in association with
the remains of extinct Mammalia—Literature relating to the Post-
Pliocene period, : : : : : : : - 344-366

CHAPTER YU XX:

The succession of life upon the globe—Gradual and successive intro-
duction of life-forms—What is meant by ‘‘ lower ” and ‘‘ higher”
groups of animals and plants—Succession in time of the great
groups of animals in the main corresponding with their zoological
order—Identical phenomena in the vegetable kingdom—Persist-
ent types of life—High organisation of many early forms—Bear-
ings of Palzontology on the general doctrine of Evolution, 367-374

APPENDIX. —Tabular view of the chief Divisions of the Animal
Kingdom, ; P , ° : ; ; ‘ - 375-378

GLOSSARY, s e e e e e e e e Ld 379-395

INDEX, . ° . : ° ° ~ : ; - - 396-407

Oo

um B

EY:

2.
=
14.

i.
kG.

17,

. Microscopic

. Organisms

EIST OF ILLUSTRATIONS.

. Cast of Zrigonia longa,
. Microscopic section of the

wood of a fossil Conifer,

. Microscopic section of the

wood of the Larch,

. Section of Carboniferous

strata, Kinghorn, Fife,

. Diagram illustrating the

formation of stratified
deposits,

. Microscopic section of a

calcareous breccia,
section of
White Chalk,

in Atlantic
Ooze, ; :

. Crinoidal marble,
. Piece of Nummulitic lime-

stone, Pyramids,
Microscopic section of Fo-
raminiferal limestone—

Carboniferous, Amer-
ica, : : F
Microscopic section of
Lower Silurian lime-
stone, ;
Microscopic section of

oolitic limestone, Ju-
rassic, ; -

Microscopic section of
ooolitic limestone, Car-
‘boniferous,

Organisms in Barbadoes
earth,

Organisms in " Richmond
earth,

Ideal section of the crust
of the earth,

PAGE FIG.
12 | 18
13

19
I3 | 20
16 | 21

22
17

23
19

24
22

25
23 | 26
24

27
25

28

29

30
27 | 31

32
27

33
29 | 34
30 | 35
33

36
BS NL:

38
43 | 39

. Microscopic

. Microscopic

. Unconformable junction

PAGE

of Chalk and Eocene :

rocks,

. Erect trunk ofa Sigillaria,
. Diagrammatic section of

the Laurentian rocks,
section of
Laurentian limestone,

. Fragment of a mass of

Eozoon Canadense,

. Diagram illustrating the

structure of Hozo0n,
section of
Lozoon Canadense,

. LVonionina and Gromia, .
. Group of shells of living

Foraminifera,

. Diagrammatic section of

Cambrian strata,

. Lophyton Linneanum,

. Oldhamia antiqua,

. Scolithus Canadensis,

. Group of Cambrian Trilo-

bites,

. Group of characteristic

Cambrian fossils, <

. Fragment of Dictyonema

soctale,

: (C@oncmlced Berio inf the

Lower Silurian rocks
of Wales, . °

Coneeliced section of the

Lower Silurian rocks
of North America,

. Licrophycus Ottawaensis,

. Astylospongia premorsa, .
. Stromatopora rugosa, :
. Dichograptus octobrachiatus, 10%

94.

06

97
08

99

XVi

LIST OF

. Didymograptus divarica-

tus,

- Diplogr aptus pristis,

. Phyllograptus typus,

: Zaphrentis Stokest, .

. Strombodes pentagonus,

. Columnaria alveolata,

. Group of Cystideans,

. Group of Lower Silurian

Crustaceans,

. Ptilodictya falciformis,
. Ptilodictya Schaffert,
. Group of Lower Silurian

Brachiopods,

. Group of Lower Silurian

Brachiopods,

. Murchisonia gracits,

. Bellerophon argo,

. Maclurea crenulata,

. Orthoceras crebriseptum,

. Restoration of Orthoceras,
. Generalised section of the

Upper Silurian rocks,

. Monograptus priodon,
. Halysites catenularia and

fH. agglomerata, .

. Group of Upper Silurian

Star-fishes,

. Protaster Sedewickii,
. Group of Upper Silurian

Crinoids,

. Planolites vulgaris, . :
. Group of Upper Silurian

Trilobites, .

. Pterygotus Anglicus,
. Group of Upper Silurian

Polyzoa,

. Spirifera hysterica,
. Group of Upper Silurian

Brachiopods,

. Group of Upper Silurian

Brachiopods,

. Pentamerus Knightit,
. Cardiola

interrupta, C.
fibrosa, and Fterinea
subfalcata, .

. Group of Upper Silurian

Univalves,

. Lentaculites ornatus,
. Pteraspis Banksii, .«
. Onchus tenuistriatus and

Thelodus, .

. Generalised section of the

of

Devonian rocks
North America,

. Psilophyton princeps,

ILLUSTRATIONS.

115.
116.

117.

. Generalised

. Prototaxites Logani, .

Stromatopora tuberculata,

. Cystiphyllum vesiculosum,
. Zaphrentis cornicula,

. Heliophyllum exiguum,

. Crepidophyllum Archiact,
. Favosites Gothlandica,

. Favosites hemispherica,

. Spirorbis omphalodes and

S. Arkonensts,

. Spirorbis laxus and S.

spinulifera,

. Group of Devonian Tri-

lobites,

. Wing of Platephemera

antiqua,

. Clathropora intertexta, :
. Certopora Hamiltonensis,
. Fenestella magnifica,

. Retepora Phillipsi,

. Lenestella cribrosa,

. Spirtfera sculptilis,

. Spirifera mucronata,

. Atrypa reticularis,

. Strophomena rhomboid -

alis,

. Platyceras dumosum,

. Conularia ornata,

. Clymenia Sedgwickit,

. Group of Fishes from

the Devonian rocks of
North America,

. Cephalaspis Lyelit,

. Pterichihys cornutus, .
. Polypterus and Osteolepis,
. Holoptychius

nobilisst-
MUS, . ‘ : ;
section of
the Carboniferous rocks
of the North of Eng-
land,

; Odontopteri 7s Schlotheimii,
. Calamites canneformis,
II0.
III.
. Stigmaria ficoides,

. Trigonocarpum ovatum,
IT4.

Lepidodendron Sternbergit,
Sigillaria Greseri,

Microscopic section of
Foraminiferal limestone
—Carboniferous, North
America, . : 4

Fusulina cylindrica, .

Group of Carboniferous
Corals,

Platycrinus tricontadac-
tylts, . . ‘ :

143

145

148

149

15!

154
154

161
164
165
167
168
169
170

172
172

174
175

LIST OF

. Pentremites pyriformis and

P. conoideus,

: A rcheocidaris ellipticus,

. Spirorbis Carbonarius,

. Prestwichia rotundato, :
. Group of Carboniferous

Crustaceans, : :
Cyclophthalmus senior, .
Aylobius Sigillaria,
Haplophlebium Barnesi,
. Group of Carboniferous

Polyzoa,

. Group of Carboniferous

Brachiopoda,

. Pupa vetusta,
. Goniatites Fosse, :
. Amblypterus macropterus,

131. Cochhodus contortus,

132. Anthracosaurus Russell,

133. Generalised section of
the Permian rocks,

134. Walchia piniformis,

135. Group of Permian Bra-
chiopods,

136. Arca antigua, : .

137. Llatysomus gibbosus,

138. Protorosaurus Speneri, .

139. Generalised section of the
Triassic rocks,

140. Zamia spiralis, ‘

141. Triassic Conifers and
Cycads,

142. Encrinus liliiformis,

Aspidura loricata,
Group of Triassic Bi-
valves, :

145. Ceratites nodosus, . .

146. Tooth of Ceratodus ser-
ratus and C. altus,

147. Ceratodus Fostert,

148. Footprints of Cheiro-
therium,

149. Section of tooth of Laby-
rinthodont,

150. Skullof Mastodonsaur US,

151. Skull of Rhynchosaurus,

152. Lelodon, Nothosaurus,
Paleosaurus, &c.,

153. Placodus gigas,

154. Skulls of Dicynodon and

Oudenodon,

. Supposed footprint of

Bird, from the Trias
of Connecticut,

. Lower jaw of ‘Droma-

thertum sylvestre,

2

ILLUSTRATIONS.
157. Molar tooth of Jficro-
176 lestes antiquus, j
177 | 158. Ayrmecobius fasciatus, .
178 | 159. Generalised section of
179 the Jurassic rocks,
160. Aantellia megalophylla,
180 | 161. Zhecosmilia annularis,
181 | 162. Pentacrinus fasciculosus,
182 | 163. Hemucidaris crenularts, .
182 | 164. Eryon arctiformis,
| 165. Group of Jurassic Bra-
183 chiopods,
166. Ostrea Marshit,
185 | 167. Gryphea incurva, .
186 | 168. Dauceras arietina,
187 | 169. Nerinea Goodhallit,
188 | 170. Ammonites Oia
189 anus,
190 | 171. Ammonttes bifrons,
172. Leloteuthis subcostata,
195 | 173. Belemnite restored ; dia-
196 gram of Belemnite ;
Belemnites canaliculata,
198 | 174. TZetragonolepis,
199 | 175. Acrodus nobilts,
199 | 176. Lehthyosaurus communts,
201 | 177. Plestosaurus dolichodetrus,
178. Pterodactylus crasstros-
206 CFOS
208 | 179. Ramphorhynchus ‘Buch-
landi, restored,
209 | 180. Skull of Mesalsaupus, | ;
210 | 181. Archeopteryx macrura,
210 | 182. Archeopteryx, restored,
183. Jaw of Amphitherium
211 Prevostit,
212 | 184. Jaws of Oolitic Mam-
mals, ;
214 | 185. Generalised section of
215 the Cretaceous rocks, .
186. Cretaceous Angiosperms,
216 | 187. Rotalia Bouecana, .
188. Szphonia ficus,
217 | 189. Ventriculites simplex,
217 | 190. Synhelia Sharpeana,
218 | 191. Galerites albogalerus,
192. Discoidea cylindrica,
219 | 193. Escharina Oceant,
220 | 194. Terebratella Astieriana, .
195. Crania [gnabergensis,
221 | 196. Ostrea Coulont,
197. Spondylus spinosus,
198. Lnoceramus sulcatus,
222 | 199. Hippurites Toucasiana, .
200. Voluta elongata,
223 | 201. Nautilus Danicus,

XVII

222
224

229
230
231
232
233
234

235
230
236
236
237

238
238
240

241
241
242
242
244

246

248
249
252
252

254
254

260
263
264.
265
265
266
267
267
268
268
269
269
270
270
271
271
272

XVili

202.

LIST OF

Ancyloceras Matheroni-
anus, :
PEt aoe Beers:

203.

204. Forms of Cretaceous
Ammonitide,

205. Belemnitella mucronata,

206. Tooth of Aybodus,

207. Fin-spine of Hybodus,

208. Beryx Lewesiensis and
Osmeroides Manitellz,

209. Teeth of /guanodon,

210. Skull of Mosasaurus
Campert,

211. Chelone Bensted, :

212. Jaws and vertebrze of
Odontornithes,

213. Fruit of Nzpadites,

214. Nummulina levigata,

215. Lurbinola sulcata,

216. Cardita planicosta,

217. Typhis tubtfer,

218. Cyprea elegans,

219. Certthium hexagonum,

220. Limnea pyramidalis,

221. Physa columnaris,

222. Cyclostoma Arnoudii,

223. Rhombus minimus,

224. Otodus obliguus,

225. Myhobatis Edwardsiz,

226. Upper jaw of Alligator,

227. Skul» of Odontopter. yx
toliapicus,

228. Zeuglodon cetoides,

220. Palazotherium magnumne,
restored, .

230. Feet of Aguide,

231. Anoplotherium commune,

232. Skull of Dinoceras mir-
abilts,

233. Vesper tilio Parisiens S05,

234. Miocene Palms,

35. Flatanus aceroides,

236. Cinnamomum PRO
phum, .

2 Textularia Mey eriana, :

. Scutella subrotunda,

ILLUSTRATIONS.
239. Hyalea Orbignyana,
273 240. Tooth of Oxyrhina,
274 | 241. Tooth of Carcharodon,
242. Andrias Scheuchzeri,
274 243. Skull of Svontotherium
275 tngens, :
275 244. Hippopotamus Sue
275 245. Skull of Stvatherium,
246. Skull of Deinotherium,
276 247. Tooth of Llephas plani-—
278 | trons and of Mastodon
| ‘ Szvalensis, .
279 | 248. Jaw of Pliopithecus,
280 | 249. Rhinoceros Etruscus and
R. megarhinus, .
282 | 250. Molar tooth of Mastodon
290 Arvernensis,
291 251. Molar tooth of Elephas
292 meridionalts, :
293 | 252. Mola tooth of Elephas
293 antiquus, .
293 | 253. Skull and tooth of Ma-
204 chairodus cultridens,
204 | 254. Fecten /slandicus,
294 | 255. Diagram of high-ley el
204 and low-level gravels,
295 | 256. Diagrammatic section of
206 | Cave,
296 | 257. Dinornis elephantopus,
297 | 258. Skull of Diprotodon,
259. Skull of 7hylacoleo,
298 | 260. Skeleton of A/egatherium,
299 | 261. Skeleton of A4/odon,
262. Glyptodon clavifpes,
301 | 263. Skull of Rhinoceros ticho-
302 | rhinus,
303 264. Skeleton of Cervus mega
CErOS,
304 | 265. Skull of Bos p imigenius,
305 266. Skeleton of Mammoth,
309 | 267. Molar tooth of Mam-
309 moth, ‘ .
268. Skull of Ursus speleus,
309 | 269. Skull of Hyena spelea,
311 | 270. Lower jaw of Zvogon-
312 | therium Cuviert, .

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PewN Clink ES OF), PALBONTOLOGY:

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ANCIENT LIPE-HISTORY

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THE BARTEL.

INTRODUCTION

THE LAws OF GEOLOGICAL ACTION.

UNDER the general title of “ Geology” are usually included at
least two distinct branches of inquiry, allied to one another in
the closest manner, and yet so distinct as to be largely capable
of separate study. Geo/ogy,* in its strict sense, is the science
which is concerned with the investigation of the materials which
compose the earth, the methods in which those materials have
been arranged, and the causes and modes of origin of these
arrangements. In this limited aspect, Geology is nothing more
than the Physical Geography of the past, just as Physical Geo-
graphy is the Geology of to-day ; and though it has to call in
the aid of Physics, Astronomy, Mineralogy, Chemistry, and
other allies more remote, it is in itself a perfectly distinct and
individual study. One has, however, only to cross the thresh-
old of Geology to discover that the field and scope of the
science cannot be thus rigidly limited to purely physical pro-
blems. The study of the physical development of the earth
throughout past ages brings us at once in contact with the
forms of animal and vegetable life which peopled its surface in
bygone epochs, and it is found impossible adequately to com-

* Gr. gé, the earth ; Jogos, a discourse.

2 PRINCIPLES OF PALAZONTOLOGY.

prehend the former, unless we possess some knowledge of the
latter. However great its physical advances may be, Geology
remains imperfect till it is wedded with Palzontology,* a study
which essentially belongs to the vast complex of the Biologi-
cal Sciences, but at the same time has its strictly geological
side. Dealing, as it does, wholly with the consideration of
such living beings as do not belong exclusively to the present
order of things, Palzeontology is, in reality, a branch of Natu-
ral History, and may be regarded as substantially the Zoology
and Botany of the past. It is the ancient life-history of the
earth, as revealed to us by the labours of palzeontologists,
with which we have mainly to do here; but before entering
upon this, there are some general questions, affecting Geology
and Paleontology alike, which may be very briefly discussed.

The working geologist, dealing in the main with purely phy-
sical problems, has for his object to determine the material
structure of the earth, and to investigate, as far as may be, the
long chain of causes of which that structure is the ultimate re-
sult. No wider or more extended field of inquiry could be
found ; but philosophical geology is not content with this. At
all the confines of his science, the transcendental geologist
finds himself confronted with some of the most stupendous
problems which have ever engaged the restless intellect of
humanity. The origin and primeeval constitution of the terres-
trial globe, the laws of geologic action through long ages of
vicissitude and development, the origin of life, the nature and
source of the myriad complexities of living beings, the advent
of man, possibly even the future history of the earth, are
amongst the questions with which the geologist has to grapple
in his higher capacity.

These are problems which have occupied the attention of
philosophers in every age of the world, and in periods long
antecedent to the existence of a science of geology. The mere
existence of cosmogonies in the religion of almost every nation,
both ancient and modern, is a sufficient proof of the eager de-
sire of the human mind to know something of the origin of the
earth on which we tread. Every human being who has gazed
on the vast panorama of the universe, though it may have been
but with the eyes of a child, has felt the longing to solve, how-
ever imperfectly, “the riddle of the painful earth,” and has,
consciously or unconsciously, elaborated some sort of a theory
as to the why and wherefore of what he sees. Apart from the
profound and perhaps inscrutable problems which lie at the
bottom of human existence, men have in all ages invented

* Gr. palaios, ancient ; onta, beings ; logos, discourse.
_

THE LAWS OF GEOLOGICAL ACTION. 3

theories to explain the common phenomena of the material
universe ; and most of these theories, however varied in their
details, turn out on examination to have a common root, and
to be based on the same elements. Modern geology has its
own theories on the same subject, and it will be well to glance
for a moment at the principles underlying the old and the new
views.

It has been maintained, as a metaphysical hypothesis, that
there exists in the mind of man an inherent principle, in virtue
of which he believes and expects that what has been, will be ;
and that the course of nature will be a continuous and unin-
terrupted one. So far, however, from any such belief existing
as a necessary consequence of the constitution of the human
mind, the real fact seems to be that the contrary belief has
been almost universally prevalent. In all old religions, and
in the philosophical systems of almost all ancient nations, the
order of the universe has been regarded as distinctly unstable,
mutable, and temporary. A beginning and an end have always
been assumed, and the course of terrestrial events between
these two indefinite points has been regarded as liable to con-
stant interruption by revolutions and catastrophes of different
kinds, in many cases emanating from supernatural sources.
Few of the more ancient theological creeds, and still fewer of
the ancient philosophies, attained body and shape without
containing, in some form or another, the belief in the existence
of periodical convulsions, and of alternating cycles of destruc-
tion and repair.

That geology, in its early infancy, should have become im-
bued with the spirit of this belief, is no more than might have
been expected ; and hence arose the at one time powerful and
generally-accepted doctrine of “ Catastrophism.” That the
succession of phenomena upon the globe, whereby the earth’s
crust had assumed the configuration and composition which
we find it to possess, had been a discontinuous and broken
succession, was the almost inevitable conclusion of the older
geologists. Everywhere in their study of the rocks they met
with apparently impassable gaps, and breaches of continuity
that could not be bridged over. Everywhere they found them-
selves conducted abruptly from one system of deposits to
others totally different in mineral character or in stratigraphical
position. Everywhere they discovered that well-marked and
easily recognisable groups of animals and plants were succeeded,
without the intermediation of any obvious lapse of time, by
other assemblages of organic beings of a different character.
Everywhere they found evidence that the earth’s crust had

4 PRINCIPLES OF PALAONTOLOGY.

undergone changes of such magnitude as to render it seemingly
irrational to suppose that they could have been produced by
any process now in existence. If we add to the above the
prevalent belief of the time as to the comparative brevity of
the period which had elapsed since the birth of the globe, we
can readily understand the general acceptance of some form of
catastrophism amongst the earlier geologists.

As regards its general sense and substance, the doctrine of
catastrophism held that the history of the earth, since first it
emerged from the primitive chaos, had been one of periods of
repose, alternating with catastrophes and cataclysms of a more
or less violent character. The periods of tranquillity were sup-
posed to have been long and protracted ; and during each of
them it was thought that one of the great geological ‘‘ forma-
tions” was deposited. In each of these periods, therefore, the
condition of the earth was supposed to be much the same as it
is now—sediment was quietly accumulated at the bottom of the
sea, and animals and plants flourished uninterruptedly in suc-
cessive generations. Each period of tranquillity, however, was
believed to have been, sooner or later, put an end to by a
sudden and awful convulsion of nature, ushering in a brief and
paroxysmal period, in which the great physical forces were
unchained and permitted to spring into a portentous activity.
The forces of subterranean fire, with their concomitant pheno-
mena of earthquake and volcano, were chiefly relied upon as
the efficient causes of these periods of spasm and revolution.
Enormous elevations of portions of the earth’s crust were thus
believed to be produced, accompanied by corresponding and
equally gigantic depressions of other portions. In this way
new ranges of mountains were produced, and previously exist-
ing ranges levelled with the ground, seas were converted into
dry land, and continents buried beneath the ocean—catastrophe
following catastrophe, till the earth was rendered uninhabitable,
and its races of animals and plants were extinguished, never to
reappear in the same form. Finally, it was believed that this
feverish activity ultimately died out, and that the ancient peace
once more came to reign upon the earth. As the abnormal
throes and convulsions began to be relieved, the dry land and
sea once more resumed their relations of stability, the condi-
tions of life were once more established, and new races of ani-
mals and plants sprang into existence, to last until the super-
vention of another fever-fit.

Such is the past history of the globe, as sketched for us, in
alternating scenes of fruitful peace and revolutionary destruc-
tion, by the earlier geologists. As before said, we cannot

THE LAWS OF GEOLOGICAL ACTION. 5

wonder at the former general acceptance of Catastrophistic
doctrines. Even in the light of our present widely-increased
knowledge, the series of geological monuments remains a broken
and imperfect one ; nor can we ever hope to fill up completely
the numerous gaps with which the geological record is defaced.
Catastrophism was the natural method of accounting for these
gaps, and, as we shall see, it possesses a basis of truth. At
present, however, catastrophism may be said to be nearly ex-
tinct, a place is taken by the modern doctrine of ‘ Con-
tinuity ” or “‘ Uniformity ”—a doctrine with which the name of
Lyell cet ever remain imperishably associated.

The fundamental thesis of the doctrine of Uniformity is,
that, in spite of all apparent violations of continuity, the se-
quence of geological phenomena has in reality been a regular
and uninterrupted one; and that the vast changes which can
be shown to have passed over the earth in former periods have
been the result of the slow and ceaseless working of the ordi-
nary physical forces—acting with no greater intensity than they
do now, but acting through enormously prolonged periods.
The essential element in the theory of Continuity is to be found
in the allotment of indefinite time for the accomplishment of
the known series of geological changes. It is obviously the
case, namely, that there are two possible explanations of all
phenomena which lie so far concealed in “the dark backward
and abysm of time,” that we can have no direct knowledge of
the manner in which they were produced. We may, on the
one hand, suppose them to be the result of some very powerful
cause, acting through a short period of time. ‘That is Catas-
trophism. Or, we may suppose them to be caused by a much
weaker force operating through a proportionately prolonged
period. This is the view of the Uniformitarians. It is a ques-
tion of exergy versus time ; and it 1s “me which is the true ele-
ment of the case. An earthquake may remove a mountain in
the course of a few seconds; but the dropping of the gentle
rain will do the same, if we extend its operations over a millen-
nium. And this is true of all agencies which are now at work,
or ever have been at work, upon our planet. The Catastro-
phists, believing that the globe is but, as it were, the birth of.
yesterday, were driven of necessity to the conclusion that its
history had been checkered by the intermittent action of par-
oxysmal and almost inconceivably potent forces. The Unifor-
mitarians, on the other hand, maintaining the “ adequacy of
existing causes,” and denying that the known physical forces
ever acted in past time with greater intensity than they do at
present, are, equally of necessity, driven to the conclusion that.

6 PRINCIPLES OF PALZONTOLOGY.

the world is truly in its “hoary eld,” and that its present state
is really the result of the tranquil and regulated action of
known forces through unnumbered and innumerable centuries.

The most important point for us, in the present connection,
is the bearing of these opposing doctrines upon the question
as to the origin of the existing terrestrial order. On any doc-
trine of uniformity that order has been evolved slowly, and,
according to law, from a pre-existing order. Any doctrine of
catastrophism, on the other hand, carries with it, by implica-
tion, the belief that the present order of things was brought
about suddenly and irrespective of any pre-existent order; and
it is important to hold clear ideas as to which of these beliefs
is the true one. In the first place, we may postulate that the
world had a beginning, and, equally, that the existing terrestrial
order had a beginning. However far back we may go, geology
does not, and cannot, reach the actual beginning of the world ;
and we are, therefore, left simply to our own speculations on
this point. With regard, however, to the existing terrestrial
order, a great deal can be discovered, and to do so is one of
the principal tasks of geological science. The first steps in the
production of that order lie buried in the profound and un-
searchable depths of a past so prolonged as to present itself to
our finite minds as almost an eternity. The last steps are in
the prophetic future, and can be but dimly guessed at. Be-
tween the remote past and the distant future, we have, however,
a long period which is fairly open to inspection ; and in saying
a ‘‘long”’ period, it is to be borne in mind that this term is
used in its geological sense. Within this period, enormously
long as it is when measured by human standards, we can trace
with reasonable certainty the progressive march of events, and
can determine the laws of geological action, by which the pre-
sent order of things has been brought about.

The natural belief on this subject doubtless is, that the
world, such as we now see it, possessed its present form and
configuration from the beginning. Nothing can be more
natural than the belief that the present continents and oceans
have always been where they are now; that we have always
had the same mountains and plains; that our rivers have
always had their present courses, and our lakes their present
positions; that our climate has always been the same; and
that our animals and plants have always been identical with
those now familiar to us. Nothing could be more natural
than such a belief, and nothing could be further removed from
the actual truth. On the contrary, a very slight acquaintance
with geology shows us, in the words of Sir John Herschel, that

THE LAWS. OF GEOLOGICAL, ACTION. Ti

“the actual configuration of our continents and islands, the
coast-lines of our maps, the direction and elevation of our
mountain-chains, the courses of our rivers, and the soundings
of our oceans, are not things primordially arranged in the con-
struction of our globe, but results of successive and complex
actions on a former state of things; /¢/at, again, of similar
actions on another still more remote; and so on, till the ori-
ginal and really permanent state is pushed altogether out of
sight and beyond the reach even of imagination ; while on the
other hand, a similar, and, as far as we can see, interminable
vista is opened out for the future, by which the habitability of
our planet is secured amid the total abolition on it of the
present theatres of terrestrial life.”

Geology, then, teaches us that the physical features which
now distinguish the earth’s surface have been produced as the
ultimate result of an almost endless succession of precedent
changes. Palzontology teaches us, though not yet in such
assured accents, the same lesson. Our present animals and
plants have not been produced, in their innumerable forms,
each as we now know it, as the sudden, collective, and simul-
taneous birth of a renovated world. On the contrary, we have
the clearest evidence that some of our existing animals and
plants made their appearance upon the earth at a much earlier
period than others. In the confederation of animated nature
some races can boast of an immemorial antiquity, whilst others
are comparative parvenus. We have also the clearest evidence
that the animals and plants which: now inhabit the globe have
been preceded, over and over again, by other different assem-
blages of animals and plants, which have flourished in. succes-
sive periods of the earth’s history, have reached their culmina-
tion, and then have given way to a fresh series of living beings.
We have, finally, the clearest evidence that these successive
groups of animals and plants (faunze and flore) are to a greater
or less extent directly connected with one another. Each
group is, to a greater or less extent, the lineal descendant of
the group which immediately preceded it in point of time, and
is more or less fully concerned with giving origin to the group
which immediately follows it. That this law of ‘“ evolution”
has prevailed to a great extent is quite certain; but it does not
meet all the exigencies of the case, and it is probable that its
action has been supplemented by some still unknown law of a
different character.

We shall have to consider the question of geological “ con-
tinuity” again. In the meanwhile, it is sufficient to state that
this doctrine is now almost universally accepted as the basis

8 PRINCIPLES OF PALZONTOLOGY.

of all inquiries, both in the domain of geology and that of
paleontology. The advocates of continuity possess one im-
mense advantage over those who believe in violent and revo-
lutionary convulsions, that they call into play only agencies
of which we have actual knowledge. We vow that certain
forces are now at work, producing certain modifications in the
present condition of the globe; and we £zow that these forces
are capable of producing the vastest of the changes which
geology brings under our consideration, provided we assign a
time proportionately vast for their operation. On the other
hand, the advocates of catastrophism, to make good their
views, are compelled to invoke forces and actions, both de-
structive and restorative, of which we have, and can have, no
direct knowledge. They endow the whirlwind and the earth-
quake, the central fire and the rain from heaven, with powers
as mighty as ever imagined in fable, and they build up the
fragments of a repeatedly shattered world by the intervention
of an intermittently active creative power.

It should not be forgotten, however, that from one point of
view there is a truth in catastrophism which is sometimes
overlooked by the advocates of continuity and uniformity.
Catastrophism has, as its essential feature, the proposition that
the known and existing forces of the earth at one time acted
with much greater intensity and violence than they do at pre-
sent, and they carry down the period of this excessive action
to the commencement of the present terrestrial order. The
Uniformitarians, in effect, deny this proposition, at any rate as
regards any period of the earth’s history of which we have
actual cognisance. If, however, the “nebular hypothesis” of
the origin of the universe be well founded—as is generally ad-
mitted—then, beyond question, the earth 1s a gradually cooling
body, which has at one time been very much hotter than it is
at present. There has been a time, therefore, in which the
igneous forces of the earth, to which we owe the phenomena of
earthquakes and volcanoes, must have been far more intensely
active than we can conceive of from anything that we can see
at the present day. By the same hypothesis, the sun is a
cooling body, and must at one time have possessed a much
higher temperature than it has at present. But increased heat
of the sun would seriously alter the existing conditions affect-
ing the evaporation and precipitation of moisture on our earth ;
and hence the aqueous forces may also have acted at one time
more powerfully than they do now. The fundamental prin-
ciple of catastrophism is, therefore, not wholly vicious; and
we have reason to think that there must have been periods—

THE LAWS OF GEOLOGICAL ACTION. 9

very remote, it is true, and perhaps unrecorded in the history
of the earth—in which the known physical forces may have
acted with an intensity much greater than direct observation
would lead us to imagine. And this may be believed, alto-
gether irrespective of those great secular changes by which hot
or cold epochs are produced, and which can hardly be called
“ catastrophistic,” as they are produced gradually, and are
liable to recur at definite intervals.

Admitting, then, that there zs a truth at the bottom of the
once current doctrines of catastrophism, still it remains certain
that the history of the earth has been one of /azw in all past
time, as itis now. Nor need we shrink back affrighted at the
vastness of the conception—the vaster for its very vagueness
—that we are thus compelled to form as to the duration of
geological time. As we grope our way backward through the
dark labyrinth of the ages, epoch succeeds to epoch, and
period to period, each looming more gigantic in its outlines
and more shadowy in its features, as it rises, dimly revealed,
from the mist and vapour of an older and ever-older past. It
is useless to add century to century or millennium to millen-
nium. When we pass a certain boundary-line, which, after all,
is reached very soon, figures cease to convey to our finite
faculties any real notion of the periods with which we have
to deal. The astronomer can employ material illustrations
to give form and substance to our conceptions of celestial
space; but such a resource is unavailable to the geologist.
The few thousand years of which we have historical evidence
sink into absolute insignificance beside the unnumbered eons
which unroll themselves one by one as we penetrate the dim
recesses of the past, and decipher with feeble vision the pon-
derous volumes in which the record of the earth is written.
Vainly does the strained intellect seek to overtake an ever-
receding commencement, and toil to gain some adequate grasp
of an apparently endless succession. A beginning there must
have been, though we can never hope to fix its point. Even
speculation droops her wings in the attenuated atmosphere of
a past so remote, and the light of imagination is quenched in
the darkness of a history so ancient. In “me, as in space, the
confines of the universe must ever remain concealed from us ;
and of the end we know no more than of the beginning. In-
conceivable as is to us the lapse of ‘“ geological time,” it is no
more than ‘‘a mere moment of the past, a mere infinitesimal
portion of eternity.” Well may “‘the human heart, that weeps
and trembles,” say, with Richter’s pilgrim through celestial
space, “I will go no farther; for the spirit of man acheth with

10 PRINCIPLES OF PALAONTOLOGY.

this infinity. Insufferable is the glory of God. Let me lie
down in the grave, and hide me from the persecution of the
Infinite, for end, I see, there is none.”

CHAPTER: §
THE SCOPE AND MATERIALS OF PALZONTOLOGY.

The study of the rock-masses which constitute the crust of the
earth, if carried out in the methodical and scientific manner of
the geologist, at once brings us, as has been before remarked,
in contact with the remains or traces of living beings which
formerly dwelt upon the globe. Such remains are found, in
greater or less abundance, in the great majority of rocks; and
they are not only of great interest in themselves, but they have
proved of the greatest importance as throwing light upon vari-
ous difficult problems in geology, in natural history, in botany,
and in philosophy. Their study constitutes the science of
paleontology ; and though it is possible to proceed to a cer-
tain length in geology and zoology without much palzontolo-
gical knowledge, it is hardly possible to attain to a satisfac-
tory general acquaintance with either of these subjects with-
out having mastered the leading facts of the first. Similarly,
it is not possible to study palzontology without some ac-
quaintance with both geology and natural history.

PALZONTOLOGY, then, is the science which treats of the
living beings, whether animal or vegetable, which have -in-
habited the earth during past periods of its history. Its object
is to eludicate, as far as may be, the structure, mode of exist-
ence, and habits of all such ancient forms of life; to determine
their position in the scale of organised beings; to lay down
the geographical limits within which they flourished ; and to
fix the period of their advent and disappearance. It is the
ancient life-history of the earth ; and were its record complete,
it would furnish us with a detailed knowledge of the form and
relations of all the animals and plants which have at any period
flourished upon the land-surfaces of the globe or inhabited its
waters ; it would enable us to determine precisely their succes-
sion in time; and it would place in our hands an unfailing key
to the problems of evolution. Unfortunately, from causes
which will be subsequently discussed, the palzontological
record is extremely imperfect, and our knowledge is inter-

THE SCOPE OF PALATSONTOLOGY. II

rupted by gaps, which not only bear a large proportion to our
solid information, but which in many cases are of such a nature
that we can never hope to fill them up.

Fossits.—The remains of animals or vegetables which we
now find entombed in the solid rock, and which constitute the
working material of the palzeontologist, are termed “fossils,” *
or “‘petrifactions.” In most cases, as can be readily under-
stood, fossils are the actual hard parts of animals and plants
which were in existence when the rock in which they are now
found was being deposited. Most fossils, therefore, are of the
nature of the shells of shell-fish, the skeletons of coral-zoophytes,
the bones of vertebrate animals, or the wood, bark, or leaves
of plants. All such bodies are more or less of a hard consist-
ence to begin with, and are capable of resisting decay for a
longer or shorter time—hence the frequency with which they
occur in the fossil condition. Strictly speaking, however, by
the term “fossil” must be understood ‘any body, or the traces
of the existence of any body, whether animal or vegetable, which
has been buried in the earth by natural causes” (Lyell).
We shall find, in fact, that many of the objects which we have
to study as “fossils” have never themselves actually formed
parts of any animal or vegetable, though they are due to the
former existence of such organisms, and indicate what was the
nature of these. Thus the footprints left by birds, or reptiles,
or quadrupeds upon sand or mud, are just as much proofs of
the former existence of these animals as would be bones,
feathers, or scales, though in themselves they are inorganic.
Under the head of fossils, therefore, come the footprints of
air-breathing vertebrate animals; the tracks, trails, and bur-
rows of sea-worms, crustaceans, or molluscs; the impressions
left on the sand by stranded jelly-fishes ; the burrows in stone
or wood of certain shell-fish; the “moulds” or “casts” of
shells, corals, and other organic remains; and various other
bodies of a more or less similar nature.

FOssILisaTIoN.—The term ‘‘fossilisation” is applied to all
those processes through which the remains of organised beings
may pass in being converted into fossils. These processes are
numerous and varied ; but there are three principal modes of
fossilisation which alone need be considered here. In the first
instance, the fossil is to all intents and purposes an actual
portion of the original organised being—such as a bone, a shell,
or a piece of wood. In some rare instances, as in the case of
the body of the Mammoth discovered embedded in ice at the
mouth of the Lena in Siberia, the fossil may be preserved

* Lat. fossus, dug up.

12 PRINCIPLES OF PALZZONTOLOGY.

almost precisely in its original condition, and even with its
soft parts uninjured. More commonly, certain changes have
taken place in the fossil, the principal being the more or less
total removal of the organic matter originally present. Thus
bones become light and porous by the removal of their gela-
tine, so as to cleave to the tongue on being applied to that
organ; whilst shells become fragile, and lose their primitive
colours. In other cases, though practically the real body it
represents, all the cavities of the fossil, down to its minutest
recesses, may have become infiltrated with mineral matter. It
need hardly be added, that it is in the more modern rocks that
we find the fossils, as a rule, least changed from their former
condition; but the original structure is often more or less com-
pletely retained in some of the fossils from even the most
ancient formations.

In the second place, we very frequently meet with fossils in
the state of “casts” or moulds of the original organic body.
What occurs in this case will be readily understood if we ima-
gine any common bivalve shell, as an Oyster, or Mussel, or
Cockle, embedded in clay or mud. If the clay were sufficiently
soft and fluid, the first thing would be that it would gain access
to the interior of the shell, and would completely fill up the
space between the valves. The pressure, also, of the surround-
ing matter would insure that the clay would everywhere ad-
here closely to the exterior of the shell. If now we suppose
the clay to be in any way hardened so as to be converted into
stone, and if we were to break up the stone, we should obvi-
ously have the following state of parts. The clay which filled
the shell would form an accurate cast of the zzferzor of the
shell, and the clay outside would give us an exact impression
or cast of the exterzor of the shell (fig. 1). We should have,
then, two casts, an interior and
an exterior, and the two would
be very different to one another,
since the inside of a shell is
very unlike the outside. In
the case, in fact, of many uni-
valve shells, the interior cast or
“mould” is so unlike the ex-
terior cast, or unlike the shell

Fig. 1.—Trigonia longa, showing casts itself, that it may be difficult to
Cretandoae (Nicaea Of the shell. determine the truc @Hemayaieme
former.

It only remains to add that there is sometimes a further
complication. If the rock be very porous and permeable by

THE SCOPE OF PALZONTOLOGY. 13

water, it may happen that the original shell is entirely dissolved
away, leaving the interior cast loose, like the kernel of a nut,
within the case formed by the exterior cast. Or it may happen
that subsequent to the attainment of this state of things, the
space thus left vacant between the interior and exterior cast—
the space, that is, formerly occupied by the shell itself—may
be filled up by some foreign mineral deposited there by the
infiltration of water. In this last case the splitting open of the
rock would reveal an interior cast, an exterior cast, and finally
a body which would have the exact form of the original shell, but
which would be really a much later formation, and which would
not exhibit under the microscope the minute structure of shell.

In the third class of cases we have fossils which present
with the greatest accuracy the external form, and even some-
times the internal minute structure, of the original organic
body, but which, nevertheless, are not themselves truly organic,
but have been formed by a ‘‘ replacement” of the particles of
the primitive organism by some mineral substance. The most
elegant example of this is afforded by fossil wood which has
been “ silicified” or converted into flint (sz/ex). In such cases
we have fossil wood which presents the rings of growth and
fibrous structure of recent wood, and which under the micro-
scope exhibits the minutest vessels which characterise ligneous
tissue, together with the even more minute markings of the
vessels (fig. 2). The whole, however, instead of being com-

BEX

tea
310)
}
©

TI
bheston

Fig. 2.— Microscopic section of the Fig. 3.—Microscopic section of the wood
silicified wood of a Conifer (Seguozia) cut of the common Larch (Ades lari), cut in
in the long direction of the fibres. Post- the long direction of the fibres. In boththe
tertiary? Colorado. (Original.) fresh and the fossil wood (fig. 2) are seen

the discs characteristic of coniferous wood,
(Original. )

posed of the original carbonaceous matter of the wood, is now
converted 8 flint. The only explanation that can be given

14 PRINCIPLES OF PALAONTOLOGY.

of this by no means rare phenomenon, is that the wood must
have undergone a slow process of decay in water charged with
silica or flint in solution. As each successive particle of wood
was removed by decay, its place was taken by a particle of
flint deposited from the surrounding water, till ultimately the
entire wood was silicified. The process, therefore, resembles
what would take place if we were to pull down a house built
of brick by successive bricks, replacing each brick as removed
by a piece of stone of precisely the same size and form. ‘The
result of this would be that the house would retain its primi-
tive size, shape, and outline, but it would finally have been
converted from a house of brick into a house of stone. Many
other fossils besides wood—such as shells, corals, sponges,
&c.—are often found silicified; and this may be regarded as
the commonest form of fossilisation by replacement. In other
cases, however, though the principle of the process is the same,
the replacing substance may be iron pyrites, oxide of iron,

sulphur, malachite, magnesite, talc, &c.; but it is rarely that
the replacement with these minerals i 1S so perfect as to Pies
the more delicate details of internal structure.

CEVA Ray Eh

THE FOSSILIFEROUS ROCKS.

Fossils are found in rocks, though not universally or pro-
miscuously ; and it is therefore necessary that the palzeonto-
logist should possess some acquaintance with, at any rate, those
rocks which yield organic remains, and which are therefore
said to be “ fosszliferous.” In geological language, all the
materials which enter into the composition of the solid crust
of the earth, be their texture what it may—from the most im-
palpable mud to the hardest granite—are termed “ rocks ;”
and for our present purpose we may divide these into two great
groups. In the first division are the Zeneous Rocks—such as
the lavas and ashes of volcanoes—which are formed within the
body of the earth itself, and which owe their structure and
origin to the action of heat. The Igneous Rocks are formed
primarily below the surface of the earth, which they only reach
as the result of volcanic action ; they are generally destitute of
distinct ‘ stratification,” or arrangement in successive layers ;
and they do not contain fossils, except in the comparatively

THE FOSSILIFEROUS ROCKS. 15

rare instances where volcanic ashes have enveloped animais
or plants which were living in the sea or on the land in the
immediate vicinity of the volcanic focus. ‘The second great
division of rocks is that of the Aossiiferous, Aqueous, or Sedt-
mentary Rocks. These are formed at the surface of the earth,
and, as implied by one of their names, are invariably deposited
in water. They are produced by vital or chemical action, or
are formed from the “sediment” produced by the disintegra-
tion and reconstruction of previously existing rocks, without
previous solution ; they mostly contain fossils; and they are
arranged in distinct layers or “strata.” The so-called ‘“ aerial”
rocks which, like beds of blown sand, have been formed by
the action of the atmosphere, may also contain fossils; but
they are not of such importance as to require special notice
here.

For all practical purposes, we may consider that the Aque-
ous Rocks are the natural cemetery of the animals and plants
of bygone ages; and it is therefore essential that the paleeon-
tological student should be acquainted with some of the prin-
cipal facts as to their physical characters, their minute structure
and mode of origin, their chief varieties, and their historical
succession.

The Sedimentary or Fossiliferous Rocks form the greater
portion of that part of the earth’s crust which is open to our
examination, and are distinguished by the fact that they are
regularly “stratified” or arranged in distinct and definite layers
or “strata.” These layers may consist of a single material,
as in a block of sandstone, or they may consist of different
materials. When examined on a large scale, they are always
found to consist of alternations of layers of different mineral
composition. We may examine any given area, and find in it
nothing but one kind of rock—sandstone, perhaps, or lime-
stone. In all cases, however, if we extend our examination
sufficiently far, we shall ultimately come upon different rocks ;
and, as a general rule, the thickness of any particular set of
beds is comparatively small, so that different kinds of rock
alternate with one another in comparatively small spaces.

As regards the origin of the Sedimentary Rocks, they are
for the most part ‘‘ derivative” rocks, being derived from the
wear and tear of pre-existent rocks. Sometimes, however, they
owe their origin to chemical or vital action, when they would
more properly be spoken of simply as Aqueous Rocks. As to
their mode of deposition, we are enabled to infer that the
materials which compose them have formerly been spread out
by the action of water, from what we see going on every day

16 PRINCIPLES OF PALAZSONTOLOGY.

at the mouths of our great rivers, and on a smaller scale wher-
ever there is running water. Every stream, where it runs into

a
a
— =

Fig. 4.—Sketch of Carboniferous strata at Kinghorn, in Fife, showing stratified beds
(limestone and shales) surmounted by an unstratified mass of trap. (Original.)

a lake or into the sea, carries with it a burden of mud, sand,
and rounded pebbles, derived from the waste of the rocks
which form its bed and banks. When these materials cease
to be impelled by the force of the moving water, they sink to
the bottom, the heaviest pebbles, of course, sinking first, the
smaller pebbles and sand next, and the finest mud last. Ulti-
mately, therefore, as might have been inferred upon theoretical
grounds, and as is proved by practical experience, every lake
becomes a receptacle for a series of stratified rocks produced
by the streams flowing into it. These deposits may vary in
different parts of the lake, according as one stream brought
down one kind of material and another stream contributed
another material; but in all cases the materials will bear ample
evidence that they were produced, sorted, and deposited by
running water. The finer beds of clay or sand will all be
arranged in thicker or thinner layers or lamine ; and if there
are any beds of pebbles these will all be rounded or smooth,
just lke the water-worn pebbles of any brook-course. In all
probability, also, we should find in some of the beds the re-

THE FOSSILIFEROUS ROCKS. 17

mains of fresh-water shells or plants or other organisms which
inhabited the lake at the time these beds were being de-
posited.

In the same way large rivers—such as the Ganges or
Mississippi—deposit all the materials which they bring down
at their mouths, forming in this way their “deltas.” When-
ever such a delta is cut through, either by man or by some
channel of the river altering its course, we find that it is com-
posed of a succession of horizontal layers or strata of sand or
mud, varying in mineral composition, in structure, or in grain,
according to the nature of the materials brought down by the
river at different periods. Such deltas, also, will contain the
remains of animals which inhabit the river, with fragments of
the plants which grew on its banks, or bones of the animals
which lived in its basin.

Nor is this action confined, of course, to large rivers only,
though naturally most conspicuous in the greatest bodies of
water. On,the contrary, all streams, of whatever size, are
engaged in the work of wearing down the dry land, and of
transporting the materials thus derived from higher to lower
levels, never resting in this work till they reach the sea.

Fig. 5.—Diagram io illustrate the formation of sedimentary deposits at the point
where a river debouches into the sea.

Lastly, the sea itself—irrespective of the materials delivered
into it by rivers—is constantly preparing fresh stratified de-

18 PRINCIPLES OF PALEONTOLOGY.

posits by its own action. Upon every coast-line the sea is
constantly eating back into the land and reducing its com-
ponent rocks to form the shingle and sand which we see upon
every shore. The materials thus produced are not, however, °
lost, but are ultimately deposited elsewhere in the form of new
stratified accumulations, in which are buried the remains of
animals inhabiting the sea at the time.

Whenever, then, we find anywhere in the interior of the land
any series of beds having these characters—composed, that is,
of distinct layers, the particles of which, both large and small,
show distinct traces of the wearing action of water—whenever
and wherever we find such rocks, we are justified in assuming
that they have been deposited by water in the manner above
mentioned. Either they were laid down in some former lake
by the combined action of the streams which flowed into it;
or they were deposited at the mouth of some ancient river,
forming its delta; or they were laid down at the bottom of the
ocean. In the first two cases, any fossils which the beds
might contain would be the remains of fresh-water or terres-
trial organisms. In the last case, the majority, at any rate, of
the fossils would be the remains of marine animals.

The term ‘ formation ” is employed by geologists to express
“any group of rocks which have some character in common,
whether of origin, age, or composition” (Lyell); so that we
may speak of stratified and unstratified formations, aqueous
or igneous formations, fresh-water or marine formations, and
sO on.

CHIEF DIVISIONS OF THE AQUEOUS ROCKS.

The Aqueous Rocks may be divided into two great sections,
the Mechanically-formed and the Chemically-formed, includ-
ing under the last head all rocks which owe their origin to
vital action, as well as those produced by ordinary chemical
agencies.

A. MECHANICALLY-FORMED Rocks. — These are all those
Aqueous Rocks of which we can obtain proofs that their
particles have been mechanically transported to their present
situation. Thus, if we examine a piece of conglomerate or
puddingstone, we find it to be composed of a number of
rounded pebbles embedded in an enveloping matrix or paste,
which is usually of a sandy nature, but may be composed of
carbonate of lime (when the rock is said to be a “ calcareous —
conglomerate”). The pebbles in all conglomerates are worn
and rounded by the action of water in motion, and thus show

THE FOSSILIFEROUS ROCKS. IQ
that they have been subjected to much mechanical attrition,
whilst they have been mechanically transported for a greater
or less distance from the rock of which they originally formed
part. The analogue of the old conglomerates at the present
day is to be found in the great beds of shingle and gravel
which are formed by the action of the sea on every coast-line,
and which are composed of water-worn and well-rounded
pebbles of different sizes. A dveccia is a mechanically-formed
rock, very similar to a conglomerate, and consisting of larger
or smaller fragments of rock embedded in a common matrix.
The fragments, however, are in this case all more or less
angular, and. are not worn or rounded. ‘The fragments in
breccias may be of large size, or they may be comparatively
small (fig. 6); and the matrix may be composed of sand (aren-
aceous) or of carbonate of
lime (calcareous). In the case
of an ordinarysandstone, again,
we have a rock which may be
regarded as simply a very fine- &, EO a
grained conglomerate or brec- yxy ia POSEN

cia, being composed of small [Weezy ieapalle
grains of sand (silica), some-
timesrounded,sometimesmore
or less angular, cemented to-
gether by some such substance
as oxide of iron, silicate of
iron, or carbonate of lime. A

sandstone, therefore, like a
conglomerate, is a mechani-
cally-formed rock, its compo-
nent grains being equally the
result of mechanical attrition

Fig. 6.—Microscopic section of a calcare-
ous breccia in the Lower Silurian (Coniston
Limestone) of Shap Wells, Westmoreland.
The fragments are all of small size, and
consist of angular pieces of transparent
quartz, volcanic ashes, and limestone em-
bedded in a matrix of crystalline limestone.

E Original.
and having equally been trans- URE

ported from a distance; and the same is true of the ordinary
sand of the sea-shore, which is nothing more than an uncon-
solidated sandstone. Other so-called sands and sandstones,
though equally mechanical in their origin, are truly calcareous
in their nature, and are more or less entirely composed of
carbonate of lime. Of this kind are the shell-sand so com-
mon on our coasts, and the coral-sand which is so largely
formed in the neighbourhood of coral-reefs. In these cases
the rock is composed of fragments of the skeletons of shell-
fish, and numerous other marine animals, together, in many
instances, with the remains of certain sea-weeds (Corallines,
Nullipores, &c.) which are endowed with the power of secret-

20 PRINCIPLES OF PALZONTOLOGY.

ing carbonate of lime from the sea-water. Lastly, in cer-
tain rocks still finer in their texture than sandstones, such
as the various mud-rocks and shales, we can still recognise a
mechanical source and origin. If slices of any of these rocks
sufficiently thin to be transparent are examined under the
microscope, it will be found that they are composed of minute
grains of different sizes, which are all more or less worn and
rounded, and which clearly show, therefore, that they have
been subjected to mechanical attrition.

All the above-mentioned rocks, then, are mechanically-formed
rocks; and they are often spoken of as “‘ Derivative Rocks,”
in consequence of the fact that their particles can be shown to
have been mechanically derived from other pre-existent rocks.
It follows from this that every bed of any mechanically-formed
rock is the measure and equivalent of a corresponding amount
of destruction of some older rock. It is not necessary to
enter here into a minute account of the subdivisions of these
rocks, but it may be mentioned that they may be divided into
two principal groups, according to their chemical composition.
In the one group we have the so-called Avenaceous (Lat. arena,
sand) or Svz/zceous Rocks, which are essentially composed of
larger or smaller grains of flint or silica. In this group are
comprised ordinary sand, the varieties of sandstone and grit,
and most conglomerates and breccias. We shall, however, after-
wards see that some siliceous rocks are of organic origin. In
the second group are the so-called Argilaceous (Lat.- argilla,
clay) Rocks, which contain a larger or smaller amount of clay or
hydrated silicate of alumina in their composition. Under this
head come clays, shales, marls, marl-slate, clay-slates, and
most flags and flagstones.

B. CHEMICALLY-FORMED Rocks.—In this section are com-
prised all those Aqueous or Sedimentary Rocks which have
been formed by chemical agencies. As many of these chemi-
cal agencies, however, are exerted through the medium of
living beings, whether animals or plants, we get into this
section a number of what may be called ‘ ovganically-formed
rocks.” These are of the greatest possible importance to the
paleontologist, as being to a greater or less extent composed
of the actual remains of animals or vegetables, and it will
therefore be necessary to consider their character and struc-
ture in some detail.

By far the most important of the chemically-formed rocks
are the so-called Calcareous Rocks (Lat. calx, lime), com-
prising all those which contain a large proportion of carbonate
of lime, or are wholly composed of this substance. Carbonate

THE FOSSILIFEROUS ROCKS. 2I

of lime is soluble in water holding a certain amount of car-
bonic acid gas in solution ; and it is, therefore, found in larger
or smaller quantity dissolved in all natural waters, both fresh
and salt, since these waters are always to some extent charged
with the above-mentioned solvent gas. A great number of
aquatic animals, however, together with some aquatic plants,
are endowed with the power of separating the lime thus held
in solution in the water, and of reducing it again to its solid
condition. In this way shell-fish, crustaceans, sea-urchins,
corals, and an immense number of other animals, are enabled
to construct their skeletons; whilst some plants form hard
structures within their tissues in a precisely similar manner.
We do meet with some calcareous deposits, such as the
“stalactites” and “‘stalagmites” of caves, the ‘‘ calcareous
tufa” and ‘‘travertine” of some hot springs, and the spongy
calcareous deposits of so-called “ petrifying springs,” which
are purely chemical in their origin, and owe nothing to the
operation of living beings. Such deposits are formed simply
by the precipitation of carbonate of lime from water, in con-
sequence of the evaporation from the water of the carbonic
acid gas which formerly held the lime in solution ; but, though
sometimes forming masses of considerable thickness and of
geological importance, they do not concern us here. Almost
all the limestones which occur in the series of the stratified
rocks are, primarily at any rate, of organic origin, and have
been, directly or indirectly, produced by the action of certain
lime-making animals or plants, or both combined. The pre-
sumption as to all the calcareous rocks, which cannot be
clearly shown to have been otherwise produced, is that they
are thus organically formed ; and in many cases this presump-
tion can be readily reduced to a certainty. There are many
varieties of the calcareous rocks, but the following are those
which are of the greatest importance :—

Chalk is a calcareous rock of a generally soft and pulver-
ulent texture, and with an earthy fracture. It varies in its
purity, being sometimes almost wholly composed of carbonate
of lime, and at other times more or less intermixed with foreign
matter. Though usually soft and readily reducible to powder,
chalk is occasionally, as in the north of Ireland, tolerably hard
and compact; but it never assumes the crystalline aspect
and stony density of limestone, except it be in immediate
contact with some mass of igneous rock. By means of the
microscope, the true nature and mode of formation of chalk
can be determined with the greatest ease. In the case of the
harder varieties, the examination can be conducted by means

‘

22 PRINCIPLES OF PALAONTOLOGY.

of slices ground down to a thinness sufficient to render them ©
transparent ; but in the softer kinds the rock must be disinte-
grated under water, and the débris examined microscopically.
When investigated by either of these methods, chalk is found
to be a genuine organic rock, being composed of the shells or
hard parts of innumerable marine animals of different kinds,
some entire, some fragmentary, cemented together by a matrix
of very finely granular carbonate of lime. Foremost amongst
the animal remains which so largely compose chalk are the
shells of the minute creatures which will be subsequently
spoken of under the name of Foraminifera (fig. 7), and which,
in spite of their, microscopic
dimensions, play a more im-
portant part in the process of
lime-making than perhaps any
other of the larger inhabitants
of the ocean.

As chalk is found in beds
of hundreds of feet in thick-
ness, and of great purity, there
was long felt much difficulty
in satisfactorily accounting for
its mode of formation and or1-
gin. By the researches of
Carpenter, Wyville Thomson,

Fig. 7.—Section of Gravesend Chalk, Huxley, Wallich, and others,
examined by transmitted light and highly.
magnified. Besides the entire shells of 1t has, however, been shown
Globigerina, Rotaha, and Textularia, that there 1s now forming, in
numerous detached chambers of G/odi-
gerina are seen. (Original.) the profound depths of our

great oceans, a deposit which
is in all essential respects identical with chalk, and which is
generally known as the “ Atlantic ooze,” from its having been
first discovered in that sea. This ooze is found at great
depths (5000 to over 15,000 feet) in both the Atlantic and
Pacific, covering enormously large areas of the sea-bottom,
and it presents itself as a whitish-brown, sticky, impalpable mud,
very like greyish chalk when dried. Chemical examination
shows that the ooze is composed almost wholly of carbonate of
lime, and microscopical examination proves it to be of organic
origin, and to be made up of the remains of living beings.
The principal forms of these belong to the Foraminifera, and
the commonest of these are the irregularly-chambered shells of
Globigerina, absolutely indistinguishable from the Globigerine
which are so largely present in the chalk (fig. 8). Along with
these occur fragments of the skeletons of other larger creatures,

THE FOSSILIFEROUS ROCKS. 23

and a certain proportion of the flinty cases of minute animal
and vegetable organisms (Polycystina and Diatoms). Though
many of the minute animals,
the hard parts of which form
the ooze, undoubtedly live at
or near the surface of the sea,
others, probably, really live
near the bottom ; and the ooze
itself forms a congenial home
for numerous sponges, sea-
lies, and other marine ani-
mals which flourish at great
depths in the sea. There is
thus established an intimate
and most interesting parallel-
ism between the chalk and Fig. 8.—Organisms in the Atlantic Ooze,
the ooze of modern oceans. chiefly Foraminifera (Globigerina and
: : Textularia), with Polycystina and sponge-
Both are formed essentially IN spicules; highly magnified. (Original.)
the same way, and the latter
only requires consolidation to become actually converted into
chalk. Both are fundamentally organic deposits, apparently
requiring a great depth of water for their accumulation, and
mainly composed of the remains of Foraminifera, together
with the entire or broken skeletons of other marine animals of
greater dimensions. It is to be remembered, however, that the
ooze, though strictly representative of the chalk, cannot be
said in any proper sense to be actually zdentical with the for-
mation so called by geologists. A great lapse of time separates
the two, and though composed of the remains of representative
classes or groups of animals, it is only in the case of the lowly-
organised G/obigerine, and of some other organisms of little
higher grade, that we find absolutely the same kinds or sfecies
of animals in both.

Limestone, \ike chalk, 1s composed of carbonate of lime,
sometimes almost pure, but more commonly with a greater or
less intermixture of some foreign material, such as alumina or
silica. The varieties of limestone are almost innumerable,
but the great majority can be clearly proved to agree with
chalk in being essentially of organic origin, and in being more
or less largely composed of the remains of living beings. In
many instances the organic remains which compose limestone
are so large as to be readily visible to the naked eye, and the
rock is at once seen to be nothing more than an agglomera-
tion of the skeletons, generally fragmentary, of certain marine
animals, cemented together by a matrix of carbonate of lime.

24 PRINCIPLES OF PALAONTOLOGY.

This is the case, for example, with the so-called “ Crinoidal
Limestones ” and “ Encrinital Marbles” with which the geolo-
gist is so familiar, especially as occurring in great beds amongst
the older formations of the earth’s crust. ‘These are seen, on
weathered or broken surfaces, or still better in polished slabs
(fig. 9), to be composed more or less exclusively of the broken

Fig 9 —Slab of Crinoidal marble, from the Carboniferous limestone of Dent, in York-
shire, of the natural size. The polished surface intersects the columns of the Crinoids at
different angles, and thus gives rise to varying appearances. (Original.)

stems and detached plates of sea-lilies (Cvzzoids). Similarly,
other limestones are composed almost entirely of the skeletons
of corals; and such old coralline limestones can readily be
paralleled by formations which we can find in actual course of
production at the present day. We only need to transport
ourselves to the islands of the Pacific, to the West Indies, or
to the Indian Ocean, to find great masses of lime formed simi-
larly by living corals, and well known to every one under the
name of “coral-reefs.” Such reefs are often of vast extent,
both superficially and in vertical thickness, and they fully equal
in this respect any of the coralline limestones of bygone ages.
Again, we find other limestones—such as the celebrated
“Nummulitic Limestone” (fig. 10), which sometimes attains a
thickness of some thousands of feet—which are almost entirely
made up of the shells of Foraminifera. In the case of the
“*Nummulitic Limestone,” just mentioned, these shells are of
large size, varying from the size of a split pea up to that ofa

THE FOSSILIFEROUS ROCKS. : 25

florin. There are, however, as we shall see, many other lime-
stones, which are likewise largely made up of /oraminzfera,

= Bol) AN \ \\ NG Ly
TRL WANA < <Za\-
i: iN nigh /}

Fig. 10.—Piece of Nummulitic Limestone from the Great Pyramid.
Of the natural size. (Original.)

but in which the shells are very much more minute, and would
hardly be seen at all without the microscope.

We may, in fact, consider that the great agents in the pro-
duction of limestones in past ages have been animals belonging
to the Crinoids, the Corals, and the Foraminifera. At the pre-
sent day, the Crinoids have been nearly extinguished, and the
few known survivors seem to have retired to great depths in
the ocean; but the two latter still actively carry on the work
of lime-making, the former being very largely helped in their
operations by certain lime- producing marine plants (lVud/ipores
and Corallines). We have to remember, however, that though
the limestones, both ancient and modern, that we have just
spoken of, are truly organic, they are not necessarily formed
out of the remains of animals which actually hved on the
precise spot where we now find the limestone itself. We may
find a crinoidal limestone, which we can show to have been
actually formed by the successive growth of generations of
sea-lilies zz place ; but we shall find many others in which the
rock is made up of innumerable fragments of the skeletons of
these creatures, which have been clearly worn and rubbed by
the sea-waves, and which have been mechanically transported
to their present site. In the same way, a limestone may be
shown to have been an actual coral-reef, by the fact that we
find in it great masses of coral, growing in their natural posi-

26 PRINCIPLES OF PALAONTOLOGY.

tion, and exhibiting plain proofs that they were simply quietly
buried by the calcareous sediment as they grew; but other
limestones may contain only numerous rolled and water-worn
fragments of corals. This is precisely paralleled by what we
can observe in our existing coral-reefs. Parts of the modern
coral-islands and coral-reefs are really made up of corals, dead
or alive, which actually grew on the spot where we now find
them; but other parts are composed of a limestone-rock
(“coral-rock”), or of a loose sand (“‘coral-sand”), which is
organic in the sense that it is composed of lime formed by
living beings, but which, in truth, is composed of fragments
of the skeletons of these living beings, mechanically trans-
ported and heaped together by the sea. To take another
example nearer home, we may find great accumulations of
calcareous matter formed zz Place, by the growth of shell-fish,
such as oysters or mussels ; but we can also find equally great
accumulations on many of our shores in the form of “shell-
sand,” which is equally composed of the shells of molluscs, but
which is formed by the trituration of these shells by the
mechanical power of the sea-waves. We thus see that though
all these limestones are primarily organic, they not uncom-
monly become ‘‘mechanically-formed” rocks in a secondary
sense, the materials of which they are composed being formed
by living beings, but having been mechanically transported to
the place where we now find them.

Many limestones, as we have seen, are composed of large
and conspicuous organic remains, such as strike the eye at
once. Many others, however, which at first sight appear com-
pact, more or less crystalline, and nearly devoid of traces of
life, are found, when properly examined, to be also composed
of the remains of various organisms. All the commoner lime-
stones, in fact, from the Lower Silurian period onwards, can
be easily proved to be thus organze rocks, if we investigate
weathered or polished surfaces with a lens, or, still better, if
we cut thin slices of the rock and grind these down till they
are transparent. When thus examined, the rock is usually
found to be composed of innumerable entire or fragmentary
fossils, cemented together by a granular or crystalline matrix
of carbonate of lime (figs. 11 and r2). When the matrix is
granular, the rock is precisely similar to chalk, except that it
is harder and less earthy in texture, whilst the fossils are only
occasionally referable to the Foraminifera. In other cases,
the matrix is more or less crystalline, and when this crystallisa-
tion has been carried to a great extent, the original organic
nature of the rock may be greatly or completely obscured

THE FOSSILIFEROUS ROCKS. 27

thereby. Thus, in limestones which have been greatly altered
or “metamorphosed” by the combined action of heat and pres-

>
Nee
,
*

Fig. 311.— Section of Carboniferous Fig. 12.—Section of Coniston Limestone
Limestone from Spergen Hill, Indiana, (Lower Silurian) from Keisley, Westmore-
U.S., showing numerous large-sized land; magnified. The matrix isvery coarse-
Foraminifera (Endothyra) and a few ly crystalline, and the included organic re-
oolitic grains; magnified. (Original.) mains are chiefly stems of Crinoids. (Ori-

ginal.)

sure, all traces of organic remains become annihilated, and the
rock becomes completely crystalline throughout. This, for
example, is the case with the ordinary white “statuary marble,”
slices of which exhibit under the microscope nothing but an
aggregate of beautifully transparent crystals of carbonate of
lime, without the smallest traces of fossils. ‘There are also
other cases, where the limestone is not necessarily highly
crystalline, and where no metamorphic action in the strict
sense has taken place, in which, nevertheless, the microscope
fails to reveal any evidence that the rock is organic. Such
cases are somewhat obscure, and doubtless depend on differ-
ent causes in different instances; but they do not affect the
important generalisation that limestones are fundamentally the
product of the operation of living beings. This fact remains
certain; and when we consider the vast superficial extent
occupied by calcareous deposits, and the enormous collective
thickness of these, the mind cannot fail to be impressed with
the immensity of the period demanded for the formation of
these by the agency of such humble and often microscopic
creatures as Corals, Sea-lilies, Foraminifers, and Shell-fish.
Amongst the numerous varieties of limestone, a few are of
such interest as to deserve a brief notice. Magnesian limestone-
or dolomite, differs from ordinary limestone in containing a cer-
tain proportion of carbonate of magnesia along with the carbon,
ate of lime. The typical dolomites contain a large proportion of

28 PRINCIPLES OF PALZONTOLOGY.

carbonate of magnesia, and are highly crystalline. The ordi-
nary magnesian limestones (such as those of Durham in the
Permian series, and the Guelph Limestones of North America
in the Silurian series) are generally of a yellowish, buff, or
brown colour, with a crystalline or pearly aspect, effervescing
with acid much less freely than ordinary limestone, exhibiting
numerous cavities from which fossils have been dissolved out,
and often assuming the most varied and singular forms in con-
sequence of what is called ‘“‘ concretionary action.’ Examina-
tion with the microscope shows that these limestones are
composed of an aggregate of minute but perfectly distinct
crystals, but that minute organisms of different kinds, or
fragments of larger fossils, are often present as well. Other
magnesian limestones, again, exhibit no striking external pecu-
liarities by which the presence of magnesia would be readily
recognised, and though the base of the rock is crystalline, they
are replete with the remains of organised beings. Thus many
of the magnesian limestones of the Carboniferous series of the
North of England are very like ordinary limestone to look at,
though effervescing less freely with acids, and the microscope
proves them to be charged with the remains of Foraminifera
and other minute organisms.

Marbles are of various kinds, all limestones which are suffi-
ciently hard and compact to take a high polish going by this
name. Statuary marble, and most of the celebrated foreign
marbles, are ‘‘metamorphic” rocks, of a highly crystalline
nature, and having all traces of their primitive organic struc-
ture obliterated. Many other marbles, however, differ from
ordinary limestone simply in the matter of density. Thus,
many marbles (such as Derbyshire marble) are simply “ cri-
noidal limestones” (fig. 9); whilst various other British
marbles exhibit innumerable organic remains under the mi-
croscope. Black marbles owe their colour to the presence of
very minute particles of carbonaceous matter, in some cases
at any rate; and they may either be metamorphic, or they
may be charged with minute fossils such as Foraminifera (eg.,
the black limestones of Ireland, and the black marble of Dent,
in Yorkshire).

“ Oolitic” limestones, or “ oolites,” as they are often called,
are of interest both to the paleontologist and geologist. The
peculiar structure to which they owe their name is that the
rock is more or less entirely composed of spheroidal or oval
grains, which vary in size from the head of a small pin or less
up to the size of a pea, and which may be in almost immediate
contact with one another, or may be cemented together by a

THE FOSSILIFEROUS ROCKS. 29

more or less abundant calcareous matrix. When the grains
are pretty nearly spherical and are in tolerably close contact,
the rock looks very like the roe of a fish, and the name of
“oolite” or ‘‘egg-stone” is in allusion to this. When the
grains are of the size of peas or upwards, the rock is often
called a “pisolite” (Lat. pzswm, a pea). Limestones having
this peculiar structure are especially abundant in the Jurassic
formation, which is often called the ‘‘ Oolitic series ” for this
reason ; but essentially similar limestones occur not uncom-
monly in the Silurian, Devonian, and Carboniferous forma-
tions, and, indeed, in almost all rock-groups in which limestones
are largely developed. Whatever may be the age of the for-
mation in which they occur, and whatever may be the size of
their component “eggs,” the structure of oolitic limestones is
fundamentally the same. All the ordinary oolitic limestones,
namely, consist of little spherical or ovoid ‘ concretions,” as
they are termed, cemented together by a larger or smaller
amount of crystalline carbonate of lime, together, in many
instances, with numerous organic remains of different kinds
(fig. 13). When examined in polished slabs, or in thin sec-
tions prepared for the micro-
scope, each of these little con-
cretions is seen to consist of
numerous concentric coats of
carbonate of lime, which some-
times simply surround an ima-
ginary centre, but which, more
commonly, have been suc-
cessively deposited round
some foreign body, such as a
little crystal of quartz, a clus-
ter of sand-grains, or a minute
shell. In other cases, as in
some of the beds of the Car- Fig. 13.—Slice of oolitic limestone
boniferous limestone in the Wun Cee ean (Oey a
North of England, where the

limestone is highly “‘arenaceous,” there isa modification of the
oolitic structure. Microscopic sections of these sandy lime-
stones (fig. 14) show numerous generally angular or oval grains
of silica or flint, each of which is commonly surrounded by a
thin coating of carbonate of lime, or sometimes by several such
coats, the whole being cemented together along with the shells
of Foraminifera and other minute fossils by a matrix of crystal-
line calcite. As compared with typical oolites, the concretions
in these oe are usually much more irregular in shape,

30 PRINCIPLES OF PALAONTOLOGY.

often lengthened out and almost cylindrical, at other times
angular, the central nucleus being of large size, and the sur-
rounding envelope of lime be-
ing very thin, and often exhib-
iting no concentric structure.
In both these and the ordinary
oolites, the structure is funda-
mentally the same. Both have
been formed in a sea, probably
of no great depth, the waters
of which were charged with
carbonate of lime in solution,
whilst the bottom was formed
of sand intermixed with minute
shells and fragments of the

Fig. 14.—Slice of arenaceous and skeletons of larger marine ani-
oolitic limestone from the Carbonifer- mals. The excess of lime in

ous series of Shap, Westmoreland ; mag- Sia
nified. The section also exhibits Fora- the sea-water was precipitated

ee and other minute fossils. (Ori- Touncitne sand-grains, Reena
the smaller shells, as so many
nuclei, and this precipitation must often have taken place time
after time, so as to give rise to the concentric structure so char-
acteristic of oolitic concretions. Finally, the oolitic grains thus
produced were cemented together by a further precipitation of
crystalline carbonate of lime from the waters of the ocean.
Phosphate of Lime is another lime-salt, which is of interest
to the paleontologist. It does not occur largely in the strati-
fied series, but it is found in considerable beds * in the
Laurentian formation, and less abundantly in some later rock-
groups, whilst it occurs abundantly in the form of nodules in
parts of the Cretaceous (Upper Greensand) and Tertiary
deposits. Phosphate of lime forms the larger proportion of
the earthy matters of the bones of Vertebrate animals, and also
occurs in less amount in the skeletons of certain of the Inver-
tebrates (¢.g., Crustacea). It is, indeed, perhaps more dis-
tinctively than carbonate of lime, an organic compound ; and
though the formation of many known deposits of phosphate of

* Apart from the occurrence of phosphate of lime in actual beds in the
stratified rocks, as in the Laurentian and Silurian series, this salt may also
occur disseminated through the rock, when it can only be detected by
chemical analysis. It is interesting to note that Dr Hicks has recently
proved the occurrence of phosphate of lime in this disseminated form in
rocks as old as the Cambrian, and that in quantity quite equal to what is
generally found to be present in the later fossiliferous rocks. This affords
a chemical proof that animal life flourished abundantly in the Cambrian
seas.

THE FOSSILIFEROUS ROCKS. 31

lime cannot be positively shown to be connected with the
previous operation of living beings, there is room for doubt
whether this salt is not in reality always primarily a product
of vital action. ‘The phosphatic nodules of the Upper Green-
sand are erroneously called ‘ coprolites,” from the belief
originally entertained that they were the droppings or fossilised
excrements of extinct animals ; and though this is not the case,
_there can be little doubt but that the phosphate of lime which
they contain is in this instance of organic origin.* It appears,
in fact, that decaying animal matter has a singular power of
determining the precipitation around it of mineral salts dis-
solved in water. Thus, when any animal bodies are undergo-
ing decay at the bottom of the sea, they have a tendency to
cause the precipitation from the surrounding water of any
mineral matters which may be dissolved in it ; and the organic
body thus becomes a centre round which the mineral matters
in question are deposited in the form of a “concretion” or
“nodule.” The phosphatic nodules in question were formed
in a sea in which phosphate of lime, derived from the destruc-
tion of animal skeletons, was held largely in solution ; and a
precipitation of it took place round any body, such as a decay-
ing animal substance, which happened to be lying on the sea-
bottom, and which offered itself as a favourable nucleus. In
the same way we may explain the formation of the calcareous
nodules, known as ‘“‘septaria” or ‘‘cement stones,” which
occur so commonly in the London Clay and Kimmeridge
Clay, and in which the principal ingredient is carbonate of
lime. A similar origin is to be ascribed to the nodules of
clay iron-stone (impure carbonate of iron) which occur so
abundantly in the shales of the Carboniferous series and in’
other argillaceous deposits ; and a parallel modern example is
to be found in the nodules of manganese, which were found
by Sir Wyville Thomson, in the Challenger, to be so numer-
ously scattered over the floor of the Pacific at great depths.
In accordance with this mode of origin, it is exceedingly
common to find in the centre of all these nodules, both old
and new, some organic body, such as a bone, a shell, or a
tooth, which acted as the original nucleus of precipitation, and

* It has been maintained, indeed, that the phosphatic nodules so largely
worked for agricultural purposes, are in themselves actual organic bodies
or true fossils. In a few cases this admits of demonstration, as it can be
shown that the nodule is simply an organism (such as a sponge) infiltrated
with phosphate of lime (Sollas) ; but there are many other cases in which
no actual structure has yet been shown to exist, and as to the true origin
of which it would be hazardous to offer a positive opinion.

“32 PRINCIPLES OF PALZONTOLOGY.

was thus preserved in a shroud of mineral matter. Many
nodules, it is true, show no such nucleus; but it has been
affirmed that all of them can be shown, by appropriate
microscopical investigation, to have been formed round an
original organic body to begin with (Hawkins Johnson).

The last lime-salt which need be mentioned is gypsum, or
sulphate of lime. This substance, apart from other modes of
occurrence, 1s not uncommonly found interstratified with the
ordinary sedimentary rocks, in the form of more or less irregu-
lar beds; and in these cases it has a paleontological import-
ance, as occasionally yielding well-preserved fossils. Whilst
its exact mode of origin is uncertain, it cannot be regarded as
in itself an organic rock, though clearly the product of chemical
action. To look at, it is usually a whitish or yellowish-white
rock, as coarsely crystalline as loaf-sugar, or more so; and the
microscope shows it to be composed entirely of crystals of
sulphate of lime.

We have seen that the calcareous or lime-containing rocks
are the most important of the group of organic deposits; whilst
the sz/ceous or flint-containing rocks may be regarded as the
most important, most typical, and most generally distributed
of the mechanically-formed rocks. We have, however, now
briefly to consider certain deposits which are more or less
completely formed of flint ; but which, nevertheless, are essen-
tially organic in their origin.

Flint or silex, hard and intractable as it is, is nevertheless
capable of solution in water to a certain extent, and even of
assuming, under certain circumstances, a gelatinous or viscous
condition. Hence, some hot-springs are impregnated with
silica to a considerable extent ; it is present in small quantity
in sea-water; and there is reason to believe that a minute pro-
portion must very generally be present in all bodies of fresh
water as well. It is from this silica dissolved in the water that
many animals and some plants are enabled to construct for
themselves flinty skeletons; and we find that these animals and
plants are and have been sufficiently numerous to give rise to
very considerable deposits of siliceous matter by the mere
accumulation of their skeletons. Amongst the animals which
require special mention in this connection are the microscopic
organisms which are known to the naturalist as Polycystina.
These little creatures are of the lowest possible grade of organ-
isation, very closely related to the animals which we ‘have pre-
viously spoken of as Foraminifera, but differing in the fact that
they secrete a shell or skeleton composed of flint instead of
lime. The folycystina occur abundantly in our present seas ;

THE FOSSILIFEROUS ROCKS. 33

and their shells are present in some numbers in the ooze which
is found at great depths in the Atlantic and Pacific oceans,
being easily recognised by their exquisite shape, their glassy
transparency, the general presence of longer or shorter spines,
and the sieve-like perforations in the walls. Both in Barbadoes
and in the Nicobar islands occur geological formations which
are composed of the flinty skeletons of these microscopic
animals; the deposit in the former locality attaining a great
thickness, and having been long known to workers with the
microscope under the name of ‘‘ Barbadoes earth” (fig. 15).
In addition to flint- producing animals, we have also the
great group of fresh-water and marine microscopic plants

Fig. 15.—Shells of Polycystina from Fig. 16.—Cases of Diatoms in the Rich-
“‘Barbadoes earth;” greatly magnified. mond ‘‘Infusorial earth;” highly magni-
(Original.) fied. (Original.)

known as Diatoms, which likewise secrete a siliceous skeleton,
often of great beauty. The skeletons of Diatoms are found
abundantly at the present day in lake-deposits, guano, the silt
of estuaries, and in the mud which covers many parts of the
sea-bottom ; they have been detected in strata of great age;
and in spite of their microscopic dimensions, they have not un-
commonly accumulated to form deposits of great thickness,
and of considerable superficial extent. Thus the celebrated
deposit of “‘tripoli” (“ Polir-schiefer”) of Bohemia, largely
worked as polishing-powder, is composed wholly, or almost
wholly, of the flinty cases of Diatoms, of which it is calculated
that no less than forty-one thousand millions go to make up a
single cubic inch of the stone. Another celebrated deposit is
the so-cailed ‘“ Infusorial earth” of Richmond in Virginia,
where there is a stratum in places thirty feet thick, composed
almost entirely of the microscopic shells of Diatoms.

Nodules or layers of fmt, or the impure variety of flint

34 PRINCIPLES ; OF PALZONTOLOGY.

known as chert, are found in limestones of almost all ages from
the Silurian upwards; but they are especially abundant in the
chalk. When these flints are examined in thin and trans-
parent slices under the microscope, or in polished sections,
they are found to contain an abundance of minute organic
bodies—such as Foraminifera, sponge-spicules, &c.—embedded
in a siliceous basis. In many instances the flint contains
larger organisms—such as a Sponge or a Sea-urchin. As the
flint has completely surrounded and infiltrated the fossils which
it contains, it is obvious that it must have been deposited from
sea-water in a gelatinous condition, and subsequently have
hardened. That silica is capable of assuming this viscous and
soluble condition is known; and the formation of flint may
therefore be regarded as due to the separation of silica from
the sea-water and its deposition round some organic body in a
state of chemical change or decay, just as nodules of phos-
phate of lime or carbonate of iron are produced. The exist-
ence of numerous organic bodies in flint has long been known;
but it should be added that a recent observer (Mr Hawkins
Johnson) asserts that the existence of an organic structure can
be demonstrated by suitable methods of treatment, even in the
actual matrix or basis of the flint.*

In addition to deposits formed of flint itself, there are other
siliceous deposits formed by certain sz/zcafes, and also of
organic origin. It has been shown, namely—by observations
carried out in our present seas—that the shells of Foraminifera
are liable to become completely infiltrated by silicates (such
as “‘ glauconite,” or silicate of iron and potash). Should the
actual calcareous shell become dissolved away subsequent to
this infiltration—as is also liable to occur—then, in place of
the shells of the Foraminifera, we get a corresponding number
of green sandy grains of glauconite, each grain being the cast
of a single shell. It has thus been shown that the green sand
found covering the sea-bottom in certain localities (as found
by the Challenger expedition along the line of the Agulhas
current) is really organic, and is composed of casts of the
shells of Foraminifera. Long before these observations had
been made, it had been shown by Professor Ehrenberg that
the green sands of various geological formations are composed
mainly of the internal casts of the shells of Foraminifera ; and

* It has been asserted that the flints of the chalk are merely fossil
sponges. No explanation of the origin of flint, however, can be satisfac-
tory, unless it embraces the origin of chert in almost all great limestones
from the Silurian upwards, as well as the common phenomenon of the
silicification of organic bodies (such as corals and shells) which are known
with certainty to have been originally calcareous.

THE FOSSILIFEROUS ROCKS. 35

we have thus another and avery interesting example how rock-
deposits of considerable extent and of geological importance
can be built up by the operation of the minutest living beings.

As regards argz//aceous deposits, containing alumina or clay
as their essential ingredient, it cannot be said that any of
these have been actually shown to be of organic origin. A
recent observation by Sir Wyville Thomson would, however,
render it not improbable that some of the great argillaceous.
accumulations of past geological periods may be really organic.
This distinguished observer, during the cruise of the Chal-
lenger, showed that the calcareous ooze which has_ been
already spoken of as covering large areas of the floor of the
Atlantic and Pacific at great depths, and which consists almost
wholly of the shells of Foraminifera, gave place at still greater
depths to a red ooze consisting of impalpable clayey mud,
coloured by oxide of iron, and devoid of traces of organic
bodies. As the existence of this widely-diffused red ooze, in
mid-ocean, and at such great depths, cannot be explained on
the supposition that it is a sediment brought down into the
sea by rivers, Sir Wyville Thomson came to the conclusion
that it was probably formed by the action of the sea-water
upon the shells of Foraminifera. ‘These shells, though mainly
consisting of lime, also contain a certain proportion of alumina,
the former being soluble in the carbonic acid dissolved in the
sea-water, whilst the latter is insoluble. There would further
appear to be grounds for believing that the solvent power of
the sea-water over lime is considerably increased at great
depths. If, therefore, we suppose the shells of Foraminifera
to be in course of deposition over the floor of the Pacific, at
certain depths they would remain unchanged, and would ac-
cumulate to form a calcareous ooze; but at greater depths they
would be acted upon by the water, their lime would be dis-
solved out, their form would disappear, and we should simply
have left the small amount of alumina which they previously
contained. In process of time this alumina would accumulate
to form a bed of clay; and as this clay had been directly
derived from the decomposition of the shells of animals, it
would be fairiy entitled to be considered an organic deposit.
Though not finally established, the hypothesis of Sir Wyville
Thomson on this subject is of the greatest interest to the palz-
ontologist, as possibly serving to explain the occurrence, espe-
cially in the older formations, of great deposits of argillaceous
matter which are entirely destitute of traces of life.

It only remains, in this connection, to shortly consider the
rock-deposits in which carbon is found to be present in greater

36 PRINCIPLES OF PALAZONTOLOGY.

or less quantity. In the great majority of cases where rocks
are found to contain carbon or carbonaceous matter, it can be
stated with certainty that this substance is of organic origin,
though it is not necessarily derived from vegetables. Carbon
derived from the decomposition of animal bodies is not uncom-
mon; though it never occurs in such quantity from this source
as it may do when it is derived from plants. Thus, many
limestones are more or less highiy bituminous ; the celebrated
siliceous flags or so-called ‘‘ bituminous schists” of Caithness
are impregnated with oily matter apparently derived from the
decomposition of the numerous fishes embedded in them ;
Silurian shales containing Graptolites, but destitute of plants,
are not uncommonly ‘‘anthracitic,’ and contain a small per-
centage of carbon derived from the decay of these zoophytes ;
whilst the petroleum so largely worked in North America has
not improbably an animal] origin. ‘That the fatty compounds
present in animal bodies should more or less extensively im-
pregnate fossiliferous rock-masses, is only what might be ex-
pected ; but the great bulk of the carbon which exists stored
up in the earth’s crust is derived from plants ; and the form in
_which it principally presents itself is that of coal. We shall
have to speak again, and at greater length, of coal, and it is
sufficient to say here that all the true coals, anthracites, and
lignites, are of organic origin, and consist principally of the
remains of plants in a more or less altered condition. The
bituminous shales which are found so commonly associated
with beds of coal also derive their carbon primarily from
plants ; and the same is certainly, or probably, the case with
similar shales which are known to occur in formations younger
than the Carboniferous. Lastly, carbon may occur as a con-
spicuous constituent of rock-masses in the form of graphite or
black-lead. In this form, it occurs in the shape of detached
scales, of veins or strings, or sometimes of regular layers ;*
and there can be little doubt that in many instances it has
an organic origin, though this is not capable of direct proof.
When present, at any rate, in quantity, and in the form of layers
associated with stratified rocks, as is often the case in the Lau-
rentian formation, there can be little hesitation in regarding it
as of vegetable origin, and as an altered coal.

* In the Huronian formation at Steel River, on the north shore of Lake
Superior, there exists a bed of carbonaceous matter which is regularly in-
terstratified with the surrounding rocks, and has a thickness of from 30 to
40 feet. This bed is shown by chemical analysis to contain about 50 per
cent of carbon, partly in the form of graphite, partly in the form of anthra-
cite ; and there can be little doubt but that it is really a stratum of ae
morphic ” coal.

CHRONOLOGICAL SUCCESSION. 37

CHAR PER Tit

CHRONOLOGICAL SUCCESSION OF THE
FOSSILIFEROUS ROCKS.

The physical geologist, who deals with rocks simply as rocks,
and who does not necessarily trouble himself about what fossils
they may contain, finds that the stratified deposits which form
so large a portion of the visible part of the earth’s crust are
not promiscuously heaped together, but that they have a cer-
tain definite arrangement. In each country that he examines,
he finds that certain groups of strata lie above certain other
groups ; and in comparing different countries with one another,
he finds that, in the main, the same groups of rocks are always
found in the same relative position to each other. It is pos-
sible, therefore, for the physical geologist to arrange the known
stratified rocks into a successive series of groups, or ‘ forma-
tions,” having a certain definite order. The establishment of
this physical order amongst the rocks introduces, however, at
once the element of “me, and the physical succession of the
strata can be converted directly into a historical or chronologt-
cal succession. ‘This is obvious, when we reflect that any bed
or set of beds of sedimentary origin is clearly and necessarily
younger than all the strata upon which it rests, and older than
all those by which it is surmounted.

It is possible, then, by an appeal to the rocks alone, to de-
termine in each country the general physical succession of the
strata, and this “‘ stratigraphical” arrangement, when once de-
termined, gives us the rve/atzve ages of the successive groups.
The task, however, of the physical geologist in this matter is
immensely lightened when he calls in palzontology to his aid,
and studies the evidence of the fossils embedded in the rocks.
Not only is it thus much easier to determine the order of suc-
cession of the strata in any given region, but it becomes now
for the first time possible to compare, with certainty and pre-
cision, the order of succession in one region with that which
exists in other regions far distant. The value of fossils as tests
of the relative ages of the sedimentary rocks depends on the
fact that they are not indefinitely or promiscuously scattered
through the crust of the earth,—as it is conceivable that they
might be. On the contrary, the first and most firmly estab-
lished law of Paleontology is, that particular kinds of fossils

\

38 PRINCIPLES OF PALAZONTOLOGY.

are confined to particular rocks, and particular groups of fossils
are confined to particular groups of rocks. Fossils, then, are
distinctive of the rocks in which they are found—much more
distinctive, in fact, than the mere mineral character of the rock
can be, for iat commonly changes as a formation is traced
from one region to another, whilst the fossils remain unaltered.
It would therefore be quite possible for the palzontologist,
by an appeal to the fossils alone, to arrange the series of sedi-
mentary deposits into a pile of strata having a certain definite
order. Not only would this be possible, but it would be found
—if sufficient knowledge had been brought to bear on both
sides—that the paleontological arrangement of the strata would
coincide in its details with the stratigraphical or physical
arrangement.

Happily for science, there is no such division between the
paleontologist and the physical geologist as here supposed ;
but by the combined researches of the two, it has been found
possible to divide the entire series of stratified deposits into a
number of definite zock-groups or formations, which have a
recognised order of succession, and each of which is charac-
terised by possessing an assemblage of organic remains which
do not occur in association in any other formation. Such an
assemblage of fossils, characteristic of any given formation, re-
presents the “fe of the particular fevzod in which the formation
was deposited. In this way the past history of the earth
becomes divided into a series of successive /ife-fertods, each of
which corresponds with the deposition of a particular forma-
tion or group of strata.

Whilst particular assemblages of organic forms characterise
particular groups of rocks, it may be further said that, in a
general way, each subdivision of each formation has its own
peculiar fossils, by which it may be recognised by a skilled
worker in Paleontology. Whenever, for instance, we meet
with examples of the fossils which are known as Graftolites, we
may be sure that we are dealing with S7/wrzan rocks (leaving
out of sight one or two forms doubtfully referred to this family).
We may, however, go much farther than this with perfect
safety. If the Graptolites belong to certain genera, we may
be quite certain that we are dealing with Zower Silurian rocks.
Furthermore, if certain special forms are present, we may be
even able to say to what exact subdivision of the Lower Silu-
rian series they belong.

As regards particular fossils, however, or even particular
classes of fossils, conclusions of this nature require to be accom-
panied by a tacit but well-understood reservation. So far as

CHRONOLOGICAL SUCCESSION. 39

our present observation goes, none of the undoubted Grapto-
lites have ever been discovered in rocks later than those known
upon other grounds to be Silurian ; but it is possible that they
might at any time be detected in younger deposits. Similarly,
the species and genera which we now regard as characteristic
of the Lower Silurian, may at some future time be found to
have survived into the Upper Silurian period. We should not
forget, therefore, in determining the age of strata by paleeonto-
logical evidence, that we are always reasoning upon generalisa-
tions which are the result of experience alone, and which are
liable to be vitiated by further and additional discoveries.
When the palzontological evidence as to the age of any
given set of strata is corroborated by the physical evidence, our
conclusions may be regarded as almost certain ; but there are
certain limitations and fallacies in the palzontological method
of inquiry which deserve a passing mention. In the first
place, fossils are not always present in the stratified rocks;
many aqueous rocks are unfossiliferous, through a thickness of
hundreds or even thousands of feet of little-altered sediments ;
and even amongst beds which do contain fossils, we often meet
with strata of many feet or yards in thickness which are wholly
destitute of any traces of fossils. ‘There are, therefore, to
begin with, many cases in which there is no palzontological
evidence extant or available as to the age of a given group
of strata. In the second place, paleontological observers in
different parts of the world are liable to give different names
to the same fossil, and in all parts of the world they are occa-
sionally lable to group together different fossils under the
same title. Both these sources of fallacy require to be guarded
against in reasoning as to the age of strata from their fossil
remains. Thirdly, the mere fact of fossils being found in beds
which are known by physical evidence to be of different ages,
‘ has commonly led palzontologists to describe them as dif-
ferent species. Thus, the same fossil, occurring in successive
groups of strata, and with the merely trivial and varietal differ-
ences due to the gradual change in its environment, has been
repeatedly described as a distinct species, with a distinct
name, in every bed in which it was found. We know, however,
that many fossils range vertically through many groups of strata,
and there are some which even pass through several forma-
tions. The mere fact of a difference of physical position
ought never to be taken into account at all in considering and
determining the true affinities of a fossil. Fourthly, the
results of experience, instead of being an assistance, are some-
times liable to operate as a source of error. When once,

40 PRINCIPLES OF PALZONTOLOGY.

namely, a generalisation has been established that certain
fossils occur in strata of a certain age, palzontologists are apt
to infer that a beds containing similar fossils must be of the
same age. ‘There is a presumption, of course, that this infer-
ence would be correct; but it is not a conclusion resting upon
absolute necessity, and there might be physical evidence to
disprove it. Fifthly, the physical geologist may lead the pale-
ontologist astray by asserting that the physical evidence as to
the age and position of a given group of beds is clear and un-
equivocal, when such evidence may be, in reality, very slight
and doubtful. In this way, the observer may be readily led |
into wrong conclusions as to the nature of the organic remains
—often obscure and fragmentary—which it is his business to
examine, or he may be led erroneously to think that previous
generalisations as to the age of certain kinds of fossils are
premature and incorrect. Lastly, there are cases in which,
owing to the limited exposure of the beds, to their being
merely of local development, or to other causes, the physical
evidence as to the age of a given group of strata may be en-
tirely uncertain and unreliable, and in which, therefore, the
observer has to rely wholly upon the fosstls which he may
meet with.

In spite of the above limitations and fallacies, there can be
no doubt as to the enormous value of palzontology in enab-
ling us to work out the historical succession of the sedimentary
rocks. It may even be said that in any case where there
should appear to be a clear and decisive discordance between
the physical and the paleontological evidence as to the age
of a given series of beds, it is the former that is to be distrusted
rather than the latter. The records of geological science con-
tain not a few cases in which apparently clear physical evi-
dence of superposition has been demonstrated to have been
wrongly interpreted ; but the evidence of paleontology, when
in any way sufficient, has rarely been upset by subsequent
investigations. Should we find strata containing plants of the
Coal-measures apparently resting upon other strata with Am-
monites and Belemnites, we may be sure that the physical
evidence is delusive ; and though the above is an extreme case,
the presumption in all such instances is rather that the physical
succession has been misunderstood or misconstrued, than that
there has been a subversion of the recognised succession of
life-forms.

We have seen, then, that as the collective result of observa-
tions made upon the superposition of rocks in different locali-
ties, from their mineral characters, and from their included

CHRONOLOGICAL SUCCESSION. 4I

fossils, geologists have been able to divide the entire stratified
series into a number of different divisions or formations, each
characterised by a genera/ uniformity of mineral composition,
and by a special and peculiar assemblage of organic forms.
Each of these primary groups is in turn divided into a series of
smaller divisions, characterised and distinguished in the same
way. It is not pretended for a moment that all these primary
rock-groups can anywhere be seen surmounting one another
regularly.* There is no region upon the earth where all
the stratified formations can be seen together; and, even
when most of them occur in the same country, they can
nowhere be seen all succeeding each other in their regular and
uninterrupted succession. The reason of this is obvious.
There are many places—to take a single example—where one
may see the the Silurian rocks, the Devonian, and the Carbon-
iferous rocks succeeding one another regularly, and in their
proper order. ‘This is because the particular region where this
occurs was always submerged beneath the sea while these for-
mations were being deposited. There are, however, many
more localities in which one would find the Carboniferous
rocks resting unconformably upon the Silurians without the
intervention of any strata which could be referred to the
Devonian period. This might arise from one of two causes:
1. The Silurians might have been elevated above the sea im-
mediately after their deposition, so as to form dry land during
the whole of the Devonian period, in which case, of course,
no strata of the latter age could possibly be deposited in that
area. 2. The Devonian might have been deposited upon the
Silurian, and then the whole might have been elevated above
the sea, and subjected to an amount of denudation sufficient to
remove the Devonian strata entirely. In this case, when the
land was again submerged, the Carboniferous rocks, or any
younger formation, might be deposited directly upon Silurian
strata. From one or other of these causes, then, or from subse-
quent disturbances and denudations, it happens that we can

* As we have every reason to believe that dry land and sea have existed, at
any rate from the commencement of the Laurentian period to the present day,
it is quite obvious that no one of the great formations can ever, under any cir-
cumstances, have extended over the entire globe. In other words, no one of
the formations can ever have had a greater geographical extent than that of
the seas of the period in which the formation was deposited. Nor is there any
reason for thinking that the proportion of dry land to ocean has ever been
materially different to what it is at present, however greatly the areas of sea
and land may have changed as regards their place. It follows from the above,
that there is no sufficient basis for the view that the crust of the earth is com-
posed of a succession of concentric layers, like the coats of an onion, each
layer representing one formation.

42 PRINCIPLES OF PALZONTOLOGY.

rarely find many of the primary formations following one
another consecutively and in their regular order.

In no case, however, do we ever find the Devonian resting
upon the Carboniferous, or the Silurian rocks reposing on the
Devonian. We have therefore, by a comparison of many
different areas, an established order of succession of the strati-
fied formations, as shown in the subjoined ideal section of the
crust of the earth (fig. 17).

The main subdivisions of the stratified rocks are known by
the following names :-—

Laurentian.

Cambrian (with Huronian ?).

Silurian.

Devonian or Old Red Sandstone.

. Carboniferous.

aces kn ew Red Sandstone.
riassic

Jurassic or Oolitic.

Cretaceous.

Eocene.

11. Miocene.

12. Pliocene.

13. Post-tertiary.

Lo]
OSS coo STNG Gy Ne

IL AINOZOIC.

PALAOZOIC.

CHRONOLOGICAL SUCCESSION.~— 43

IDEAL SECTION OF THE CRUST OF THE EARTH.

_—<———
SSS
sag a ———. a — -

SSS Se

we eee Ste Neate
aay (a at Tae Fa |

9G 0% cf 9090 05SCO040 67900
02 DO 0°%°eD0P2% OS 5°

Fig. 17.

f Pliocene.

Eocene.

Cretaceous.

Oolitic or Jurassic.

Triassic.

Permian.

Carboniferous.

Devonian or Old Red Sandstone.

Silurian.

Cambrian.

Huronian.

Laurentian.

44 PRINCIPLES OF PALAONTOLOGY.

Of these primary rock divisions, the Laurentian, Cambrian,
Silurian, Devonian, Carboniferous, and Permian are collec-
tively grouped together under the name of the Przmary or
Paleozoic rocks (Gr. palaios, ancient ; z0¢, life). Not only do
they constitute the oldest stratified accumulations, but from
the extreme divergence between their animals and plants and
those now in existence, they may appropriately be considered
as belonging to an “ Old-Life” period of the world’s history.
The Triassic, Jurassic, and Cretaceous systems are grouped to-
gether as the Secondary or Mesozoic formations (Gr. mesos, inter-
mediate ; 20¢, life) ; the organic remains of this “‘ Middle-Life ”
period being, on the whole, intermediate in their characters
between those of the palzeozoic epoch and those of more
modern strata. Lastly, the Eocene, Miocene, and Pliocene
formations are grouped together as the Zertiary or Kainozoic
rocks (Gr. azmos, new; z0e, life); because they constitute a
“ New-Life” period, in which the organic remains approximate
in character to those now existing upon the globe. The so-
called /ost-Tertiary deposits are placed with the Kainozoic, or
may be considered as forming a separate Quaternary system.

CHAPTERSAV:

THE BREAKS IN THE GEOLOGICAL AND
PALA ONTOLOGICAL RECORD.

The term “contemporaneous” is usually applied by geolo-
gists to groups of strata in different regions which contain the
same fossils, or an assemblage of fossils in which many iden-
tical forms are present. That is to say, beds which contain
identical, or nearly identical, fossils, however widely separated
they may be from one another in point of actual distance, are
ordinarily believed to have been deposited during the same
period of the earth’s history. This belief, indeed, constitutes
the keystone of the entire system of determining the age of
strata by their fossil contents; and if we take the word “con-
temporaneous” in a general and strictly geological sense, this
belief can be accepted as proved beyond denial. We must,
however, guard ourselves against too literal an interpretation
of the word ‘‘contemporaneous,” and we must bear in mind
the enormously - prolonged periods of time with which the
geologist has to deal. When we say that two groups of strata

BREAKS IN THE GEOLOGICAL RECORD. 45

in different regions are ‘“‘contemporaneous,” we simply mean
that they were formed during the same geological period, and
perhaps at different stages of that period, and we do not mean to
imply that they were formed at precisely the same instant of time.

A moment’s consideration will show us that it is only in the
former sense that we can properly speak of strata being ‘ con-
temporaneous ;” and that, in point of fact, beds containing
the same fossils, if occurring in widely distant areas, can hardly
be ‘‘contemporaneous” in any literal sense ; but that the very
identity of their fossils is proof that they were deposited one
after the other. If we find strata containing identical fossils
within the limits of a single geographical region—say in Europe
—then there is a reasonable probability that these beds are
strictly contemporaneous, in the sense that they were deposited
at the same time. ‘There is a reasonable probability of this,
because there is no improbability involved in the idea of an
ocean occupying the whole area of Europe, and peopled
throughout by many of the same species of marine animals. At
the present day, for example, many identical species of animals
are found living on the western coasts of Britain and the
eastern coasts of North America, and beds now in course of
deposition off the shores of Ireland and the seaboard of the
state of New York would necessarily contain many of the
same fossils. Such beds would be both hterally and geologi-
cally contemporaneous; but the case is different if the distance
between the areas where the strata occur be greatly increased.
We find, for example, beds containing identical fossils (the
Quebec or Skiddaw beds) in Sweden, in the north of England,
in Canada, and in Australia. Now, if all these beds were con-
temporaneous, in the literal sense of the term, we should have
to suppose that the ocean at one time extended uninterrup-
tedly between all these points, and was peopled throughout
the vast area thus indicated by many of the same animals.
Nothing, however, that we see at the present day would justify
us in imagining an ocean of such enormous extent, and at the
same time so uniform in its depth, temperature, and other
conditions of marine life, as to allow the same animals to
flourish in it from end to end; and the example chosen is
only one of a long and ever-recurring series. It is therefore
much more reasonable to explain this, and all similar cases, as
Owing to the migration of the fauna, in whole or in part, from
one marine area to another. Thus, we may suppose an ocean
to cover what is now the European area, and to be peopled by
certain species of animals. Beds of sediment—clay, sands,
and ee vl be deposited over the sea-bottom, and

46 PRINCIPLES OF PALA‘ON TOLOGY.

will entomb the remains of the animals as fossils. After this
has lasted for a certain length of time, the European area may
undergo elevation, or may become otherwise unsuitable for the
perpetuation of its fauna; the result of which would be that
some or all of the marine animals of the area would mzgrate to
some more suitable region. Sediments would then be accumu-
lated in the new area to which they had betaken themselves,
and they would then appear, for the second time, as fossils in
a set of beds widely separated from Europe. The second set
of beds would, however, obviously not be strictly or literally
contemporaneous with the first, but would be separated from
them by the period of time required for the migration of the
animals’ from the one area into the other. It is only in a wide
and comprehensive sense that such strata can be said to be
contemporaneous.

It is impossible to enter further into this subject here ; but
it may be taken as certain that beds in widely remote geogra-
phical areas can only come to contain the same fossils by
reason of a migration having taken place of the animals of
the one area to the other. ‘That such migrations can and do
take place is quite certain, and this isa much more reasonable
explanation of the observed facts than the hypothesis that in
former periods the conditions of life were much more uniform —
than they are at present, and that, consequently, the same
organisms were able to range over the entire globe at the same
time. It need only be added, that taking the evidence of the
present as explaining the phenomena of the past—the only
safe method of reasoning in geological matters—we have
abundant proof that deposits which ave actually contempo-
raneous, in the strict sense of the term, do net contain the same
fossils, of far removed from one another in point of distance.
Thus, deposits of various kinds are now in process of forma-
tion in our existing seas, as, for example, in the Arctic Ocean,
the Atlantic, and the Pacific, and many of these deposits are
known to us by actual examination and observation with the
sounding-lead and dredge. But it is hardly necessary to add
that the animal remains contained in these deposits—the
fossils of some future period—instead of being identical, are
widely different from one another in their characters.

We have seen, then, that the entire stratified series is capable
of subdivision into a number of definite rock-groups or ‘‘forma-
tions,” each possessing a peculiar and characteristic assem-
blage of fossils, representing the “life” of the “period” in
which the formation was deposited. We have still to inquire
shortly how it came to pass that two successive formations

BREAKS IN THE GEOLOGICAL RECORD. 47

should thus be broadly distinguished by their life-forms, and
why they should not rather possess at any rate a majority of
identical fossils. It was originally supposed that this could be
explained by the hypothesis that the close of each formation
was accompanied by a general destruction of all the living
beings of the period, and that the commencement of each
new formation was signalised by the creation of a number of
brand-new organisms, destined to figure as the characteristic
fossils of the same. This theory, however, ignores the fact
that each formation—as to which we have any sufficient
evidence—contains a few, at least, of the life-forms which
existed in the preceding period; and it. invokes forces and
processes of which we know nothing, and for the supposed
action of which we cannot account. The problem is an un-
deniably difficult one, and it will not be possible here to give
more than a mere outline of the modern views upon the sub-
ject. Without entering into the at present inscrutable question
as to the manner in which new life-forms are introduced upon
the earth, it may be stated that almost all modern geologists
hold that the living beings of any given formation are in the
main modified forms of others which have preceded them. It
is not believed that any general or universal destruction of
life took place at the termination of each geological period, or
that a general introduction of new forms took place at the
commencement of a new period. It is, on the contrary,
believed that the animals and plants of any given period are
for the most part (or exclusively) the lineal but modified
descendants of the animals and plants of the immediately pre-
ceding period, and that some of them, at any rate, are con-
tinued into the next succeeding period, either unchanged, or
so far altered as to appear as new species. To discuss these
views in detail would lead us altogether too far, but there is
one very obvious consideration which may advantageously
receive some attention. It is obvious, namely, that the great
discordance which is found to subsist between the animal
life of any given formation and that of the next succeeding
formation, and which no one denies, would be a fatal blow to
the views just alluded to, unless admitting of some satisfactory
explanation. Nor is this discordance one purely of life-forms,
for there is often a physical break in the successions of strata
as well. Let us therefore briefly consider how far these
interruptions and breaks in the geological and palzonto-
logical record can be accounted for, and still allow us to
believe in some theory of continuity as opposed to the doc-
trine of intermittent and occasional action.

48 PRINCIPLES OF PALZONTOLOGY.

In the first place, it is perfectly clear that if we admit the
conception above mentioned of a continuity of life from the
Laurentian period to the present day, we could never prove
our view to be correct, unless we could produce in evidence
fossil examples of a@// the kinds of animals and plants that
have. lived and died during that period. In order to do this,
we should require, to begin with, to have access to an abso-
lutely unbroken and perfect succession of all the deposits
which have ever been laid down since the beginning. If,
however, we ask the physical geologist if he is in possession
of any such uninterrupted series, he will at once answer in the
negative. So far from the geological series being a perfect one,
it is interrupted by numerous gaps of unknown length, many
of which we can never expect to fillup. Nor are the proofs
of this far to seek. Apart from the facts that we have hitherto
examined only a limited portion of the dry land, that nearly
two-thirds of the entire area of the globe is inaccessible to
geological investigation in consequence of its being covered
by the sea, that many deposits can be shown to have been
more or less completely destroyed subsequent to their depo-
sition, and that there may be many areas in which living beings
exist where no rock is in process of formation, we have the broad
fact that rock-deposition only goes on to any extent in water,
and that the earth must have always consisted partly of dry
land and partly of water—at any rate, so far as any period of
which we have geological knowledge is concerned. There
must, therefore, always have existed, at some part or another
of the earth’s surface, areas where no deposition of rock was
going on, and the proof of this is to be found in the well-
known phenomenon of “‘wnconformadbility.” Whenever, namely,
deposition of sediment is continuously going on within the
limits of a single ocean, the beds which are laid down succeed
one another in uninterrupted and regular sequence. Such
beds are said to be ‘‘ conformable,” and there are many rock-
groups known where one may pass through fifteen or twenty
thousand feet of strata without a break—indicating that the
beds had been deposited in an area which remained continu-
ously covered by the sea. On the other hand, we commonly
find that there is no such regular succession when we pass
from one great formation to another, but that, on the contrary,
the younger formation rests “ unconformably,” as it is called,
either upon the formation immediately preceding it in point of
time, or upon some still older one. The essential physical
feature of this unconformability is that the beds of the younger
formation rest upon a worn and eroded surface formed by the

BREAKS IN THE GEOLOGICAL RECORD. 49

beds of the older series (fig. 18); and a moment’s considera-
tion will show us what this indicates. It indicates, beyond

Fig. 18.—Section showing strata of Tertiary age (a) resting upon a worn and eroded
surface of White Chalk (4), the stratification of which is marked by lines of flint.

the possibility of misconception, that there was an interval
between the deposition of the older series and that of the
newer series of strata ; and that during this interval the older
beds were raised above the sea-level, so as to form dry land,
‘and were subsequently depressed again beneath the waters, to
receive upon their worn and wasted upper surface the sedi-
ments of the later group. During the interval thus indicated,
the deposition of rock must of necessity have been proceeding
more or less actively in other areas. Every unconformity,
therefore, indicates that at the spot where it occurs, a more or
less extensive series of beds must be actually mzssemg ; and
though we may sometimes be able to point to these missing
strata in other areas, there yet remains a number of unconfor-
mities for which we cannot at present supply the deficiency
even in a partial manner.

It follows from the above that the series of stratified deposits
is to a greater or less extent irremediably imperfect ; and in
this imperfection we have one great cause why we can never
obtain a perfect series of all the animals and plants that have
lived upon the globe. Wherever one of these great physical
gaps occurs, we find, as we might expect, a corresponding
break in the series of life-forms. In other words, whenever we
find two formations to be unconformable, we shall always find
at the same time that there is a great difference in their fossils,
and that many of the fossils of the older formation do not sur-
vive into the newer, whilst many of those in the newer are not
known to occur in the older. ‘The cause of this is, obviously,

50 PRINCIPLES OF PALZZONTOLOGY.

that the lapse of time, indicated by the unconformability, has
been sufficiently great to allow of the dying out or modifica-
tion of many of the older forms of life, and the introduction of
new ones by immigration.

Apart, however, altogether, from these great physical breaks
and their corresponding breaks in life, there are other reasons
why we can never become more than partially acquainted with
the former denizens of the globe. Foremost amongst these is
the fact that an enormous number of animals possess no hard
parts of the nature of a skeleton, and are therefore incapable,
under any ordinary circumstances, of leaving behind them any
traces of their existence. It is true that there are cases in
which animals in themselves completely soft-bodied are never-
theless able to leave marks by which their former presence can
be detected. Thus every geologist is familiar with the wind-
ing and twisting “trails” formed on the surface of the strata
by sea-worms; and the impressions left by the stranded
carcases of Jelly-fishes on the fine-grained lithographic slates
of Solenhofen supply us with an example of how a creature
which is little more than “organised sea- water” may still
make an abiding mark upon the sands of time. As a general
tule, however, animals which have no skeletons are incapable
of being preserved as fossils, and hence there must always
have been a vast number of different kinds of marine animals
of which we have absolutely no record whatever. Again,
almost all the fossiliferous rocks have been laid down in water;
and it is a necessary result of this that the great majority of
fossils are the remains of aquatic animals. The remains of
air-breathing animals, whether of the inhabitants of the land
or of the air itself, are comparatively rare as fossils, and the
record of the past existence of these is much more imperfect
than is the case with animals living in water. Moreover, the
fossiliferous deposits are not only almost exclusively aqueous
formations, but the great majority are marine, and only a com-
paratively small number have been formed by lakes and rivers.
It follows from the foregoing that the paleontological record
is fullest and most complete so far as sea-animals are concerned,
though even here we find enormous gaps, owing to the absence
of hard structures in many great groups; of animals inhabiting
fresh waters our knowledge is rendered still further incomplete
by the small proportion that fluviatile and lacustrine deposits
bear to marine; whilst we have only a fragmentary acquaint-
ance with the air-breathing animals which inhabited the earth
during past ages.

Lastly, the imperfection of the paleontological record, due

~~

BREAKS IN THE GEOLOGICAL RECORD. 51

to the causes above enumerated, is greatly aggravated, especi-
ally as regards the earlier portion of the earth’s history, by the
fact that many rocks which contained fossils when deposited
have since been rendered barren of organic remains. The
principal cause of this common phenomenon is what is known
as “metamorphism ”—that is, the subjection of the rock to a
sufficient amount of heat to cause a rearrangement of its par-
ticles. When at all of a pronounced character, the result of
metamorphic action is invariably the obliteration of any fossils
which might have been originally present in the rock. Meta-
morphism may affect rocks of any age, though naturally more
prevalent in the older rocks, and to this cause must be set
down an irreparable loss of much fossil evidence. The most
stfiking example which is to be found of this is the great Lau-
rentian series, which comprises some 30,000 feet of highly-
metamorphosed sediments, but which, with one not wholly
undisputed exception, has as yet yielded no remains of living
beings, though there is strong evidence of the former existence
in it of fossils.

Upon the whole, then, we cannot doubt that the earth’s
crust, so far as yet deciphered by us, presents us with but a
very imperfect record of the past. Whether the known and
admitted imperfections of the geological and palzontological
records are sufficiently serious to account satisfactorily for the
deficiency of direct evidence recognisable in some modern
hypotheses, may be a matter of individual opinion. ‘There
can, however, be little doubt that they are sufficiently extensive
to throw the balance of evidence decisively in favour of some
theory of continuity, as opposed to any theory of intermittent
and occasional action. The apparent breaks which divide the
great series of the stratified rocks into a number of isolated
formations, are not marks of mighty and general convulsions
of nature, but are simply indications of the imperfection of
our knowledge. Never, in all probability, shall we be able to
point to a complete series of deposits, or a complete succession
of life linking one great geological period to another. Never-
theless, we may well feel sure that such deposits and such an
unbroken succession must have existed at one time. We are
compelled to believe that nowhere in the long series of the
fossiliferous rocks has there been a total break, but that there
must have been a complete continuity of life, and a more or
less complete continuity of sedimentation, from the Laurentian
period to the present day. One generation hands on the
lamp of life to the next, and each system of rocks is the direct
offspring of those which preceded it in time. Though there

52 PRINCIPLES OF PALAONTOLOGY.

has not been continuity in any given area, still the geological
chain could never have been snapped at one point, and taken -
up again at a totally different one. Thus we arrive at the
conviction that continuity is the fundamental law of geology,
as it is of the other sciences, and that the lines of demarca-
tion between the great formations are but gaps in our own
knowledge.

CHAR TER V.
CONCLUSIONS TO BE DRAWN FROM FOSSILS.

We have already seen that geologists have been led by the
study of fossils to the all-important generalisation that the vast
series of the Fossiliferous or Sedimentary Rocks may be
divided into a number of definite groups or “ formations,”
each of which is characterised by its organic remains. It may
simply be repeated here that these formations are not properly
and strictly characterised by the occurrence in them of any
one particular fossil. It may be that a formation contains ~
some particular fossil or fossils not occurring out of that
formation, and that in this way an observer may identify a
given group with tolerable certainty. It very often happens,
indeed, that some particular stratum, or sub-group of a series,
contains peculiar fossils, by which its existence may be deter-
mined in various localities. As before remarked, however, the
great formations are characterised properly by the association
of certain fossils, by the predominance of certain families or
orders, or by an assemblage of fossil remains representing the
“life” of the period in which the formation was deposited.

Fossils, then, enable us to determine the age of the deposits
in which they occur. Fossils further enable us to come to
very important conclusions as to the mode in which the fossil-
iferous bed was deposited, and thus as to the condition of the
particular district or region occupied by the fossiliferous bed
at the time of the formation of the latter. If, in the first
place, the bed contain the remains of animals such as now
inhabit rivers, we know that it is “ fluviatile”’ in its origin, and
that it must at one time have either formed an actual river-
bed, or been deposited by the overflowing of an ancient
stream. Secondly, if the bed contain the remains of shell-
fish, minute crustaceans, or fish, such as now inhabit lakes,

CONCLUSIONS TO BE DRAWN FROM FOSSILS. 53
we know that it is “lacustrine,” and was deposited beneath
the waters of a former lake. ‘Thirdly, if the bed contain the
remains of animals such as now people the ocean, we know
that it is ‘‘ marine ” in its origin, and that it is a fragment of
an old sea-bottom.

We can, however, often determine the conditions under
which a bed was deposited with greater accuracy than this.
If, for example, the fossils are of kinds resembling the marine
animals now inhabiting shallow waters, if they are accompanied
by the detached relics of terrestrial organisms, or if they are
partially rolled and broken, we may conclude that the fossil-
iferous deposit was laid down in a shallow sea, in the immediate
vicinity of a coast-line, or as an actual shore-deposit. If, again,
the remains are those of animals such as now live in the deeper
parts of the ocean, and there is a very sparing intermixture of
extraneous fossils (such as the bones of birds or quadrupeds,
or the remains of plants), we may presume that the deposit is
one of deep water. In other cases, we may find, scattered
through the rock, and still in their natural position, the valves
of shells such as we know at the present day as living buried
in the sand or mud of the sea-shore or of estuaries. In other
cases, the bed may obviously have been an ancient coral-reef,
or an accumulation of social shells, like Oysters. Lastly, if we
find the deposit to contain the remains of marine shells, but
that these are dwarfed of their fair proportions and distorted
in figure, we may conclude that it was laid down in a brackish
sea, such as the Baltic, in which the proper saltness was want-
_ing, owing to its receiving an excessive supply of fresh water.

In the preceding, we have been dealing simply with the
remains of aquatic animals, and we have seen that certain con-
clusions can be accurately reached by an examination of these.
As regards the determination of the conditions of deposition
from the remains of aerial and terrestrial animals, or from
plants, there is not such an absolute certainty. The remains
of land-animals would, of course, occur in “‘ sub-aerial ” deposits
—that is, in beds, like blown sand, accumulated upon the land.
Most of the remains of land-animals, however, are found in
deposits which have been laid down in water, and they owe
their present position to the fact that their former owners were
drowned in rivers or lakes, or carried out to sea by streams.
Birds, Flying Reptiles, and Flying Mammals might also simi-
larly find their way into aqueous deposits; but it is to be re-
membered that many birds and mammals habitually spend a
great part of their time in the water, and that these might there-
fore be naturally expected to present themselves as fossils in

54 PRINCIPLES OF PALAZSONTOLOGY.

Sedimentary Rocks. Plants, again, even when undoubtedly
such as must have grown on land, do not prove that the bed
in which they occur was formed on land. Many of the remains
of plants known to us are extraneous to the bed in which they
are now found, having reached their present site by falling into
lakes or rivers, or being carried out to sea by floods or gales of
wind. There are, however, many cases in which plants have
undoubtedly grown on the very spot where we now find them.
Thus it is now generally admitted that the great coal-fields

of the Carboniferous age are the result of the growth zu satu

of the plants which compose coal, and that these grew
on vast marshy or partially
submerged tracts of level
alluvial land. We _ have,
however, distinct evidence
of old land-surfaces, both in
the Coal-measures and in
other cases (as, for instance,
in the well-known “ dirt-
bed” of the Purbeck series).
When, for example, we find
the erect stumps of trees
standing at right angles
to the surrounding strata,
we know that the surface
through which these send
their roots was at one time
the surface of the dry land,
or, in other words, was an
ancient soil (fig. 19).

In many cases fossils en-

conclusions as to the climate
Fig. 19.—Erect Tree containing Reptilian of the period in which they
ea re ee Nova Scotia. (After lived, but only 4 fem
stances of this can be here

adduced. As fossils in the majority of instances are the re-
mains of marine animals, it is mostly the temperature of the
sea which can alone be determined in this way; and it is import-
ant to remember that, owing to the existence of heated currents,
the marine climate of a given area does not necessarily imply a
correspondingly warm climate in the neighbouring land. Land-
climates can only be determined by the remains of land-ani-
mals or land-plants, and these are comparatively rare as fossils.
It is also important to remember that all conclusions on this

able us to come to important

——

CONCLUSIONS TO BE DRAWN FROM FOSSILS. 55

head are really based upon the present distribution of animal
and vegetable life on the globe, and are therefore liable to be
vitiated by the following considerations :—

a. Most fossils are extinct, and it is not certain that the
habits and requirements of any extinct animal were exactly
similar to those of its nearest living relative.

b. When we get very far back in time, we meet with groups

of organisms so unlike anything we know at the present day as
to render all conjectures as to climate founded upon their sup-
posed habits more or less uncertain and unsafe.
_¢. In the case of marine animals, we are as yet very far from
knowing the exact limits of distribution of many species within
our present seas ; so that conclusions drawn from living forms
as to extinct species are apt to prove incorrect. For instance,
it has recently been shown that many shells formerly believed
to be confined to the Arctic Seas have, by reason of the ex-
tension of Polar currents, a wide range to the south ; and this
has thrown doubt upon the conclusions drawn from fossil
shells as to the Arctic conditions under which certain beds
were supposed to have been deposited.

d. The distribution of animals at the present day is certainly
dependent upon other conditions beside climate alone ; and
the causes which now limit the range of given animals are
certainly such as belong to the existing order of things. But
the establishment of the present order of things does not date
back in many cases to the introduction of the present species
of animals. Even in the case, therefore, of existing species of
animals, it can often be shown that the past distribution of the
species was different formerly to what it is now, not necessarily
because the climate has changed, but because of the alteration
of other conditions essential to the life of the species or con-
- ducing to its extension.

Still, we are in many cases able to draw completely reliable
conclusions as to the climate of a given geological period, by
an examination of the fossils belonging to that period. Among
the more striking examples of how the past climate of a region
may be deduced from the study of the organic remains con-
tained in its rocks, the following may be mentioned: It has
been shown that in Eocene times, or at the commencement
of the Tertiary period, the climate of what is now Western
Europe was of a tropical or sub-tropical character. Thus the
Eocene beds are found to contain the remains of shells such
as now inhabit tropical seas, as, for example, Cowries and
Volutes ; and with these are the fruits of palms, and the
remains of other tropical plants. It has been shown, again,

56 PRINCIPLES OF PALZONTOLOGY.

that in Miocene times, or about the middle of the Tertiary
period, Central Europe was peopled with a luxuriant flora
resembling that of the warmer parts of the United States, and
leading to the conclusion that the mean annual temperature
must have been at least 30° hotter than it is at present. It
has been shown that, at the same time, Greenland, now buried
beneath a vast ice-shroud, was warm enough to support a large
number of trees, shrubs, and other plants, such as inhabit the
temperate regions of the globe. Lastly, it has been shown,
upon physical as well as paleontological evidence, that the
greater part of the North Temperate Zone, at a comparatively
recent geological period, has been visited with all the rigours
of an Arctic climate, resembling that of Greenland at the pre-
sent day. This is indicated by the occurrence of Arctic shells
in the superficial deposits of this period, whilst the Musk-ox
and the Reindeer roamed far south of their present limits.

Lastly, it was from the study of fossils that geologists learnt
originally to comprehend a fact which may be regarded as of
cardinal importance in all modern geological theories and
speculations—namely, that the crust of the earth is liable to
local elevations and subsidences. For long after the remains
of shells and other marine animals were for the first time ob-
served in the solid rocks forming the dry land, and at great
heights above the sea-level, attempts were made to explain this
almost unintelligible phenomenon upon the hypothesis that
the fossils in question were not really the objects they repre-
sented, but were in truth mere /usus nature, due to some
‘plastic virtue latent in the earth.” The common-sense of
scientific men, however, soon rejected this idea, and it was
agreed by universal consent that these bodies really were the
remains of animals which formerly lived in the sea. When
once this was admitted, the further steps were comparatively
easy, and at the present day no geological doctrine stands on
a firmer basis than that which teaches us that our present con-
tinents and islands, fixed and immovable as they appear, have
been repeatedly sunk beneath the ocean.

THE BIOLOGICAL RELATIONS OF FOSSILS. 57

CHAPTER VE
THE BIOLOGICAL RELATIONS OF FOSSILS.

Not only have fossils,.as we have seen, a most important
bearing upon the sciences of Geology and Physical Geography,
but they have relations of the most complicated and weighty
character with the numerous problems connected with the
study of living beings, or in other words, with the science of
- Biology. To such an extent is this the case, that no adequate
comprehension of Zoology and Botany, in their modern
form, is so much as possible without some acquaintance with
the types of animals and plants which have passed away.
There are also numerous speculative questions in the domain
of vital science, which, if soluble at all, can only hope to find
their key in researches carried out on extinct organisms. To
discuss fully the biological relations of fossils would, there-
fore, afford matter for a separate treatise; and all that can be
done here is to indicate very cursorily the principal points to
which the attention of the palzontological student ought to
be directed.

In the first place, the great majority of fossil animals and
plants are ‘‘ extinct’”—that is to say, they belong to species
which are no longer in existence at the present day. So far,
however, from there being any truth in the old view that there
were periodic destructions of all the living beings in existence
upon the earth, followed by a corresponding number of new
creations of animals and plants, the actual facts of the case show
that the extinction of old forms and the introduction of new
forms have been processes constantly going on throughout the
whole of geological time. Every species seems to come into
being at a certain definite point of time, and to finally dis-
appear at another definite point; though there are few in-
stances indeed, if there are any, in which our present know-
ledge would permit us safely to fix with precision the times of
entrance and exit. There are, moreover, marked differences
in the actual time during which different species remained in
existence, and therefore corresponding differences in their
“vertical range,” or, in other words, in the actual amount and
thickness of strata through which they present themselves as
fossils. Some species are found to range through two or even
three formations, and a few have an even more extended life.
More commonly the species which begin in the commence-

58 PRINCIPLES OF PALEONTOLOGY.

ment of a great formation die out at or before its close, whilst
those which are introduced for the first time near the ‘middle
or end of the formation may either become extinct, or may
pass on into the next succeeding formation. As a general
rule, it is the animals which have the lowest and simplest
organisation that have the longest range in time, and the
additional possession of microscopi¢ or minute dimensions
seems also to favour longevity. Thus some of the Foramz-
uifera appear to have survived, with little or no perceptible
alteration, from the Silurian period to the present day ; whereas
large and highly-organised animals, though long-lived as zmdz-
viduals, rarely seem to live long sfecéfically, and have, there-
fore, usually a restricted yertical range. Exceptions to this,
however, are occasionally to be found in some “persistent
types,” which extend through a succession of geological
periods with very little modification. Thus the existing
Lampshells of the genus Zzzgw/a are little changed from the
Lingule which swarmed in the Lower Silurian seas; and the
existing Pearly Nautilus is the last descendant of a clan
nearly as ancient. On the other hand, some forms are singu-
larly restricted in their limits, and seem to have enjoyed a
comparatively brief lease of life. An example of this is to
be found in many of the Ammonites—close allies of the Nau-
tilus—which are often confined strictly to certain zones of
strata, in some cases of very insignificant thickness.

Of the causes of extinction amongst fossil animals and
plants, we know little or nothing. All we can say is, that the
attributes which constitute a species do not seem to be intrin-
sically endowed with permanence, any more than the attri-
butes which constitute an zudividual, though the former may
endure whilst many successive generations of the latter have
disappeared. Each species appears to have its own life-
period, its commencement, its culmination, and its gradual
decay ; and the life-periods of different species may be of very
different duration.

From what has been said above, it may be gathered that
our existing species of animals and plants are, for the most
part, quite of modern origin, using the term ‘modern ” in its
geological acceptation. Measured by human standards, the
majority of existing animals (which are capable of being
preserved as fossils) are known to have a high antiquity;
and some of them can boast of a pedigree which even the
geologist may regard with respect. Not a few of our shell-
fish are known to have commenced their existence at some
point of the Tertiary period; one Lampshell (Zerebratulina

THE BIOLOGICAL RELATIONS OF FOSSILS. 59

caput-serpentis) is believed to have survived since the Chalk ;
and some of the Foraminifera date, at any rate, from the
Carboniferous period. We learn from this the additional
fact that our existing animals and plants do not constitute an
assemblage of organic forms which were introduced into the
world collectively and simultaneously, but that they com-
menced their existence at very different periods, some being
extremely old, whilst others may be regarded as compara-
tively recent animals. And this introduction of the existing
fauna and flora was a slow and gradual process, as shown
admirably by the study of the fossil shells of the Tertiary
period. ‘Thus, in the earlier Tertiary period, we find ‘about
95 per cent of the known fossil shells to be species that are
no longer in existence, the remaining 5 per cent being
forms which are known to live in our present seas. In the
middle of the Tertiary period we find many more recent
and still existing species of shells, and the extinct types are
much fewer in number; and this gradual introduction of
forms now living goes on steadily, till, at the close of the Ter-
ulary period, the proportions with which we started may be
reversed, as many as 9o or 95 per cent of the fossil shells
being forms still alive, while not more than 5 per cent may
have disappeared.

All known animais at the present day may be divided into
some five or six primary divisions, which are known technically
as “sub-kingdoms.” ach of these sub-kingdoms* may be
regarded as representing a certain type or plan of structure,
and all the animals comprised in each are merely modified forms
of this common type. Not only are all known living animals
thus reducible to some five or six fundamental plans of struc-
ture, but amongst the vast series of fossil forms no one has
yet been found — however unlike any existing animal—to
' possess peculiarities which would entitle it to be placed ina
new sub-kingdom. All fossil animals, therefore, are capable
of being referred to one or other of the primary divisions of
the animal kingdom. Many fossil groups have no closely-
related group now in existence; but in no case do we meet
with any grand structural type which has not survived to the
present day.

The old types of life differ in many réspects from those now
upon the earth; and the further back we pass in time, the
more marked does this divergence become. Thus, if we were
to compare the animals which lived in the Silurian seas with

* In the Appendix a brief definition is given of the sub-kingdoms, and
the chief divisions of each are enumerated,

60 PRINCIPLES OF PALAZZONTOLOGY.

those inhabiting our present oceans, we should in most in-
stances find differences so great as almost to place us in
another world. ‘This divergence is the most marked in the
Paleozoic forms of life, less so in those of the Mesozoic period,
and less still in the Tertiary period. Each successive formation
has therefore presented us with animals becoming gradually
more and more like those now in existence ; and though there
is an immense and striking difference between the Silurian
animals and those of to-day, this difference is greatly reduced
if we compare the Silurian fauna with the Devonian; shat
again with the Carboniferous; and so on till we reach the
present.

It follows from the above that the animals of any given
formation are more like those of the next formation below,
and of the next formation above, than they are to any others ;
and this fact of itself is an almost inexplicable one, unless we
believe that the animals of any given formation are, in part at
any rate, the lineal descendants of the animals of the preced-
ing formation, and the progenitors, also in part at least, of the
animals of the succeeding formation. In fact, the paleeon-
tologist is so commonly confronted with the phenomenon of
closely-allied forms of animal life succeeding one another in
point of time, that he is compelled to believe that such forms
have been developed from some common ancestral type by
some process of “evolution.” On the other hand, there are
many phenomena, such as the apparently sudden introduction
of new forms throughout all past time, and the common occur-
rence of wholly isolated types, which cannot be explained in
this way. Whilst it seems certain, therefore, that many of the
phenomena of the succession of animal life in past periods can
only be explained by some law of evolution, it seems at the
same time certain that there has always been some other
deeper and higher law at work, on the nature of which it
would be futile to speculate at present.

Not only do we find that the animals of each successive
formation become gradually more and more like those now
existing upon the globe, as we pass from the older rocks into
the newer, but we also find that there has been a gradual pro-
gression and development in the ¢yses of animal life which
characterise the geological ages. If we take the earliest-known
and oldest examples of any given group of animals, it can
sometimes be shown that these primitive forms, though in
themselves highly organised, possessed certain characters such
as are now only seen in the young of their existing representa-
tives. In technical language, the early forms of life in some

THE BIOLOGICAL RELATIONS OF FOSSILS. 6!

instances possess “‘ embryonic” characters, though this does
not prevent them often attaining a size much more gigantic
than their nearest living relatives. Moreover, the ancient
forms of life are often what is called ‘“‘comprehensive types”
—that is to say, they possess characters in combination such
as we nowadays only find separately developed in different
groups of animals. Now, this permanent retention of embry-
onic characters and this ‘‘comprehensiveness” of structural
type are signs of what a zoologist considers to be a compara-
tively low grade of organisation ; and the prevalence of these
features in the earlier forms of animals is a very striking phe-
nomenon, though they are none the less perfectly organised so
far as their own type is concerned. As we pass upwards in
the geological scale, we find that these features gradually dis-
appear, higher and ever higher forms are introduced, and
“specialisation ” of type takes the place of the former com-
prehensiveness. We shall have occasion to notice many of
the facts on which these views are based at a later period, and
in connection with actual examples. In the meanwhile, it is
sufficient to state, as a widely-accepted generalisation of palee-
ontology, that there has been in the past a general progression
of organic types, and that the appearance of the lower forms
of life has in the main preceded that of the higher forms in
point of time.

1 a eG heed La

PistORICAL, PALAON TOLOGY:

Pee Ro ii

CEA PE Re Vill

THE LAURENTIAN AND HURONIAN PERIODS.

THE Laurentian Rocks constitute the base of the entire strati-
fied series, and are, therefore, the oldest sediments of which
we have as yet any knowledge. They are more largely and
more typically developed in North America, and especially in
Canada, than in any knowr vart of the world, and they derive
their title from the range of hills which the old French geo-
graphers named the “Laurentides.” These hills are com-
posed of Laurentian Rocks, and form the watershed Letween
the valley of the St Lawrence river on the one hand, and the
great plains which stretch northwards to Hudson Bay on the
other hand. The main area of these ancient deposits forms
a great belt of rugged and undulating country, which extends
from Labrador westwards to Lake Superior, and then bends
northwards towards the Arctic Sea. Throughout this extensive
area the Laurentian Rocks for the most part present themselves
in the form of low, rounded, ice-worn hills, which, if generally
wanting in actual sublimity, have a certain geological grandeur
from the fact that they “Shave endured the battles and the storms
of time longer than any other mountains” (Dawson). In some
places, however, the Laurentian Rocks produce scenery of the
most magnificent character, as in the great gorge cut through
them by the river Saguenay, where they rise at times into ver-
tical precipices 1500 feet in height. In the famous group of
the Adirondack mountains, also, in the state of New York,
they form elevations no less than 6000 feet above the level of
the sea. As a general rule, the character of the Laurentian
region is that of a rugged, rocky, rolling country, often densely

66 HISTORICAL PALZONTOLOGY.

timbered, but rarely well fitted for agriculture, and chiefly
attractive to the hunter and the miner.

As regards its mineral characters, the Laurentian series is
composed throughout of metamorphic and highly crystalline
rocks, which are in a high degree crumpled, folded, and
faulted. By the late Sir William Logan the entire series was
divided into two great groups, the Lower Laurentian and the
Upper Laurentian, of which the latter rests unconformably
upon the truncated edges of the former, and is in turn uncon-
formably overlaid by strata of Huronian and Cambrian age
(fig. 20).

The Lower Laurentian series attains the enormous thickness of

a
Fig. 20.—Diagrammatic section of the Laurentian Rocks in Lower Canada. @ Lower
Laurentian ; 6 Upper Laurentian, resting unconformably upon the lower series; ¢ Cam-
brian strata (Potsdam Sandstone), resting unconformably on the Upper Laurrentian.

Over 20,000 feet, and is composed mainly of great beds of gneiss,
altered sandstones (quartzites), mica-schist, hornblende-schist,
magnetic iron-ore, and hematite, together with masses of lime-
stone. ‘The limestones are especially interesting, and have an
extraordinary development—three principal beds being known,
of which one is not less than 1500 feet thick; the collective
thickness of the whole being about 3500 feet.

The Upper Laurentian series, as before said, reposes uncon-
formably upon the Lower Laurentian, and attains a thickness
of at least 10,000 feet. Like the preceding, it is wholly meta-
morphic, and is composed partly of masses of gneiss and quartz-
ite ; but it is especially distinguished by the possession of great
beds of felspathic rock, consisting principally of ‘‘ Labrador
felspar.”

Though typically developed in the great Canadian area |
already spoken of, the Laurentian Rocks occur in other locali-
ties, both in America and in the Old World. In Britain, the
so-called ‘fundamental gneiss” of the Hebrides and of Suther-
landshire is probably of Lower Laurentian age, and the “ hy-
persthene rocks” of the Isle of Skye may, with great proba-
bility, be regarded as referable to the Upper Laurentian. In
other localities in Great Britain (as in St David’s, South
Wales ; the Malvern Hills; and the North of Ireland) occur
ancient metamorphic deposits which also are probably refer-
able to the Laurentian series. The so-called “ primitive gneiss”
of Norway appears to belong to the Laurentian, and the

THE LAURENTIAN AND HURONIAN PERIODS. 67

ancient metamorphic rocks of Bohemia and Bavaria may oe
regarded as being approximately of the same age.

‘By some geological writers the ancient and highly meta-
morphosed sediments of the Laurentian and the succeeding
Huronian series have been spoken of as the ‘“‘ Azoic rocks”
(Gr. a, without ; zoe, life) ; but even if we were wholly destitute
of any evidence of life during these periods, this name would be
objectionable upon theoretical grounds. * Ifa general name be
needed, that of ‘‘ Eozoic” (Gr. eos, dawn; z0e, life), proposed
by Principal Dawson, is the most appropriate. Owing to their
metamorphic condition, geologists long despaired of ever de-
tecting any traces of life in the vast pile of strata which con-
stitute the Laurentian System. Even before any direct traces
were discovered, it was, however, pointed out that there were
good reasons for believing that the Laurentian seas had been
tenanted by an abundance of living beings. ‘These reasons
are briefly as follows :—(1) Firstly, the Laurentian series con-
sists, beyond question, of marine sediments which originally
differed in no essential respect from those which were subse-
quently laid down in the Cambrian or Silurian periods.: (2)
In all formations later than the Laurentian, any limestones
which are present can be shown, with few exceptions, to be
organic rocks, and to be more or less largely made up of the,
comminuted debris of marine or fresh-water animals. ‘The
Laurentian limestones, in consequence of the metamorphism
towhich they have been subjected, are so highly crystalline
(fig. 21) that the microscope fails to detect any organic struc-
ture in the rock, and no fos-
sils beyond those which will
bespoken of immediately have
as yet been discovered in
them. We know, however, of
numerous cases 1n which lime-
stones, of later age, and un-
doubtedly organic to begin
with, have been rendered so
intensely crystalline by meta-
morphic action that all traces
of organic structure have been
obliterated. We have there- ees.
fore, by analogy, the strongest _ Fig. 21.—Section of Lower Laurentian
possible ground for believing Limstore, fom Hull, Quawa;, enlarged
that the vast beds of Lauren- crystalline, and contains mica and other
tian limestone have been ori- ee eal Ones rie ay
ginally organic in their origin,
and primitively composed, in the main, of the calcareous skele-

fy) iy
AY ROA Ag a
ARR Nt ne Hes
AK HR ny ‘\

a
NA

68 HISTORICAL PALAZONTOLOGY.

tons of marine animals. It would, in fact, be a matter of
great difficulty to account for the formation of these great cal-
careous masses on any other hypothesis. (3) The occurrence of
phosphate of lime in the Laurentian Rocks in great abundance,
and sometimes in the form of irregular beds, may very possibly
be connected with the former existence in the strata of the re-
mains of marine animals of whose skeleton this mineral is a con-
stituent. (4) The Laurentian Rocks contain a vast amount of
carbon in the form of black-lead or graphite. This mineral is
especially abundant in the limestones, occurring in regular beds,
in veins or strings, or disseminated through the body of the lime-
stone in the shape of crystals, scales, or irregular masses. The
amount of graphite in some parts of the Lower Laurentian is
so great that it has been calculated as equal to the quantity of
carbon present in an equal thickness of the Coal-measures.
The general source of solid carbon in the crust of the earth
is, however, plant-life ; and it seems impossible to account for
the Laurentian graphite, except upon the supposition that it
is metamorphosed vegetable matter. (5) Lastly, the great
beds of iron-ore (peroxide and magnetic oxide) which occur
in the Laurentian series interstratified with the other rocks,
point with great probability to the action of vegetable life ;
since similar deposits in later formations can commonly be
shown to have been formed by the deoxidising power of vege-
table matter in a state of decay.

In the words of Principal Dawson, “any one of these rea-
sons might, in itself, be held insufficient to prove so great and,
at first sight, unlikely a conclusion as that of the existence of
abundant animal and vegetable life in the Laurentian; but the
concurrence of the whole in a series of deposits unquestion-
ably marine, forms a chain of evidence so powerful that it
might command belief even if no fragment of any organic or
living form or structure had ever been recognised in these an-
cient rocks.” Of late years, however, there have been dis-
covered in the Laurentian Rocks certain bodies which are
believed to be truly the remains of animals, and of which by
far the most important is the structure known under the now
celebrated name of Zozeon. If truly organic, a very special
and exceptional interest attaches itself to Hozoon, as being the
most ancient fossil animal of which we have any knowledge ;
but there are some who regard it really a peculiar form of
mineral structure, and a severe, protracted, and still unfinished
controversy has been carried on as to its nature. Into this
controversy it is wholly unnecessary to enter here; and it will
be sufficient to briefly explain the structure of Zozodn, as eluci-
dated by the elaborate and masterly investigations of Car-

THE LAURENTIAN AND HURONIAN PERIODS. 69

penter and Dawson, from the standpoint that it is a genuine
organism—the balance of evidence up to this moment inclin-
ing decisively to this view.

The structure known as Zozoon is found in various localities
in the Lower Laurentian limestones of Canada, in the form of
isolated masses or spreading layers, which are composed of
thin alternating laminz, arranged more or less concentrically
(fig. 22). The laminz of these masses are usually of different

Fig. 22.—Fragment of Zozo6n, of the natural size, showing alternate laminz
of loganite and dolomite. (After Dawson.)

colours and composition ; one series being white, and com-
posed of carbonate of lim:e—whilst the laminz of the second
series alternate with the preceding, are green in colour, and
are found by chemical analysis to consist of some silicate,
generally serpentine or the closely-related “‘loganite.” In
some instances, however, all the laminz are calcareous, the
concentric arrangement still remaining visible in consequence
of the fact that the Jaminze are composed alternately of lighter
and darker coloured limestone.

When first discovered, the masses of /ozo0n were supposed
to be of a mineral nature; but their striking general resem-
blance to the undoubted fossils which will be subsequently
spoken of under the name of Stromatopora was recognised by
Sir William Logan, and specimens were submitted for minute
examination, first to Principal Dawson, and subsequently to
Dr W. B. Carpenter. After a careful microscopic examina-
tion, these two distinguished observers came to the conclusion
that 2ozoon was truly organic, and in this opinion they were
afterwards corroborated by other high authorities (Mr W. K.
Parker, Profesor Rupert Jones, Mr H. B. Brady, Professor
Gumbel, &c.) Stated briefly, the structure of Zozodn, as ex-
hibited by the microscope, is as follows :—

7O HISTORICAL PALZHEONTOLOGY.

The concentrically-laminated: mass of Zozodn is composed
of numerous calcareous layers, representing the original skele-
ton of the organism (fig. 23, 4). These calcareous layers serve

to separate and de-

= HY y . fine aseries of cham-
As aaa oO . bers arranged a ae
C

oe Pe an cessive tiers, one
a ON /7) above the other (fig.
hs Aad ~ and 23, A; By ©) ead
they are perforated

not only by passages
(fig. 23, c¢), which
serve to place suc-
cessive tiers of cham-
bers in communica-
tion, but also by a
system of. delicate

Fig. 23.—Diagram of a portion of Zozodéx cut verti- branching canals (fig.
cally. A, B, C, Three tiers of chambers communicating
with one another by slightly constricted apertures: @ a, 23) a). Moreover,
The true shell-wall, perforated by numerous delicate the central and prin-
tubes; 4 6, The main calcareous skeleton (‘‘intermedi- el : f h
ate skeleton”); c, Passage of communication (‘‘stolon- ClPa portion OI €ac

passage”) from one tier of chambers to another; @,Rami- calcareous layer with
fying tubes in the calcareous skeleton. (After Car- : 2
penter.) the ramified canal-
system just spoken
of, is bounded both abové and below by a thin lamina which has
a structure of its own, and which may be regarded as the proper
shell-wall (fig. 23,@a@). This proper wall forms the actual lin-
ing of the chambers, as well as the outer surface of the whole
mass; and it is perforated with numerous fine vertical tubes
(fig. 24, @ a), opening into the chambers and on to the sur-
face by corresponding fine pores. From the resemblance of
this tubulated layer to similar structures in the shell of the
Nummulite, it is often spoken of as the ‘‘ Nummuline layer.”
The chambers are sometimes piled up one above the other in
an irregular manner; but they are more commonly arranged
in regular tiers, the separate chambers being marked off from
one another by projections of the wall in the form of parti-
tions, which are so far imperfect as to allow of a free communi-
cation between contiguous chambers. In the original condi-
tion of the organism, all these chambers, of course, must have
been filled with living matter; but they are found in the present
state of the fossil to be generally filled with some silicate, such
as serpentine, which not only fills the actual chambers, but has
also penetrated the minute tubes of the proper wall and the
branching canals of the intermediate skeleton. In some cases

y
tia

THE LAURENTIAN AND HURONIAN PERIODS. 71

the chambers are simply filled with crystalline carbonate of
lime. When the originally porous fossil has been permeated

Fig. 24.—Portion of one of the calcareous layers of Hozoéu, magnified 100 diameters.
a a, The proper wall (‘‘ Nummuline layer”) of one of the chambers, showing the fine ver-
tical tubuli with which it is penetrated, and which are slightly bent along the line a’ a’.
cc, The intermediate skeleton, with numerous branched canals. The oblique lines are
the cleavage planes of the carbonate of lime, extending across both the intermediate
skeleton and the proper wall. (After Carpenter.)

by a silicate, it is possible to dissolve away the whole of the
talcareous skeleton by means of acids, leaving an accurate and
Yeautiful cast of the chambers and the tubes connected with
them in the insoluble silicate.

The above are the actual appearances presented by Lozoon
when examined microscopically, and it remains to see how
far they enable us to decide upon its true position in the
animal kingdom. Those who wish to study this interesting
subject in detail must consult the admirable memoirs by Dr
W. B. Carpenter and Principal Dawson: it will be enough
here to indicate the results which have been arrived at. The
only animals at the present day which possess a continuous
calcareous skeleton, perforated by pores and penetrated by
canals, are certain organisms belonging to the group of the
Foraminifera. We have had occasion before to speak of these
animals, and as they are not conspicuous or commonly-known
forms of life, it may be well to say a few words as to the
structure of the living representatives of the group. The
Foraminifera are all inhabitants of the sea, and are mostly of
small or even microscopic dimensions. Their bodies are com-

72 HISTORICAL PALZONTOLOGY.

posed of an apparently structureless animal substance of an
albuminous nature (‘‘sarcode”), of a gelatinous consistence,
transparent, and exhibiting numerous minute granules or
rounded particles. The body-substance cannot be said in
itself to possess any definite form, except in so far as it may
be bounded by a shell; but it has the power, wherever it may
be exposed, of emitting long thread-like filaments (‘ pseudo-
podia”), which interlace with one another to form a network
(fig. 25,2). These filaments can be thrown out at will, and

Fig. 25.—The animal of Vozonina, one of the Foraminifera, after the shell has been
removed by a weak acid; 4, Gvomia, a single-chambered Foraminifer (after Schultze),
showing the shell surrounded by a network of filaments derived from the body substance.

to considerable distances, and can be again retracted into the
soft mass of the general body-substance, and they are the
agents by which the animal obtains its food. The soft bodies
of the Foraminifera are protected by a shell, which is usually
calcareous, but may be composed of sand-grains cemented

THE LAURENTIAN AND HURONIAN PERIODS. 73

together ; and it may consist of a single chamber (fig. 26, a),
or of many chambers arranged in different ways (fig. 26, 0/).

Fig. 26.—Shells of living Foraminifera. a, Orbulina universa, in its perfect condi-
tion, showing the tubular spines which radiate from the surface of the shell; 6, Glodz-
gerina bulloides, in its ordinary condition, the thin hollow spines which are attached to
the shell when perfect having been broken off; c, Textularia variabilis; d, Peneroplis
planatus; e, Rotalia concamerata; f, Cristellaria subarcuatula. (Fig. a is after
pile Thomson; the others are after Williamson. All the figures are greatly en-
arged.]

Sometimes the shell has but one large opening into it—the
mouth ; and then it is from this aperture that the animal pro-
trudes the delicate net of filaments with which it seeks its
food. In other cases the entire shell is perforated with
minute pores (fig. 26, e), through which the soft body-substance
gains the exterior, covering the whole shell with a gelatinous
film of animal matter, from which filaments can be emitted at
any point. When the shell consists of many chambers, all of
these are placed in direct communication with one another,
and the actual substance of the shell is often traversed by
minute canals filled with living matter (e.g., in Calcarina and
LVummulina). ‘The shell, therefore, may be regarded, in such
cases, asa more or less completely porous calcareous structure,

74 PRINCIPLES OF PALASONTOLOGY.

filled to its minutest internal recesses with the substance of the
living animal, and covered externally with a layer of the same
substance, giving off a network of interlacing filaments.

Such, in brief, is the structure of the living Foraminifera;
and it is believed that in Zozodn we have an extinct example
of the same group, not only of special interest from its imme-
morial antiquity, but hardly less striking from its gigantic
dimensions. In its original condition, the entire chamber-
system of ozoon is believed to have been filled with soft
structureless living matter, which passed from chamber to
chamber through the wide apertures connecting these cavities,
and from tier to tier by means of the tubuli in the shell-wall and
the branching canals in the intermediate skeleton. Through
the perforated shell-wall covering the outer surface the soft
body-substance flowed out, forming a gelatinous investment,
from every point of which radiated an interlacing net of deli-
cate filaments, providing nourishment for the entire colony.
In its present state, as before said, all the cavities originally
occupied by the body-substance have been filled with some
mineral substance, generally with one of the silicates of mag-
nesia; and it has been asserted that this fact militates strongly
against the organic nature of ozodn, if not absolutely dis-
proving it. As a matter of fact, however—as previously no-
ticed—it is by no means very uncommon at the present day
to find the shells of living species of Foraminifera in which
all the cavities primitively occupied by the body-substance,
down to the minutest pores and canals, have been similarly
injected by some analogous silicate, such as glauconite.

Those, then, whose opinions on such a subject deservedly
carry the greatest weight, are decisively of opinion that we are
presented in the Zozodn of the Laurentian Rocks of Canada
with an ancient, colossal, and in some-respects abnormal type
of the Foraminifera. In the words of Dr Carpenter, it is not
pretended that ‘‘the doctrine of the Foraminiferal nature of
Lozoon can be proved in the demonstrative sense;” but it
may be affirmed “that the convergence of a number of separate
and independent probabilities, all accordant with that hypothesis,
while a separate explanation must be invented for each of
them on any other hypothesis, gives it that high probability
on which we rest in the ordinary affairs of life, in the verdicts
of juries, and in the interpretation of geological phenomena
generally.”

It only remains to be added, that whilst Zozodn is by far
the most important organic body hitherto found in the Lauren-
tian, and has been here treated at proportionate length, other

Ps

THE LAURENTIAN AND HURONIAN PERIODS. 75

traces of life have been detected, which may subsequently
prove of great interest and importance. Thus, Principal
Dawson has recently described under the name of Archeo-
spherine certain singular rounded bodies which he has dis-
covered in the Laurentian limestones, and which he believes
to be casts of the shells of Foraminifera possibly somewhat
allied to the existing Glodigering. The same eminent palzeon-
tologist has also described undoubted worm-burrows from
rocks probably of Laurentian age. Further and more extend-
ed researches, we may reasonably hope, will probably bring
to light other actual remains of organisms in these ancient
deposits.

THE HURONIAN PERIOD.

The so-called AWuronian Rocks, like the Laurentian, have
their typical development in Canada, and derive their name
from the fact that they occupy an extensive area on the borders
of Lake Huron. They are wholly metamorphic, and consist
principally of altered sandstones or quartzites, siliceous, fels-
pathic, or talcose slates, conglomerates, and limestones. They
are largely developed on the north shore of Lake Superior,
and give rise to a broken and hilly country, very hke that
occupied by the Laurentians, with an abundance of timber,
but rarely with sufficient soil of good quality for agricultural
purposes. They are, however, largely intersected by mineral
veins, containing silver, gold, and other metals, and they will
ultimately doubtless yield a rich harvest to the miner. The
Huronian Rocks have been identified, with greater or less
certainty, in other parts of North America, and also in the
Old World.

The total thickness of the Huronian Rocks in Canada is
estimated as being not less than 18,000 feet, but there is con-
siderable doubt as to their precise geological position. In
their typical area they rest unconformably on the edges of
strata of Lower Laurentian age ; but they have never been seen
in direct contact with the Upper Laurentian, and their exact
relations to this series are therefore doubtful. It is thus open
to question whether the Huronian Rocks constitute a distinct
formation, to be intercalated in point of time between the
Laurentian and the Cambrian groups; or whether, rather, they
should not be considered as the metamorphosed representa-
tives of the Lower Cambrian Rocks of other regions.

As regards the fossils of the Huronian Rocks, little can be
said. Some of the specimens of Zozo0on Canadense which have

76. < HISTORICAL PALASONTOLOGY. :

been discovered in Canada are thought to come from rocks
which are probably of Huronian age. In Bavaria, Dr Gumbel
has described a species of Zozoon under the name of Zozo0n
Bavaricum, from certain metamorphic limestones which he
refers to the Huronian formation. Lastly, the late Mr Billings
described, from rocks in Newfoundland apparently referable to
the ehcagaeae certain problematical limpet-shaped fossils, to
which he gave the name of Asfpidella.

LITERATURE.

Amongst the works and memoirs which the student may consult with
regard to the Laurentian and Huronian deposits may be mentioned the
following :*—

(1) ‘Report of Progress of the Geological Survey of Canada from its

Commencement to 1863,’ pp. 38-49, and pp. 50-66.

(2) ‘ Manual of Geology.’ Dana. 2d Ed. 1875.

(3) ‘The Dawn of Life.’ J. W. Dawson. 1876.

(4) ‘On the Occurrence of Organic Remains in the Laurentian Rocks

of Canada.” Sir W. E. Logan. ‘ Quart. Journ. Geol. Soc.,’
XX1. 45-50.

(5) ‘*On the Structure of Certain Organic Remains in the Laurentian
Limestones of Canada.” J. W. Dawson. ‘ Quart. Journ. Geol.
Soc.,’ xxi. 51-59.

(6) ‘* Additional Note on the Structure and Affinities of Eozoon Cana-
dense.”” W. B. Carpenter. ‘Quart. Journ. Geol. Soc.,* xxi
59-66.

(7) ‘‘Supplemental Notes on the Structure and Affinities of Eozoon
Canadense.” W. B. Carpenter. ‘Quart. Journ. Geol. Soc.,
XXil. 219-228.

(8) ‘‘ Onthe So-Called Eozodnal Rocks.” King & Rowney. ‘ Quart.
Journ. Geol. Soc.,’ xxii. 185-218.

(9) ‘ Chemical and Geological Essays.’ Sterry Hunt.

The above list only includes some of the more important memoirs which
may be consulted as to the geological and chemical features of the Lauren-
tian and Huronian Rocks, and as to the true nature of Zozodn. Those
who are desirous of studying the later phases of the controversy with re-
gard to Hozoém must consult the papers of Carpenter, Carter, Dawson,
King & Rowney, Hahn, and others, in the ‘ Quart. Journ. of the Geological
Society,’ the ‘ Proceedings of the Royal Irish Academy,’ the ‘Annals of Nat-
ural History,’ the ‘Geological Magazine,’ &c. Dr Carpenter’s ‘ Introduc-
tion to the Study of the Foraminifera’ should also be consulted.

* In this and in all subsequently following bibliographical lists, not only
is the selection of works and memoirs quoted necessarily extremely limited;
but only such have, asa general rule, been chosen for mention as are easily
accessible to students who are in the position of being able to refer toa
good library. Exceptions, however, are occasionally made to this rule,
in favour of memoirs or works of special historical interest. It is also un-
necessary to add that it has not been thought requisite to insert in these
lists the well-known handbooks of geological and palzontological science,
except in such instances as where they contain special information on
special points.

THE CAMBRIAN PERIOD. T7.

Cire Re VLE.
THE CAMBRIAN PERIOD.

The traces of life in the Laurentian period, as we have seen,
are but scanty ; but the Camérian Rocks—so called from their
occurrence in North Wales and its borders (‘‘ Cambria”)—have
yielded numerous remains of animals and.some dubious plants.
The Cambrian deposits have thus a special interest as being
the oldest rocks in which occur any number of well-preserved
and unquestionable organisms. We have here the remains of
the first fawna, or assemblage of animals, of which we have at
present knowledge. As regards their geographical distribu-
tion, the Cambrian Rocks have been recognised in many parts
of the world, but there is some question as to the precise limits
of the formation, and we may consider that their most typical
area is in South Wales, where they have been carefully worked
out, chiefly by Dr Henry Hicks. In this region, in the neigh-
bourhood of the promontory of St David’s, the Cambrian Rocks
are largely developed, resting upon an ancient ridge of Pre-
Cambrian (Laurentian?) strata, and overlaid by the lowest
beds of the Lower Silurian. The subjoined sketch-section
(fig. 27) exhibits in a general manner the succession of strata
in this locality.

From this section it will be seen that the Cambrian
Rocks in Wales are divided in the first place into a lower and
an upper group. The Lower Cambrian is constituted at the
base by a great series of grits, sandstones, conglomerates, and
slates, which are known as the “‘ Longmynd group,” from their
vast development in the Longmynd Hills in Shropshire, and
which attain in North Wales a thickness of 8000 feet or more.
The Longmynd beds are succeeded by the so-called “ Mene-
vian group,” a series of sandstones, flags, and grits, about 600
feet in thickness, and containing a considerable number of
fossils. The Upper Cambrian series consists in its lower por-
tion of nearly 5000 feet of strata, principally shaly and slaty,
which are known as the “Lingula Flags,” from the great
abundance in them of a shell referable to the genus Lingula.
These are followed by tooo feet of dark shales and flaggy
sandstones, which are known as the “ Tremadoc slates,” from
their occurrence near Tremadoc in North Wales; and these
in turn are surmounted, apparently quite conformably, by the
basement Pe of the Lower Silurian,

7 8 HISTORICAL PALAZONTOLOGY.

GENERALISED SECTION OF THE CAMBRIAN ROCKS IN WALES.

Arenig Group (Base of the
Lower Silurian).

Tremadoc Slates.

Z

4

: Upper Lingula Flags.

3

y Middle Lingula Flags,

:

=)
Lower Lingula Flags,
Menevian Group.

Z

3

ea

=

=

<

O

a Longmynd or Harlech Group.

°

a

Pre-Cambrian Rocks.

The above may be regarded as giving a typical series of the
Cambrian Rocks in a typical locality ; but strata of Cambrian
age are known in many other regions, of which it is only
possible here to allude to a few of the most important. In
Scandinavia occurs a well-developed series of Cambrian de-
posits, representing both the lower and upper parts of the

THE CAMBRIAN PERIOD. 79

formation. In Bohemia, the Upper Cambrian, in particular,
is largely developed, and constitutes the so-called “ Primordial
zone” of Barrande. Lastly, in North America, whilst the
Lower Cambrian is only imperfectly developed, or is repre-
sented by the Huronian, the Upper Cambrian formation has
a wide extension, containing fossils similar in character to the
analogous strata in Europe, and known as the “ Potsdam Sand-
stone.” The subjoined table shows the chief areas where Cam-
brian Rocks are developed, and their general equivalency :

TABULAR VIEW OF THE CAMBRIAN FORMATION.

Britain. Lurope. America.
a. Tremadoc Slates. a. Primordial zone | a. Potsdam
of Bohemia. Sandstone.
6. Lingula Flags. 6. Paradoxides 6. Acadian
Upper Schists, Olenus group of New
Cambrian. Schists, and Dict- Brunswick.
yonema schists of
Sweden.

a. Longmynd Beds. | a. Fucoidal Sand- Huronian
stone of Sweden. Formation ?
6, Lianberis Slates. b. Eophyton Sand-
stone of Sweden.

c. Harlech Grits.

ad. Oldhamia Slates
of Ireland.

é. Conglomerates and
Sandstones’ of
Sutherlandshire ?
~. Menevian Beds.

Lower
Cambrian.

Like all the older Palzeozoic deposits, the Cambrian Rocks,
though by no means necessarily what would be called actually
““metamorphic,” have been highly cleaved, and otherwise
altered from their original condition. Owing partly to their
indurated state, and partly to their great antiquity, they are
usually found in the heart of mountainous districts, which have
undergone great disturbance, and have been subjected to an
enormous amount of denudation. In some cases, as in the
Longmynd Hills in Shropshire, they form low rounded eleva-
tions, largely covered by pasture, and with few or no elements
of sublimity. In other cases, however, they rise into bold and
rugged mountains, girded by precipitous cliffs. Industrially,
the Cambrian Rocks are of interest, if only for the reason that
the celebrated Welsh slates of Llanberis are derived from
highly-cleaved beds of this age. Taken as a whole, the Cam-
brian formation is essentially composed of arenaceous and

80 HISTORICAL PALZONTOLOGY.

muddy sediments, the latter being sometimes red, but more
commonly nearly black in colour. It has often been supposed
that the Cambrians are a deep-sea deposit, and that we may
thus account for the few fossils contained in them; but the
paucity of fossils is to a large extent imaginary, and some of _
the Lower Cambrian beds of the Longmynd Hills would ap-
pear to.have been laid down in shallow water, as they exhibit
rain-prints, sun-cracks, and ripple-marks—incontrovertible evi-
dence of their having been a shore-deposit. ‘The occurrence
of innumerable worm-tracks and burrows in many Cambrian
strata is also a proof of shallow-water conditions ; and the gen-
eral absence of limestones, coupled with the coarse mechani-
cal nature of many of the sediments of the Lower Cambrian,
may be taken as pointing in the same direction..

The Zfe of the Cambrian, though not so rich as in the suc-
ceeding Silurian period, nevertheless consists of representa-
tives of most of the great classes of invertebrate animals. The
coarse sandy deposits of the formation, which abound more
particularly towards its lower part, naturally are to a large
extent barren of fossils; but the muddy sediments, when not
too highly cleaved, and especially towards the summit of the
group, are replete with organic remains. This is also the case, in
many localities at any rate, with the finer beds of the Potsdam
Sandstone in America. Limestones are known to occur in
only a few areas (chiefly in America), and this may account for
the apparent total absence of corals. It is, however, interest-
ing to note that, with this exception, almost all the other lead-
ing groups of Invertebrates are known to have come into
existence during the Cambrian period.

Of the land- surfaces of the Cambrian period we know
nothing ; and there is, therefore, nothing surprising in the fact
that our acquaintance with the Cambrian vegetation is confined
to some marine plants or sea-weeds, often of a very obscure and
problematical nature. The ‘‘ Fucoidal Sandstone” of Sweden,
and the “ Potsdam Sandstone” of North America, have both
yielded numerous remains which have been regarded as mark-
ings left by sea-weeds or “ Fucoids ;” but these are highly enig-
matical in their characters, and would, in many instances, seem
to be rather referable to the tracks and burrows of marine
worms. ‘The first-mentioned of these formations has also
yielded the curious, furrowed and striated stems which have
been described as a kind of land-plant under the name of
Lophyton (fig. 28). It cannot be said, however, that the vege-
table origin of these singular bodies has been satisfactorily
proved. Lastly, there are found in certain green and purple

THE CAMBRIAN PERIOD. Sr

beds of Lower Cambrian age at Bray Head, Wicklow, Ireland,
some very remarkable fossils, which are well known under the

(htdllli

2 —————_——————

Fig. 28.—Fragment of Zophyton Linneanum, a supposed land-p'ant, Lower
Jambrian, Sweden, of the natural size.

name of O/d¢hamza, but the true nature of which is very doubtful.
The commonest form of Ol/dhamia (fig. 29) consists of a
thread-like stem or axis, from which spring at regular intervals
bundles of short filamentous branches in a fan-like manner.
In the locality where it occurs, the fronds of O/dhamia are very
abundant, and are spread over the surfaces of the strata in
tangled layers. That it is organic is certain, and that it is a
calcareous sea-weed is probable ; but it may possibly belong to
the sea-mosses (Polyzoa), or to the sea-firs (Sevtularians).
Amongst the lower forms of animal life (Protozoa), we find
the Sponges represented by the curious bodies, composed of
netted fibres, to which the name of Protospongia has been given
(fig. 32, a); and the comparatively gigantic, conical, or cylin-

82 HISTORICAL PALZONTOLOGY.

drical fossils termed Archeocyathus by Mr Billings are certainly
referable either to the Foraminifera or to the Sponges. The
almost total absence of lime-

MG stones in the formation may

i) EE be regarded as a sufficient ex-

\ Ci planation of the fact that the

) Foraminifera are not more
AE Wy largely and unequivocally re-
SV“ AW argely a quivocally re

GAA 2 presented ; though the exist-
ence of greensands in the
Cambrian beds of Wisconsin

\ “My l) Y

as an indication that this class
of animals was by no means
wholly wanting. The same
fact may explain the total ab-
sence of corals, so far as at
present known.

The group of the Echinoder-

Fig. 29.—A portion of Oldhamia an- mata (Sea-lilies, Sea-urchins,
tigua, Lower Cambrian, Wicklow, Ire- : ° :
land, of the natural size. (After Salter.) and their allies) 18 represented
by a few forms, which are prin-
cipally of interest as being the earliest-known examples of the
class. It is also worthy of note that these precursors of a
group which subsequently attains such geological importance,
are referable to no less than three distinct orders—the Crinoids
or Sea-lilies, represented by a species of Dendrocrinus; the
Cystideans by Protocystites ; and the Star-fishes by Padasterina
and some other forms. Only the last of these groups, how-
ever, appears to occur in the Lower Cambrian.

The Ringed-worms (Azmnelida), if rightly credited with all
the remains usually referred to them, appear to have swarmed
in the Cambrian seas. Being soft-bodied, we do not find the
actual worms themselves in the fossil condition, but we have,
nevertheless, abundant traces of their existence. In some
cases we find vertical burrows of greater or less depth, often
expanded towards their apertures, in which the worm must
have actually lived (fig. 30), as various species do at the pre-
sent day. In these cases, the tube must have been rendered
more or less permanent by receiving a coating of mucus, or
perhaps a genuine membranous secretion, from the body of
the animal, and it may be found quite empty, or occupied by
a.cast of sand or mud. Of this nature are the burrows which
have been described under the names of Scolithus and Scoleco-
derma, and probably the Azstioderma of the Lower Cambrian

-

and Tennessee may be taken ©

THE CAMBRIAN PERIOD. 83

of Ireland. In other cases, as in Avenicolites (fig. 32, 4), the
worm seems to have inhabited a double burrow, shaped like

Fig. 30.—Annelide-burrows (Scolithus linearis), from the Potsdam Sandstone of
Canada, of the natural size. (After Billings.) °

the letter U, and having two openings placed close together
on the surface of the stratum. Thousands of these twin-
burrows occur in some of the strata of the Longmynd, and it
is supposed that the worm used one opening to the burrow as
an aperture of entrance, and the other as one of exit. In other
cases, again, we find simply the meandering trails caused by
the worm dragging its body over the surface of the mud.
Markings of this kind are commoner in the Silurian Rocks,
and it is generally more or less doubtful whether they may
not have been caused by other marine animals, such as shell-
fish, whilst some of them have certainly nothing whatever to
do with the worms. Lastly, the Cambrian beds often show
twining cylindrical bodies, commonly more or less matted
together, and not confined to the surfaces of the strata, but
passing through them. These have often been regarded as
the remains of sea-weeds, but it is more probable that they
represent casts of the underground burrows of worms of sim1-
lar habits to the common lob-worm (Avevzcola) of the present
day.

The Articulate animals are numerously represented in the
Cambrian deposits, but exclusively by the class of Crustaceans.
Some of these are little double-shelled creatures, resembling
our living water-fleas (Ostracoda). A few are larger forms, and
belong to the same group as the existing brine-shrimps and
fairy-shrimps (PhyMopoda). One of the most characteristic of

- 84 HISTORICAL PALHZONTOLOGY.

these is the Hymenocaris vermicauda of the Lingula Flags (fig.
32, @). By far the Jarger number of the Cambrian Crustacea
belong, however, to the remarkable and wholly extinct group
of the Zyrzobites. These extraordinary animals must have
literally swarmed in the seas of the later portion of this and
the whole of the succeeding period; and they survived in
greatly diminished numbers till the earlier portion of the
Carboniferous period. They died out, however, wholly before
the close of the Palzozoic epoch, and we have no Crusta-
ceans at the present day which can be considered as their
direct representatives. They have, however, relationships of
amore or less intimate character with the existing groups of
the Phyllopods, the King-crabs (Zzmulus), and the Isopods
(‘‘Slaters,” Wood-lice, &c.) Indeed, one member of the last-
mentioned order, namely, the Sevo/zs of the coasts of Patagonia,
has been regarded as the nearest living ally of the Trilobites.
Be this as it may, the Trilobites possessed a skeleton which,
though capable of undergoing almost endless variations, was
wonderfully constant in its pattern of structure, and we may
briefly describe here the chief features of this.

The upper surface of the body of a Trilobite was defended
by a strong shell or “‘ crust,” partly horny and partly calcare-
ous in its composition. This shell (fig. 31) generally exhibits
a very distinct “ trilobation ” or division into three longitudinal
lobes, one central and two lateral. It also exhibits a more
important and more fundamental division into three transverse
portions, which are so loosely connected with one another as
very commonly to be found separate. The first and most
anterior of these divisions is a shield or buckler which covers
the head ; the second or middle portion is composed of mov-
able rings covering the trunk (“‘ thorax”); and the third is a
shield which covers the tail or “‘abdomen.” The head-shield
(fig. 31, €) is generally more or less semicircular in shape ; and
its central portion, covering the stomach of the animal, is usu-
ally strongly elevated, and generally marked by lateral furrows.
A little on each side of the head are placed the eyes, which
are generally crescentic in shape, and resemble the eyes of
insects and many existing Crustaceans in being ‘‘ compound,”
or made up of numerous simple eyes aggregated together.
So excellent is the state of preservation of many specimens of
Tnilobites, that the numerous individual lenses of the eyes
have been uninjured, and as many as four hundred have been
counted in each eye of some forms. The eyes may be sup-
ported upon prominences, but they are never carried on mov-
able stalks (as they are in the existing lobsters and crabs) ; and

THE CAMBRIAN PERIOD. 85

in some of the Cambrian Trilobites, such as the little Agnostz
(fig. 31 g), the animal was blind. ‘The lateral portions of the

Fig. 2r.—Cambrian Trilobites: a, Paradoxides Bohemicus, reduced in size; 6, Ellip-
socephalus Hoffi; c, Sao hirsuta; d, Conocoryphe Sultzeri (all the above, together with
fig. g, are from the Upper Cambrian or “‘ Primordial Zone” of Bohemia); ¢, Head-shield
of Dikellocephalus Celticus, from the Lingula Flags of Wales; 74, Head-shield of Cozo-
coryphe Matthewi, from the Upper Cambrian (Acadian Group) of New Brunswick; g,
A gnostus rex, Bohemia ; 4, Tail-shield of Dikellocephalus Minnesotensis, from the Upper
Cambrian (Potsdam Sandstone) of Minnesota. (After Barrande, Dawson, Salter, and
Dale Owen.)

head-shield are usually separated from the central portion by
a peculiar line of division (the so-called “facial suture”) on
each side; but this is also wanting in some of the Cambrian
species. The backward angles of the head-shield, also, are
often prolonged into spines, which sometimes reach a great
length. Following the head-shield behind, we have a portion
of the body which is composed of movable segments or “‘body-
rings,” and which is technically called the ‘‘ thorax.” Ordi-
narily, this region is strongly trilobed, and each ring consists of
a central convex portion, and of two flatter side-lobes. The
number of body-rings in the thorax is very variable (from two
to twenty-six), but is fixed for the adult forms of each group of
the Tnlobites. The young forms have much fewer rings than
the full-grown ones ; and it is curious to find that the Cam-

86 HISTORICAL PALZONTOLOGY.

brian Trilobites very commonly have either a great many rings
(as in Paradoxides, fig. 31, a), or else very few (as in Agnostus,
fig. 31, g). In some instances, the body-rings do not seem to
have been so constructed as to allow of much movement, but
in other cases this region of the body is so flexible that the
animal possessed the power of rolling itself up completely, like
a hedgehog ; and many individuals have been permanently
preserved as fossils in this defensive condition. Finally, the
body of the Trilobite was completed by a tail-shield (techni-
cally termed the ‘“‘ pygidium”), which varies much in size and
form, and is composed of a greater or less number of rings,
similar to those which form the thorax, but immovably amalga-
mated with one another (fig. 31, 4).

The under surface of the body in the Trilobites appears to
have been more or less entirely destitute of hard structures,
with the exception of a well-developed upper lip, in the form
of a plate attached to the inferior side of the head-shield in
front. ‘There is no reason to doubt that the animal possessed
legs; but these structures seem to have resembled those of
many living Crustaceans in being quite soft and membranous.
This, at any rate, seems to have been generally the case;
though structures which have been regarded as legs have been
detected on the under surface of one of the larger species of
Trilobites. ‘There is also, at present, no direct evidence that
the Trilobites possessed the two pairs of jointed feelers (‘“an-
tennz”) which are so characteristic of recent Crustaceans.

The Trilobites vary much in size, and the Cambrian forma-
tion presents examples of both the largest and the smallest
members of the order. Some of the young forms may be little
bigger than a millet-seed, and some adult examples of the
smaller species (such as Agwostus) may be only a few lines in
length ; whilst such giants of the order as Faradoxides and
Asaphus may reach a length of from one to two feet. Judging
from what we actually know as to the structure of the Trilo-
bites, and also from analogous recent forms, it would seem that
these ancient Crustaceans were mud-haunting creatures, deni-
zens of shallow seas, and affecting the soft silt of the bottom
rather than the clear water-above. Whenever muddy sedi-
ments are found in the Cambrian and Silurian formations,
there we are tolerably sure to find Tnilobites, though they are
by no means absolutely wanting in limestones. They appear
to have crawled about upon the sea-bottom, or burrowed in the
yielding mud, with the soft under surface directed downwards;
and it is probable that they really derived their nutriment from
the organic matter contained in the ooze amongst which they

THE CAMBRIAN PERIOD. 87

lived. The vital organs seem to have occupied the central lobe
of the skeleton, by which they were protected ; and a series of
delicate leaf-like paddles, which probably served as respiratory
organs, would appear to have been carried on the under surface
of the thorax. That they had their enemies may be regarded
as certain; but we have no evidence that they were furnished
with any offensive weapons, or, indeed, with any means of
defence beyond their hard crust, and the power, possessed by
so many of them, of rolling themselves into a ball. An addi-
tional proof of the fact that they for the most part crawled
along the sea-bottom is found in the occurrence of tracks and
markings of various kinds, which can hardly be ascribed to
any other creatures with any show of probability. That this
is the true nature of some of the markings in question cannot
be doubted at all ; and in other cases no explanation so pro-
bable has yet been suggested. If, however, the tracks which
have been described from the Potsdam Sandstone of North
America nnder the name of Profschnites are really due to the
peregrinations of some Trilobite, they must have been pro-
duced by one of the largest examples of the order.

As already said, the Cambrian Rocks are very rich in the
remains of Trilobites. In the lowest beds of the series (Long-
mynd Rocks), representatives of some half-dozen genera have
now been detected, including the dwarf Agvostus and the giant
Paradoxtdes. In the higher beds, the number both of genera
and species is largely increased ; and from the great compara-
tive abundance of individuals, the Trilobites have every right
to be considered as the most characteristic fossils of the Cam-
brian period,—the more so as the Cambrian species belong to
peculiar types, which, for the most part, died out before the
commencement of the Silurian epoch.

All the remaining Cambrian fossils which demand any notice
here are members of one or other division of the great class
of the Mollusca, or “ Shell-fish” properly so called. In the
Lower Cambrian Rocks the Lamp-shells (Lvachiopoda) are the
principal or sole representatives of the class, and appear chiefly
in three interesting and important types—namely, Lzngulella,
Discina, and Obolella. Of these the last (fig. 32, 2) is highly
characteristic of these ancient deposits; whilst Dzscewa is one
of those remarkable persistent types which, commencing at
this early period, has continued to be represented by varying
forms through all the intervening geological formations up to
the present day. Lzngulella (fig. 32, c), again, is closely allied
to the existing ‘‘ Goose-bill ” Lamp-shell (Zzzgula anatina), and
thus presents us with another example of an extremely long-

88 HISTORICAL PALZ ONTOLOGY.

lived type. The Zzngulelle and their successors, the Zingule,
are singular in possessing a shell which is of a horny texture,
and contains but a small proportion of calcareous matter. In
the Upper Cambrian Rocks, the Zzmgulelle become much more
abundant, the broad satchel-shaped species known as JZ.
Davisii (fig. 32, e) being so abundant that one of the great
divisions of the Cambrian is termed the “ Lingula Flags.”
Here, also, we meet for the first time with examples of the
genus Orthis (fig. 32, 7, &, 2) a characteristic Paleozoic type of

i
t

Fig. 32.—Cambrian Fossils: a, Protospongia fenestrata, Menevian Group; 6, Avenz-
colites didymus, Longmynd Group; c, Lingulella ferruginea, Longmynd and Menevian,
enlarged; ad, Hymenocaris vermicauda, Lingula Flags; e, Lingulella Davzsi, Lingula
Flags; 74, Orthts lenticularis, Lingula Flags; g, Theca Davidiz, Tremadoc Slates; %,
Modiolopsis Solvensis, Yremadoc Slates; 2, Obolella sagittalis, interior of valve, Mene-
vian; 7, Exterior of the same; 4, Orthts Hicksii, Menevian; @Z, Cast of the same; 7,
Olenus micrurus, Lingula Flags. (After Salter, Hicks, and Davidson.)

the Brachiopods, which is destined to undergo a vast extension
in later ages.
Of the higher groups of the A/ol/usca the record is as yet
but scanty. In the Lower Cambrian, we have but the thin,
fragile, dagger-shaped shells of the free-swimming oceanic
Molluscs or ‘‘ Winged-snails” (Pteropoda), of which the most
characteristic is the genus Zheca (fig. 32, g). In the Upper
Cambrian, in addition to these, we have a few Univalves
(Gasteropoda), and, thanks to the researches of Dr Hicks,
quite a small assemblage of Bivalves (Lamellibranchiata),
though these are mostly of no great dimensions (fig. 32, #).
Of the chambered Cephalopoda (Cuttle-fishes and their allies),

THE CAMBRIAN PERIOD. 89

we have but few traces, and these wholly confined to the higher
beds of the formation. We meet, however, with examples of
the wonderful genus Orthoceras, with its
straight, partitioned shell, which we shall
find in an immense variety of forms in the
Silurian rocks. Lastly, it is worthy of
note that the lowest of all the groups of
the Mollusca — namely, that of the Sea-
mats, Sea-mosses, and Lace-corals (Po/y-
zoa)—is only doubtfully known to have
any representatives in the Cambrian,
though undergoing a large and varied
development in the Silurian deposits.

An exception, however, may with much | |
probability be made to this statement in Big ohimemention
favour of the singular genus Diuctyonema Dictyonema sociale, cow
(fig. 33), which is highly characteristic -of fis ne Inoumy eel es
the highest Cambrian beds (Tremadoc Win te onharos
Slates). This curious fossil occurs in the of cells on each side.
form of fan-like or funnel-shaped expan- 0”!
sions, composed of slightly-diverging horny branches, which
are united in a net-like manner by numerous delicate cross-
bars, and exhibit a row of little cups or cells, in which the ani-
mals were contained, on each side. Dzctyonema has generally
been referred to the Gvaffolites ; but it has a much greater
affinity with the plant-like Sea-firs (Sertularians) or the Sea-
mosses (Polyzoa), and the balance of evidence is perhaps in
favour of placing it with the latter.

LITERATURE.

The following are the more important and accessible works and memoirs
which may be consulted in studying the stratigraphical and palzeontolo-
gical relations of the Cambrian Rocks :—
(1) ‘Siluria.” Sir Roderick Murchison. 5th ed., pp. 21-46.
_ (2) ‘Synopsis of the Classification of the British Palzozoic Rocks.’
Sedgwick. Introduction to the 3d Fasciculus of the ‘ Descrip-
tions of British Palzeozoic Fossils in the Woodwardian Museum,’
by F. M‘Coy, pp. i-xcviii, 1855.
(3) ‘Catalogue of the Cambrian and Silurian Fossils in the Geological
Museum of the University of Cainbridge.’ Salter. With a Pref-
ace by Prof. Sedgwick. 1873.

(4) ‘ Thesaurus Siluricus.’ Bigsby. 1868. ;

(5) ‘“‘ History of the Names Cambrian and Silurian.” Sterry Hunt.—
‘Geological Magazine.’ 1873.

_ (6) ‘Systeme Silurien du Centre de la Bohéme.’ Barrande. Vol. I.

(7) ‘ Report of Progress of the Geological Survey of Canada, from its

Commencement to 1863,’ pp. 87-109.

go HISTORICAL PALAON TOLOGY.

(8) ‘Acadian Geology.’ Dawson. Pp. 641-657.

(9) ‘Guide to the Geology of New York,” Lincklaen; and ‘‘ Contribu-
tions to the Paleontology of New York,” James Hall.—‘ Four-
teenth Report on the State Cabinet.’ 1861.

(10) ‘ Palzeozoic Fossils of Canada.’ Billings. 1865.

(11) ‘ Manual of Geology.’ Dana. Pp. 166-182. 2ded. 1875.

(12) ‘*Geology of North Wales,” Ramsay; with Appendix on the
Fossils, Salter.—‘ Memoirs of the Geological Survey of Great

_ Britain,’ vol. iii. 1866.

(13) ‘fOnthe Ancient Rocks of the St David’s Promontory, South Wales,
and their Fossil Contents.” Harkness and Hicks.—‘ Quart.
Journ. Geol. Soc.,’ xxvii. 384-402. 1871.

(14) *fOn the Tremadoc Rocks in the Neighbourhood of St David’s,
South Wales, and their Fossil Contents.” Hicks.—‘ Quart. ~
Journ. Geol. Soc.,’ xxix. 39-52. 1873.

In the above list, allusion has necessarily been omitted to numerous
works and memoirs on the Cambrian deposits of Sweden and Norway,
Central Europe, Russia, Spain, and various parts of North America, as
well as to a number of important papers on the British Cambrian strata by
various well-known observers. Amongst these latter may be mentioned
memoirs by Prof. Phillips, and Messrs Salter, Hicks, Belt, Plant, Hom-
fray, Ash, Holl, &c.

CoEPALP ER ik
THE LOWER SILURIAN PERIOD.

The great system of deposits to which Sir Roderick Murchi-
son applied the name of “Silurian Rocks” reposes directly
upon the highest Cambrian beds, apparently without any
marked unconformity, though with a considerable change in
the nature of the fossils. The name ‘‘Silurian” was originally
proposed by the eminent geologist just alluded to for a great
series of strata lying below the Old Red Sandstone, and occu-
pying districts in Wales and its borders which were at one
time inhabited by the ‘‘Silures,” a tribe of ancient Britons.
Deposits of a corresponding age are now known to be largely
developed in other parts of England, in Scotland, and in Ire-
land, in North America, in Australia, in India, in Bohemia,
Saxony, Bavaria, Russia, Sweden and Norway, Spain, and in
various other regions of less note. In some regions, as in the
neighbourhood of St Petersburg, the Silurian strata are found
not only to have preserved their original horizontality, but also
to have retained almost unaltered their primitive soft and inco-
herent nature. In other regions, as in Scandinavia and many

THE LOWER SILURIAN PERIOD. Ql

parts of North America, similar strata, now consolidated into
shales, sandstones, and limestones, may be found resting with
a very slight inclination on still older sediments. In a great
many regions, however, the Silurian deposits are found to have
undergone more or less folding, crumpling, and dislocation,
accompanied by induration and “‘cleavage” of the finer and
softer sediments ; whilst in some regions, as in the Highlands
of Scotland, actual ‘‘metamorphism” has taken place. In
consequence of the above, Silurian districts usually present
the bold, rugged, and picturesque outlines which are char-
acteristic of the older ‘‘ Primitive” rocks of the earth’s crust in
general. In many instances, we find Silurian strata rising into
mountain-chains of great grandeur and sublimity, exhibiting
the utmost diversity of which rock-scenery is capable, and de-
lighting the artist with endless changes of valley, lake, and
cliff. Such districts are little suitable for agriculture, though this
is often compensated for by the valuable mineral products con-
tained in the rocks. On the other hand, when the rocks are
tolerably soft and uniform in their nature, or when few disturb-
ances of the crust of the earth have taken place, we may find
Silurian areas to be covered with an abundant pasturage or to
be heavily timbered.

Under the head of “Silurian Rocks,” Sir Roderick Murchi-
son included all the strata between the summit of the ‘‘ Long-
mynd” beds and the Old Red Sandstone, and he divided these
into the two great groups of the Zower Silurian and Upper Silu-
rian. It is, however, now generally admitted that a considerable
portion of the basement beds of Murchison’s Silurian series
must be transferred—if only upon palzontological grounds—to
the Upper Cambrian, as has here been done; and much contro-
versy has been carried on as to the proper nomenclature of the
Upper Silurian and of the remaining portion of Murchison’s
Lower Silurian. Thus, some would confine the name “ Silu-
rian” exclusively to the Upper Silurian, and would apply the
name of ‘ Cambro-Silurian” to the Lower Silurian, or would
include all beds of the latter age in the ‘‘ Cambrian ” series of
Sedgwick. It is not necessary to enter into the merits of these
conflicting views. For our present purpose, it is sufficient to
recognise that there exist two great groups of rocks between
the highest Cambrian beds, as here defined, and the base of
the Devonian or Old Red Sandstone. ‘These two great groups
are so closely allied to one another, both physically and pale-
ontologically, that many authorities have established a third
or intermediate group (the “ Middle Silurian”), by which a pas-

Q2 HISTORICAL PALAONTOLOGY.

sage is made from one into the other. This method of pro-
cedure involves disadvantages which appear to outweigh its
advantages ; and the two groups in question are not only gen-
erally capable of very distinct stratigraphical separation, but at
the same time exhibit, together with the alliances above spoken
of, so many and such important paleontological differences,
that it is best to consider them separately. We shall there-
fore follow this course in the present instance; and pending
the final solution of the controversy as to Cambrian and Silu-
rian nomenclature, we shall distinguish these two groups of
strata as the ‘‘ Lower Silurian” and the “‘ Upper Silurian.”

The Lower Silurian Rocks are known already to be devel-
oped in various regions ; and though their geweral succession
in these areas is approximately the same, each area exhibits
peculiarities of its own, whilst the subdivisions of each are
known by special names. | All, therefore, that can be attempted
here, is to select two typical areas—such as Wales and North
America—and to briefly consider the grouping and divisions
of the Lower Silurian in each.

In Wales, the line between the Cambrian and Lower Silurian
is somewhat ill-defined, and is certainly not marked by any
strong unconformity. There are, however, grounds for accept-
ing the line proposed, for paleontological reasons, by Dr
Hicks, in accordance with which the Tremadoc Slates (‘Lower
Tremadoc” of Salter) become the highest of the Cambrian
deposits of Britain. If we take this view, the Lower Silurian
rocks of Wales and adjoining districts are found to have the
following gezera/ succession from below upwards (fig. 34) :—

1. The Avenig Group.—This group derives its name from
the Arenig mountains, where it is extensively developed. It
consists of about 4000 feet of slates, shales, and flags, and is
divisible into a lower, middle, and upper division, of which the
former is often regarded as Cambrian under the name of
“ Upper Tremadoc Slates.”

2. The Llandeilo Group.—The thickness of this group varies
from about 4000 to as much as 10,000 feet; but in this latter
case a great amount of the thickness is made up of volcanic
ashes and interbedded traps. The sedimentary beds of this
group are principally slates and flags, the latter occasionally
with calcareous bands; and the whole series can be divided
into a lower, middle, and upper Llandeilo division, of which
the last is the most important. The name of ‘“ Llandeilo” is
derived from the town of the same name in Wales, where strata
of this age were described by Murchison.

THE LOWER SILURIAN PERIOD. 93

3. The Caradoc or Bala Group.—The alternative names of
this group are also of local origin, and are derived, the one
from Caer Caradoc in Shropshire, the other from Bala 1 in Wales, -
strata of this age occurring in both localities. ‘The series is
divided into a Tower and upper group, the latter chiefly com-
posed of shales and flags, and the former of sandstones and
shales, together with the important and interesting calcareous
band known as the “ Bala Limestone.” The thickness of the
entire series varies from 4000 to as much as 12,000 feet, ac-
cording as it contains more or less of interstratified igneous
rocks.

4. The Llandovery Group (Lower Llandovery of Murchison).
—This series, as developed near the town of Llandovery, in
Caermarthenshire, consists of less than 1ooo feet of conglom-
erates, sandstones, and shales. It is probable, however, that
the little calcareous band known as the ‘‘ Hirnant Limestone,”
together with certain pale-coloured slates which le above the
Bala Limestone, though usually referred to the Caradoc series,
should in reality be regarded as belonging to the Llandovery
group.

The general succession of the Lower Silurian strata of Wales
and its borders, attaining a maximum thickness (along with
contemporaneous igneous matter) of nearly 30,000 feet, is
diagramatically represented in the annexed sketch-section

(fig. 34) :—

[GENERALISED SECTION

O4 HISTORICAL PALZONTOLOGY.

GENERALISED SECTION OF THE LOWER SILURIAN Rocks
OF WALES.

Fig. 34.

May Hill Sandstone (base
of Upper Silurian).

Llandovery Group.

LLANDO-
VERY
GROUP

a

5

©)

g Upper Bala.

oO

<

—

<

=

ee

fo)

3)

2 Lower Bala.

<

fo

=

O

a 2, Upper hiandenet

m2

oO
————

3 SNe Seabee eee Bs Middle Llandeilo.

ae ee ae

5 Sea ee ay eS rae ee

2 | Gerona

4 a ower llandelea:
ees Upper Arenig.

5

io) /

c —— | bite bser

= TIA LPF PTT

ee Lower Arenig (Upper

SO ———————— Tremadoc Group).

——S— Tremadoc Slates (Lower
= Tremadoc Group).

In North America, both in the United States and in Can-
ada, the Silurian rocks are very largely developed, and may be

THE LOWER SILURIAN PERIOD. 95

regarded as constituting an exceedingly full and typical series
of the deposits of this period. The chief groups of the Silurian
rocks of North America are as follows, beginning, as_ before,
with the lowest strata, and proceeding upwards (fig. 35) :—

1. Quebec Group. —'This group is typically developed in
the vicinity of Quebec, where it consists of about 5000 feet of
strata, chiefly variously - coloured shales, together with some
sandstones and a few calcareous bands. It contains a number
of peculiar Graptolites, by which it can be identified without
question with the Arenig group of Wales and the correspond-
ing Skiddaw Slates of the North of England. It is also to be
noted that numerous Trilobites of a distinct Cambrian /aczes
have been obtained in the limestones of the Quebec group,
near Quebec. These fossils, however, have been exclusively
obtained from the limestones of the group; and as these lime-
stones are principally calcareous breccias or conglomerates,
there is room for believing that these primordial fossils are
really derived, in part at any rate, from fragments of an upper
Cambrian limestone. In the State of New York, the Grapto-
litic shales of Quebec are wanting ; and the base of the Silurian
is constituted by the so-called ‘‘ Calciferous Sand-rock” and
““Chazy Limestone.”* The first of these is essentially and
typically calcareous, and the second is a genuine limestone.

2. The Zrenton Group.—This is an essentially calcareous
group, the various limestones of which it is composed being
known as the “ Bird’s-eye,” ‘‘ Black River,” and ‘‘ Trenton ”
Limestones, of which the last is the thickest and most import-
ant. The thickness of this group is variable, and the bands of
limestone in it are often separated by beds of shale.

3. The Cincinnati Group (Hudson River Formation t).—
This group consists essentially of a lower series of shales, often
black in colour and highly charged with bituminous matter
(the ‘‘ Utica Slates”), and of an upper series of shales, sand-

* The precise relations of the Quebec shales with Graptolites (Levis
Formation) to the Calciferous and Chazy beds are still obscure, though
there seems little doubt but that the Quebec Shales are superior to the
Calciferous Sand-rock.

+ There is some difficulty about the precise nomenclature of this group.
It was originally called the ‘‘ Hudson River Formation;’’ but this name
is inappropriate, as rocks of this age hardly touch anywhere the actual
Hudson River itself, the rocks so called formerly being now known to be
of more ancient date. There is also some want of propriety in the name of
** Cincinnati Group,” since the rocks which are known under this name in
the vicinity of Cincinnati itself are the representatives of the Trenton
Limestone, Utica Slates, and the old Hudson River group, inseparably
united in what used to be called the ‘‘ Blue Limestone Series,”

96 HISTORICAL PALZONTOLOGY.

stones, and limestones (the ‘‘ Cincinnati” rocks proper). The
exact parallelism of the Trenton and Cincinnati groups with
the subdivisions of the Welsh Silurian series can hardly be
stated positively. Probably no precise equivalency exists ;
but there can be no doubt but that the Trenton and Cincin-
nati groups correspond, as a whole, with the Llandeilo and
Caradoc groups of Britain. The subjoined diagrammatic
section (fig. 35) gives a general idea of the succession of the
Lower Silurian rocks of North America :—

GENERALISED SECTION OF THE LOWER SILURIAN ROCKS
oF NORTH AMERICA.
Fig.

5-

Oo

Medina Sandstone (base of
Upper Silurian).

5
O
a
= == Cincinnati Group proper.
=:
Fp
2
3)
Ai =
= = Utica Slates.
5
eS — ~Trenton Limestone.
O
Zz.
°
& aa a
= | {ft} __Black River Limestone.
=
an! - . .
iinnnTTin eae Rea os. Tne eee
. BOA d
Ae a Ht} Chazy Limestone.
> HH} i
=
= SS ____ Quebec Shales (Levis Beds).
o |___Calciferous Sand-rock.

--.... Potsdam Sandstone.

THE LOWER SILURIAN PERIOD. 97

Of the “fe of the Lower Silurian period we have record in a
vast number of fossils, showing that the seas of this period
were abundantly furnished with living denizens. We have,
however, in the meanwhile, no knowledge of the land-surfaces
of the period. We have therefore no means of speculating
as to the nature of the terrestrial animals of this ancient age,
nor is anything known with certainty of any land-plants which
may have existed. The only relics of vegetation upon which
a positive opinion can be expressed belong to the obscure
‘group of the “ Fucoids,” and are supposed to be the remains
of sea-weeds. Some of the fossils usually placed under this
head are probably not of a vegetable nature at all, but others

Fig. 36.— Licrophycus Ottawaensis, a “‘ Fucoid,” from the Trenton Limestone
(Lower Silurian) of Canada. (After Billings.)

(fig. 36) appear to be unquestionable plants. The true affin-
ities of these, however, are extremely dubious. All that can
be said is, that remains which appear to be certainly vegetable,

98 HISTORICAL PALAZAONTOLOGY. -

and which are most probably due to marine plants, have been
recognised nearly at the base of the Lower Silurian (Arenig),
and that they are found throughout the series whenever suitable
conditions recur.

The Protozoans appear to have flourished extensively in the
Lower Silurian seas, though to a large extent under forms
which are still little understood. We have here for the first
time the appearance of /oraminzfera of the ordinary type—one
of the most interesting observations in this connection being
that made by Ehrenberg, who showed that the Lower Silurian
sandstones of the neighbourhood of St Petersburg contained
casts in glauconite of Foraminiferous shells, some of which are
referable to the existing genera Rofa/ia and Textularia. True
Sponges, belonging to that section of the group in which the
skeleton is calcareous, are also not unknown, one of the most
characteristic genera being As-
tylospongia (fig. 37). In this
genus are included more or less
globular, often lobed sponges,
which are believed not to have
been attached toforeign bodies.
In the form here figured there
is a funnel-shaped cavity at the
summit; and the entire mass of
the sponge is perforated, as in
living examples, by a system
of canals which convey the
sea-water to all parts of the

Fig. 37-—Astylospongia premorsa, cut organism. The canals by
vertically so as to exhibit the canal-system which the sea-water gains en-
ee cn Tennessee trance open on the exterior of

the sphere, and those by which
it again escapes from the sponge open into the cup-shaped
depression at the summit.

The most abundant, and at the same time the least under-
stood, of Lower. Silurian Protozoans belong, however, to the
genera S/romatopora and Receptaculites, the structure of which
can merely be alluded to here. The specimens of Stromato-
pora (fig. 38) occur as hemispherical, pear-shaped, globular, or
irregular masses, often of very considerable size, and some-
times demonstrably attached to foreign bodies. In their struc-
ture these masses consist of numerous thin calcareous lamine,
usually arranged concentrically, and separated by narrow
interspaces. These interspaces are generally crossed by
numerous vertical calcareous pillars, giving the vertical section

THE LOWER SILURIAN PERIOD. 99

of the fossil a lattice-like appearance. There are also usually
minute pores in the concentric lamine, by which the successive

Fig. 38.—A small and perfect specimen of Stromatopora rugosa, of the natural
size, from the Trenton Limestone of Canada. (After Billings.)

interspaces are placed in communication ; and sometimes the
surface presents large rounded openings, which appear to corre-
spond with the water-canals of the Sponges. Upon the whole,
though presenting some curious affinities to the calcareous
Sponges, Stromatopora is perhaps more properly regarded as
a gigantic Foraminifer. If this view be correct, it is of special
interest as being probably the nearest ally of Fozoon, the
general appearance of the two being strikingly similar, though
their minute structure is not at all the same. Lastly, in the
fossils known as Receptaculites and [schadites we are also pre-
sented with certain singular Lower Silurian Protozoans, which
may with great probability be regarded as gigantic Foram-
nifera. Their structure 1s very complex; but fragments are
easily recognised by the fact that the exterior is covered with
numerous rhomboidal calcareous plates, closely fitting together,
and arranged in peculiar intersecting curves, presenting very
much the appearance of the engine-turned case of a watch.
Passing next to the sub-kingdom of Ce/enterate animals
(Zoophytes, Corals, &c.), we find that this great group, almost
or wholly absent in the Cambrian, is represented in Lower

100, HISTORICAL PALHONTOLOGY.,

Silurian deposits by a great number of forms belonging on the
one hand to the true Corals, and on the other hand to the
singular family of the Graf/olites. If we except certain plant-
like fossils which probably belong rather to the Sertularians
or the Polyzoans (e. g., Dzctyonema, Dendrograptus, &c.), the
family of the Gyraptolites may be regarded as exclusively
Silurian in its distribution. Not only is this the case, but it
attained its maximum development almost upon its first ap-
pearance, in the Arenig Rocks; and whilst represented by a
great variety of types in the Lower Silurian, it only,exists in
the Upper Silurian in a much diminished form. The Grag-
tolites (Gr. grapho, 1 write; “thos, stone) were so named by
Linnzus, from the resemblance of some of them to written or
pencilled marks upon the stone, though the great naturalist him-
self did not believe them to be true fossils at all) ‘They occur
as linear or leaf-like bodies, sometimes simple, sometimes com-
pound and branched; and no doubt whatever can be enter-
tained as to their being the skeletons of composite organisms,
or colonies of semi-independent animals united together by
a common fleshy trunk, similar to what is observed in the
colonies of the existing Sea-firs (Sertularians). This fleshy
trunk or common stem of the colony was protected by a deli-
cate horny sheath, and it gave origin to the little flower-like
‘“‘polypites,” which constituted the active element of the whole
assemblage. These semi-independent beings were, in turn,
protected each by a little horny cup or cell, directly connected
with the common sheath below, and terminating above in an
opening through which the polypite could protrude its tentacled
head or could again withdraw itself for safety. The entire
skeleton, again, was usually, if not universally, supported by
a delicate horny rod or ‘‘axis,” which appears to have been
hollow, and which often protrudes to a greater or less extent
beyond one or both of the extremities of the actual colony.
The above gives the elementary constitution of any Grafpfo-
/ite, but there are considerable differences as to the manner in
which these elements are arranged and combined. In some
forms the common stem of the colony gives origin to but a
single row of cells on one side. If the common stem is a
simple, straight, or slightly-curved linear body, then we have
the simplest form of Graptolite known (the genus M/onograptus) ;
and it is worthy of note that these simple types do not come
into existence till comparatively late (Llandeilo), and last
nearly to the very close of the Upper Silurian. In other
cases, whilst there is still but a single row of cells, the colony
may consist of two of these simple stems springing from a

THE LOWER SILURIAN PERIOD. IOI

common point, as in the so-called ‘“ twin Graptolites ” (Dzdy-
mograptus, fig. 40). This type is entirely confined to the earlier
portion of the Lower Silu-
rian period (Arenig and
Llandeilo). In other cases,
again, there may be four
of such stems springing
from acentral point (Zer-
ragrapius). Lastly, there
are numerous complex
forms (such as Dichograp-
tus, Loganograptus, &c.) in
which there are eight or
more of these simple bran-
ches, all arising from a
common centre (fig. 39),
which is sometimes fur-
nished with a_ singular
horny disc. ‘These com-
plicated branching forms,
as well as the Zetragrapiz,
are characteristic of the
horizon of the Avenig
# group. Similar forms, of-
&, & ff ten specifically identical,

<> =
<LiT bite
=

1\
gift Cr \

Fig. 39.—Dichograptus octobrachiatus, a branched, “unicellular” Graptolite from
the Skiddaw and Quebec Groups (Arenig). (After Hall.)

are found at this horizon in Wales, in the great series of the
Skiddaw Slates of the north of England, in the Quebec group
in Canada, in equivalent beds in Sweden, and in certain gold-
bearing slates of the same age in Victoria in Australia.

In another great group of Graptolites (including the genera
Diplograptus, Dicranograptus, Climacograptus, &c.) the common
stem of the colony gives origin, over part or the whole of its
length, to wo rows of cells, one on each side (fig. 41). These
double-celled ” Graptolites are highly characteristic of the
Lower Silurian deposits; and, with an exception more appa-

102 HISTORICAL PALAZAONTOLOGY.

rent than real in Bohemia, they are exclusively confined to
strata of Lower Silurian age, and are not known to occur in

Fig. 40.—Central portion of the colony of Didymograptus divaricatus, Upper
Llandeilo, Dumfriesshire. (Original.)

the Upper Silurian. Lastly, there is a group of Graptolites
(Phyllograptus, fig. 42) in which the colony is leaf-like in form,

Fig. 41.—Examples of Diplograptus Fig. 42.—Group of individuals of Phydlo- .
pristzs, showing variations in the appen- gvafptus typus, from the Quebec group of .
dages at the base. Upper Llandeilo, Canada. (After Hall.) One of the four rows f
Dumfriesshire. (Original.) of cells is hidden on the under surface.

and is composed of four rows of cells springing in a cross-like

THE LOWER SILURIAN PERIOD. 103

manner from the common stem. These {UH are highly char-
acteristic of the Arenig group.

The Graptolites are usually found in dark-coloured, often
black shales, which sometimes contain so much carbon as to
become “anthracitic.” ‘They may be simply carbonaceous ;
but they are more commonly converted into iron-pyrites, when
they glitter with the brilliant lustre of silver as they he scattered
on the surface of the rock, fully deserving in their metallic
tracery the name of “written stones.” ‘They constitute one
of the most important groups of Silurian fossils, and are of the
greatest value in determining the precise stratigraphical posi-
tion of the beds in which they occur. They present, however,
special difficulties in their study ; and it is still a moot point as
to their precise position in the zoological scale. ‘The balance
of evidence is in favour of regarding them as an ancient and
peculiar group of the Sea-firs (Hydroid Zoophytes), but some
regard them as belonging rather to the Sea-mosses (/o/yzoa).
Under any circumstances, they cannot be directly compared
either with the ordinary Sea-firs or the ordinary Sea-mosses ;
for these two groups consist of fixed organisms, whereas the
Graptolites were certainly free-floating creatures, living at
large in the open sea. The only Hydroid Zoophytes or Poly-
zoans which have a similar free mode of existence, have either
no skeleton at all, or have hard structures quite unlike the
horny sheaths of the Graptolites.

The second great group of Ccelenterate animals ( Actinozoa)
is represented in the Lower Silurian rocks by numerous
Corals. These, for obvious reasons, are much more abundant
in regions where the Lower Silurian series is largely calcareous
(as in North America) than in districts like Wales, where
limestones are very feebly developed. The Lower Silurian
Corals, though the first of their class, and presenting certain
peculiarities, may be regarded as essentially similar in nature
to existing Corals. These, as is well known, are the calcareous
skeletons of animals —the so-called ‘ Coral - Zoophytes ”—
closely allied to the common Sea-anemones in structure and
habit. A szmple coral (fig. 43) consists of a calcareous cup
embedded in the soft tissues of the flower-like polype, and hav-
ing at its summit a more or less deep depression (the ‘‘calice’’)
in which the digestive organs are contained. The space within
the coral is divided into compartments by numerous vertical
calcareous plates (the “‘ septa”), which spring from the inside
of the wall of the cup, and of which some generally reach the
centre. Compound corals, again (fig. 44), consist of a greater
or less number of structures similar in structure to the above,

104 HISTORICAL PALZONTOLOGY.

but united together in different ways into a common mass.
Simple corals, therefore, are the skeletons of szzg/e and inde-

Fig. 43.— Zaphrentis Stokesi, a simple Fig. 44.—Upper surface of a mass of
“cup-coral,” Upper Silurian, Canada. (After Strombodes pentagonus, Upper Silurian,
Billings.) Canada. (After Billings.)

pendent polypes ; whilst compound corals are the skeletons of
assemblages or colonies of similar polypes, living united with
one another as an organic community.

In the general details of their structure, the Lower Silurian
Corals do not differ from the ordinary Corals of the present
day. The latter, however, have the vertical calcareous plates
of the coral (‘‘septa”) arranged in multiples of six or five;
whereas the former have these structures arranged in multiples
of four, and often showing a cross-like disposition. For this
reason, the common Lower Silurian Corals are separated to
form a distinct group under the name of Augose Corals or
Rugosa. They are further distinguished by the fact that the
cavity of the coral (“ visceral chamber ”) is usually subdivided
by more or less numerous 4orizontal calcareous plates or
partitions, which divide the coral into so many tiers or storeys,
and which are known as the “ tabule” (fig. 45).

In addition to the Rugose Corals, the Lower Silurian rocks
contain a number of curious compound corals, the tubes
of which have either no septa at all or merely rudimentary
ones, but which have the transverse partitions or “ tabule-”
very highly developed. These are known as the Zadbulate
Corals ; and recent researches on some of their existing allies
(such as Helopora) have shown that they are really allied to

THE LOWER SILURIAN PERIOD. 105

the modern Sea-pens, Organ-pipe Corals, and Red Coral,
rather than to the typical stony Corals. Amongst the charac-

im

&

Coal afi

Muy

ss 3
wa

Fig. 45.—Columnaria alveolata, a Rugose compound coral, with imperfect septa, but
having the corallites partitioned off into storeys by ‘“‘tabule.” Lower Silurian, Canada.
(After Billings.)

teristic Rugose Corals of the Lower Silurian may be mentioned
species belonging to the genera Columnarta, Favistella, Strep-
telasma, and Zaphrentis; whilst amongst the ‘“ Tabulate”
Corals, the principal forms belong to the genera Chetetes,
Flalysites (the Chain-coral), Constellaria, and ffeliolites. ‘These
groups of the Corals, however, attain a greater development
at a later period, and they will be noticed more particularly
hereafter.

Passing on to higher animals, we find that the class of the
Echinodermata is represented by examples of the Star-fishes
(Asteroidea), the Sea-lilies (Crinotdea), and the peculiar extinct
group of the Cystideans (Cystozdea), with one or two of the
Brittle-stars (Op/iuroidea)—the Sea-urchins (/chinoidea) being
still wanting. The Crinoids, though in some places extremely
numerous, have not the varied development that they possess
in the Upper Silurian, in connection with which their structure
will be more fully spoken of: In the meanwhile, it is sufficient
to note that many of the calcareous deposits of the Lower
Silurian are strictly entitled to the name of “ Crinoidal lme-
stones,” being composed in great part of the detached joints,
and plates, and broken stems, of these beautiful but fragile
organisms (see fig. 12). Allied to the Crinoids are the singular
creatures which are known as Cystideans (fig. 46). These are
generally composed of a globular or ovate body (the “ calyx”),
supported upon a short stalk (the column”), by which the
organism was usually attached to some foreign body. The
body was enclosed by closely-fitting calcareous plates, accu-

106 HISTORICAL PALZONTOLOGY.

rately jointed together ; and the stem was made up of numerous
distinct pieces or joints, flexibly united to each other by mem-

Fig. 46.—Group of Cystideans. A, Caryocrinus ornatus,* Upper Silurian, America};
B, Pleurocystites squamosus, showing two short ‘‘arms,” Lower Silurian, Canada; C,
Pseudocrinus bifasciatus, Upper Silurian, England ; D, Lepadocrinus Gebhardi, Upper
Silurian, America. (After Hall, Billings, and Salter.)

brane. The chief distinction which strikes one in comparing
the Cystideans with the Crinoids is, that the latter are always
furnished, as will be subsequently seen, with a beautiful crown
of branched and feathery appendages, springing from the sum-
mit of the calyx, and which are composed of innumerable
calcareous plates or joints, and are known as the ‘‘arms.” In
the Cystideans, on the other hand, there are either no “arms”
at all, or merely short, unbranched, rudimentary arms. The
Cystideans are principally, and indeed nearly exclusively,
Silurian fossils; and though occurring in the Upper Silurian
in no small numbers, they are pre-eminently characteristic of
the Llandeilo-Caradoc period of Lower Silurian time. They
commenced their existence, so far as known, in the Upper
Cambrian ; and though examples are not absolutely unknown

* The genus Caryocrinus is sometimes regarded as properly belonging
to the Crznoids, but there seem to be good reasons for rather considering
it as an abnormal form of Cystidean.

THE LOWER SILURIAN PERIOD. 107

in later periods, they are pre-eminently characteristic of the
earlier portion of the Palzeozoic epoch.

The Ringed Worms (Azmelides) are abundantly represented
in the Lower Silurian, but principally by tracks and burrows
similar in essential respects to those which occur so commonly
in the Cambrian formation, and calling for no special com-
ment. Much more important are the Articulate animals, rep-
resented. as heretofore, wholly by the remains of the aquatic

J A
4 \\K\,

s)
))) \
Wy Arid INI uw —S

MLA.

‘
l

=
Seer
SPM
Pa ——
fr HN
TES |
i! WH

Fig. 47.—Lower Silurian Crustaceans. a, Asaphus tyrannus, Upper Llandeilo; 4,
Ozgygia Buchii, Upper Llandeilo; c, Trzxucleus concentricus, Caradoc; d, Caryocaris,
Wrightiz, Arenig (Skiddaw Slates) ; e, Beyrichia complicata, natural size and enlarged,
Upper Llandeilo and Caradoc; 4, Primitia strangulata, Caradoc: g, Head-shield of
Calymene Blumenbachii, var. brevicapitata, Caradoc; h, Head-shield of Triarthrus
Becki (Utica Slates), United States; z, Shield of Leperditia Canadensis, var. Foseph-
zana, of the natural size, Trenton Limestone, Canada; 7, The same, viewed from the
front. (After Salter, M‘Coy, Rupert Jones, and Dana.)

group of the Crustaceans. Amongst these are numerous little
bivalved forms—such as species of Primitia (fig. 47, f), Bey-

108 HISTORICAL PALZONTOLOGY.

richia (fig. 47, e), and Leperditia (fig. 47, ¢ and 7). Most of
these are very small, varying from the size of a pin’s head up
to that of a hemp seed; but they are sometimes as large as
a small bean (fig. 47, z), and they are commonly found in
myriads together in the rock. As before said, they belong to
the same great group as the living Water-fleas (Ostracoda).
Besides these, we find the pod-shaped head-shields of the
shrimp-like Phyllopods—such as Caryocaris (fig. 47, @) and
Ceratiocaris. More important, however, than any of these are
the 7rilobites, which may be considered as attaining their maxi-
mum development in the Lower Silurian. The huge Paradoxides
of the Cambrian have now disappeared, and with them almost
all the principal and characteristic ‘‘ primordial” genera, save
Olenus and Agnostus. In their place we have a great number
of new forms—some of them, like the great Asaphus tyrannus
of the Upper Llandeilo (fig. 47,.@), attaining a length of a foot
or more, and thus hardly yielding in the matter of size to their
ancient rivals. Almost every subdivision of the Lower Silurian
series has its own special and characteristic species of Trilo-
bites ; and the study of these is therefore of great importance
to the geologist. A few widely-dispersed and characteristic
species have been here figured (fig. 47); and the following
may be considered as the principal Lower Silurian genera—
Asaphus, Ogygia, Chetrurus, Ampyx, Calymene, Trinucleus,
Lichas, Illenus, A:glina, Harpes, Remopleurides, Phacops,
Acidaspis, and Homalonotus, a few of them passing upwards
under new forms into the Upper Silurian.

Coming next to the J/o//usca, we find the group of the Sea-
mosses and Sea-mats (Po/yzoa) represented now by quite a
number of forms. Amongst these are examples of the true
Lace-corals (Retepora and Féenestella), with their netted fan-like
or funnel-shaped fronds ; and along with these are numerous
delicate encrusting forms, which grew parasitically attached to
shells and corals (Azppothoa, Alecto, &c.); but perhaps the
most characteristic forms belong to the genus P/z/odictya (figs.
48 and 49). In this group the frond is flattened, with thin
striated edges, sometimes sword-like or scimitar-shaped, but
often more or less branched ; and it consists of two layers of
cells, separated by a delicate membrane, and opening upon
opposite sides. Each of these little chambers or “ cells” was
originally tenanted by a minute animal, and the whole thus
constituted a compound organism or colony.

The Lamp-shells or Brachiopods are so numerous, and pre-
sent such varied types, both in this and the succeeding period
of the Upper Silurian, that the name of ‘“‘ Age of Brachiopods”

THE LOWER SILURIAN PERIOD.

109

has with justice been applied to the Silurian period as a whole.
It would be impossible here to enter into details as to the

Fig. 48.—Ptilodictya falctformis. a,
Small specimen of the natural size; 4,
Cross-section, showing the shape of the
frond ; c, Portion of the surface, enlarged.

Fig. 49.—A, Ptilodictya acuta ; B, Ptzt-
odictya Schaffert. a, Fragment, of the
natural size; 4, Portion, enlarged to show
the cells. Cincinnati Group of Ohio and

Trenton Limestone and Cincinnati Group, Canada. (Original.)

America. (Original.)

many different forms of Brachiopods which present themselves
in the Lower Silurian deposits; but we may select the three
genera Orthis, Strophomena, and Leptena for illustration, as
being specially characteristic of this period, though not exclu-

Fig. 50.—Lower Silurian Brachiopods. a@ and a’, Orthis btforata, Llandeilo-Caradoc,
Britain and America; 4, Orthts flabellulum, Caradoc, Britain; c, Orthis subqguadrata,
Cincinnati Group, America; c’, Interior of the dorsal valve of the same; da, Stropho-

mena deltoidea, Liandeilo-Caradoc, Britain and America. (After Meek, Hall, and

Salter.)

sively confined to it. The numerous shells which belong to

the extensive and cosmopolitan genus Orthis (fig. 50, a, 3, ¢,
9 23

IIo HISTORICAL PALZONTOLOGY.

and fig. 51, ¢ and @), are usually more or less transversely-
oblong or subquadrate, the two valves (as more or less in all

Fig. 51.—Lower Silurian Brachiopods. a, Strophomena alternata, Cincinnati Group,
America ; 6, Strophomena filitexta, Trenton and Cincinnati Groups, America ; c, Orthis
zestudinaria, Caradoc, Europe, and America; d, d@, Orthis plicatella, Cincinnati
Group, America ; ¢, e’, e’, Leptena sericea, Llandeilo and Caradoc, Europe and Ame-
rica. (After Meek, Hall, and the Author.)

the Brachiopods) of unequal sizes, generally more or less con-
vex, and marked with radiating ribs or lines. The valves of
the shell are united to one another by teeth and sockets, and
there is a straight hinge-line. The beaks are also separated
by a distinct space (“‘hinge-area”’), formed in part by each
valve, which is perforated by a triangular opening, through
which, in the living condition, passed a muscular cord attach-
ing the shell to some foreign object. The genus Strophomena
(fig. 50, d, and 51, @ and A) is very like Or¢/zs in general char-
acter ; but the shell is usually much flatter, one or other valve
often being concave, the hinge-line is longer, and the aperture
for the emission of the stalk of attachment 1s partially closed
by a calcareous plate. In Leftena, again (fig. 51, e), the shell
is like Stvophomena in many respects, but generally compara-
tively longer, often completely semicircular, and having one
valve convex and the other valve concave. Amongst other
genera of Brachiopods which are largely represented in the
Lower Silunan rocks may be mentioned Lzngula, Crantza,
Discina, Trematis, Siphonotreta, Acrotreta, Rhynchonella, and
Athyris ; but none of these can claim the importance to which
the three previously-mentioned groups are entitled.

The remaining Lower Silurian groups of A/ollusca can be
but briefly glanced at here. The Bivalves (Lamellibranchiata)
find numerous representatives, belonging to such genera as

THE LOWER SILURIAN PERIOD. ELE

Modiolopsis, Ctenodonta, Orthonota, Palearca, Lyrodesma, Am-
bonychia, and Cleidophorus. ‘The Univalves (Gasteropoda) are
also very numerous, the two most important genera being
Murchisonia (fig. 52) and Plewrotomaria. In both these groups
the outer lip of the shell is notched ; but the shell
in the former is elongated and turreted, whilst in
the latter it is depressed. The curious oceanic
Univalves known as the Heteropods are also very
abundant, the principal forms belonging to Be/-
lerophon and Maclurea. In the former (fig. 53)
there is a symmetrical convoluted shell, like that
of the Pearly Nautilus in shape, but without any
internal partitions, and having the aperture of-
ten expanded and notched behind. The species
of Maclurea (fig. 54) are found both in North
America and in Scotland, and are exclusively
confined to the Lower Silurian period, so far
as known. ‘They have the shell coiled into a
flat spiral, the mouth being furnished with a
very curious, thick, and solid lid or ‘‘ opercu- ee
jum.” The Lower Silurian Preropods, or ‘“‘Wing- Trenton” Lime:
ed Snails,” are numerous, and belong principally UGE Billmee
to the genera Zheca, Conularia, and Tentaculites,
the last-mentioned of these often being extremely abundant in
certain strata.

Lastly, the Lower Silurian Rocks have yielded a vast number

Fig. 53-—Different views of Bellerophon Argo, Trenton Limestone, Canada.
(After Billings.)

of chambered shells, referable to animals which belong to the
same great division as the Cuttle-fishes (the Cephalopoda), and
of which the Pearly Nautilus is the only living representative at
the present day. In this group of Cephalofods the animal
possesses a well-developed external shell, which is divided
into chambers by.shelly partitions (“septa”). The animal
‘lives in the last-formed and largest chamber of the shell, to

112 HISTORICAL PALAJONTOLOGY.

which it is organically connected by muscular attachments.
The head is furnished with long muscular processes or ‘‘ arms,”

Fig. 54.—Different views of Maclurea crenulata, Quebec Group, Newfoundland.
(After Billings.)
and can be protruded from the mouth of the shell at will, or
again withdrawn within it. We learn, also, from the Pearly
Nautilus, that these animals must have possessed two pairs of
breathing organs or “gills ;” hence all these forms are grouped
together under the name of the ‘‘ Tetrabranchiate ” Cephalo-
pods (Gr. ¢etra, four; dragchia, gill). On the other hand, the
ordinary Cuttle-fishes and Calamaries either possess an internal
skeleton, or if they have an external shell, it is not chambered ;
their “arms” are furnished with powerful organs of adhesion
in the form of suckers ; and they possess only a single pair of
gills. For this last reason they are termed the “ Dibranchiate ”
Cephalopods (Gr. ds, twice ; bragchia, gill). No trace of the
true Cuttle-fishes has yet been found in Lower Silurian deposits;
but the Tetrabranchiate group is represented by a great num-
ber of forms, sometimes of great size. The principal Lower
Silurian genus is the well-known and widely-distributed O7tho-
ceras (fig. 55). The shell in this genus agrees with that of the
existing Pearly Nautilus, in consisting of numerous chambers
separated by shelly partitions (or septa), the latter being per-
forated by a tube which runs the whole length of the shell
after the last chamber, and is known as the “siphuncle” (fig.
56, 5). The last chamber formed is the largest, and in it the
animal lives. The chambers behind this are apparently filled
with some gas secreted by the animal itself; and these are sup-
posed to act as a kind of float, enabling the creature to move
with ease under the weight of its shell. The various air-
chambers, though the siphuncle passes through them, have no
direct connection with one another ; and it is believed that the
animal has the power of slightly altering its specific gravity,
and thus of rising or sinking in the water by driving additional
fluid into the siphuncle or partially emptying it. The Ortho-

THE LOWER SILURIAN PERIOD. 113

ceras further agrees with the Pearly Nautilus in the fact that
the partitions or septa separating the different air-chambers are

\\Y

ny \\iy
\,

‘ \
\\\

fy ny \
A

WY) YY

|
i)

<
;
|

|

Fj

Fig. 55.—Fragment of Orthoceras crebri-
septum, Cincinnati Group, North America,

of the natural size. The lower figure is a
section showing the air-chambers, and the

Fig. 56, —Restoration of Orthoceras,
the shell being supposed to be divided ver-
tically, and only its upper part being
shown. a, Arms; /, Muscular tube
(‘‘funnel”) by which water is expelled

form and position of the siphuncle. (After

Billings.) from the mantle-chamber; c, Air-cham-

bers; s, Siphuncle.

simple and smooth, concave in front and convex behind, and
devoid of the elaborate lobation which they exhibit in the
Ammonites ; whilst the siphuncle pierces the septa either in
the centre or near it. In the Nautilus, however, the shell is
coiled into a flat spiral; whereas in Orthoceras the shell is a
straight, longer or shorter cone, tapering behind, and gradu-
ally expanding towards its mouth in front. ‘The chief objec-
tions to the belief that the animal of the Orthoceras was essen-
tially like that of the Pearly Nautilus are—the comparatively
small size of the body-chamber, the often contracted aperture
of the mouth, and the enormous size of some specimens of

* This illustration is taken from a rough sketch made by the author

many years ago, but he is unable to say from what original source it was
copied.

II4 HISTORICAL PALAZONTOLOGY.

the shell. Thus, some Ovrthocerata have been discovered
measuring ten or twelve feet in length, with a diameter of a
foot at the larger extremity. These colossal dimensions cer-
tainly make it difficult to imagine that the comparatively small
body-chamber could have held an animal large enough to move
a load so ponderous as its own shell. To some, this difficulty
has appeared so great that they prefer to believe that the
Orthoceras did not live in its shell at all, but that its shell was
an internal skeleton similar to what we shall find to exist in
many of the true Cuttle-fishes. There is something to be said
in favour of this view, but it would compel us to believe in the
existence in Lower Silurian times of Cuttle-fishes fully equal
in size to the giant “Kraken” of fable. It need only be
added in this connection that the Lower Silurian rocks have
yielded the remains of many other Tetrabranchiate Cephalo-
pods besides Orthoceras. Some of these belong to Cyrtoceras,
which only differs from Orthoceras in the bow-shaped form of
the shell; others belong to Phragmoceras, Lituites, &c. ; and,
lastly, we have true autili, with their spiral shells, closely
resembling the existing Pearly Nautilus.

Whilst all the sub- kingdoms of the Invertebrate animals are
represented in the Lower Silurian rocks, no traces of Verte-
brate animals have ever been discovered in these ancient
deposits, unless the so-called ‘‘ Conodonts”’ found by Pander
in vast numbers in strata of this age * in Russia should prove
to be really of this nature. These problematical bodies are of
microscopic size, and have the form of minute, conical, tooth-
shaped spines, with sharp edges, and hollow at the base.
Their original discoverer regarded them as the horny teeth
of fishes allied to the Lampreys; but Owen came to the con-
clusion that they probably belonged to Invertebrates. The
recent investigation of a vast number of similar but slightly
larger bodies, of very various forms, in the Carboniferous rocks
of Ohio, has led Professor Newberry to the conclusion that
these singular fossils really are,as Pander thought, the teeth of
Cyclostomatous fishes. The whole of this difficult question
has thus been reopened, and we may yet have to record the
first advent of Vertebrate animals in the Lower Silurian.

* According to Pander, the ‘‘Conodonts” are found not only in the

Lower Silurian beds, but also in the ‘‘ Ungulite Grit” (Upper Cambrian),
as well as in the Devonian and Carboniferous deposits of Russia. Should
the Conodonts prove to be truly the remains of fishes, we should thus have
to transfer the first appearance of Vertebrates to, at any rate, as early a
period as the Upper Cambrian,

THE UPPER SILURIAN PERIOD. II5

CEA ARE REX.
TEED UPRER SULORLAN TE RIOD:

Having now treated of the Lower Siiurian period at consider-
able length, it will not be necessary to discuss the succeeding
group of the Upper St/urzan in the same detail—the more so,
as with a general change of sfecies the Upper Silurian animals
belong for the most part to the same great ¢yfes as those which
distinguish the Lower Silurian. As compared, also, as regards
the total bulk of strata concerned, the thickness of the Upper
Silurian is generally very much below that of the Lower Silurian,
indicating that they represent a proportionately shorter period
of time. In considering the general succession of the Upper
Silurian beds, we shall, as before, select Wales and America as
being two regions where these deposits are typically developed.

In Wales and its borders the general succession of the
Upper Silurian rocks may be taken to be as follows, in ascend-
ing order (fig. 57) :—

(1) The base of the Upper Silurian series 1s constituted by
a series of arenaceous beds, to which the name of ‘“‘ May Hill
Sandstone” was applied by Sedgwick. ‘These are succeeded
by a series of greenish-grey or pale-grey slates (“‘ Tarannon
Shales”), sometimes of great thickness ; and these two groups
of beds together form what may be termed the “ A/Zay Ail
Group” (Upper Llandovery of Murchison). ‘Though not very
extensively developed in Britain, this zone 1s one very well
marked by its fossils; and it corresponds with the ‘‘ Clinton
Group” of North America, in which similar fossils occur. In
South Wales this group is clearly unconformable to the highest
member of the subjacent Lower Silurian (the Llandovery group);
and there is reason to believe that a similar, though less con-
spicuous, physical break occurs very generally between the
base of the Upper and the summit of the Lower Silurian.

(2) The Wenlock Group succeeds the May Hull group, and
constitutes the middle member of the Upper Silurian. At its
base it may have an irregular limestone (‘‘Woolhope Lime-
stone”), and its summit may be formed bya similar but thicker
calcareous deposit (“‘Wenlock Limestone”); but the bulk of the
group 1s made up of the argillaceous and shaly strata known as
the ‘ Wenlock Shale.” In North Wales the Wenlock group is
represented by a great accumulation of flaggy and gritty strata
(the “ Denbighshire Flags and Grits”), and similar beds (the

116 HISTORICAL PALZONTOLOGY.

“Coniston Flags” and “ Coniston Grits ”) take the same place
in the north of England.

(3) The Ludlow Group is the highest member of the Upper
Silurian, and consists typically of a lower arenaceous and shaly
series (the “‘Lower Ludlow Rock”) a middle calcareous
member (the ‘ Aymestry Limestone”), and an upper shaly and
sandy series (the ‘‘ Upper Ludlow Rock” and ‘‘ Downton Sand-
stone”). At the summit, or close to the summit, of the Upper
Ludlow, is a singular stratum only a few inches thick (vary-
ing from an inch to a foot), which contains numerous remains
of crustaceans and fishes, and is well known under the name
of the ‘‘bone-bed.” Finally, the Upper Ludlow rock graduates
invariably into a series of red sandy deposits, which, when of
a flaggy character, are known locally as the ‘ Tile-stones.”
These beds are probably to be regarded as the highest member
of the Upper Silurian ; but they are sometimes looked upon as
passage-beds into the Old Red Sandstone, or as the base of
this formation. It is, in fact, apparently impossible to draw
any actual line of demarcation between the Upper Silurian and
the overlying deposits of the Devonian or Old Red Sandstone
series. Both in Britain and in America the Lower Devonian
beds repose with perfect conformity upon the highest Silurian
beds, and the two formations appear to pass into one another
by a gradual and imperceptible transition.

The Upper Silurian strata of Britain vary from perhaps
3000 or 4000 feet in thickness up to 8000 or 10,000 feet. In
North America the corresponding series, though also variable,
is generally of much smaller thickness, and may be under 1000
feet. The general succession of the Upper Silurian deposits
of North America is as follows :—

(1) Medina Sandstone.—This constitutes the base of the
Upper Silurian, and consists of sandy strata, singularly devoid
of life, and passing below in some localities into a conglo-
merate (‘‘ Oneida Conglomerate”), which is stated to contain
pebbles derived from the older beds, and which would thus
indicate an unconformity between the Upper and Lower
Silurian.

(2) Clinton Group.— Above the Medina sandstone are
beds of sandstone and shale, sometimes with calcareous bands,
which constitute what is known as the ‘‘ Clinton Group.” The
Medina and Clinton groups are undoubtedly the equivalent of
the “‘ May Hill Group” of Britain, as shown by the identity of
their fossils.

THE UPPER SILURIAN PERIOD. 117

GENERALISED SECTION OF THE UPPER SILURIAN STRATA
OF WALES AND SHROPSHIRE.

Fig. 57.

{ Base of Old Red Sand-
(jaustone:

S o==. (eoimennpmeweneafesNE [am — | Ti ezstones:

Sc NS y ial RT WES : 4 \

oO EEE

z Upper Ludlow Rock.

5 ——

a Aymestry Limestone.

5

of Lower Ludlow Rock.

: Wenlock Limestone.

4

oe) Wenlock Shale (Denhbigh-
M4 -—-- shire Flags and Grits of
rz) North Wales).

Z

=)

= --=-- Woolhope Limestone.

Tarannon Shales.

Sy a ie oe ee Sean
sence Oe Wi tan Fhe Se — May Hill Sandstone.

Po af By Org OT Eh He On OS”
Qa os ef "Ss se eha® ee? >

MAY-
HILL
GROUP

_|---- Llandovery Rocks.

(3) Miagara Group.—This group consists typically of a
series of argillaceous beds (‘‘ Niagara Shale”) capped by
limestones (‘Niagara Limestone’); and the name of the
group is derived from the fact that it is over limestones of this
age that the Niagara river is precipitated to form the great
Falls. In places the Niagara group is wholly calcareous,
and it is continued upwards into a series of marls and sand-
stones, with beds of salt and masses of gypsum (the “Salina
Group’), or into a series of magnesian limestones (“ Guelph
Limestones”). The Niagara group, as a whole, corresponds
unequivocally with the Wenlock group of Britain.

(4) Lower Helderberg Group.—TVhe Upper Silurian period
in North America was terminated by the deposition of a series
of calcareous beds, which derive the name of ‘‘ Lower Helder-
berg” from the Helderberg mountains, south of Albany, and

118 HISTORICAL PALZONTOLOGY.

which are divided into several zones, capable of recognition by
their fossils, and known by local names (Tentaculite Lime-
stone, Water-lime, Lower Pentamerus Limestone, Delthyris
Shaly Limestone, and Upper Pentamerus Limestone). As a
whole, this series may be regarded as the equivalent of the
Ludlow group of Britain, though it is difficult to establish any
precise parallelism. The summit of the Lower Helderberg
grqup is constituted by a coarse-grained sandstone (the “ Oris-
kany Sandstone”), replete with organic remains, which have
to a large extent a Silurian faces. Opinions differ as to whether
this sandstone is to be regarded as the highest bed of the Upper
Silurian or the base of the Devonian. We thus see that in
America, as in Britain, no other line than an artificial one can be
drawn between the Upper Silurian and the overlying Devonian.

As regards the “/e of the Upper Silurian period, we have, as
before,.a number of so-called ‘‘ Fucoids,” the true vegetable
nature of which is in many instances beyond doubt. In addi-
tion to these, however, we meet for the first time, in deposits
of this age, with the remains of genuine land-plants, though
our knowledge of these is still too scanty to enable us to con-
struct any detailed picture of-the terrestrial vegetation of the
period. Some of these remains indicate the existence of the
remarkable genus Lepidodendron—a genus which played a part
of great importance in the forests of the Devonian and Carbon-
iferous periods, and which may be regarded as a gigantic and
extinct type of the Club-mosses (Lycofodiacee). Near the
summit of-the Ludlow formation in Britain there have also
been found beds charged with numerous small globular bodies,
which Dr Hooker has shown to be the seed-vessels or “ spor-
angia” of Club-mosses. Principal Dawson further states that
he has seen in the same formation fragments of wood with the
structure of the singular Devonian Conifer known as Pvrofo-
taxites. Lastly, the same distinguished observer has described
from the Upper Silurian of North America the remains of the
singular land-plants belonging to the genus Psz/ophyton, which
will be referred to at greater length hereafter.

The marine life of the Upper Silurian is in the main con-
stituted by types of animals similar to those characterising the
Lower Silurian, though for the most part belonging to different
species. The /rofozoans are represented principally by Séro-
matopora and Sschadites, along with a number of undoubted
sponges (such as Amphispongia, Astreospongia, Astylospongia,
and Paleomanon).

Amongst the Celenterates, we find the old group of Grap-
folites now verging on extinction. Individuals still remain

THE UPPER SILURIAN PERIOD: II9

numerous, but the variety of generic and specific types has
now become greatly reduced. All the branching and complex
forms of the Arenig, the twin-Grap-
tolites and Dicranograpti of the
Llandeilo, and the double-celled
Diplograptt and Climacograpti of
the Bala group, have now disap-
peared. In their place we have
the singular Refzolztes, with its curi-
ously-reticulated skeleton; and seve-
ral species of the single-celled genus
Monograptus, of which a character-
istic species (JZ. priodon) is here
figured. If we remove from this
group the plant-like Ductyonema,
which are still present, and which
survive into the Devonian, no
known species of Gvaptolite has
hitherto been detected in strata
higher in geological position than
the Ludlow. This, therefore, pre-
sents us with the first instance we
have as yet met with of the total
disappearance and extinction ofa op og Mee es
great and important series of or- ow, slightly enlarged. B, Frag-
ganic forms. Hoi ie eae conane Oe
The Corals are very numerously viewed in front, showing the mouths
3 : g of the cellules. D, Cross-section
represented in the Upper Silurian of the same. From the Wenlock
Eeks, some of the limestones (sucly (7p Oh nse Ne
as the Wenlock Limestone) being
often largely composed of the skeletons of these animals.
Almost all the known forms of this period belong to the
two great divisions of the Rugose and Tabulate corals, the
former being represented by species of Zaphrentis, Omphyma,
Cystiphyllum, Strombodes, Acervularia, Cyathophylum, &c. ;
whilst the latter belong principally to the genera /avosites,
Chetetes, Halysites, Syringopora, Feliolites, and Plasmopora.
Amongst the Augosa, the first appearance of the great and
important genus Cyathophyllum, so characteristic of the Pale-
ozoic period, is to be noted; and amongst the TZadulata
we have similarly the first appearance, in force at any rate,
of the widely-spread genus Favosites — the ‘‘ Honeycomb-
corals.” The “Chain-corals” (alysites), figured below (fig. 59),
are also very common examples of the Tabulate corals during
this period, though they occur likewise in the Lower Silurian,

=
C)
=

—

SS

SS

120 HISTORICAL PALAONTOLOGY.

Amongst the £c/inodermata, all those orders which have .
hard parts capable of ready preservation are more or less

Fig. 59.—a, Halysites catenularvia, small variety, of the natural size ; 46, Fragment of _
a large variety of the same, of the natural size; c, Fragment of limestone with the tubes
of Halysites agglomerata, of the natural size; d, Vertical section of two tubes of the
same, showing the tabule, enlarged. Niagara Limestone (Wenlock), Canada. (Original.)

largely represented. We have no trace of the Holothurians
or Sea-cucumbers ; but this is not surprising, as the record of
the past is throughout almost silent as to the former existence
of these soft-bodied creatures, the scattered plates and spicules
in their skin offering a very uncertain chance of preservation
in the fossil condition. The Sea-urchins (Zchznoids) are said
to be represented by examples of the old genus Palechinus.
The Star-fishes (Asterotds) and the Brittle-stars (Op/zuroids)
are, comparatively speaking, largely represented; the former
by species of Palasterina (fig. 60), Paleaster (fig. 60), Palgo-
coma (fig. 60), Petraster, Glyptaster, and Lepidaster—and the
latter by species of Protaster (fig. 61), Paleodiscus, Acroura,
and Eucladia. The singular Cystideans, or ‘‘ Globe Crinoids,”
with their globular or ovate, tesselated bodies (fig. 46, A, C, D.),
are also not uncommon in the Upper Silurian ; and if they do.
not become finally extinct here, they certainly survive the close
of this period by but a very brief time. By far the most im-
portant, however, of the Upper Silurian Echinoderms, are the
Sea-lilies or Crinoids. The limestones of this period are often
largely composed of the fragmentary columns and detached

THE UPPER SILURIAN PERIOD. E21

plates of these creatures, and some of them (such as the Wen-
lock Limestone of Dudley) have yielded perhaps the most

Fig. 60.—Upper Silurian Star-fishes. 1, Palasterina primeva, Lower Ludlow ; 2,
PEE ter Feathvend: Lower Ludlow; 3, Paleocoma Colvini, Lower Ludlow. (After
Salter.)

exquisitely-preserved examples of this group with which we
are as yet acquainted. However varied in their forms, these

_ Fig. 61.—A, Protaster Sedgwickii, showing the disc and bases of the arms; B, Por-
tion of an arm, greatly enlarged. Lower Ludlow. (After Salter.)

beautiful organisms consist of a globular, ovate, or pear-shaped
body (the ‘‘ calyx”), supported upon a longer or shorter
jointed stem (or “ column”). The body is covered externally
with an armour of closely-fitting calcareous plates (fig. 62), and
its upper surface is protected by similar but smaller plates
more loosely connected by a leathery integument. From the
upper surface of the body, round its margin, springs a series
of longer or shorter flexible processes, composed of innu-
merable calcareous joints or pieces, movably united with one

122 HISTORICAL PALZONTOLOGY.

another. The arms are typically five in number; but they
generally subdivide at least once, sometimes twice, and they

[

=) )5)
POET
i]
an

MBB
BEIT

P
B

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a
ap
ae
as
Ze
oe
Bs
E|
a
F |

eee aaa

SABER
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TTL TT]
Edit eel

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ts
BS aa

€,

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318 ed

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Fig. 62.—Upper Silurian Crinoids. a, Calyx and arms of Eucalyptocrinus polydacty-
lus, Wenlock Limestone ; 4, Ichthyocrinus levis, Niagara Limestone, America ; ¢,
Taxocrinus tuberculatus, Wenlock Limestone. (After M‘Coy and Hall.)

are furnished with similar but more slender lateral branches
or “ pinnules,” thus giving rise to a crown of delicate feathery
plumes. The ‘ column” is the stem by which the animal is
attached permanently to the bottom of the sea; and it is com-
posed of numerous separate plates, so jointed together that
whilst the amount of movement between any two pieces must
be very limited, the entire column acquires more or less flexi-
bility, allowing the organism as a whole to wave backwards and
forwards on its stalk. Into the exquisite mznutze of structure
by which the innumerable parts entering into the composition
of a single Crinoid are adapted for their proper purposes in
the economy of the animal, it is impossible to enter here. No
period, as before said, has yielded examples of greater beauty
than the Upper Silurian, the principal genera represented
being Cyathocrinus, Platycrinus, Marsupiocrinus, Taxocrinus,
Eucalyptocrinus, Ichthyocrinus, Mariacrinus, Pertechocrinus,
Glyptocrinus, Crotalocrinus, and Edriocrinus.

The tracks and burrows of Azmelides are as abundant in
the Upper Silurian strata as in older deposits, and have just
as commonly been regarded as plants. The most abundant
forms are the cylindrical, twisted bodies (Planolites), which are

THE UPPER SILURIAN PERIOD. 123

so frequently found on the surfaces of sandy beds, and which
have been described as the stems of sea-weeds. These fossils
(fig. 63), however, can be nothing more, in most cases, than

Fig. 63.—P/lanolites vulgaris, the filled-up burrows of a marine worm.
Upper Silurian (Clinton Group), Canada. (Original.)

the filled-up burrows of marine worms resembling the living
Lob-worms. ‘There are also various remains which belong to
the group of the tube-inhabiting Annelides (Zudzcola). Of
this nature are the tubes of Serpulites and Cornulites, and the
little spiral discs of Spzrorbis Lewrszt.

Amongst the Articulates, we still meet only with the remains
of Crustaceans. Besides the little bivalved Ostracoda—which
here are occasionally found of the size of beans—and various
Phyllopods of different kinds, we have an abundance of 77z/o-
bites. These last-mentioned ancient types, however, are now
beginning to show signs of decadence ; and though still indi-
vidually numerous, there is a great diminution in the number
of generic types. Many of the old genera, which flourished
so abundantly in Lower Silurian seas, have now died out;
and the group is represented chiefly by species of Cheirurus,
Encrinurus, Harpes, Proetus, Lichas, Acidaspis, Ilenus, Caly-
mene, Lomalonotus, and Phacops—the last of these, one of the

124 HISTORICAL PALAZONTOLOGY.

highest and most beautiful of the groups of Trilobites, attaining
here its maximum of development. In the annexed illustra-
tion (fig. 64) some of the characteristic Upper Silurian Tnilo-

SBE EU

Fig. 64.—Upper Silurian Trilobites. a, Chezrurus bimuucronatus, Wenlock and Cara-
doc; 4, Phacops longicaudatus, Wenlock, Britain, and America; c, Phacops Downingia,
Wenlock and Ludlow; ad, Harges ungula, Upper Silurian, Bohemia. (After Salter
and Barrande.)

bites are represented—all, however, belonging to genera which
have their commencement in the Lower Silurian period. In
addition to the above, the Ludlow rocks of Britain and the
Lower Helderberg beds of North America have yielded the
remains of certain singular Crustaceans belonging to the
extinct order of the Eusypterida. Some of these wonderful
forms are not remarkable for their size; but others, such as
Prterygotus Anglicus (fig. 65), attain a length of six feet or more,
and may fairly be considered as the giants of their class. The
Eurypterids are most nearly allied to the existing King-crabs
(Zimulti), and have-the anterior end of the body covered with
a great head-shield, carrying two pairs of eyes, the one simple
and the other compound. The feelers are converted into
pincers, whilst the last pair of limbs have their bases covered
with spiny teeth so as to act as jaws, and are flattened and
widened out towards their extremities so as to officiate as
swimming-paddles. The hinder extremity of the body is com-
posed of thirteen rings, which have no legs attached to them ;
and the last segment of the tail is either a flattened plate or a

THE) UPPER SILURIAN PERIOD. 125
narrow, sword-shaped spine. Fragments of the skeleton are
easily recognised by the peculiar scale-like markings with
which the surface is adorned, and
which look not at all unlike the
scales of a fish. The most fam-
ous locality for these great Crus-
taceans is Lesmahagow, in Lan-
arkshire, where many different
species have been found. The
true King-crabs (Zim) of exist-
ing seas also appear to have been
represented by at least one form
(Neolimulus) in the Upper Silu-
rian.

Coming to the JZollusca, we
note the occurrence of the same
great groups as in the Lower
Silurian. Amongst the Sea-
mosses (fo/yzoa), we have the
ancient Lace-corals (/enestella
and efepora), with the nearly-
allied Glauconome, and species of
Ptilodictya (fig. 66) ; whilst many
forms often referred here may

probably have to be transferred
to the Corals, just as some so-
called Corals will ultimately be
removed to the present group.
The Brachiopods continued
to flourish during the Upper
Silurian period in immense num-

Fig.
viewed from the under side, reduced
in size, and restored. cc, The feelers

65. — Pterygotus Anglicus,

(antenne), terminating in nipping-
claws ; 0 0, Eyes; we m, Three pairs of
jointed limbs, with pointed extremi-
ties ; 72 2, Swimming-paddles, the bases
of which are spiny and act as jaws.
Upper Silurian, Lanarkshire. (After

; Henry Woodward.)
bers and under a greatly in-

creased variety of forms. The three prominent Lower
Silurian genera O7this, Strophomena, and Lepiena are still
well represented, though they have lost their former pre-
eminence. Amongst the numerous types which have now
come upon the scene for the first time, or which have now a
special development, are Sfirifera and Pentamerus. In the
first of these (fig. 69, 4, c), one of the valves of the shell (the
dorsal) is furnished in its interior with a pair of great calca-
reous spires, which served for the support of the long and
fringed fleshy processes or “ arms” which were attached to the
sides of the mouth.* In the genus Pentamerus (fig. 70) the

*In all the Lamp-shells the mouth is provided with two long fleshy
organs, which carry delicate filaments on their sides, and which are

10

126 HISTORICAL PALZONTOLOGY.

shell is curiously subdivided in its interior by calcareous
plates. The /entameri commenced their existence at the very

Fig. 66.—Upper Silurian Polyzoa. 1, Fan-shaped frond of RAznopora verrucosa; 1a,
Portion of the surface of the same, enlarged; 2 and 2a, Phenopora ensiformts, of the
natural size and enlarged; 3 and 3a, Helopora fragilis, of the natural size and en-
larged ; 4 and 4a, Ptilodictya rarifora, of the natural size and enlarged. The speci-
mens are all from the Clinton Formation (May Hill Group) of Canada. (Original.)

close of the Lower Silurian (Llandovery), and survived to the
close of the Upper Silurian; but they are specially character-
istic of the May Hill and Wenlock groups, both in Britain
and in other regions. One species, Pentamerus galeatus, is
common to Sweden, Britain, and America. Amongst the
remaining Upper Silurian Brachiopods are the extraordinary

usually coiled into a spiral. These organs are known as the ‘‘arms,”
and it is from their presence that the name of ‘‘ Brachiopoda” is derived
(Gr. drachion, arm ; fodes, feet). In some cases the arms are merely coiled
away within the shell, without any support; but in other cases they are
carried upon a more or less elaborate shelly loop, often spoken of as the
‘*carriage-spring apparatus.” In the Sfz7zfers, and in other ancient
genera, this apparatus is coiled up into a complicated spiral (fig. 67). It

Fig. 67.—Spirifera hysterica. The right-hand figure shows the interior of the
dorsal valve, with the calcareous spires for the support of the arms.

is these “farms,” with or without the supporting loops or spires, which

serve as one of the special characters distinguishing the Arachiopods from
the true Bivalves (Zamellibranchiata).

THE UPPER SILURIAN PERIOD. 127

Trimerelids ; the old and at the same time modern Linguwie,
Discine, and Cranié ; together with many species of Adrypa

Fig. 68.— Upper Silurian Brachiopods. aa’, Leptocelia plano-convexa, Clinton
Group, America; 44’, Rhynchonella neglecta, Clinton Group, America; c, Rhynchonella
cuneata, Niagara Group, America, and Wenlock Group, Britain; d a’, Orthis elegan-
tua, Llandeilo to Ludlow, America and Europe; e e, Atrypfa hemispherica, Clinton
Group, America, and Llandovery and May Hill Groups, Britain ; 7 /’, Atrypa congesta,
Clinton Group, America; ¢ 2’, Orthis Davidsonz, Clinton Group, America. (After Hall,
Billings, and the Author.)

(fig. 68, 2), Leptocelia (fig. 68, a), Rhynchonella (fig. 68, b, c),
Meristella (fig. 69, a, ¢, f), Athyris, ketzta, Chonetes, &c.

ios
\\ \

Yj, iti \
ne

q

Fig. 69.—a, a’ Meristella intermedia, Niagara Group, America; 6, Spirifera Niagar-
ensts, Niagara Group, America; ¢,c’, Spirifera crispa, May Hill to Ludlow, Britain, and
Niagara Group, America ; d, Strophomena (Streptorhynchus) subplana, Niagara Group,
America ; ¢, Meristella naviformis, Niagara Group, America ; 7, Meristella cylindrica,
Niagara Group, America. (After Hall, Billings, and the Author.)

The higher groups of the M/ol/usca are also largely repre-
sented in the Upper Silurian. Apart from some singular types,

128 HISTORICAL PALASONTOLOGY.

such as the huge and thick-shelled M/egalomi of the American
Wenlock formation, the Bivalves (Lameliibranchiata) present

Fig. 70.—Pentamerus Knightit. Wenlock and Ludlow. The right-hand
figure shows the internal partitions of the shell.

little of special interest ; for though sufficiently numerous, they
are rarely well preserved, and their true affinities are often un-
certain. Amongst the most characteristic genera of this period
may be mentioned Cardioda (fig. 71, A and C) and Prerinea (fig.

Fig. 71.—Upper Silurian Bivalves. A, Cardiola interrupta, Wenlock and Ludlow;
B, Pterinea subfalcata, Wenlock; C, Cardiola fibrosa, Ludlow. (After Salter and
M ‘Coy.)

71, B), though the latter survives to a much later date. The
Univalves (Gastervopoda) are very numerous, and a few charac-
teristic forms are here figured (fig. 72). Of these, no genus
is perhaps more characteristic than Luwomphalus (fig. 72, 4),
with its flat discoidal shell, coiled up into an oblique spiral,
and deeply hollowed out on one side; but examples of this
group are both of older and of more modern date. Another
very extensive genus, especially in America, is Platyceras (fig.
72, a and /), with its thin fragile shell—often hardly coiled up
at all—its minute spire, and its widely-expanded, often sinuated
mouth. The British Acroculie should probably be placed
here, and the group has with reason been regarded as allied
to the Violet-snails (/anthina) of the open Atlantic. The

THE UPPER SILURIAN PERIOD. 129

species of Platyostoma (fig. 72, %) also belong to the same
family ; and the entire group is continued throughout the
Devonian into the Carboniferous. Amongst other well-known
Upper Silurian Gasteropods are species of the genera Holopea

Fig. 72.—Upper Silurian Gasteropods. a, Platyceras ventricosum, Lower Helder-
berg, America; 4, Exomphalus discors, Wenlock, Britain; c, Holopella obsoleta, Lud-
low, Britain; d, Platyschisma helicites, Upper Ludlow, Britain; e, Holopella gractlior,
Wenlock, Britain; 4, Platyceras multisinuatum, Lower Helderberg, America; g, Holo-
pea subconica, Lower Helderberg, America; , h', Platyostoma Niagarense, Niagara
Group, America. (After Hall, M‘Coy, and Salter.)

(fig. 72, g), Holopella (fig. 72, ¢), Platyschisma (fig. 72, 2),
Cyclonema, Pleurotomaria, Murchisonia, Trochonema, &c. ‘The
oceanic Univalves (eteropods) are rep-
resented mainly by species of Lellero-
phon ; and the Winged Snails, or Prero-
pods, can still boast of the gigantic Thece
and Conulari@, which characterise yet
older deposits. The commonest genus
of Preropoda, however, is Tentaculites (fig.
73), which clearly belongs here, though
it has commonly been regarded as the
tube of an Annelide. The shell in this
group is a conical tube, usually adorned
with prominent transverse rings, and Fig Reeth eA
often with finer transverse or longitudi- furopeand North America,
nal striz as well; and many beds of the

Upper Silurian exhibit myriads of such tubes scattered promis-
cuously over their surfaces.

130 HISTORICAL PALAZONTOLOGY.

The last and highest group of the J/o//usca—that of the
Cephalopoda —is still represented only by TZéerabranchiate
forms; but the abundance and variety of these is almost
beyond belief. Many hundreds of different species are known,
chiefly belonging to the straight Orthoceratites, but the slightly-
curved Cyrtoceras is only little less common. There are also
numerous forms of the genera Phragmoceras, Ascoceras, Gyro-
ceras, Lituites, and Nautilus. Here, also, are the first-known
species of the genus Goniatites—a group which attains con-
siderable importance in later deposits, and which is to be
regarded as the precursor of the Ammonites of the Secondary
period.

Finally, we find ourselves for the first time called upon to
consider the remains of undoubted vertebrate animals, in the
form of fishes. ‘The oldest of these remains, so far as yet
known, are found in the Lower Ludlow rocks, and they con-
sist of the bony head-shields or bucklers
of certain singular armoured fishes belong-
ing to the group of the Gazozds, repre-
sented at the present day by the Stur-
geons, the Gar-pikes of North America,
and a few other less familiar forms. The
principal Upper Silurian genus of these is
Fteraspis, and the annexed illustration (fig.
74) will give some idea of the extraordi-
nary form of the shield covering the head
in these ancient fishes. ‘The remarkable

Fig. 74.—Head-shield stratum near the top of the Ludlow for-
er en “<i mation known as the “bone-bed” has
Murchison.) also yielded the remains of shark-hke

fishes. Some of these, for which the name
of Onchus has been proposed, are in the form of com-
pressed, slightly-curved spines (fig. 75, A), which would appear

Fig. 75.—A, Spine of Oxchus tenuistriatus ; B, Shagreen-scales of Thelodus. Both
from the “‘ bone-bed” of the Upper Ludlow rocks. (After Murchison.)

to be of the nature of the strong defensive spines implanted
in front of certain of the fins in many living fishes. Besides
these, have been found fragments of prickly skin or shagreen
(Sphagodus), along with minute cushion-shaped bodies ( Zhe/o-

THE UPPER SILURIAN PERIOD. _ 131

dus, fig. 75, B), which are doubtless the bony scales of some
fish resembling the modern Dog-fishes. As the above mentioned
remains belong to two distinct, and at the same time highly-
organised, groups of the fishes, it is hardly lkely that we are
really presented here with the first examples of this great class.
On the contrary, whether the so-called ‘“ Conodonts” should
prove to be the teeth of fishes or not, we are- justified in ex-
pecting that unequivocal remains of this group of animals will
still be found in the Lower Silurian. It is interesting, also, to
note that the first appearance of fishes—the lowest class of
vertebrate animals—so far as known to us at present, does not
take place until after all the great sub-kingdoms of invertebrates
have been long in existence ; and there is no reason for think-
ing that future discoveries will materially affect the veladzve
order of succession thus indicated.

LITERATURE.

From the vast and daily-increasing mass of Silurian literature, it is im-
possible to do more than select a small number of works which have a
classical and historical interest to the English-speaking geologist, or which
embody researches on special groups of Silurian animals—anything like an
enumeration of all the works and papers on this subject being wholly out
of the question. Apart, therefore, from numerous and in many cases
extremely important memoirs, by various well-known observers, both at
home and abroad, the following are some of the more weighty works to
which the student may refer in investigating the physical characters and
succession of the Silurian strata and their fossil contents :—

(1) ‘Siluria.? Sir Roderick Murchison.

(2) ‘Geology of Russia in Europe.’ Murchison (with M. de Verneuil

and Count von Keyserling).

(3) ‘ Bassin Silurien de Bohéme Centrale.’ Barrande.

(4) ‘ Introduction to the Catalogue of British Palaeozoic Fossils in the

Woodwardian Museum of Cambridge.’ Sedgwick.

(5) ‘Die Urwelt Russlands.’ Eichwald.

6) ‘ Report on the Geology of Londonderry, Tyrone,’ &c. Portlock.

(7) “‘Geology of North Wales” —‘ Mem. Geol. Survey of Great Britain,’

vol. ii. Ramsay.

(8) ‘ Geology of Canada,’ 1863, Sir W. E. Logan; and the ‘ Reports of

Progress of the Geological Survey’ since 1863.

(9) ‘ Memoirs of the Geological Survey of Great Britain.’

(10) ‘ Reports of the Geological Surveys of the States of New York,
Illinois, Ohio, Iowa, Michigan, Vermont, Wisconsin, Minne-
sota,’ &c. By Emmons, Hall, Worthen, Meek, Newberry,
Orton, Winchell, Dale Owen, &c.

(11) ‘ Thesaurus Siluricus.’ Bigsby.

(12) ‘ British Palzeozoic Fossils.’ M‘Coy.

(13) ‘ Synopsis of the Silurian Fossils of Ireland,’ M‘Coy.

(14) ‘‘ Appendix to the Geology of North Wales rit Mon Geol. Survey,’
vol. iii, Salter.

—

132 HISTORICAL PALAONTOLOGY.

(15) ‘ Catalogue of the Cambrian and Silurian Fossils in the Woodward-
ian Museum of Cambridge.’ Salter.
(16) ‘ Characteristic British Fossils.’ Baily.
(17) ‘ Catalogue of British Fossils.” Morris.
(18) ‘ Palzeozoic Fossils of Canada.’ Billings.
(19) ‘ Decades of the Geological Survey of Canada.’ Billings, Salter,
Rupert Jones. .
(20) ‘ Decades of the Geological Survey of Great Britain.’ Salter, Edward
Forbes.
(21) ‘ Paleontology of New York,’ vols. i.-iii. Hall.
(22) ‘ Paleontology of Illinois.’ Meek and Worthen.
(23) ‘ Paleontology of Ohio.” Meek, Hall, Whitfield, Nicholson.
(24) ‘Silurian Fauna of West Tennessee’ (Silurische Fauna des WeS&t-
lichen Tennessee). Ferdinand Reemer.
(25) ‘ Reports on the State Cabinet of New York.’ Hall.
) ‘ Lethza Geognostica.’ Bronn.
) ‘Index Paleontologicus.’ Bronn.
(28) ‘ Lethea Rossica.’? Eichwald.
)
)

‘ Lethzea Suecica.’ Hisinger.

(30) ‘ Paleeontologica Suecica.’ Angelin.

(31) ‘ Petrefacta Germaniz.’ Goldfuss.

(32) ‘ Versteinerungen der Grauwacken-Formation in Sachsen.’ Geinitz.
(33) ‘ Organisation of Trilobites’ (Ray Society). Burmeister.

(34) ‘Monograph of the British Trilobites’ (Palzeontographical Society).

Salter.

(35) ‘Monograph of the British Merostomata’ ( Palzeontographical Society).
Henry Woodward.

(36) Monograph of British Brachiopoda’ (Palzontographical Society).
Thomas Davidson.

(37) ‘ Graptolites of the Quebec Group.’ James Hall.

(38) ‘ Monograph of the British Graptolitidz.’ Nicholson.

(39) ‘Monographs on the Trilobites, Pteropods, Cephalopods, Grapto-
lites,’ &c. Extracted from the ‘Systeme Silurien du Centre de
la Bohéme.’ Barrande.

(40) ‘ Polypiers Fossiles des Terrains Paleozoiques,’ and ‘ Monograph of

the British Corals’ (Palzontographical Society). Milne Ed-
wards and Jules Haime.

CALA PA HE Ra ext:

THE DEVONIAN AND OLD RED SANDSTONE
PERIOD:

Between the summit of the Ludlow formation and the strata
which are universally admitted to belong to the Carboniferous

©

-
'
a %

DEVONIAN AND OLD RED PERIOD. B'S

series is a great system of deposits, to which the narne of “‘ Old
Red Sandstone” was originally applied, to distinguish them
from certain arenaceous strata which lie above the coal (“‘ New
Red Sandstone”). The Old Red Sandstone, properly so
called, was originally described and investigated as occurring
in Scotland and in South Wales and its borders; and similar
strata occur in the south of Ireland. Subsequently it was
discovered that sediments of a different mineral nature, and
containing different organic remains, intervened between the
Silurian and the Carboniferous rocks on the continent of Eu-
rope, and strata with similar paleontological characters to these
were found occupying a considerable area in Devonshire. The
name of ‘‘ Devonian” was applied to these deposits ; and this
title, by common usage, has come to be regarded as synony-
mous with the name of “Old Red Sandstone.” Lastly, a
magnificent series of deposits, containing marine fossils, and
undoubtedly equivalent to the true “Devonian” of Devon-
shire, Rhenish Prussia, Belgium, and France, is found to inter-
vene in North America between the summit of the Silurian
and the base of the Carboniferous rocks.

Much difficulty has been felt in correlating the true ‘‘ Devon-
ian Rocks” with the typical “Old Red Sandstone”—this diffi-
culty arising from the fact that though both formations are
fossiliferous, the peculiar fossils of each have only been rarely
and partially found associated together. The characteristic
crustaceans and many of the characteristic fishes of the Old
Red are wanting in the Devonian; whilst the corals and
marine shells of the latter do not occur inthe former. It is
impossible here to enter into any discussion as to the merits
of the controversy to which this difficulty has given origin.
' No one, however, can doubt the importance and reality of the
Devonian series as an independent system of rocks to be in-
tercalated in point of time between the Silurian and the Car-
boniferous. The want of agreement, both lithologically and
palzontologically, between the Devonian and the Old Red,
can be explained by ‘supposing that these two formations,
though wholly or in great part contemporaneous, and therefore
strict equivalents, represent deposits in two different geographi-
cal areas, laid down under different conditions. On this view,
the typical Devonian rocks of Europe, Britain, and North
America are the deep-sea deposits of the Devonian period, or,
at any rate, are genuine marine sediments formed far from
land. On the other hand, the “‘Old Red Sandstone” of
Britain and the corresponding ‘‘Gaspé Group” of Eastern

134 HISTORICAL PALZONTOLOGY.

Canada represent the shallow-water shore-deposits of the same
period. In fact, the former of these last-mentioned de-
posits contains no fossils which can be asserted positively
to be marine (unless the Eurypterids be considered so) ; and
it is even conceivable that it represents the sediments of an
inland sea. Accepting this explanation in the meanwhile,
we may very briefly consider the general succession of the
deposits of this period in Scotland, in Devonshire, and in
North America.

In Scotland the “Old Red” forms a great series of arena-
ceous and conglomeratic strata, attaining a thickness of many
thousands of feet, and divisible into three groups. Of these,
the Lower Old Red Sandstone reposes with perfect conform-
ity upon the highest beds of the Upper Silurian, the two for-
mations being almost inseparably united by an intermediate
series of “ passage-beds.”” In mineral nature this group con-
sists principally of massive conglomerates, sandstones, shales,
and concretionary limestones ; and its fossils consist chiefly of
large crustaceans belonging to the family of the Auryfrerids,
fishes, and plants. The J/ddle Old Red Sandstone consists of
flagstones, bituminous shales, and conglomerates, sometimes
with irregular calcareous bands ; and its fossils are principally
fishes and plants. It may be wholly wanting, when the Upger
Old Red seems to repose unconformably upon the lower divi-
sion of the series. The Upper Old Red Sandstone consists of
conglomerates and grits, along with a great series of red and
yellow sandstones—the fossils, as before, being fishes and re-
mains of plants. The Upper Old Red graduates -upwards
conformably into the Carboniferous series.

The Devonian rocks of Devonshire are likewise divisible
into a lower, middle, and upper division. The Lower
Devonian or Lynton Group consists of red and purple sand-
stones, with marine fossils, corresponding to the ‘‘Spirifer
Sandstein ” of Germany, and to the arenaceous deposits (Scho-
harie and Cauda-Galli Grits) at the base of the American
Devonian. The A@ddle Devonian or Lifracombe Group consists
of sandstones and flags, with calcareous slates and crystalline
limestones, containing many corals. It corresponds with the
great “Eifel Limestone” of the Continent, and, in a general
way, with the Corniferous Limestone and Hamilton group of
North America. The Upper Devonian or Filton Group, lastly,
consists of sandstones and calcareous shales which correspond
with the “‘Clymenia Limestone” and “ Cypridina Shales” of
the Continent, and with the Chemung and Portage groups of

DEVONIAN AND OLD RED PERIOD. 135

North America. It seems quite possible, also, that the so-
called ‘Carboniferous Slates” of Ireland correspond with
this group, and that the former would be more properly re-
garded as forming the summit of the Devonian than the
base of the Carboniferous.

In no country in the world, probably, is there a finer

or more complete exposition of the strata intervening be-
tween the Silurian and Carboniferous deposits than in the
United States. The following are the main subdivisions
of the Devonian rocks in the State of New York, where
the series may be regarded as being typically developed
fig. 67) :—
4) Cauda-Galli Grit and Schoharie Grit.—Considering the
“Oriskany Sandstone” as the summit of the Upper Silurian,
the base of the Devonian is constituted by the arenaceous
deposits known by the above names, which rest quite conform-
ably upon the Silurian, and which represent the Lower
Devonian of Devonshire.~ The Cauda-Galli Grit is so called
from the abundance of a peculiar spiral fossil (Spzrophyton
cauda-Galli), which is of common occurrence in the Carbon-
iferous rocks of Britain, and is supposed to be the remains
of a sea-weed.

(2) The Cornzferous or Upper Helderberg Limestone. — A
series of limestones usually charged with considerabie quan-
tities of siliceous matter in the shape of hornstone or chert
(Lat. cornu, horn). The thickness of this group rarely exceeds
300 feet; but it is replete with fossils, more especially with
the remains of corals. The Corniferous Limestone is the
equivalent of the coral-bearing limestones of the Middle De-
vonian of Devonshire and the great ‘‘ Eifel Limestone” of
Germany.

(3) The Hamilton Group—consisting of shales at the base
(‘Marcellus shales”); flags, shales, and impure limestones
(‘Hamilton beds”) in the middle; and again a series of shales
(“Genesee Slates”) at the top. The thickness of this group
varies from 200 to 1200 feet, and it is richly charged with
marine fossils.

(4) The Portage Group.—A great series of shales, flags, and
shaly sandstones, with few fossils.

(5) The Chemung Group.—Another great series of sand-
stones and shales, but with many fossils. The Portage and
Chemung groups may be regarded as corresponding with the
Upper Devonian of Devonshire. The Chemung beds are
succeeded by a great series of red sandstones and shales—the

136 HISTORICAL PALAEONTOLOGY.

“ Catskill Group”—which pass conformably upwards into the
Carboniferous, and which may perhaps be regarded as the
equivalent of the great sandstones of the Upper Old Red in
Scotland.

Throughout the entire series of Devonian deposits in North
America no unconformability or physical break of any kind
has hitherto been detected ; nor is there any marked interrup-
tion to the current of life, though each subdivision of the series
has its own fossils. No completely natural line can thus be
indicated, dividing the Devonian in this region from the Silu-
rian on the one hand, and the Carboniferous on the other
hand. At the same time, there is the most ample evidence,
both stratigraphical and paleontological, as to the complete
independence of the American Devonian series as a distinct
life-system between the older Silurian and the later Carbon-
iferous. The subjoined section (fig. 76) shows diagrammati-
cally the general succession of the Devonian rocks of North
America.

As regards the “fe of the Devonian period, we are now
acquainted with a large and abundant terrestrial #4ova—this
being the first time that we have met with a land vegetation
capable of reconstruction in any fulness. By the researches
of Goeppert, Unger, Dawson, Carruthers, and other botanists,
a knowledge has been acquired of a large number of Devonian
plants, only a few of which can be noticed here. As might
have been anticipated, the greater number of the vegetable
remains of this period have been obtained from such shallow-
water deposits as the Old Red Sandstone proper and the Gaspé
series of North America, and few traces of plant-life occur in
the strictly marine sediments. Apart from numerous remains,
mostly of a problematical nature, referred to the comprehensive
group of the Sea-weeds, a large number of Ferns have now
been recognised, some being of the ordinary plant-like type
(Pecopteris, Neuropteris, Alethopteris, Sphenopteris, &c.), whilst
others belong to the gigantic group of the “ Tree - ferns”
(Psaronius, Caulopteris, &c.) Besides these there is an abun-
dant development of the singular extinct types of the Lepzdo-
dendrowds, the Sigillarioids, and the Calamites, all of which
attained their maximum in the Carboniferous. Of these, the
Lepidodendra may be regarded as gigantic, tree-like Club-mosses
(Lycopodiacee) ; the Calamites are equally gigantic Horse-tails
(Equisetacee); and the Sigillarioids, equally huge in size, in
some respects hold a position intermediate between the Club-
mosses and the Pines (Conifers). The Devonian rocks have

.

DEVONIAN AND OLD RED PERIOD. 37:

GENERALISED SECTION OF THE DEVONIAN ROCKS OF
NortH AMERICA,

Sy SORE Rah edges Gy tate Catskill Group.

——— eS —— - Chemung Group.

UPPER DEVONIAN.
Or
e
}

Portage Group.

Z
<
Z 3
O Hamilton Group.
> 3
x
Q
<2}
4
5 ° °
= Corniferous Limestone.
—
qa Te | ER | a ee |
: (EST | | | |
2 & Schoharie Grit.
ie
= PS. er r25 PEP "Se. [ener } :
BO. Wiser eo ee eee Cauda-Galli Grit.
> : :
‘ 2 09 89 0 9D VG BY Ufn----- Oriskany Sandstone.
=

Lower Helderberg.

also yielded traces of many other plants (such as Annularia,
Asterophyllites, Cardiocarpon, &c.), which acquire a greater pre-
dominance in the Carboniferous period, and which will be
spoken of in discussing the structure of the plants of the Coal-
measures. Upon the whole, the one plant which may be con-
sidered as specially characteristic of the Devonian (though not
confined to this series) is the Pszophyton (fig. 77) of Dr Daw-
son. These singular plants have slender branching stems,
with sparse needle-shaped leaves, the young stems being at
first coiled up, crosier-fashion, like the young fronds of ferns,
whilst the old branches carry numerous spore-cases. The

138 - HISTORICAL PALAZONTOLOGY.

stems and branches seem to have attained a height of two or
three feet; and they sprang from prostrate “root-stocks” or
creeping stems. Upon the whole,
Principal Dawson is disposed to
regard Pszlophyton as a ‘ general-
ised type” of plants intermediate
between the Ferns and the Club-
mosses. Lastly, the Devonian de-
posits have yielded the remains of
the first actual ¢vees with which we
are as yet acquainted. About.the
nature of some of these (Ormoxylon
and Dadoxylon) no doubt can be
entertained, since their trunks not
only show the concentric nngs of
growth characteristic of exogen-
ous trees in general, but their
woody tissue exhibits under the
microscope the ‘‘ discs” which are
characteristic of the wood of the
Pines and Firs (see fig. 2). The

i j } singular genus LPrototaxites, how-
A 1 | ever, which occurs in an older por-
Y WY tion of the Devonian series than
| | Jz the above, is not in an absolutely

i / unchallenged position. By Prin-
\ ae cipal Dawson it is regarded as the
\ / trunk of an ancient Conzfer—the

\\
i
Via
SSS

most ancient known; but Mr
Carruthers regards it as more pro-
bably the stem of a gigantic sea-
weed. The trunks of Prototaxites
my (fig. 78, A) vary from one to three
CURCEUD AY! feet in diameter, and exhibit con-
iene _ centric rings of growth; but its
Bea ee ee &2 woody fibres have not hitherto
ada. (After Dawson.) been clearly demonstrated to pos-
sess discs. Before leaving the

Devonian vegetation, it may be mentioned that the hornstone
or chert so abundant in the Corniferous limestone of North
America has been shown to contain the remains of various
microscopic plants (Dzatoms and Desmids). We find also in
the same siliceous material the singular spherical bodies, with
radiating spines, whith occur so abundantly in the chalk flints,
and which are termed Xanthidia. ‘These may be regarded

DEVONIAN AND OLD RED PERIOD. 139

as probably the spore-cases of the minute plants known as
Desmidia.

WHY

\ AN \.
i x
WW
; os :

SAN Wy
XQ S WSN XS

Fig 78.—A, Trunk of Prototaxites Logani, eighteen inches in diameter, as seen in the
cliff near L’Anse Brehaut, Gaspé; B, Two wood-cells showing spiral fibres and obscure
pores, highly magnified. Lower Devonian, Canada. (After Dawson.)

The Devonian Protozoans have still to be fully investigat-
ed. True Sponges (such as Astreospongia, Spherospongia,
&c.) are not unknown; but by far the commonest repre-
sentatives of this sub-kingdom in the Devonian strata are
Stromatopora and its allies. These singular organisms (fig.
79) are not only very abundant in some of the Devonian lime-
stones—both in the Old World and the New—but they often
attain very large dimensions. However much they may differ
in minor details, the general structure of these bodies is that
of numerous, concentrically-arranged, thin, calcareous lamine,
separated by narrow interspaces, which in turn are crossed by
numerous delicate vertical pillars, giving the whole mass a
cellular structure, and dividing it into innumerable minute
quadrangular compartments. Many of the Devonian Stromato-
pore also exhibit on their surface the rounded openings of
canals, which can hardly have served any other purpose than
that of permitting the sea-water to gain ready access to every
part of the organism.

No true Graptolites have ever been detected in strata of

I40 HISTORICAL PALAZZONTOLOGY.

Devonian age; and the whole of this group has become ex-
tinguished—unless we refer here the still surviving Dictyonema.

Fig. 79.—a@, Part of the under surface of Stromatofora tuberculata, showing the
wrinkled basement membrane and the openings of water-canals, of the natural size; 4,
Portion of the upper surface of the same, enlarged ; c, Vertical section ofa fragment, mag-
nified to show the internal structure. Corniferous Limestone, Canada. (Oniginal.)

The Celenterates, however, are represented by a vast number

of Corals, of beautiful forms and very varied types. The
marbles of Devonshire, the Devonian limestones of the Eifel
and of France, and the calcareous strata of the Corniferous
and Hamilton groups of America, are often replete with the
skeletons of these organisms—so much so as to sometimes
entitle the rock to be considered as representing an ancient
coral-reef. In some instances the Corals have preserved their
primitive calcareous composition ; and: if they are embedded
in soft shales, they may weather out of the rock in almost all
their original perfection. In other cases, as in the marbles of
Devonshire, the matrix is so compact and crystalline that the
included corals can only be satisfactorily studied by means of
polished sections. In other cases, again, the corals have been
more or less completely converted into flint, as in the Cornifer-
ous limestone of North America. When this is the case, they
often come, by the action of the weather, to stand out from

~
;

DEVONIAN AND OLD RED PERIOD. I4fi

the enclosing rock in the boldest relief, exhibiting to the ob-
server the most minute details of their organisation. As before,

Fig. 81.—Zaphrentis cornicula, of the
natural size. Devonian, America, (Ori-
ginal.)

Fig. 80.— Cystiphyllum vesiculosum,
showing a succession of cups produced by

budding from the original coral. Of the Fig. 82.—Heliophyllum exiguumt, view-
natural size. Devonian, America and ed from in front and behind. Of the natu-
Europe. (Original.) ral size. Devonian, Canada. (Original.)

the principal representatives of the Corals are still referable to

the groups of the Rugosa and Tabulata. Amongst the Rugose

group we find a vast number of simple “‘ cup-corals,” generally

known by the quarrymen as “horns,” from their shape. Of
11

142 HISTORICAL PALAONTOLOGY.

the many forms of these, the species of Cyathophyllum, Helio-
phylum (fig. 82), Zaphrentis (fig. 81), and Cystiphyllum (fig. 80),
are perhaps those most abundantly represented—none of these
genera, however, except Ae/iophyllum, being peculiar to the
Devonian period. There are also numerous compound Ru-
_gose corals, such as species of Eridophyllum, Diphyphyl-
lum, Syringopora, Phillipsastrea, and some of the forms of
Cyathophyllum and Crepidophyllum (fig. 83). Some of these
compound corals attain a very large size, and form of them-

Fig. 83.—Portion of a mass of Crepidophyllum Archiact, of the natural size.
Hamilton Formation, Canada. (After Billings.)

selves regular beds, which have an analogy, at any rate, with
existing coral-reefs, though there are grounds for believing that
these ancient types differed from the modern reef-builders in
being inhabitants of deep water. The “‘Tabulate Corals” are
hardly less abundant in the Devonian rocks than the Augosa ;
and being invariably compound, they hardly yield to the latter
in the dimensions of the aggregations which they sometimes
form.

The commonest, and at the same time the largest, of these
are the ‘‘ honeycomb corals,” forming the genus /avosites
(figs. 84, 85), which derive both their vernacular and their
technical names from their great likeness to masses of petrified
honeycomb. The most abundant species are Favosites Goth-
landica and F. hemispherica, both here figured, which form
masses sometimes not less than two or three feet in diameter.
Whilst Favosites has acquired a popular name by its honey-
combed appearance, the resemblance of A/ichelinia to a fossil-

DEVONIAN AND OLD RED PERIOD. 143

ised wasp’s nest with the comb exposed is hardly less strik-
ing, and has earned for it a similar recognition from the

Senetteutsoates
eatcecacensseecess

aa5 socal ittaes
ESS AEH EES eT L280)
taseeeseninuersiristacwscegee
Oo a2,
RB 256 |
HHH HRA
aaterscensseteticy ety

Fig. 84.—Portion of amass of Favo- Fig. 85.—Fragment of Favesztes hemt-
sites Gothlandica, of the natural size. spherica, of the natural size. Upper Silu-
Upper Silurian and Devonian of Europe rian and Devonian of America. (After
and America. (Original.) Billings.)

non-scientific public. In addition to these, there are numer-
ous branching or plant-like Tabulate Corals, often of the most
graceful form, which are distinctive of the Devonian in all
parts of the world.

The L£chinoderms of the Devonian period call for little
special notice. Many of the Devonian limestones are “‘crin-
oidal ;” and the Crznozds are the most abundant and widely-
distributed representatives of their class in the deposits of
this period.

The Cystideans, with doubtful exceptions, have not been
recognised in the Devonian ; and their place is taken by the
allied group of the “‘ Pentremites,” which will be further spoken
of as occurring in the Carboniferous rocks. On the other hand,
the Star-fishes, Brittle-stars, and Sea-urchins are all continued
by types more or less closely allied to those of the preceding
Upper Silurian.

Of the remains of Ringed-worms (Anmnelides), the most numer-
ous and the most interesting are the calcareous envelopes of
some small tube-inhabiting species. No one who has visited
the seaside can have failed to notice the little spiral tubes of
the existing Spzrorbzs growing attached to shells, or covering
the fronds of the commoner Sea-weeds (especially Fucus ser-
ratus). ‘These tubes are inhabited by a small Annelide, and
structures of a similar character occur not uncommonly from
the Upper Silurian upwards. In the Devonian rocks, Sfz7r-
orbis 1s an extremely common fossil, growing in hundreds
attached to the outer surface of corals and shells, and appearing

144 HISTORICAL PALAONTOLOGY.

in many specific forms (figs. 86 and 87); but almost all the
known examples are of small size, and are liable to escape a

Fig. 87.—a, Spivorbis omphalodes, natural size
and enlarged, Devonian, Europe and America;
b, Spirorbis Arkonensis, of the natural size and
enlarged ; c, The same, with the tube twisted in
the reverse direction. Devonian, America. (Ori-
ginal.)

Fig. 88.—a 6, Spirorbis laxus, enlarged, Upper
Silurian, America; c, Spirorbis spinulifera, of the
natural size and enlarged, Devonian, Canada. (Af-
ter Hall and the Author.)

cursory examination.
The Crustaceans of
the Devonian are prin-
cipally Zurypterids and
Trilobites. Some of the
former attain gigantic
dimensions, and the
quarrymen intheScotch
Old Red give them the
name of “ seraphim,”
from their singular
scale-like ornamenta-
tion. The Z7rilobites,
though still sufficiently
abundant in some local-
ities, have undergone a
yet further diminution
since the close of the
Upper Silurian. In both
America and Europe
quite a number of gen-

eric types have survived from the Silurian, but few or no new
ones make their appearance during this period in either the Old

Fig. 88.—Devonian Trilobites. a, Phacops latifrons, Devonian of Britain, the Conti-
nent of Europe, and South America; 4, Homalonotus armatus, Europe; c, Phacops
(Trimerocephalus) levis, Europe; d@, Head-shield of Phacops (Portlockia) granulatus,

Europe. (After Salter and Burmeister.)

World orthe New. The sfecies, however, are distinct ; and the

2}

DEVONIAN AND OLD RED PERIOD. 145

principal forms belong to the genera Phacops (fig. 88, a, ¢, @),
Flomalonotus (fig. 88, 4), Proetus, and Bronteus. The species
figured above under the name of Phacops latifrons (fig. 88, a),
has an almost world-wide distribution, being found in the
Devonian of Britain, Belgium, France, Germany, Russia, Spain,
and South America ; whilst its place is taken in North Ame-
rica by the closely-allied Phacops rana. In addition to the
Trilobites, the Devonian deposits have yielded the remains of
a number of the minute Ostracoda, such as Entomis (“ Cypri-
dina”), Leperditia, &c., which sometimes occur in vast num-
bers, as in the so-called “ Cypridina Slates” of the German
Devonian. There are also a few forms of Phyllopods (Es-
theria). Taken as a whole, the Crustacean fauna of the
Devonian period presents many alliances with that of the
Upper Silurian, but has only slight relationships with that of
the Lower Carboniferous.

Besides Crustaceans, we meet here for the first time with
the remains of air-breathing Articulates, in the shape of Lnsects.
So far, these have only been obtained from the Devonian
rocks of North America, and they indicate the existence of at
least four generic types, all more or less allied to the existing
May-flies (Zphemeride). One of these interesting primitive
insects, namely, Platephemera antiqua (fig. 89), appears to have
measured five inches in ex-.
panse of wing ; and another AS TY
(Xenoneura antiquorum) has ‘
attached to its wing the re “& ESS
mains of a “stridulating- |
organ ” similar to that pos-
sessed by the modern Grass-
hoppers—the instrument, as
Principal Dawson remarks,
of “the first music of living
Game that Geology as yet. * "pasar aeuue Ake Dewey
reveals to us.”

Amongst the AZo//usca, the Devonian rocks have yielded a
great number of the remains of Sea-mosses (Polyzoa). Some
of these belong to the ancient type Prlodictya, which seems to
disappear here, or to the allied Clathropora (fig. 90), with its
fenestrated and reticulated fronds. We meet also with the
graceful and delicate stems of Cerzopora (fig. 91).

The majority of the Devonian Polyzoa belong, however, to
the great and important Palzozoic group of the Lace- corals
(Fenestella, figs. 92 and 94, Retefora, fig. 93, Polypora, and
their allies). In all these forms there is a horny skeleton, of a

146 HISTORICAL PALAZONTOLOGY.

fan-like or funnel-shaped form, which grew attached by its
base to some foreign body. The frond consists of slightly-

Fig. or. — Fragment of
Ceriopora Hamiltonensis, of
the natural size and enlarg-

Fig. 90.—Fragment of Clathropora intertexta, of the ed. Devonian, Canada. (On-
natural! size and enlarged. Devonian, Canada. (Original.) ginal.)

diverging or nearly parallel branches, which are either united
by delicate cross-bars, or which bend alternately from side to
side, and become directly united with one another at short
intervals—in either case giving origin to numerous oval or

Bee we Sees
rere

SEAS a ew oo ah

>.
=?

see
Se eeeranees®

a
oy

Fig. o93.—Fragment of Retepora
Phillipsi, of the natural size and
enlarged. Devonian, Canada. (Ori-
ginal.)

Fig. 92.—Fragment of Fenestella magnifica, Fig. o4.—Fragment of Fenxestella
of the natural size and enlarged. Devonian, c¢vzbrvosa, of the natural size and enlarg-
Canada. (Original.) ed. Devonian, Canada. (Original.)

oblong perforations, which communicate to the whole plant-
like colony a characteristic netted and lace-like appearance.
On one of its surfaces—sometimes the internal, sometimes the
external—the frond carries a number of minute chambers or

ig

DEVONIAN AND OLD RED PERIOD. | 147

“cells,” which are generally borne in rows on the branches, -
and of which each originally contained a minute animal.

The Srachiopods still continue to be represented in great
force through all the Devonian deposits, though not occurring
in the true Old Red Sandstone. Besides such old types as
Orthis, Strophomena, Lingula, Athyris, and Rhynchonella, we
find some entirely new ones; whilst various types which only
commenced their existence in the Upper Silurian, now under-
go a great expansion and development. This last is especially
the case with the two families of the Spzrzferide and the Pro-
ductide. ‘The Sfirifers, in particular, are especially character-
istic of the Devonian, both in the Old and New Worlds—some
of the most typical forms, such as Spzrifera mucronata (fig. 96),
having the shell ‘‘ winged,” or with the lateral angles prolonged

Fig. 95. — Spirifera : Bi : 2
sculptilis. Devonian, Ca- Fig. 96.—Spirifera mucronata. Devonian, America.

nada. (After Billings.) (After Billings.)

to such an extent as to have earned for them the popular name
of ‘‘fossil-butterflies.” The closely-allied Spirifera disjuncta
occurs in Britain, France, Spain, Belgium, Germany, Russia,
and China. The family of the Productide commenced to exist
in the Upper Silurian, in the genus Chonefes; and we shall
heieafter find it culminating in the Carboniferous in many
forms of the great genus Producta* itself. In the Devonian
period, there is an intermediate state of things, the genus
Chonetes being continued in new and varied types, and the
Carboniferous Producte being represented by many forms of
the allied group Productella. Amongst other well-known De-
vonian Brachiopods may be mentioned the two long-lived and
persistent types Atrypa reticularis (fig. 97) and Strophomena
rhomboidalis (fig. 98). The former of these commences in the
Upper Silurian, but is more abundantly developed in the De-
vonian, having a geographical range that is nothing less than
world-wide; whilst the latter commences in the Lower Silurian,

* The name of this genus is often written Productus, just as Spirifera
is often given in the masculine gender as Sfzvifer (the name originally given
to it). The masculine termination to these names is, however, grammati-
cally incorrect, as the feminine noun cochlea (shell) is in these cases under-

stood,

148 _ HISTORICAL PALEONTOLOGY.

and, with an almost equally cosmopolitan range, survives into
the Carboniferous period.

—

“Fig. 97.—Atrvyfa reticularis. Upper Silurian and Devonian o
and America. (After Billings.)

urope

The Bivalves (Zamellibranchiata) of the Devonian call for
no special comment, the genera Prerinea and Megalodon being,

Hts
aennne

jaw

Wy

Uy yi;

Vip ) i

Y)

Yj

Yj

Zy
BY

Fig. 98.—Strophomena rhomboidaiis. Lower Silurian, Upper Silurian, and
Devonian of Europe and America.

perhaps, the most noticeable. The Univalves (Gasteropods),
also, need not be discussed in detail, though many interesting
forms of this group are known. The type most abundantly
represented, especially in America, is VPlatyceras (fig. 99),
comprising thin, wide-
mouthed shells, probably
most nearly allied to the
existing ‘‘Bonnet-limpets,”
and sometimes attaining
very considerable dimen-
sions. We may also note
the continuance of the
genus Luomphalus, with
Fig. 99.—Different views of Platyceras du- ts discoidal spiral shell.
ey ee Devonian, Canada. Amongst fhe Heteropods,
the survival of Bellerophon

is to be recorded ; and in the “‘ Winged-snails,” or Preropods, we
find new forms of the old genera Zentaculites and Conularia

DEVONIAN AND OLD RED PERIOD. 149

(fig. 100). The latter, with its fragile, conical, and often beauti-
fully ornamented shell, is especially noticeable.
The remains of Cephalopoda are far from uncommon in the

Devonian deposits, all the known forms
being still Tetrabranchiate. Besides the
ancient types Orthoceras and Cyrtoceras,
we have now a predominance of the
spirally-coiled chambered shells of Goze-
atites and Clymenia. In the former of
these the shell is shaped like that of the
Nautilus ; but the partitions between the
chambers (“septa”) are more or less
lobed, folded, or angulated, and the
‘“‘siphuncle” runs along the Jack or con-
vex side of the shell—these being char-
acters which approximate Gowzatites to
the true Ammonites of the later rocks.
In Clymenia, on the other hand, whilst
the shell (fig. ror) is coiled into a flat
spiral, and the partitions or septa are
simple or only slightly lobed, there is still

Fig. 100.—Conularia or-
nata, of the natural size.
Devonian, Europe.

this difference, as compared with the /Vautilus, that the tube of
the siphuncle is placed on the zzmer or concave side of the

Fig. 101.—Clymenia Sedgwickiz. Devonian, Europe.

shell, The species of Clymenia are exclusively Devonian in

I50 HISTORICAL PALAEONTOLOGY.

their range; and some of the limestones of this period in ©
Germany are so richly charged with fossils of this genus as to
have received the name of “‘ Clymenien-kalk.”

The sub-kingdom of the Vertebrates is still represented by
Fishes only ; but these are so abundant, and belong to such
varied types, that the Devonian period has been appropriately
called the “‘ Age of Fishes.”’ Amongst the existing fishes there
are three great groups which are of special geological import-
ance, as being more or less extensively represented in past time.
These groups are: (1) The Bony Fishes ( Téeleostei), comprising
most existing fishes, in which the skeleton is more or less com-
pletely converted into bone; the tail is symmetrically lobed or
divided into equal moieties; and the scales are usually thin,
horny, flexible plates, which overlap one another to a greater
or less extent. (2) The Ganoid Fishes (Ganoidei), comprising
the modern Gar-pikes, Sturgeons, &c., in which the skeleton
usually more or less completely retains its primitive soft and
cartilaginous condition ; the tail is generally markedly unsym-
metrical, being divided into two unequal lobes ; and the scales
(when present) have the form of plates of bone, usually cov-
ered by a layer of shining enamel. These scales may overlap ;
or they may be rhomboidal plates, placed edge to edge in
oblique rows ; or they have the form of large-sized bony plates,
which are commonly united in the region of the head to form
a regular buckler. (3) The Placoid Fishes, or Elasmobranchit,
comprising the Sharks, Rays, and Chimere of the present day,
in which the skeleton is cartilaginous ; the tail is unsymmetri-
cally lobed; and the scales have the form of detached bony
plates of variable size, scattered in the integument.

It is to the two last of these groups that the Devonian fishes
belong, and they are more specially referable to the Ganozds.
The order of the Ganoid fishes at the present day comprises
but some seven or eight genera, the species of which princi-
pally or exclusively inhabit fresh waters, and all of which are
confined to the northern hemisphere. As compared, there-
fore, with the Bony fishes, which constitute the great majority
of existing forms, the Ganoids form but an extremely small and
limited group. It was far otherwise, however, in Devonian
times. At this period, the bony fishes are not known to have
come into existence at all, and the Ganoids held almost undis-
puted possession of the waters. To what extent the Devonian
Ganoids were confined to fresh waters remains yet to be proved ;
and that many of them lived in the sea is certain. It was
formerly supposed that the Old Red Sandstone of Scotland
and Ireland, with its abundant fish-remains, might perhaps be
a fresh-water deposit, since the habitat of its fishes is uncer-

’

DEVONIAN AND OLD RED PERIOD. I51

tain, and it contains no indubitable marine fossils. It has
been now shown, however, that the marine Devonian strata of
Devonshire and the continent of Europe contain some of the
most characteristic of the Old Red Sandstone fishes of Scot-
land ; whilst the undoubted marine deposit of the Corniferous
limestone of North America contains numerous shark-like and
Ganoid fishes, including such a characteristic Old Red genus
as Coccosteus. There can be little doubt, therefore, but that the
majority of the Devonian fishes were truly marine in their habits,
though it is probable that many of them lived in shallow water,
in the immediate neighbourhood of the shore, or in estuaries.
The Devonian Ganoids belong to a number of groups ; and

{| Kon) Fa ain} i | fi :
ie tig
toe
es ae fi iia
ia oie Mi
i h Hi he bin ly:
rae

ms
==-——s—

iy

WY
Wi Vy

Yf

mM

' it
lay ast
TWA |()n|4 AA
Wilh) it
h i, HE ,
HY I
SHG LA Hula

Fig. 102.—Fishes of the Devonian rocks of America. a, Diagram of the jaws and teeth
of Dinichthys Hertzeri, viewed from the front, and greatly reduced ; 4, Diagram of the
skull of Macropetalichthys Sullivanti, reduced in size; c, A portion of the enamelled sur-
face of the skull of the same, magnified ; d, One of the scales of Onychodus sigmoides, of
the natural size ; 2, One of the front teeth of the lower jaw of the same, of the natural size ;/,
Fin-spine of Machzracanthus major, ashark-like fish, reduced insize. (After Newberry.)

it is only possible to notice a few of the most important forms
here. The modern group of the Sturgeons is represented,

152 HISTORICAL PALZONTOLOGY.

more or less remotely, by a few Devonian fishes—such as As-
terosteus ; and the great Macropetalichthys of the Corniferous
limestone of North America is believed by Newberry to belong
to this group. In this fish (fig. 102, 4) the skull was of large
size, its outer surface being covered with a tuberculated en-
amel ; and, as in the existing Sturgeons, the mouth seems to
have been wholly destitute of teeth. Somewhat allied, also, to
the Sturgeons, is a singular group of armoured fishes, which is
highly characteristic of the Devonian of Britain and Europe,
and less so of that of America. In these curious forms the
head and front extremity of the body were protected by a
buckler composed of large enamelled plates, more or less
firmly united to one another ; whilst the hinder end of the body ©
was naked, or was protected with small scales. Some forms of
this group—such as Freraspis and Coccosteus—date from the
Upper Silurian; but they attain their maximum in the Devo-
nian, and none of them are known to pass upwards into the
overlying Carboniferous rocks. Amongst the most character-
istic forms of this group may be mentioned Cephalaspis (fig.
103) and Prerichthys (fig. 104). In the former of these the

Fig. 103.—Cefphalaspis Lyellit. Old Red Sandstone, Scotland. (After Page.)

head-shield is of a crescentic shape, having its hinder angles
produced backwards into long “ horns,” giving it the shape of
a “‘saddler’s knife.” No teeth have been discovered ; but the
body was covered with small ganoid scales, and there was an
unsymmetrical tail-fin. In Prerichthys—which, like the preced-
ing, was first brought to light by the labours of Hugh Miller—
the whole of the head and the front part of the body were de-
fended by a buckler of firmly-united enamelled plates, whilst
the rest of the body was covered with small scales. The form
of the “pectoral fins” was quite unique—these having the
shape of two long, curved spines, somewhat like wings, covered
by finely-tuberculated ganoid plates, All the preceding forms

DEVONIAN AND OLD RED PERIOD. 153

of this group are of small size ; but few fishes, living or extinct,
could rival the proportions of the great Dzwzchthys, referred to

Fig. 104.—Pterichthys cornutus. Old Red Sandstone, Scotland. (After Agassiz.)

this family by Newberry. In this huge fish (fig. 102, a) the
head alone is over three feet in length, and the body is sup-
posed to have been twenty-five or thirty feet long. The head
was protected by a massive cuirass of bony plates firmly articu-
lated together, but the hinder end of the body seems to have
been simply enveloped in a leathery skin. ‘The teeth are of
the most formidable description, consisting in both jaws of
serrated dental plates behind, and in front of enormous coni-
cal tusks (fig. 102, a). Though immensely larger, the teeth of .
Dinichthys present a curious resemblance to those of the exist-
ing Mud-fishes (Lepzdoszren).

In another great group of Devonian Ganoids, we meet with
fishes more or less closely allied to the living Polypteri (fig.
105) of the Nile and Senegal. In this group (fig. 106) the
pectoral fins consist of a central scaly lobe carrying the fin-
rays on both sides, the scales being sometimes rounded and
overlapping (fig. 106), or more commonly rhomboidal and
placed edge to edge (fig. 105, A). Numerous forms of these
“ Fringe-finned” Ganoids occur in the Devonian strata, such
as Holoptychius, Glyptolemus, Osteolepis, Phaneropleuron, &c.
To this group is also to be ascribed the huge Oxychodus (fig.
102, @ and é), with its large, rounded, overlapping scales, an
inch in diameter, and its powerful pointed teeth. It is to be
remembered; however, that some of these “ Fringe- finned ”
Ganoids are probably referable to the small but singular group
of the ‘‘ Mud-fishes” (Dzpzoz), represented at the present day
by the singular LZepzdosiren of South America and Africa, and
the Ceratodus of the rivers of Queensland.

Leaving the Ganoid fishes, it still remains to be noticed that
the Devonian deposits have yielded the remains of a number
of fishes more or less closely allied to the existing Sharks,

154 HISTORICAL PALEONTOLOGY.

Rays, and Chimere (the Elasmobranchii). The majority of
the forms here alluded to are allied not to the true Sharks and

SS

Le,

SS

=

ee.

=

Fig. 105.—A, Polypterus, a recent Ganoid fish; B, Osteolepis, a Devonian Ganoid ;
@ a, Pectoral fins, showing the fin-rays arranged round a central lobe.

Dog-fishes, but to the more peaceable “ Port Jackson Sharks,”
with their blunt teeth, adapted for crushing the shells of Mol-
luscs. ‘The collective name of ‘“ Cestracionts” is applied to
these; and we have evidence of their past existence in the

Fig. 106.—Holoptychius nobilissimus, restored. Old Red Sandstone, Scotland.
A, Scale of the same.

Devonian seas both by their teeth, and by the defensive spines
which were implanted in front of a greater or less number of
the fins. These are bony spines, often variously grooved,
serrated, or ornamented, with hollow bases, implanted in the
integument, and capable of being erected or depressed at will.

DEVONIAN AND OLD RED PERIOD. 155

Many of these “ fin-spines” have been preserved to us in the
fossil condition, and the Devonian rocks have yielded examples
belonging to many genera. As some of the true Sharks and
Dog-fishes, some of the Ganoids, and even some Bony Fishes,
possess similar defences, it is often a matter of some uncer-
tainty to what group a given spine is to be referred. One of
these spines, belonging to the genus MZacheracanthus, from the
Devonian rocks of America, has been figured in a peda
illustration (fig. 102, /).

In conclusion, a very few words may be said as to the
validity of the Devonian series as an independent system of
rocks, preserving in its successive strata the record of an
independent system of life. Some high authorities have been
inclined to the view that the Devonian formation has in nature
no actual existence, but that it is made up partly of beds
which should be referred to the summit of the Upper Silurian,
and partly of beds which properly belong to the base of the
Carboniferous. ‘This view seems to have been arrived at in
consequence of a too exclusive study of the Devonian series
of the British Isles, where the physical succession is not wholly
clear, and where there is a striking discrepancy between the
organic remains of those two members of the series which are
known as the “Old Red Sandstone” and the “ Devonian”
rocks proper. This discrepancy, however, is not complete ;
and, as we have seen, can be readily explained on the sup-
position that the one group of rocks presents us with the
shallow water and littoral deposits of the period, while in the
other we are introduced to the deep-sea accumulations of the
same period. Nor can the problem at issue be solved by an
appeal to the phenomena of the British area alone, be the
testimony of these what it may. As a matter of fact, there is
at present no sufficient ground for believing that there is any
irreconcilable discordance between the succession of rocks
and of life in Britain during the period which elapsed between
the deposition of the Upper Ludlow and the formation of the
Carboniferous Limestone, and the order of the same phe-
nomena during the same period in other regions. Some of
the Devonian types of life, as is the case with all great forma-
tions, have descended unchanged from older types; others
pass upwards unchanged to the succeeding period: but the
fauna and flora of the Devonian period are, as a whole, quite
distinct from those of the preceding Silurian or the succeeding
Carboniferous ; and they correspond to an equally distinct
rock-system, which in point of time holds an intermediate
position between the two great groups just mentioned. As

156 HISTORICAL PALZONTOLOGY.

before remarked, this conclusion may be regarded as _ suffi-
ciently proved even by the phenomena of the British area ;
but it may be said to be rendered a certainty by the study of
the Devonian deposits of the continent of Europe—or, still
more, by the investigation of the vast, for the most part un-
interrupted and continuous series of sediments which com-
menced to be laid down in North America at the beginning of
the Upper Silurian, and did not cease till, at any rate, the close
of the Carboniferous.

LITERATURE.

The following list comprises the more important works and memoirs to

which the student of Devonian rocks and fossils may refer :—

(1) ‘Siluria.? Sir Roderick Murchison.

(2) ‘Geology of Russia in Europe.’ Murchison (together with De
Verneuil and Count von Keyserling).

(3) ‘‘Classification of the Older Rocks of Devon and Cornwall”—‘ Proc.
Geol. Soc.,’ vol. ii1., 1839. Sedgwick and Murchison.

(4) ‘* On the Physical Structure of Devonshire ;” and on the ‘ Classifi-
cation of the Older Stratified Rocks of Devonshire and Cornwall”
—‘ Trans. Geol. Soc.,’ vol. v., 1840. Sedgwick and Murchison.

(5) ‘‘ On the Distribution and Classification of the Older or Palzeozoic
Rocks of North Germany and Belgium”—‘ Geol. Trans.,’ 2d ser.,
vol. vi., 1842. Sedgwick and Murchison.

(6) ‘Report on the Geology of Cornwall, Devon, and West Somerset.’
De la Beche.

(7) ‘Memoirs of the Geological Survey of Ireland and Scotland.’
Jukes and Geikie.

(8) *‘On the Carboniferous Slate (or Devonian Rocks) and the Old
Red Sandstone of South Ireland and North Devon ”’—‘ Quart.
Journ. Geol. Soc.,’ vol. xxii. Jukes.

(9) ‘* On the Physical Structure of West Somerset and North Devon;”’
and on the ‘‘ Palzeontological Value of Devonian Fossils” —‘ Quart.
Journ. Geol. Soc.,’ vol. iii. Etheridge.

(10) ‘*On the Connection of the Lower, Middle, and Upper Old Red
Sandstone of Scotland” —‘Trans. Edin. Geol. Soc.,’ vol. i. part il.
Powrie.

(11) ‘The Old Red Sandstone,’ ‘The Testimony of the Rocks,’ and
‘ Footprints of the Creator.’ Hugh Miller.

(12) ‘* Report on the 4th Geological District”—‘ Geology of New York,’
vol. iv. James Hall.

(13) ‘Geology of Canada,’ 1863. Sir W. E. Logan.

(14) ‘ Acadian Geology.’ Dawson.

(15) ‘ Manual of Geology.’ Dana.

(16) ‘Geological Survey of Ohio,’ vol. i.

(17) ‘ Geological Survey of Illinois,’ vol. i.

(18) ‘ Paleozoic Fossils of Cornwall, Devon, and West Somerset.’ ~
Phillips.

(19) ‘ Recherches sur les Poissons Fossiles.” Agassiz.

(20) ‘ Poissons de l’Old Red.’ Agassiz.

(21) ‘* On the Classification of Devonian Fishes””—‘ Mem. Geol. Survey
of Great Britain,’ Decade X. Huxley.

~~

THE CARBONIFEROUS PERIOD. 157

(22) ‘Monograph of the Fishes of the Old Red Sandstone of Britain’
(Palzeontographical Society). Powrie and Lankester.

(23) ‘Fishes of the Devonian System, Palzontology of Ohio.’ New-
benty:

(24) ‘ Meescaph of British Trilobites’ (Palzeontographical Society).
Salter.

(25) ‘ Monograph of British Merostomata’ (Palzeontographical Society).
Henry Woodward.

(26) ‘ Monograph of British Brachiopoda’ (Paleeontographical Society).
Davidson.

(27) ‘ Monograph of British Fossil Corals’ (Paleeontographical Society).
Milne-Edwards and Haime.

(28) ‘Polypiers Foss. des Terrains Paléozoiques.’ Milne-Edwards
and Jules Haime.

(29) ‘* Devonian Fossils of Canada West ”—‘ Canadian Journal,’ new ser.,
vols. iv.-vi. Billings.

(30) ‘ Paleontology of New York,’ vol. iv. James Hall.

(31) ‘ Thirteenth, Fifteenth, and Twenty-third Annual Reports on the
State Cabinet.’ James Hall.

(32) ‘ Paleozoic Fossils of Canada,’ vol. ii. Billings.

(33) ‘Reports on the Palzeontology of the Province of Ontario for 1874
and 1875.’ Nicholson.

(34) ‘* The Fossil Plants of the Devonian and Upper Silurian Formations
of Canada”—‘ Geol. Survey of Canada.’ Dawson.

(35) ‘ Petrefacta Germaniz.’ Goldfuss.

(36) ‘ Versteinerungen der Grauwacken-formation,’ &c. Geinitz.

(37) ‘ Beitrag zur Palzontologie des Thiiringer-Waldes.’ Richter and
Unger.

(38) ‘ Weber die Placodermen der Devonischen System.’ Pander.

(39) ‘ Die Gattungen der Fossilen Pflanzen.’ Gceppert.

(40) ‘ Genera et Species Plantarum Fossilium.’ Unger.

CEVA PAE Reet:

THE CARBONIFEROUS PERIOD.

Overlying the Devonian formation is the great and import-
ant series of the Carboniferous Rocks, so called because workable
beds of coal are more commonly and more largely developed
in this formation than in any other. Workable coal-seams,
however, occur in various other formations (Jurassic, Cretace-
ous, Tertiary), so that coal is not an exclusively Carboniferous
product ; whilst even in the Coal-measures themselves the coal
bears but a very small proportion to the total thickness of
strata, occurring only in comparatively thin beds intercalated
in a great series of sandstones, shales, and other genuine
aqueous sediments.

12

158 HISTORICAL PALAAONTOLOGY.

Stratigraphically, the Carboniferous rocks usually repose
conformably upon the highest Devonian beds, so that the line
of demarcation between the Carboniferous and Devonian for-
mations is principally a paleontological one, founded on the
observed differences in the fossils of the two groups. On the
other hand, the close of the Carboniferous period seems to
have been generally, though not universally, signalised by
movements of the crust of the earth, so that the succeeding
Permian beds often lie unconformably upon the Carboniferous
sediments.

Strata of Carboniferous age have been discovered in almost
every large land-area which has been sufficiently investigated ;
but they are especially largely developed in Britain, in various
parts of the continent of Europe, and in North America.
Their general composition, however, is, comparatively speak-
ing, so uniform, that it will suffice to take a comprehensive
view of the formation without considering any one area in
detail, though in each region the subdivisions of the formation
are known by distinctive local names. ‘Taking such a com-
prehensive view, it is found that the Carboniferous series is
generally divisible into a Lower and essentially calcareous
group (the ‘‘ Sub-Carboniferous” or ‘Carboniferous Lime-
stone”); a Middle and principally arenaceous group (the
“Millstone Grit”); and an Upper group, of alternating shales
and sandstones, with workable seams of coal (the “ Coal-
measures ”),

I. The Carboniferous, Sub-Carboniferous, or Mountain Lime-
stone Series constitutes the general base of the Carboniferous
system. As typically developed in Britain, the Carboniferous
Limestone is essentially a calcareous formation, sometimes
consisting of a mass of nearly pure limestone from Iooo to
2000 feet in thickness, or at other times of successive great
beds of limestone with subordinate sandstones and shales.
In the north of England the base of the series consists of
pebbly conglomerates and coarse sandstones; and in Scot-
land generally, the group is composed of massive sandstones
with a comparatively feeble development of the calcareous
element. In Ireland, again, the base of the Carboniferous
Limestone is usually considered.to be formed by a locally-
developed group of grits and shales (the ‘‘ Coomhola Grits”
and ‘‘ Carboniferous Slate”), which attain the thickness of
about 5000 feet, and contain an intermixture of Devonian
with Carboniferous types of fossils. Seeing that the Devonian
formation is generally conformable to the Carboniferous, we
need feel no surprise at this intermixture of forms ; nor does it

THE CARBONIFEROUS PERIOD. 159

appear to be of great moment whether these strata be referred
to the former or to the latter series. Perhaps the most satis-
factory course is to regard the Coomhola Grits and Carbon-
iferous Slates as ‘‘ passage-beds” between the Devonian and
Carboniferous; but any view that may be taken as to the
position of these beds, really leaves unaffected the integrity
of the Devonian series as a distinct life-system, which, on the
whole, is more closely allied to the Silurian than to the Car-
boniferous. In North America, lastly, the Sub-Carboniferous
series is never purely calcareous, though in the interior of the
continent it becomes mainly so. In other regions, however,
it consists principally of shales and sandstones, with subor-
dinate beds of limestone, and sometimes with thin beds of
coal or deposits of clay-ironstone.

Il. Zhe Millstone Grit.—The highest beds of the Carbon-
iferous Limestone series are succeeded, generally with perfect
conformity, by a series of arenaceous beds, usually known as
the Afil/stone Grit. As typically developed in Britain, this
group consists of hard quartzose sandstones, often so large-
grained and coarse in texture as to properly constitute fine
conglomerates. In other cases there are regular conglomer-
ates, sometimes with shales, limestones, and thin beds of coal—
the thickness of the whole series, when well developed, varying
from 1000 to 5000 feet. In North America, the Millstone
Grit rarely reaches 1000 feet in thickness ; and, like its Brit-
ish equivalent, consists of coarse sandstones and grits, some-
times with regular conglomerates. Whilst the Carboniferous
Limestone was undoubtedly deposited in a tranquil ocean
of considerable depth, the coarse mechanical sediments of
the Millstone Grit indicate the progressive shallowing of
the Carboniferous seas, and the consequent supervention
of shore-conditions.

III. Zhe Coal-measures—The Coal-measures properly so
called rest conformably upon the Millstone Grit, and usually
consist of a vast series of sandstones, shales, grits, and coals,
sometimes with beds of limestone, attaining in some regions a
total thickness of from 7000 to nearly 14,000 feet. Beds of
workable coal are by no means unknown in some areas in the
inferior group of the Sub-Carboniferous; but the general state-
ment is true, that coal is mostly obtained from the true Coal-
measures—the largest known, and at present most produc-
tive coal-fields of the world being in Great Britain, North
America, and Belgium. Wherever they are found, with
limited exceptions, the Coal- measures present a singular
general uniformity of mineral composition. They consist,

160 HISTORICAL PALAONTOLOGY.

namely, of an indefinite alternation of beds of sandstone,
shale, and coal, sometimes with bands of clay-ironstone or beds
of limestone, repeated in no constant order, but sometimes
attaining the enormous aggregate thickness of 14,000 feet, or
little short of 3 miles. The beds of coal differ in number and
thickness in different areas, but they seldom or never exceed
one-fiftieth part of the total bulk of the formation in thickness.
The characters of the coal itself, and the way in which the
coal-beds were deposited, will be briefly alluded to in speaking
of the vegetable life of the period. In Britain, and in the Old
World generally, the Coal-measures are composed partly of
genuine terrestrial deposits—such as the coal—and partly of
sediments accumulated in the fresh or brackish waters of vast
lagoons, estuaries, and marshes. The fossils of the Coal-
measures in these regions are therefore necessarily the remains
either of terrestrial plants and animals, or of such forms of
life as inhabit fresh or brackish waters, the occurrence of strata
with marine fossils being quite a local and occasional phe-
nomenon. In various parts of North America, on the other
hand, the Coal-measures, in addition to sandstones, shales,
coal-seams, and bands of clay-ironstone, commonly include
beds of limestone, charged with marine remains, and indicating
marine conditions. The subjoined section (fig. 107) gives, in
a generalised form, the succession of the Carboniferous strata
in such a British area as the north of England, where the series
is developed in a typical form.

As regards the /zfe of the Carboniferous period, We naturally
find, as has been previously noticed, great differences in dif-
ferent parts of the entire series, corresponding to the different
mode of origin of the beds. Speaking generally, the Lower
Carboniferous (or the Sub-Carboniferous) is characterised by
the remains of marine animals; whilst the Upper Carbon-
iferous (or Coal-measures) is characterised by the remains
of plants and terrestrial animals. In all those cases, how-
ever, in which marine beds are found in the series of the
Coal-measures, as ls common in America, then we find that the
fossils agree in their general characters with those of the older
marine deposits of the period.

Owing to the fact that coal is simply compressed and other-
wise altered vegetable matter, and that it 1s of the highest
economic value to man, the Coal-measures have been more
thoroughly explored than any other group of strata of equiva-
lent thickness in the entire geological series. Hence we have
already a very extensive acquaintance with the plants of the
Carboniferous period ; and our knowledge on this subject is

daily undergoing increase.

THE CARBONIFEROUS PERIOD. 16]

It is not to be supposed, however,

that the remains of plants are found solely in the Coal.

GENERALISED SECTION OF THE CARBONIFEROUS STRATA
OF THE NORTH OF ENGLAND.

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--~=-- Coal-measures.

Millstone Grit.

Yoredale Series.

Scar-Limestone Series,

Basement Beds (Conglom-
erates and Sandstones).

for though most abundant towards the summit,

they are found in less numbers in all parts of the series.
Wherever found, they belong to the same great types of vege-

162 HISTORICAL PALZONTOLOGY.

tation ; but, before reviewing these, a few words must be said
as to the origin and mode of formation of coa/.

The coal-beds, as before mentioned, occur interstratified
with shales, sandstones, and sometimes limestones ; and there
may, within the limits of a single coal-field, be as many as 80
or 100 of such beds, placed one above the other at different
levels, and varying in thickness from a few inches up to 20 or
30 feet. Asa general rule, each bed of coal rests upon a bed
of shale or clay, which is termed the ‘‘under-clay,” and in
which are found numerous roots of plants; whilst the strata
immediately on the top of the coal may be shaly or sandy,
but in either case are generally charged with the leaves and
stems of plants, and often have upright trunks passing vertically
through them. When we add to this that the coal itself is,
chemically, nearly wholly composed of carbon, and that its
microscopic structure shows it tobe composed almost entirely
of fragments of stems, leaves, bark, seeds, and vegetable débris
derived from /and-plants, we are readily enabled to understand
how the coal was formed. The “wnder-clay” immediately
beneath the coal-bed represents an old land-surface—some-
times, perhaps, the bottom of a swamp or marsh, covered
with a luxuriant vegetation ;-the coa/ ded itself represents the
slow accumulation, through long periods, of the leaves, seeds,
fruits, stems, and fallen trunks of this vegetation, now hardened
and compressed into a fraction of its original bulk by the pres-
sure of the superincumbent rocks; and the strata of sand or
shale above the coal-bed—the so-called “‘roof” of the coal—
represent sediments quietly deposited as the land, after a long
period of repose, commenced to sink beneath the sea. On
this view, the rank and long-continued vegetation which gave
rise to each coal-bed was ultimately terminated by a slow
depression of the surface on which the plants grew. The
land-surface then became covered by the water, and aqueous
sediments were accumulated to a greater or less thickness upon
the dense mass of decaying vegetation below, enveloping any
trunks of trees which might still be in an erect position, and
preserving between their layers the leaves and branches of
plants brought down from the neighbouring land by streams,
or blown into the water by the wind. Finally, there set in a
slow movement of elevation,—the old land again reappeared
above the water; a new and equally luxuriant vegetation
flourished upon the new land-surface ; and another coal-bed
was accumulated, to be preserved ultimately in a similar
fashion. Some few beds of coal may have been formed by
drifted vegetable matter brought down into the ocean by rivers,

THE CARBONIFEROUS PERIOD. 1623

and deposited directly on the bottom of the sea; but in the
majority of cases the coal is undeniably the result of the slow
growth and decay of plants zz sctw: and as the plants of the
coal are not marine plants, it is necessary to adopt some such
theory as the above to account for the formation of coal-
seams. By this theory, as is obvious, we are compelled to
suppose that the vast alluvial and marshy flats upon which the
coal-plants grew were liable to constantly-recurring oscillations
of level, the successive land-surfaces represented by the suc-
cessive coal- beds of any coal-field being thus successively
buried beneath accumulations of mud or sand. We have no
need, however, to suppose that these oscillations affected large
areas at the same time; and geology teaches us that local
elevations and depressions of the land have been matters of
constant occurrence throughout the whole of past time.

All the varieties of coal (bituminous coal, anthracite, cannel-
coal, &c.) show a more or less distinct ‘‘lamination ”—that is
to say, they are more or less obviously composed of successive
thin layers, differing slightly in colour and texture. All the
varieties of coal, also, consist chemically of carbon, with vary-
ing proportions of certain gaseous constituents and a small
amount of incombustible mineral or ‘‘ash.” By cutting thin
and transparent slices of coal, we are further enabled, by
means of the microscope, to ascertain precisely not only that
the carbon of the coal is derived from vegetables, but also, in
many cases, what kinds of plants, and what parts of these, enter
into the formation of coal. When examined in this way, all
coals are found to consist more or less entirely of vegetable
matter; but there is considerable difference in different coals as
to the exact nature of this. By Professor Huxley it has been
shown that many of the English coals consist largely of ac-
cumulations of rounded discoidal sacs or bags, which are
unquestionably the seed-vessels or “‘ spore-cases”’ of certain of
the commoner coal-plants (such as the Lepzdodendra). ‘The
best bituminous coals seem to be most largely composed of
these spore-cases ; whilst inferior kinds possess a progressively
increasing amount of the dull carbonaceous substance which is
known as ‘mineral charcoal,” and which is undoubtedly com-
posed of “the stems and leaves of plants reduced to little
more than their carbon.” On the other hand, Principal Daw-
son finds that the American coals only occasionally exhibit
spore-cases to any extent, but consist principally of the cells,
vessels, and fibres of the bark, integumentary coverings, and
woody portions of the Carboniferous plants.

The number of plants already known to have existed during

164 HISTORICAL PALZONTOLOGY.

the Carboniferous period is so great, that nothing more can be
done here than to notice briefly the typical and characteristic
groups of these—such as the Ferns, the Calamites, the Lepido-
dendroids, the Sigillarioids, and the Conifers.

In accordance with M. Brongniart’s generalisation, that
the Palzozoic period is, botanically speaking, the “ Age of
Acrogens,” we find the Carboniferous plants to be still mainly
referable to the Flowerless or ‘‘ Cryptogamous” division of the
vegetable kingdom. The flowering or “ Phanerogamous”
plants, which form the bulk of our existing vegetation, are hardly
known, with certainty, to have existed at all in the Carbon-
iferous era, except as represented by trees related to the existing

ili ia = —s == ee eZ

Fig. 108.—Odontopteris Schlotheimii. Carboniferous, Europe and North America.

Pines and Firs, and possibly by the Cycads or “false palms.”*
Amongst the ‘“ Cryptogams,” there is no more striking or
beautiful group of Carboniferous plants than the Ferns. Re-
mains of these are found all through the Carboniferous, but in
exceptional numbers in the Coal-measures, and include both
herbaceous forms like the majority of existing species, and
arborescent forms resembling the living Tree-ferns of New
Zealand. Amongst the latter, together with some new types,
are examples of the genera Psaronius and Caulopteris, both of

* Whilst the vegetation of the Coal-period was mainly a terrestrial one,
aquatic plants are not unknown. Sea-weeds (such as the Sfrrophyton
cauda-Galli) are common in some of the marine strata; whilst coal,
according to the researches of the Abbé Castracane, is asserted commonly
to contain the siliceous envelopes of Diatoms.

THE CARBONIFEROUS PERIOD. 165

which date from the Devonian. ‘The simply herbaceous ferns
are extremely numerous, and belong to such widely-distributed

Fig. 109.—Calamites canneformis. Carboniferous Rocks, Europe aad
North America. :

and largely-represented genera as (Vewropteris, Odontopteris (fig.
108), Alethopteris, Pecopteris, Sphenopteris, Hymenophyllites, &c.
The fossils known as Calamites (fig. 109) are very common

166 HISTORICAL PALASONTOLOGY.

in the Carboniferous deposits, and have given occasion to an
abundance of research and speculation. They present them-
selves as prostrate and flattened striated stems, or as similar
uncompressed stems growing in an erect position, and some-
times attaining a length of twenty feet or more. Externally, the
stems are longitudinally ribbed, with transverse joints at regular
intervals, these joints giving origin to a whorl of branchlets,
which may or may not give origin to similar whorls of smaller
branchlets still. The stems, further, were hollow, with trans-
verse partitions at the joints, and having neither true wood nor
bark, but only a thin external fibrous shell. There can be little
doubt but that the Ca/amzfes are properly regarded as colossal
representatives of the little Horse-tails (Zguzsetacee) of the
present day. They agree with these not only in the general
details of their organisation, but also in the fact that the fruit
was a species of cone, bearing ‘‘spore-cases’’ under scales.
According to Principal Dawson, the Ca/amites “ grew in dense
brakes on the sandy and muddy flats, subject to inundation,
or perhaps even in water ; and they had the power of budding
out from the base of the stem, so as to form clumps of plants,
and also of securing their foothold by numerous cord-like roots
proceeding from various heights on the lower part of the
stem.”

The Lepidodendroids, represented mainly by the genus
Lepidodendron itself (fig. 110), were large tree-like plants,
which attain their maximum in the Carboniferous period, but
which appear to commence in the Upper Silurian, are well
represented in the Devonian, and survive in a.diminished form
into the Permian. The trunks of the larger species of Lepzdo-
dendron at times reach a length of fifty feet and upwards, giv-
ing off branches in a regular bifurcating manner. The bark
is marked with numerous rhombic or oval scars, arranged in
quincunx order, and indicating the points where the long,
needle-shaped leaves were formerly attached. The fruit con-
sisted of cones or spikes, carried at the ends of the branches,
and consisting of a central axis surrounded by overlapping
scales, each of which supports a ‘‘spore-case” or seed-vessel.
These cones have commonly been described under the name
of Zepzdostrobi. In the structure of the trunk there is nothing
comparable to what is found in existing trees, there being
a thick bark surrounding a zone principally composed of
“‘scalariform” vessels, this in turn enclosing a large central pith.
In their general appearance the Lepidodendra bring to mind
the existing Araucarian Pines; but they are true ‘“ Crypto-
gams,’”’ and are to be regarded as a gigantic extinct type of the

a

THE CARBONIFEROUS PERIOD. 167

modern Club-mosses (Zycopodiacee). ‘They are amongst the
commonest and most characteristic of the Carboniferous

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Fig. 110.—Lepidodendron Sternbergii, Carboniferous, Europe. The central figure
represents a portion of the trunk with its branches, much reduced in size. ‘The right-
hand figure is a portion of a branch with the leaves partially attached to it ; and the left-
hand figure represents the end of a branch bearing a cone of fructification.

plants; and the majority of the “‘spore-cases” so commonly

found in the coal appear to have been derived from the cones
of Lepidodendroids.

168 HISTORICAL PALZONTOLOGY.

The so-called Sigz//arioids, represented mainly by Szg¢laria
itself (fig. 111), were no less abundant and characteristic of the
Carboniferous forests than the Zepzdodendra. ‘They commence
their existence, so far as known, in the Devonian period, but
they attain their maximum in the Carboniferous ; and—unlike
the Lepidodendroids—they are not known to occur in the
Permian period. They are comparatively gigantic in size,
often attaining a height of from thirty to fifty feet or more;
but though abundant and well preserved, great divergence of
opinion prevails as to their true affinities. The zame of Sigil-
larioids (Lat. szgz//a, littie seals or images) is derived from the
fact that the bark is marked with seal-like impressions or leaf-
scars (fig. IIT).

Externally, the trunks of S%gz//arza present strong longitudinal
ridges, with vertical‘alternating rows of oval leaf-scars indicating

Fig. 111.—Fragment of the external surface of Sigil/aria Greseri, showing the ribs andi
jeans: The left-hand figure represents a small portion enlarged. Carboniferous,,
urope.

the points where the leaves were originally attached. The trunk
was furnished with a large central pith, a thick outer bark, and
an intermediate woody zone,—composed, according to Dawson,
partly of the disc-bearing fibres so characteristic of Conifers ;
but, according to Carruthers, entirely made up of the “ scalari-
form ” vessels characteristic of Cryptogams. The size of the
pith was very great, and the bark seems to have been the most
durable portion of the trunk. Thus we have evidence that
in many cases the stumps and “stools” of Sigi/arie, standing

THE CARBONIFEROUS PERIOD. 169

upright in the old Carboniferous swamps, were completely
hollowed out by internal decay, till nothing but an exterior
shell of bark was left. Often these hollow stumps became:
ultimately filled up with sediment, sometimes enclosing the
remains of galley-worms, land-snails, or Amphibians, which
formerly found in the cavity of the trunk a congenial home;
and from the sandstone or shale now filling such trunks some
of the most interesting fossils of the Coal-period have been
obtained. ‘There is little certainty as to either the leaves or
fruits of Svgz//aria, and there is equally little certainty as to the
true botanical position of these plants. By Principal Dawson
they are regarded as being probably flowering plants allied to
the existing “‘ false palms” or ‘‘ Cycads ;” but the high author-
ity of Mr Carruthers is to be quoted in support of the belief
that they are Cryptogamic, and most nearly allied to the Club-
mosses.

Leaving the botanical position of Szg7//arza thus undecided,
we find that it is now almost universally conceded that the
fossils originally described under the name of Stigmaria are
the roots of Szgi//aria, the actual connection between the two
having been in numerous instances demonstrated in an unmis-
takable manner. The Stgmarze (fig. 112) ordinarily present
themselves in the form of long, compressed or rounded frag-

Fig. 112.—Stigmaria ficoides. Quarter natural size. Carboniferous.

ments, the external surface of which is covered with rounded
pits or shallow tubercles, each of which has a little pit or de-
pression in its centre. From each of these pits there proceeds,
in perfect examples, a long cylindrical rootlet ; but in many
cases these have altogether disappeared. In their internal
structure, Stigmaria exhibits a central pith surrounded by a
sheath of scalariform vessels, the whole enclosed in a cellular
envelope. The Stigmarie are generally found ramifying in

170 HISTORICAL PALZONTOLOGY.

the “under-clay,” which forms the floor of a bed of coal, and
which represents the ancient soil upon which the Szgz//arz@ grew.
The Lepidodendroids and Sigillarioids, though the first were
certainly, and the second possibly, Cryptogamic or flowerless
plants, must have constituted the main mass of the forests of
the Coal period; but we are not without evidence of the exist-
ence at the same time of genuine “trees,” in the technical
sense of this term—namely, flowering plants with large woody
stems. So far as is certainly known, all the true trees of the
Carboniferous formation were Conzfers, allied to the existing
Pines and Firs. They are recognised by the great size and
concentric woody rings of their prostrate, rarely erect trunks,
and by the presence of disc-bearing fibres in their wood, as
demonstrated by the microscope; and the principal genera
which have been recognised are Dadoxylon, Paleoxylon,
Araucarioxylon, and Pinites. Their fruit is not known with
absolute certainty, unless it be represented, as often conjectured,
by Zvrigonocarpon (fig. 113). The fruits known under this
name are nut-like, often of consider-
able size, and commonly three- or six-
angled. They probably originally pos-
sessed a fleshy envelope ; and if truly
referable to the Conzfers, they would
indicate that these ancient evergreens
2 produced berries instead of cones,
Fig. 113. — Trigonocarfon and thus resembled the modern Yews
ovatum, Coal-measures, Britain. .
Csior tle idler aaceetneron) rather than the Pines.-. It seems,
further, that the great group of the
Cycads, which are nearly allied to the Conzfers, and which
attained such a striking prominence in the Secondary period,
probably commenced its existence during the Coal period ;
but these anticipatory forms are comparatively few in number,
and for the most part of somewhat dubious affinities.

C PAPE LE Re, OChits

THE CARBONIFEROUS PERIOD—Continued.
ANIMAL LIFE OF THE CARBONIFEROUS.

3
We have seen that there exists a great difference as to the
mode of origin of the Carboniferous sediments, some being
purely marine, whilst others are terrestrial; and others, again,

THE CARBONIFEROUS PERIOD. EY

have been formed in inland swamps and morasses, or in brack-
ish-water lagoons, creeks, or estuaries. A corresponding dif-
ference exists necessarily in the animal remains of these de-
posits, and in many regions this difference is extremely well
marked and striking. The great marine lmestones which
characterise the lower portion of the Carboniferous series in
Britain, Europe, and the eastern portion of America, and the
calcareous beds which are found high up in the Carboniferous
in the western States of America, may, and do, often contain
the remains of drifted plants ; but they are essentially charac-
terised by marine fossils; and, moreover, they can be demon-
strated by the microscope to. be almost wholly composed of
the remains of animals which formerly inhabited the ocean.
On the other hand, the animal remains of the beds accompany-
ing the coal are typically the remains of air-breathing, terres-
trial, amphibious, or aerial animals, together with those which
inhabit fresh or brackish waters. Marine fossils may be found
in the Coal-measures, but they are invariably confined to spe-
cial horizons in the strata, and they indicate temporary depres-
sions of the land beneath the sea. Whilst the distinction here
mentioned is one which cannot fail to strike the observer, it is
convenient to consider the animal life of the Carboniferous as
a whole: and it is simply necessary, in so doing, to remember
that the marine fossils are in general derived from the inferior
portion of the system; whilst the air-breathing, fresh-water, and
brackish-water forms are almost exclusively derived from the
superior portion of the same.

The Carboniferous Protozoans consist mainly of Foramint-
Jera and Sponges. ‘The latter are still very insufficiently known,
but the former are very abundant, and belong to very varied
types. Thin slices of the limestones of the period, when ex-
amined by the microscope, very commonly exhibit the shells
of Foraminifera in greater or less plenty. Some limestones,
indeed, are made up of little else than these minute and elegant
shells, often belonging to types, such as the Textularians and
Rotalians, differing little or not at all from those now in exist-
ence. ‘This is the case, for exarnple, with the Carboniferous
Limestone of Spergen Hill in Indiana (fig. 114), which is
almost wholly made up of the spiral shells of a species of
Lndothyra. In the same way, though to a less extent, the
black Carboniferous marbles of Ireland, and the similar mar-
bles of Yorkshire, the limestones of the west of England and
of Derbyshire, and the great “Scar Limestones” of the north
of England, contain great numbers of Foraminiferous shells ;
whilst similar organisms commonly occur in the shale-beds

172 HISTORICAL PALAONTOLOGY.

associated with the limestones throughout the Lower Carbon-
iferous series. One of the most interesting of the British Car-
boniferous forms is the Sac-
cammina of Mr Henry Brady,
which is sometimes present in
considerable numbers in the
limestones of Northumberland,
Cumberland, and the west °
of Scotland, and which is con-
spicuous for the comparatively
large size of its spheroidal or
pear-shaped shell (reaching
from an eighth to a fifth of an
inch in size). More widely dis-
tributed are the generally spin-

. dle-shaped shells of Fusulina
Fig. 114.—Transparent slice of Carbon-

iferous Limestone, from Spergen Hill, In- (fig. I 15), which occur im vast
diana, U.S., showing numerous shells of pumbers in the Carboniferous

Boe Oat» Batleye slightly en- 7 i estone of Russia, Arme-

nia, the Southern Alps, and
Spain, similar forms occurring in equal profusion in the higher
limestones which are found in the Coal-measures of the United
States, in Ohio, Illinois,
Indiana, Missouri, &c. Mr
Henry Brady, lastly, has
shown that we have in the
Nummulina pristina of the
Carboniferous Limestone of
Namur a genuine Vummu-
‘ite, precursor of the great and important family of the Tertiary
Nummulites.

The sub-kingdom of the Ce/enterates, so far as certainly
known, is represented only by Cora/s ;* but the remains of
these are so abundant in many of the limestones of the Car-
boniferous formation as to constitute a feature little or not at
all less conspicuous than that afforded by the Crinoids. As is
the case in the preceding period, the Corals belong, almost
exclusively, to the groups of the Augosa and Tabulata; and
there is a general and striking resemblance and relationship
between the coral-fauna of the Devonian as a whole, and that

Fig. 115.—Fusulina cylindrica, Carbon-
iferous Limestone, Russia.

mA. singular fossil has been described by Professor Martin Duncan and
Mr Jenkins from the Carboniferous rocks under the name of Paleocoryne,
and has been referred to the Hydroid Zoophytes (Corynida). Doubt,
however, has been thrown by other observers on the correctness of this
reference,

THE CARBONIFEROUS PERIOD. 173

of the Carboniferous. Nevertheless, there is an equally decid-
ed and striking amount of difference between these successive
faunas, due to the fact that the great majority of the Carbon-
iferous sfeczes are new ; whilst some of the most characteristic
Devonian genera have nearly or quite disappeared, and several
new genera now make their appearance for the first time.
Thus, the characteristic Devonian types Helophyllum, Pachy-
phyllum, Chonophyllum, Acervularia, Spongophyllum, Smithia,
Endophyllum, and Cystiphyllum, have now disappeared; and
the great masses of Favosites which are such a striking feature in
the Devonian limestones, are represented but by one or two
degenerate and puny successors. On the other hand, we meet
in the Carboniferous rocks not only with entirely new genera—
such as Axophyllum, Lophophyllum, and Londsdaleia—but we
have an enormous expansion of certain types which had just
begun to exist in the preceding period. ‘This is especially
well seen in the case of the genus Lzthostrotion (fig. 116, 0),
which more than any other may be considered as the predo-
minant Carboniferous group of Corals. All the species of
Lithostrotion are compound, consisting either of bundles of
loosely-approximated cylindrical stems, or of similar “coral-
lites” closely aggregated together into astrzeiform colonies, and
rendered polygonal by mutual pressure. This genus has a
historical interest, as having been noticed as early as in the
year 1699 by Edward Lhwyd ; and it is geologically important
from its wide distribution in the Carboniferous rocks of both
the Old and New Worlds. Manyspecies are known, and whole
beds of limestone are often found to be composed of little else
than the skeletons of these ancient corals, still standing upright
as they grew. Hardly less characteristic of the Carboniferous
than the above is the great group of simple “cup-corals,” of
which C/istophyllum is the central type. Amongst types which
commenced in the Silurian and Devonian, but which are still
well represented here, may be mentioned Syringopora (fig. 116,
e), with its colonies of delicate cylindrical tubes united at in-
tervals by cross-bars; Zaphrentis (fig. 116, @), with its cup-
shaped skeleton and the well-marked depression (or “‘fossula”)
on one side of the calice; Amplexus (fig. 116, ¢c), with its
cylindrical, often irregularly swollen coral and short septa;
Cyathophyllum (fig. 116, a), sometimes simple, sometimes form-
ing great masses of star-like corallites; and Chetetes, with its
branched stems, and its minute, “‘ tabulate” tubes (fig. 116, /).
The above, together with other and hardly less characteristic
forms, combine to constitute a coral-fauna which is not only in
itself perfectly distinctive, but which is of especial interest,

13

174 HISTORICAL PALZONTOLOGY.

from the fact that almost all the varied types of which it is
composed disappeared utterly before the close of the Carbon-

Fig. 116.—Corals of the Carboniferous Limestone. a. Cyathophyllum paracida, show-
ing young corallites budded forth from the disc of the old one; a’, One of the corallites
of the same, seen in cross-section; 4, Fragment of a mass of Lithostrotion trregulare ;
6’, One of the corallites of the same, divided transversely ; c, Portion of the simple cylin-
drical coral of Awzplexus coralloides; c’, Transverse section of the same species; d,
Zaphrentis vermicularis, showing the depression or “‘ fossula’”’ on one side of the cup;
e, Fragment of a mass of Syringopora ramulosa; f, Fragment of Chetetes tumidus; J’,
Portion of the surface of the same, enlarged. From the Carboniferous Limestone of
Britain and Belgium, (After Thomson, De Koninck, Milne-Edwards and Haime, and
the Author.)

iferous period. In the first marine sediments of a calcareous
nature which succeeded to the Coal-measures (the magnesian
limestones of the Permian), the great group of the Augose
corals, which flourished so largely throughout the Silurian, De-
vonian, and Carboniferous periods, is found to have all but

THE CARBONIFEROUS PERIOD. 175

disappeared, and it is never again represented save sporadi-
cally and by isolated forms.

Amongst the Zchinoderms, by far the most important forms
are the Sea-lilies and the Sea-urchins—the former from their
great abundance, and the latter from their singular structure ;
but the little group of the ‘“ Pentremites” also requires to be
noticed. The Sea-lilies are so abundant in the Carboniferous
rocks, that it has been proposed to call the earlier portion of
the period the ‘‘ Age of Crinoids.” Vast masses of the lime-
stones of the period are “ crinoidal,” being more or less ex-
tensively composed of the broken columns, and detached plates
and joints of Sea-lilies, whilst perfect ‘ heads ” may be exceed-
ingly rare and difficult to procure. In North America the re-
mains of Crinoids are even more abundant at this horizon than
in Britain, and the specimens found seem to be commonly
more perfect. The commonest of the Carboniferous Crinoids
belong to the genera Cyathocrinus, Actinocrinus, Platycrinus,

Fig. 117.—Platycrinus tricontadactylus, Lower Carboniferous. The left-hand figure
shows the calyx, arms, and upper part of the stem; and the figure next this shows the sur-
ice of one of the joints of the column. The right-hand figure shows the proboscis. (After

A‘Coy.)

( fig. 117), Potertocrinus, Zeacrinus, and Forbestocrinus. Closely
allied to the Crinoids, or forming a kind of transition between

2

176 HISTORICAL PALZONTOLOGY.

these and the Cystideans, is the little group of the “ Pentre-
mites,” or Blastoids (fig. 118). This group is first known to

UMbthhhd.
Vililitlize,

ELL Ls
LOCLLL.

hha

SEP.
CGF
HB
7
x
4,
YY
4Y
47
14
4Y
i

CLE,
“thay

et
tite

_Fig. 118.—A, Pentremites pyriformis, side-view of the body (“calyx”); B, The same
viewec from below, showing the arrangement of the plates; C, Body of Pentremites
conoideus, viewed from above. Carboniferous.

have commenced its existence in the Upper Silurian, and it
increased considerably in numbers in the Devonian ; but it
was in the seas of the Carboniferous period that it attained its
maximum, and no certain representative of the family has been
detected in any later deposits. The ‘‘ Pentremites ” resemble
the Crinoids in having a cup-shaped body (fig. 118, A) enclosed
by closely-fitting calcareous plates, and supported on a short
stem or ‘‘ column,” composed of numerous calcareous pieces
flexibly articulated together. They differ from the Crinoids,
however, in the fact that the upper surface of the body does
not support the crown of branched feathery “‘ arms,” which are
so characteristic of the latter. On the contrary, the summit of
the cup is closed up in the fashion of a flower-bud, whence the
technical name of lastoidea applied to the group (Gr. d/astos,
a bud; ezdos, form). From the top of the cup radiate five broad,
transversely-striated areas (fig. 118, C), each with a longitudi-
nal groove down its middle; and along each side of each of

es | es

THE CARBONIFEROUS PERIOD. 177

these grooves there seems to have been attached a row of
short jointed calcareous filaments or “ pinnules.”__

A few Star-fishes and Brittle-stars are known to occur in the
Carboniferous rocks; but the only other Echinoderms of this
period which need be noticed are the Sea-urchins (Zchznozds).
Detached plates and spines of these are far from rare in the
Carboniferous deposits ; but anything like perfect specimens
are exceedingly scarce. The Carboniferous Sea-urchins agree
with those of the present day in having the body enclosed in
a shell, formed by an enormous number of calcareous plates
articulated together. The shell may be regarded as, typically,
nearly spherical in shape, with the mouth in the centre of the
base, and the excretory opening or vent at its summit. In both
the ancient forms and the recent ones, the plates of the shell

Fig. 119.—Palechinus ellipticus, one of the Carboniferous Sea-urchins. The left-
hand figure shows one of the “‘ambulacral areas” enlarged, exhibiting the perforated
plates. The right-hand figure exhibits a single plate from one of the “‘inter-ambulacral
areas.” (After M‘Coy.)

are arranged in ten zones which generally radiate from the
summit to the centre of the base. In five of these zones—
termed the “ambulacral areas”—the plates are perforated by
minute apertures or ‘ pores,” through which the animal can
protrude the little water-tubes (‘‘ tube-feet”) by which its loco-
motion is carried on. In the other five zones—the so-called
“‘inter-ambulacral areas” —the plates are of larger size, and
are not perforated by any apertures. In all the modern Sea-
urchins each of these ten zones, whether perforate or imper-
forate, is composed of two rows of plates; and there are thus
twenty rows of plates in all. In the Palzozoic Sea-urchins, on
the other hand, the ‘‘ambulacral areas” are often like those
of recent forms, in consisting of wo rows of perforated plates
(fig. 119); but the “inter-ambulacral areas’ are always quite

178 HISTORICAL PALZONTOLOGY.

peculiar in consisting each of three, four, five, or more rows of
large imperforate plates, whilst there are sometimes four or ten
rows of plates in the “‘ambulacral areas” also: so that there
are many more than twenty rows of plates in the entire shell.
Some of the Paleozoic Sea-urchins, also, exhibit a very pecu-
liar singularity of structure which is only known to exist ina
very few recently-discovered modern forms (viz., Ca/verta and
Phormosoma). The plates of the inter-ambulacral areas,
namely, overlap one another in an imbricating manner, so as
to communicate a certain amount of flexibility to the shell;
whereas in the ordinary living forms these plates are firmly
articulated together by their edges, and the shell forms a rigid
immovable box. The Carboniferous Sea-urchins which ex-
hibit this extraordinary peculiarity belong to the genera Lefv-
dechinus and Lepidesthes, and it seems tolerably certain that
a similar flexibility of the shell existed to a less degree in
the much more abundant genus Archeocidaris. ‘The Carbon-
iferous Sea-urchins, like the modern ones, possessed movable
spines of greater or less length, articulated to the exterior of
the shell; and these structures are of very common occur-
rence in a detached condition. The most abundant genera
are Archeocidaris and FPalechinus; but the characteristic
American forms belong principally to A/elonites, Oligoporus,
and Lepidechinus.

Amongst the Annelzdes it is only necessary to notice the little
spiral tubes of Sfzvorbis Carbonarius (fig. 120), which are

v
y

IK

ih

Fig. 120.—Spirorbis (Microconchus) Carbonarius, of the natural size, attached to a fossil
plant, and magnified. Carboniferous -Britain and North America. (After Dawson.)

commonly found attached to the leaves or stems of the Coal-
plants. This fact shows that though the modern species of
Spirorbis are inhabitants of the sea, these old representatives
of the genus must have been capable of living in the brackish
waters of lagoons and estuaries.

The Crustaceans of the Carboniferous rocks are numerous,

THE CARBONIFEROUS PERIOD. 179

and belong partly to structural types with which we are already
familiar, and partly to higher groups which come into existence
here for the first time. The gigantic Aurypterids of the Upper
Silurian and Devonian are but feebly represented, and make
their final exit here from the scene of life. ‘Their place, how-
ever, is taken by peculiar forms belonging to the allied group
of the Xzphosura, represented at the present day by the King-
crabs or ‘‘ Horse-shoe Crabs” (Zzmulus). Characteristic forms
of this group appear in the Coal-measures both of Europe and
America; and though constituting three distinct genera (Prest-
wichia, Belinurus, and Euproops), they are all nearly related
to one another. The best known of them, perhaps, is the
Prestwichia rotundata of Coalbrookdale, here figured (fig. 121).
The ancient and for-
merly powerful order
of the Z7rzobites also
undergoes its final ex-
tinction here, not sur-
viving the deposition
of the Carboniferous
Limestone series in Eu-
rope, but extending its
range in America into i
the Coal-measures. All \ Le
the known Carbonifer- | |
ous forms are small in
size and degraded in
point of structure, and
they are referable to
but three genera (P/z/-
lipsia, Griffithides, and _ Fig. 121.—Prestwichia votundata, a Limuloid
Brachymetopus), be- eas Coal-measures, Britain. (After Henry
longing to a single fa-

mily. The Phillipsia seminifera here figured (fig. 122, a) isa
characteristic species in the Old World. The Water- fleas
(Ostracoaa) are extremely abundant in the Carboniferous rocks,
whole strata being often made up of little else than the little
bivalved shells of these Crustaceans. Many of them are ex-
tremely small, averaging about the size of a millet-seed ; but a
few forms, such as Entomoconchus Scouleri (fig. 122, ¢), may attain
a length of from one to three quarters of aninch. The old
group of the PryHopods is likewise still represented in some
abundance, partly by tailed forms of a shrimp-like appearance,
such as Dithyrocaris (fig. 122, @), and partly by the curious
striated Lstherwe and their allies, which present a curious

uJ I) IW)

il) ll)

180 HISTORICAL PALAZZONTOLOGY.

resemblance to the true Bivalve Molluscs (fig. 122,64). Lastly,
we meet for the first time in the Carboniferous rocks with the
remains of the highest of all the groups of Crustaceans—name-

ly, the so-called ‘‘ Decapods,” in which there are five pairs of ©

walking-limbs, and the hinder end of the body (‘‘ abdomen ”)
is composed of separate rings, whilst the anterior end is coy-
ered by a head-shield or “carapace.” All the Carboniferous
Decapods hitherto discovered resemble the existing Lobsters,

TTT,

aiey

Fig. 122.—Crustaceans of the Carboniferous Rocks. a, Phillipsia seminifera, of the
natural size—Mountain Limestone, Europe; 4, One valve of the shell of Esthervza tenella,
of the natural size and enlarged—Coal-measures, Europe; c, Bivalved shell of Zxtomnzo-
conchus Scouleri, of the natural size—Mountain Limestone, Europe; d, Dithyrocaris
Scouler7, reduced in size—Mountain Limestone, Ireland ; e, Pa/gocaris typus, slightly
enlarged—Coal-measures, North America; 4, Axthrapalemon gracilis, of the natural
size—Coal-measures, North America. (After De Koninck, M‘Coy, Rupert Jones, and
Meek and Worthen.)

Prawns, and Shrimps (the Wacrura), in having a long and well-
developed abdomen terminated by an expanded tail-fin. The
Paleocaris typus (fig. 122, e) and the Anthrapalemon gracilis
(fig. 122, f), from the Coal-measures of Illinois, are two of the
best understood and most perfectly preserved of the few known
representatives of the ‘‘ Long-tailed”? Decapods in the Car-
boniferous series. The group of the Crabs or “Short-tailed”

THE CARBONIFEROUS PERIOD. T8r

Decapods (Brachyura), in which the abdomen is short, not
terminated by a tail-fin, and tucked away out of sight beneath
the body, is at present not known to be represented at all in
the Carboniferous deposits.

In addition to the water-inhabiting group of the Crustaceans,
we find the articulate animals to be represented by members
belonging to the air-breathing classes of the Arachnida, Myria-
poda, and /nsecta. The remains of these, as might have been
expected, are not known to occur in the marine limestones of
the Carboniferous series, but are exclusively found in beds asso-
ciated with the Coal, which have been deposited in lagoons,
estuaries, or marshes, in the immediate vicinity of the land, and
which actually represent an old land-surface. The Arachnids
are at present the oldest known of their class, and are repre-
sented both by true Spiders and Scorpions. Remains of the
latter (fig. 123) have been found both in the Old and New

Fig. 123.—Cyclophthalmus senior. A fossil Scorpidn from the Coal-measures
; of Bohemia.

Worlds, and indicate the existence in the Carboniferous period
of Scorpions differing but very little from existing forms. The
group of the IZyrzapoda, including the recent Centipedes and
Galley-worms, is likewise represented in the Carboniferous strata,

182 HISTORICAL PALZONTOLOGY.

but by forms in many respects very unlike any that are known
to exist at the present day. The most interesting of these
were obtained by Principal Dawson, along with the bones of
Amphibians and the shells of Land-snails, in the sediment filling
the hollow trunks of Szgz//aria, and they belong to the genera
Xylobius (fig. 124) and Archiulus. Lastly, the true zvsects are

Fig. 124.—AXylobius Sigillarie, a Carboniferous Myriapod. a@, A specimen, of the
natural size; 6, Anterior portion of the same, enlarged ; c, Posterior portion, enlarged.
From the Coal-measures of Nova Scotia. (After Dawson.)

represented by various forms of Beetles (Coleoptera), Orthoptera
(such as Cockroaches), and /Veuropterous insects resembling
those which we have seen to have existed towards the close of

Wii \ T=
ANY}! \\ \y SQXQN ~S
S\N \ Ss

\\\ \\\ Ney: a f

SNS
YESS

a ; -

Fig. 125.—Haplophilebium Barnesi, a Carboniferous insect, from the Coal-measures
of Nova Scotia. (After Dawson.)

the Devonian period. One of the most remarkable of the
latter is a huge May-fly (Haplophlebium Barnest, fig. 125), with

THE CARBONIFEROUS PERIOD. 183

netted wings attaining an expanse of fully seven inches, and
therefore much exceeding any existing Ephemerid in point
of size.

The lower groups of the Jod/usca are abundantly represented
in the marine strata of the Carboniferous series by Polyzoans

Fig. 126.—Carboniferous Polyzoa. a, Fragment of Polypora dendroides, of the natural
size, Ireland ; a’ Small portion of the same, enlarged to show the cells; 4, Glauconome
pulcherrima, a fragment, of the natural size, Ireland; 4, Portion of the same, enlarged ;
c, Thecentral screw-like axis of Archimedes Worthenz, of the natural size—Carboniferous,
America ; c’, Portion of the exterior of the frond of the same, enlarged ; c”, Portion of
the interior of the frond of the same showing the mouths of the cells, enlarged. (After
M ‘Coy and Hall.)

and Lrachiopods. Amongst the former, although a variety of
other types are known, the majority still belong to the old
group of the “‘ Lace-corals” (Fenestellide), some of the charac-
teristic forms of which are here figured (fig. 126). The graceful

184 HISTORICAL PALZONTOLOGY.

netted fronds of Fenestella, Retepora, and Polypora (fig. 126, a)
are highly characteristic, as are the slender toothed branches
of Glauconome (fig. 126, 6). Amore singular form, however, is
the curious Archimedes (fig. 126, c), which is so characteristic
of the Carboniferous formation of North America. In this re-
markable type, the colony consists of a succession of funnel-
shaped fronds, essentially similar to Aeveste//a in their structure,
springing ina continuous spiral from a strong screw-like vertical
axis. The outside of the fronds is simply striated; but the
branches exhibit on the interior the mouths of the little cells:
in which the semi-independent beings composing the colony
originally lived.

The Brachiopods are extremely abundant, and for the most
part belong to types which are exclusively or principally
Paleozoic in their range. The old genera Stvophomena, Orthis
(fig. 127, ¢), Athyris (fig. 127, e), Rhynchonella (fig. 127, g), and
Spirifera (fig. 127, h), are still w Si represented—the latter, in
particular, existing under numerous specific forms, conspicuous
by their abundance and sometimes by their size. Along with
these ancient groups, we have representatives—for the first time
in any plenty—of the great genus Zerebratula (fig. 127, @),
which underwent a great expansion during later periods, and
still exists at the present day. The most characteristic Car-
boniferous Brachiopods, however, belong to the family of the
Productide, of which the principal genus is FProducta itself.
This family commenced its existence in the Upper Silurian
with the genus CZonefes, distinguished by its spinose hinge-
margin. This genus lived through the Devonian, and flourished
in the Carboniferous (fig. 127, f). The genus Producta itself,
represented in the Devonian by the nearly allied Productella,
appeared first in the Carboniferous, at any rate in force, and
survived into the Permian ; but no member of this extensive
family has yet been shown to have over-lived the Paleozoic
period. The Producte of the Carboniferous are not only ex-
ceedingly abundant, but they have in many instances a most
extensive geographical range, and some species attain what
may fairly be considered gigantic dimensions. ‘The shell (fig.
127, a and 4) is generally more or less semicircular, with a
straight hinge-margin, and having its lateral angles produced
into larger or smaller ears (hence its generic name—“ cochlea
producta”). One valve (the ventral) is usually strongly convex,
whilst the other (the dorsal) is flat or concave, the surface of
both being adorned with radiating ribs, and with hollow
tubular spines, often of great length. The valves are not
locked together by teeth, and there is no sign in the fully- |

THE CARBONIFEROUS PERIOD. 185

grown shell of an opening in or between the valves for the
emission of a muscular stalk for the attachment of the shell to.
foreign objects. It is probable, therefore, that the Producte,
unlike the ordinary Lamp-shells, lived an independent exist-
ence, their long spines apparently serving to anchor them
firmly in the mud or ooze of the sea-bottom ; but Mr Robert
Etheridge, jun., has recently shown that in one species the

Fig. 127.—Carboniferous Brachiofoda. a, Producta semireticulata, showing the
slightly concave dorsal valve; a’ Side view of the same, showing the convex ventral
valve; 4, Producta longispina; c, Orthis resupinata; dad, Terebratula hastata; e,
Athyris subtilita; f, Chonetes Hardrensis; g, Rhynchonella pleurodon; h, Spirifera
trigonalts. Most of these forms are widely distributed in the Carboniferous Limestone
of Britain, Europe, America, &c. All the figures are of the natural size. (After David-
son, De Koninck, and Meek.)

spines were actually employed as organs of adhesion, whereby
the shell was permanently attached to some extraneous object,
such as the stem of a Crinoid. ‘The two species here figured
are interesting for their extraordinarily extensive geographical
range—Producta semireticulata (fig. 127, 2) being found in the
Carboniferous rocks of Britain, the continent of Europe,
Central Asia, China, India, Australia, Spitzbergen, and North

186 HISTORICAL PALZONTOLOGY.

and South America; whilst P. dongispina (fig. 127, 6) has a
distribution little if at all less wide.

The higher JZo//usca are abundantly represented in the
Carboniferous rocks by Bivalves (Lamellibranchs), Univalves
(Gasteropoda), Winged-snails (Pteropoda), and Cephalopods.
Amongst the Bivalves we may note the great abundance of
Scallops (Aviculopecten and other allied forms), together with
numerous other types—some of ancient origin, others repre-
sented here for the first time. Amongst the Gasteropods, we
find the characteristically Paleozoic genera Macrocheilus and
Loxonema, the almost exclusively Paleozoic Luomphalus, and
the persistent genus /leurotomaria ; whilst the free-swimming
Univalves (eteropoda) are represented by Bellerophon and Porcel-
Zia, and the Preropoda by the old genus Conularia. With regard
to the Carboniferous Univalves, it is also of interest to note here
the first appearance of true air-breathing or terrestrial Molluscs,
as discovered by Dawson and Bradley in the Coal-measures of
Nova Scotia and Illinois. Some of these (Conulus priscus) are
true Land-snails, resembling the existing Zonztes ; whilst others
(Pupa vetusta, fig. 128) appear to be generically inseparable
from the ‘“ Chrysalis-shells ”
(Pupa) of the present day.
All the known forms—three
in number—are of small size,
and appear to have been local
in their distribution or in their
preservation. More import-
ant, however, than any of the
preceding, are the Cephalo-
poda, represented, as_ before,
exclusively by the chambered
shells of the Tetrabranchiates.
The older and simpler type of
these, with simple plain septa,
and mostly a central siphuncle,
is represented by the straight
conical shells of the ancient

Fig. 128.—Pufa (Dendropupa)vetusta, genus Orthoceras, and the bow-
a Carboniferous Lead sail fromthe Coal shaped shells. of the! eeaail
the natural size; 4, The same, magnified; ancient Cyrtoceras —some of
Cte Cate cnlurzed. eAfter Dancon) _ theformer attaining a great size.

The spirally-curved discoidal
shells of the persistent genus /Vaufz/us are also not unknown,
and some of these likewise exhibit very considerable dimen-
sions. Lastly, the more complex family of the Ammonitide,

THE CARBONIFEROUS PERIOD. I 87

with lobed or angulated septa, and a dorsally-placed siphuncle
(situated on the convex side of the curved shells), now for the
first time commences to acquire a considerable prominence.
The principal representative of this group is the genus Govza-
tites (fig. 129), which commenced its existence in the Upper
Silurian, is well represented in the De-
vonian, and attains its maximum here.
In this genus, the shell is spirally
curved, the septa are strongly lobed
or angulated, though not elaborately
frilled as in the Ammonites, and the
siphuncle is dorsal. In addition to
Gontatites, the shells of true Ammon-
ites, so characteristic of the Secondary
period, have been described by Dr
Waagen as occurring in the Carbon-
iferous rocks of India.

Fig. 129.—Goniatites (Aganides) Fosse. Carboniferous Limestone.

Coming finally to the Vertebrata, we have in the first place
to very briefly consider the Carboniferous fishes. These are
numerous ; but, with the exception of the still dubious “ Cono-
donts,” belong wholly to the groups of the Ganords and the
Placoids (including under the former head remains which per-
haps are truly referable to the group of the Dzpmoz or Mud-
fishes). Amongst the Ganozds, the singular buckler-headed
fishes of the Upper Silurian and Devonian (Cephalaspide) have

188 HISTORICAL PALZONTOLOGY.

apparently disappeared ; and the principal types of the Car-
boniferous belong to the groups respectively represented at
the present day by the Gar-pike (Lepzdosteus) of the North
American lakes, and the Polypferus of the rivers of Africa. Of
the former, the genera Palgoniscus and Amblypterus (fig. 130),

Fig. 130.—A mdlypterus macropterus. Carboniferous.

with their small rhomboidal and enamelled scales, and their
strongly unsymmetrical tails, are perhaps the most abundant.
Of the latter, the most important are species belonging to
the genera Megalichthys and Rhizodus, compnising large fishes,
with rhomboidal scales, unsymmetrical (‘‘ heterocercal”’) tails,
and powerful conical teeth. These fishes are sometimes said
to be ‘‘ sauroid,” from their presenting some Reptilian features
in their organisation, and they must have been thé scourges
of the Carboniferous seas. The remains of P/acoid fishes in
the Carboniferous strata are very numerous, but consist wholly
of teeth and fin-spines, referable to forms more or less closely
allied to our existing Port Jackson Sharks, Dog-fishes, and
Rays. The teeth are of very various shapes and sizes,—some
with sharp, cutting edges (Petalodus, Cladodus, &c.) ; others in
the form of broad crushing plates, adapted, like the teeth of the
existing Port Jackson Shark (Cestracion Philippi), for breaking
down the hard shells of Molluscs and Crustaceans. Amongst
the many kinds of these latter, the teeth of Psammodus and
Cochliodus (fig. 131) may be mentioned as specially charac-
teristic. The fin-spines are mostly similar to those so common
in the Devonian deposits, consisting of hollow defensive spines
implanted in front of the pectoral or other fins, usually slightly
curved, often superficially ribbed or sculptured, and not un-
commonly serrated or toothed. The genera Cvenacanthus,
Gyracanthus, Homacanthus, &c., have been founded for the
reception of these defensive weapons, some of which indicate
fishes of great size and predaceous habits.

THE CARBONIFEROUS PERIOD. 189

In the Devonian rocks we meet with no other remains of
Vertebrated animals save fishes only; but the Carboniferous
deposits -have yielded re-
mains of the higher group
of the Amphibians. ‘This

class, comprising our ex-
isting Frogs, Toads, and

between the class of the
fishes and that of the true
reptiles, being distinguished
from the latter by the fact
that its members invariably

; SS S ! i i
Newts, stands to some ex- Ss SY iS)
+ RS S~’ he
tent in a position midway SSS SSSN i) IN
gS RS "is

RS KS : Wi

Wy

1)

My ——

yy /

We i
\\ q f

fe Se bij ff

1 A no LAY
Mp, hy BA De

4

\ Ll
UMMA

(Wey

Fig. 131.—Teeth of Cochliodus contortus.
Carboniferous Limestone, Britain.

possess gills in their early

condition, if not throughout life; whilst they are separated from
the former by always possessing true lungs when adult, and
by the fact that the limbs (when present at all) are never in
the form of fins. ‘The Amphibians, therefore, are all water-
breathers when young, and have respiratory organs adapted
for an aquatic mode of life; whereas, when grown up, they
develop lungs, and with these the capacity for breathing air
directly. Some of them, like the Frogs and Newts, lose their
gills altogether on attaining the adult condition ; but others,
such as the living Proteus and Menobranchus, retain their gills
even after acquiring their lungs, and are thus fitted indiffer-
ently for an aquatic or terrestrial existence. The name of
“ Amphibia,” though applied to the whole class, is thus not
precisely appropriate except to these last-mentioned forms
(Gr. amphi, both; dz0s, life). The Amphibians also differ
amongst themselves according as to whether they keep per-
manently the long tail which they all possess when young (as
do the Newts and Salamanders), or lose this appendage when
grown up (as do the Frogs and Toads). Most of them have
naked skins, but a few living and many extinct forms have
hard structures in the shape of scales developed in the integu-
ment. All of them have well-ossified skeletons, though some
fossil types are partially deficient in this respect; and all of
them which possess limbs at all have these appendages sup-
ported by bones essentially similar to those found in the limbs
of the higher Vertebrates. All the Carboniferous Amphibians
belong to a group which has now wholly passed away—namely,
that of the Labyrinthodonts. In the marine strata which form
the base of the Carboniferous series these creatures have only
been recognised by their curious hand-shaped footprints, simila

14

190 HISTORICAL PALZZONTOLOGY.

in character to those which occur in the Triassic rocks, and which
will be subsequently spoken of under the name of Cheirotherium.
In the Coal-measures of Britain, the continent of Europe, and.
North America, however, many bones of these animals have
been found, and we are now tolerably well acquainted with a
considerable number of forms. All of them seem to have be-
longed to the division of Amphibians in which the long tail
of the young is permanently retained; and there is evidence
that some of them kept the gills also throughout life. The
skull is of the characteristic Amphibian type (fig. 132, @), with

Fig. 132.—a, Upper surface of the skull of Axthracosaurus Russelli, one-sixth of the
natural size; 4, Part of one of the teeth cut across, and highly magnified to show the
characteristic labyrinthine structure ; c, One of the integumentary shields or scales, one-
half of the natural size. Coal-measures, Northumberland. (After Atthey.)

two occipital condyles, and having its surface singularly pitted
and sculptured ; and the vertebrze are hollowed out at both
ends. The lower surface of the body was defended by an
armour of singular integumentary shields or scales (fig. 132, ¢);
and an extremely characteristic feature (from which the entire
group derives its name) is, that the walls of the teeth are deeply
folded, so as to give rise to an extraordinary “labyrinthine”
pattern when they are cut across (fig. 132, 4). Many of the
Carboniferous Labyrinthodonts are of no great size, some of

THE CARBONIFEROUS PERIOD, IQI

them very small, but others attain comparatively gigantic
dimensions, though all fall short in this respect of the huge
examples of this group which occur in the Trias. One of the
largest, and at the same time most characteristic, forms of the
Carboniferous series, is the genus Anthracosaurus, the skull of
which is here figured,

No remains of true Reptiles, Birds, or Quadrupeds have as
yet been certainly detected in the Carboniferous deposits in
any part of the world. It should, however, be mentioned,
that Professor Marsh, one of the highest authorities on the
subject, has described from the Coal-formation of Nova Scotia
certain vertebree which he believes to have belonged to a
marine reptile (Zosaurus Acadianus), allied to the great
Ichthyosaurt of the Lias. Up to this time no confirmation
of this determination has been obtained by the discovery of
other and more unquestionable remains, and it therefore
remains doubtful whether these bones of Hosaurus may not
really belong to large Labyrinthodonts.

LITERATURE.

The following list contains some of the more important of the original
sources of information to which the student of Carboniferous rocks and
fossils may refer :—

(1) ‘Geology of Yorkshire,’ vol. 11. ; ‘The Mountain Limestone Dis-

trict.’ John Phillips.

(2) ‘Siluria.” Sir Roderick Murchison.

(3) ‘ Memoirs of the Geological Survey of Great Britain and Ireland.’

(4) ‘Geological Report on Londonderry,’ &c. Portlock.

(5) ‘ Acadian Geology.’ Dawson.

(6) ‘ Geology of Iowa,’ vol. i. James Hall.

(7) ‘ Reports of the Geological Survey of Illinois’ (Geology and Pale-
ontology). Meek, Worthen, &c.

(8) ‘ Reports of the Geological Survey of Ohio’ (Geology and Palzon-
tology). Newberry, Cope, Meek, Hall, &c.

(9) ‘ Description des Animaux fossiles qui se trouvent dans le Terrain
Carbonifere de la Belgique,’ 1843 ; with subsequent monographs
on the genera Productus and Chonetes, on Crinotds, on Corals,
&c. De Koninck.

(10) ‘ Synopsis of the Carboniferous Fossils of Ireland.’ M ‘Coy.

(11) ‘ British Palzeozoic Fossils.’ M ‘Coy.

(12) ‘ Figures of Characteristic British Fossils.’ Baily.

(13) ‘ Catalogue of British Fossils.’ Morris.

(14) ‘ Monograph of the Carboniferous Brachiopoda of Britain’ (Paleeon-
tographical Society). Davidson.

(15) ‘ Monograph of the British Carboniferous Corals’ (Palzeontographical
Society). Milne-Edwards and Haime.

(16) ‘ Monograph of the Carboniferous Bivalve Entomostraca of Britain’
(Palzontographical Society). Rupert Jones, Kirkby, and George
S. Brady.

192 HISTORICAL PALAONTOLOGY.

(17) ‘ Monograph of the Carboniferous Foraminifera of Britain’ (Palzeon-
tographical Society). H. B. Brady.

(18) ‘*On the Carboniferous Fossils of the West of Scotland”—‘ Trans.
Geol. Soc.,’ of Glasgow, vol. iii, Supplement. Young and
Armstrong.

(19) ‘Poissons Fossiles.’ Agassiz.

(20) ‘‘Report on the Labyrinthodonts of the Coal-measures ” —‘ British
Association Report,’ 1873. L. C. Miall.

(21) ‘Introduction to the Study of Palzontological Botany.’ John
Hutton Balfour.

(22) ‘ Traité de Paléontologie Végétale.’ Schimper.

(23) ‘ Fossil Flora.’ Lindley and Hutton.

(24) ‘ Histoire des Végétaux Fossiles.’ Brongniart.

(25) ‘On Calamites and Calamodendron’ (Monographs of the Palzeonto-
graphical Society). Binney.

(26) ‘On the Structure of Fossii Plants found in the Carboniferous
Strata’ (Palzeontographical Society). Binney.

Also numerous memoirs by Huxley, Davidson, Martin Duncan, Profes-
sor Young, John Young, R. Etheridge, jun., Baily, Carruthers, Dawson,

Binney, Williamson, Hooker, Jukes, Geikie, Rupert Jones, Salter, and

many other British and foreign observers,

CHA PiDRIR: axe
THE PERMIAN PERIOD.

The Permian formation closes the long series of the Palzo-
zoic deposits, and may in some respects be considered as a
kind of appendix to the Carboniferous system, to which it can-
not be compared in importance, either as regards the actual
bulk of its sediments or the interest and variety of its life-
record. Consisting, as it does, largely of red rocks—sand-
stones and marls—for the most part singularly destitute of
organic remains, the Permian rocks have been regarded as a
lacustrine or fluviatile deposit; but the presence of well-devel-
oped limestones with indubitable marine remains entirely
negatives this view. It is, however, not improbable that we
are presented in the Permian formation, as known to us at
present, with a series of sediments laid down in inland seas of
great extent, due to the subsidence over large areas of the
vast land-surfaces of the Coal-measures. ‘This view, at any
rate, would explain some of the more puzzling physical char-
acters of the formation, and would not be definitely negatived
by any of its fossils.

A large portion of the Permian series, as already remarked,
consists of sandstones and marls, deeply reddened by peroxide

THE PERMIAN PERIOD. - 193

of iron, and often accompanied by beds of gypsum or deposits
of salt. In strata of this nature few or no fossils are found ;
but their shallow-water origin is sufficiently proved by the
presence of the footprints of terrestrial animals, accompanied
in some cases by well-defined “ ripple-marks.” Along with
these are occasionally found massive breccias, holding larger
or smaller blocks derived from the older formations; and these
have been supposed to represent an old “ boulder-clay,” and
thus to indicate the prevalence of an arctic climate. Beds of
this nature must also have been deposited in shallow water.
In all regions, however, where the Permian formation is well
developed, one of its most characteristic members is a Mag-
nesian limestone, often highly and fantastically concretionary,
but containing numerous remains of genuine marine animals,
and clearly indicating that it was deposited beneath a mod-
erate depth of salt water.

It is not necessary to consider here whether this formation
can be retained as a distinct division of the geological series.
The name of Permian was given to it by Sir Roderick Murchi-
son, from the province of Perm in Russia, where rocks of this
age are extensively developed. Formerly these rocks were
grouped with the succeeding formation of the Trias under the
common name of “New Red Sandstone.” This name was
given them because they contain a good deal of red sandstone,
and because they are superior to the Carboniferous rocks,
while the Old Red Sandstone is inferior. Nowadays, how-
ever, the term “‘ New Red Sandstone” is rarely employed,
unless it be for red sandstones and associated rocks, which
are seen to overlie the Coal-measures, but which contain no
fossils by which their exact age may be made out. Under
these circumstances, it is sometimes convenient to employ the
term ‘“‘ New Red Sandstone.” The New Red, however, of the
older geologists, is now broken up into the two formations of
the Permian and Triassic rocks—the former being usually con-
sidered as the top of the Paleozoic series, and the latter con-
stituting the base of the Mesozoic.

In many instances, the Permian rocks are seen to repose
unconformably upon the underlying Carboniferous, from which
they can in addition be readily separated by their lithological
characters. In other instances, however, the Coal-measures
terminate upwards in red rocks, not distinguishable by their
mineral characters from the Permian; and in other cases no
physical discordance between the Carboniferous and Per-
mian strata can be detected. As a general rule, also, the
Permian rocks appear to pass upwards conformably into the

194 HISTORICAL PALAZONTOLOGY.

Trias. The division, therefore, between the Permian and Tri- .
assic rocks, and consequently between the Paleozoic and Me-
sozoic series, is not founded upon any conspicuous or universal
physical break, but upon the difference in life which is ob-
served in comparing the marine animals of the Carboniferous
and Permian with those of the Trias. It is to be observed, how-
ever, that this difference can be solely due to the fact that the
Magnesian Limestone of the Permian series presents us with
only a small, and not a typical, portion of the marine deposits
which must have been accumulated in some area at present
unknown to us during the period which elapsed between the
formation of the great marine limestones of the Lower Carbon-
iferous and the open-sea and likewise calcareous sediments of
the Middle Tnas.

The Permian rocks exhibit their most typical features in
Russia and Germany, though they are very well developed in
parts of Britain, and they occur in North America. When
well developed, they exhibit three main divisions: a lower set
of sandstones, a middle group, generally calcareous, and an
upper series of sandstones, constituting respectively the Lower,
Middle, and Upper Permians.

In Russia, Germany, and Britain, the Permian rocks con-
sist of the following members :—

1. The Lower Permians, consisting mainly of a great series
of sandstones, of different colours, but usually red. The base
of this series is often constituted by massive breccias with
included fragments of the older rocks, upon which they may
happen to repose ; and similar breccias sometimes occur in
the upper portion of the series as well. The thickness of this
group varies a good deal, but may amount to 3000 or 4000
fect.

2. The Middle Permians, consisting, in their typical de-
velopment, of laminated marls, or ‘ marl-slate,’ surmounted
by beds of magnesian limestone (the ‘‘ Zechstein ” of the Ger-
man geologists). Sometimes the limestones are degenerate or
wholly deficient, and the series may consist of sandy shales
and gypsiferous clays. ‘The magnesian limestone, however, of
the Middle Permians is, as a rule, so well marked a feature
that it was long spoken of as he Magnesian Limestone.

3. The Upper Permians, consisting of a series of sandstones
and shales, or of red or mottled marls, often gypsiferous, and
sometimes including beds of limestone.

In North America, the Permian rocks appear to be confined
to the region west of the Mississippi, being especially well de-
veloped in | Kansas. Their exact limits have not as yet been

THE PERMIAN PERIOD. 195

made out, and their total thickness is not more than a few
hundred feet. They consist of sandstones, conglomerates,
limestones, marls, and beds of gypsum.

The following diagrammatic section shows the general
sequence of the Permian deposits in the north of England,
where the series is extensively developed (fig. 133) :—

GENERALISED SECTION OF THE PERMIAN ROCKS
IN- THE NORTH OF ENGLAND.

Bige133)

Z
w <
a = Upper Red Sandstones
A of .
25 and Marls.
=
Zz
s
S
= :
Stevia HN eS Ma ane shoul eons - Magnesian Limestone,
=)
=
a
A
a SS
= ------ Marl Slate.
Z
=
3
a ___.__ § Lower Red Sandstones
= and Breccias.
4
is}
=
ro)
~

SOV OV ONOmOnomOn©
< 9 G00 0 ©
SS pases — Coal-measures.

The record of the “fe of the Permian period is but a scanty
one, owing doubtless to the special peculiarities of such of the

196 HISTORICAL PALAZZXONTOLOGY.

deposits of this age with which we are as yet acquainted. Red
rocks are, as a general rule, more or less completely unfossil-
iferous, and sediments of this nature are highly characteristic of
the Permian. Similarly, magnesian limestones are rarely as
highly charged with organic remains as is the case with normal
calcareous deposits, especially when they have been subjected
to concretionary action, as is observable to such a marked ex-
tent in the Permian limestones. Nevertheless, much interest
is attached to the organic remains, as marking a kind of transi-
tion-period between the Palzozoic and Mesozoic epochs.

The plants of the Permian period, as a whole, have a dis-
tinctly Palzeozoic aspect, and are far more nearly allied to those
of the Coal-measures than they are to those of the earlier
Secondary rocks; though the Permian sfeczes are mostly dis-
tinct from the Carboniferous, and there are some new genera.
Thus, we find species of Lepidodendron, Calamites, E-quitsetites,
Asterophyllites, Annularia, and other highly characteristic
Carboniferous genera. On the other hand, the Szgz//ariozds of
the Coal seem to have finally disappeared at the close of the
Carboniferous period. Ferns are abundant in the Permian
rocks, and belong for the most part to the well-known Carbon-
iferous genera Alethopteris, Neuropteris, Sphenopteris, and Pecop-
terts. There are also Tree-ferns referable to the ancient genus
Psaronius. The Conzfers of the Permian period are numerous,
and belong in part to Carboniferous genera. . A characteristic
genus, however, is Wadchia (fig. 134), distinguished by its lax

Fig. 134.—Walchia pintformis, from the Permian of Saxony.
a, Branch; 6, Twig. (After Gutbier.)

short leaves. This genus, though not exclusively Permian, is
mainly so, the best-known species being the W. piniformis.
Here, also, we meet with Conifers which produce true cones,
and which differ, therefore, in an important degree from the

THE PERMIAN PERIOD. 197

Taxoid Conifers of the Coal-measures. Besides Wadlchia, a
characteristic form of these is the UWmania selaginotdes, which
occurs in the Magnesian Limestone of Durham, the Middle
Permian of Westmorland, and the ‘“ Kupfer-schiefer” of Ger-
many. ‘The group of the Cycaids, which we shall subsequently
find to be so characteristic of the vegetation of the Secondary
period, is, on the other hand, only doubtfully represented in
the Permian deposits by the singular genus Veggerathia.

The /rotozoans of the Permian rocks are few in number, and
for the most part imperfectly known. A few Foraminifera have
been obtained from the Magnesian Limestone of England,
and the same formation has yielded some ill- understood
Sponges. It does not seem, however, altogether impossible
that some of the singular ‘“‘ concretions” of this formation may
ultimately prove to have an organic structure, though others
would appear to be clearly of purely inorganic origin. From
the Permian of Saxony, Professor Geinitz has described two
species of Spongillopsis, which he believes to be most nearly
allied to the existing fresh-water Sponges (Sfongil/a). ‘This
observation has an interest as bearing upon the mode of de-
position and origin of the Permian sediments.

The Cwlenterates are represented in the Permian by but a
few Corals. These belong partly to the 7abulate and partly
to the Rugose division; but the latter great group, so abun-
dantly represented in Silurian, Devonian, and Carboniferous
seas, Is now extraordinarily reduced in numbers, the British
strata of this age yielding only species of the single genus
Polycelia. So far, therefore, as at present known, all the
characteristic genera of the Rugose Corals of the Carboniferous
had become extinct before the deposition of the limestones of
the Middle Permian.

The Echinoderms are represented by a few Crznozds, and by a
Sea-urchin belonging to the genus Hoczdaris. ‘The latter genus
is nearly allied to the Avcheocidaris of the Carboniferous, so
that this Permian form belongs to a characteristically Palaeozoic
type.

A few Annelides (Spirorbis, Vermilia, &c.) have been de-
scribed, but are. of no special importance. Amongst the
Crustaceans, however, we have to note the total absence of
the great Palzozoic group of the Z7z/obites ; whilst the little
Ostracoda and Phyllopods still continue to be represented.
We have also to note the first appearance here of the “ Short-
tailed ” Decapods or Crabs (4rachyura), the highest of all the
groups of Crustacea, in the person of Hemitrochiscus paradoxus,
an extremely minute Crab from the Permian of Germany.

198 HISTORICAL PALAEONTOLOGY.

Amongst the JZod/usca, the remains of Folyzoa may fairly be
said to be amongst the most abundant of all the fossils of the
Permian formation. The principal forms of these are the
fronds of the Lace-corals (Fenestella, Retepora, and Synocladia),
which are very abundant in the Magnesian Limestone of the
north of England, and belong to various highly characteristic
species (such as Fenestella retiformis, Retepora E-hrenbergi, and
Synocladia virgulacea). The Brachiopoda are also represented
in moderate numbers in the Permian. Along with species of
the persistent genera Duscina, Crania, and Lingula, we still
meet with representatives of the old groups Spzvifera, Athyris,
and Streptorhynchus; and the Carboniferous Producte yet
survive under well-marked and characteristic types, though in
much-diminished numbers. ‘The species of Brachiopods here
figured (fig. 135) are characteristic of the Magnesian Limestone
in Britain and of the corresponding strata on the Continent.

Fig. 135.—Brachiopods of the Permian formation. a, Producta horrida; 6b, Lingula
Credneri ; c, Terebratula elongata; d and e, Camarophoria globulina. (After King.)

Upon the whole, the most characteristic Permian Brachiopods
belong to the genera Producta, Strophalosia, and Camaro-
phoria.

The Livalves (Lamellibranchiata) have a tolerably varied
development in the Permian rocks; but nearly all the old
types, except some of those which occur in the Carboniferous,
have now disappeared. The principal Permian Bivalves
belong to the groups of the Pearl Oysters (Aviculide) and the
Trigoniade, represented by genera such as. Bakewellia and
Schizodus; the true Mussels (AZvtz/ide), represented by species
which have been referred to AZpt/us itself; and the Arks
(Arcade), represented by species of the genera 47ca (fig. 136)
and 4yssoarca. The first and last of these three families have
a very ancient origin; but the family of the 77zgonzade, though

a

THE PERMIAN PERIOD. 199

feebly represented at the present day, is one which attained its
maximum development in the Mesozoic period.

The Univalves (Gasteropoda) are rare, and do not demand
special notice. It may be ob-
served, however, that the Palzo-
zoic genera Luomphalus, Mur-
chisonia, Loxonema, and Macro-
cheilus are still in existence, to-
gether with the persistent genus
Pleurotomaria. Pteropods of the
old genera Zheca and Conula-
via have been discovered ; but
the first of these characteristi-
cally Palzozoic types finally
dies out here, and the second
only survives but a short time
longer. Lastly, a few Cephalopods have been found, still wholly
referable to the Tetrabranchiate group, and belonging to the old
genera Orthoceras and Cyrtoceras and the long-lived Wautilus.

Amongst Vertebrates, we meet in the Permian period not
only with the remains of Fishes and Amphibians, but also, for
the first time, with true Reptiles. The fishes are mainly
- Ganoids, though there are also ~emains of a few Cestraciont

Fig. 136.—A7ca antiqua. Permian.

Fig. 137.—Platysomus gibbosus, a ‘‘heterocercal” Ganoid, from the
Middle Permian of Russia.

Sharks. Not only are the Ganozds still the predominant group
of Fishes, but all the known forms possess the unsymmetrical
(‘‘heterocercal”) tail which is so characteristic of the Palaeozoic
Ganoids. Most of the remains of the Permian Fishes have
been obtained from the “ Marl-slate” of Durham and the
corresponding “‘ Kupfer-schiefer” of Germany, on the horizon

200 HISTORICAL PALAZONTOLOGY.

of the Middle Permian; and the principal genera of the
Ganoids are Paleoniscus and Platysomus (fig. 137).

The Amphibians of the Permian period belong principally
to the order of the Zadyrinthodonts, which commenced to be
represented in the Carboniferous, and has a large development
in the Trias. Under the name, however, of Paleosiren Beinertz,
Professor Geinitz has described an Amphibian from the Lower
Permian of Germany, which he believes to be most nearly
allied to the existing “ Mud-eel” (Szven lacertina) of North
America, and therefore to be related to the Newts and Sala-
manders ( Urodela).

Finally, we meet in the Permian deposits with the first un-
doubted remains of true Reptiles. These are distinguished, as
a class, from the Amphibians, by the fact that they are air-
breathers throughout the whole of their'life, and therefore are
at no time provided with gills; whilst they are exempt from
that metamorphosis which all the AmpAzbza undergo in early
life, consequent upon their transition from an aquatic to a
more or less purely aerial mode of respiration. ‘Their skel-
eton is well ossified ; they usually have horny or bony plates,
singly or in combination, developed in the skin; and their
limbs (when present) are never either in the form of fs or
wings, though sometimes capable of acting in either of these
capacities, and liable to great modifications of form and struc-
ture. Though there can be no doubt whatever as to the occur-
rence of genuine Reptiles in deposits of unquestionable Per-
mian age, there is still uncertainty as to the precise number
of types which may have existed at this period. This uncer-
tainty arises partly from the difficulty of deciding in all cases
whether a given bone be truely Labyrinthodont or Reptilian,
but more especially from the confusion which exists at pres-
ent between the Permian and the overlying Triassic deposits.
Thus there are various deposits in different regions which
have yielded the remains of: Reptiles, and which cannot in
the meanwhile be definitely referred either to the Permian
series or to the Trias by clear stratigraphical or paleonto-
logical evidence. All that can be done in such cases is to be
guided by the characters of the Reptiles themselves, and to
judge by their affinities to remains from known Triassic or Per-
mian rocks to which of these formations the beds containing
them should be referred ; but it is obvious that this method
of procedure is seriously liable to lead to error. In accor-
dance, however, with this, the only available mode of deter-
mination in some cases, the remains of Zhecodontosaurus and
faleosaurus discovered in the dolomitic conglomerates near

THE PERMIAN PERIOD. 201

Bristol will be considered as Triassic, thus leaving Protoro-
saurus * as the principal and most important representative of

8

Fig. 138.—Pvrotovosaurus Speneri, Middle Permian, Thuringia, reduced in size.
(After Von Meyer.) [Copied from Dana. ]

the Permian Reptiles.t The type-species of the genus Pro-
torosaurus isthe P. Speneri (fig. 138) of the “ Kupfer-schiefer” of

* Though commonly spelt as above, it is probable that the name of this
Lizard was really intended to have been /roterosaurus—from the Greek
proteros, first ; and saura, lizard: and this spelling is followed by many
writers.

+ In an extremely able paper upon the subject (Quart. Journ. Geol.
Soc., vol. xxvi.), Mr Etheridge has shown that there are good physical
grounds for regarding the dolomitic conglomerate of Bristol as of Triassic
age, and as probably corresponding in time with the Muschelkalk of the

ontinent.

202 HISTORICAL PALAZONTOLOGY.

Thuringia, but other allied species have been detected in the
Middle Permian of Germany and the north of England. This
Reptile attained a length of from three to four feet ; and it has
been generally referred to the group of the Lizards (Zacertclia),
to which it is most nearly allied in its general structure, at the
same time that it differs from all existing members of this group
in the fact that its numerous conical and pointed teeth were
implanted in distinct sockets in the jaws—this being a Croco-
dilian character. In other respects, however, Protorosaurus
approximates closely to the living Monitors ( Varanide) ; and
the fact that the bodies of the vertebree are slightly cupped or
hollowed out at the ends would lead to the belief that the
animal was aquatic in its habits. At the same time, the
structure of the hind-limbs and their bony supports proves
clearly that it must have also possessed the power of progres-
sion upon the land. Various other Reptilian bones have been
described from the Permian formation, of which some are pro-
bably really referable to Labyrinthodonts, whilst others are
regarded by Professor Owen as referable to the order of the
‘“Theriodonts,” in which the teeth are implanted in sockets,
and resemble those of carnivorous quadrupeds in consisting
of three groups in each jaw (namely, incisors, canines, and
molars). Lastly, in red sandstones of Permian age in Dum-
friesshire have been discovered the tracks of what would ap-
pear to have been Chelonians (Tortoises and Turtles); but it
would not be safe to accept this conclusion as certain upon the
evidence of footprints alone. The Chelichnus Duncani, how-
ever, described by Sir William Jardine in his magnificent work
on the ‘Ichnology of Annandale,’ bears a great resemblance
to the track of a Turtle.

No remains of Birds or Quadrupeds have hitherto been
detected in deposits of Permian age.

LITERATURE.

The following works may be consulted by the student with regard to the
Permian formation and its fossils :—

(1) ‘*On the Geological Relations and Internal Structure of the Magne-
sian Limestone and the Lower Portions of the New Red Sand-
stone Series, &c.”—‘ Trans. Geol. Soc.,’ ser. 2, vol. ili. Sedg-
wick.

2) ‘The Geology of Russia in Europe.’ Murchison, De Verneuil, and
Von Keyserling.

(3) ‘Siluria.’ Murchison.

(4) ‘ Permische System in Sachsen.’ Geinitz and Gutbier.

(5) ‘Die Versteinerungen des Deutschen Zechsteingebirges.’ Geinitz.
(6) ‘Die Animalischen Ueberreste der Dyas.’ Geinitz.

*

HE LRIASSICG PERIOD: 203

(7) ‘Monograph of the Permian Fossils of England’ (Palzeontographical
Society). Kung.

(8) ‘Monograph of the Permian Brachiopoda of Britain’ (Palzeonto-
graphical Society). Davidson.

(9) ‘*Onthe Permian Rocks of the North-West of England and their
Extension into Scotland’”’—‘ Quart. Journ. Geol. Soc.,’ vol. xx.
Murchison and Harkness.

(10) ‘Catalogue of the Fossils of the Permian System of the Counties of
Northumberland and Durham.’ Howse.

(11) ‘ Petrefacta Germaniz.’ Goldfuss.

(12) ‘ Beitrage zur Petrefaktenkunde.’ Miinster..

(13) ‘Ein Beitrag zur Paleeontologie des Deutschen Zechsteingebirges.’
Von Schauroth.

(14) ‘Saurier aus dem Kupfer-schiefer der Zechstein-formation.’ Von
Meyer.

(15) EViaaaal of Paleontology.’ Owen.

(16) ‘Recherches sur les Poissons Fossiles.? Agassiz.

(17) ‘Ichnology of Annandale.’ Sir William Jardine.

(18) ‘Die Fossile Flora der Permischen Formation.’ Gceppert.

(19) ‘Genera et Species Plantarum Fossilium.’ Unger.

(20) ‘‘Onthe Red Rocks of England of older Date than the Trias”
—‘ Quart. Journ. Geol. Soc.,’ vol. xxvii. Ramsay.

CPCAGP ae TRE Xan
MELE TIAA S SLO Eh OD:

We come now to the consideration of the great A/esozozc, or
Secondary series of formations, consisting, in ascending order,
of the Triassic, Jurassic, and Cretaceous systems. ‘The Trias-
sic group forms the base of the Mesozoic series, and corre-
sponds with the higher portion of the New Red Sandstone of
the older geologists. Like the Permian rocks, and as implied
by its name, the Z7zas admits of a subdivision into three
groups—a Lower, Middle, and Upper Trias. Of these sub-
divisions the middle one is wanting in Britain; and all have
received German names, being more largely and typically de-
veloped in Germany than in any other country. Thus, the
Lower Trias is known as the Bunter Sandstein ; the Middle
Tnias is called the MZuschelkalk ; and the Upper Trias 1s known
as the Keuper.

I. The lowest division of the Trias is known as the Bunter
Sandstein (the Gres bigarré of the French), from the generally
variegated colours of the beds which compose it (German,
bunt, variegated). The Bunter Sandstein of the continent of
Europe consists of red and white sandstones, with red clays,

204 HISTORICAL PALAZZONTOLOGY.
and thin limestones, the whole attaining a thickness of about
1500 feet. The term “marl” is very generally employed to
designate the clays of the Lower and Upper Trias; but the
term is Inappropriate, as they may contain no lime, and are.
therefore not always genuine marls. In Bnitain the Bunter
Sandstein consists of red and mottled sandstones, with uncon-
solidated conglomerates, or ‘‘ pebble-beds,” the whole having
a thickness of 1000 to 2000 feet. The Bunter Sandstein, as
a rule, is very barren of fossils.

Ii. The Middle Trias is not developed in Britain, but it
is largely developed in Germany, where it constitutes what is
known as the Wuschelkalk (Germ. Mluschel, mussel ; Radlk, lime-
stone), from the abundance of fossil shells which it contains.
The Muschelkalk (the Cadlcazre coguillier of the French) consists
of compact grey or yellowish limestones, sometimes dolomitic,
and including occasional beds of gypsum and rock-salt.

III. The Upper Trias, or Keupfer (the A/arnes zrisées of the
French), as it is generally called, occurs in England; but is
not so well developed as it is in Germany. In Britain, the
Keuper is 1000 feet or more in thickness, and consists of white
and brown sandstones, with red marls, the whole topped by
red clays with rock-salt and gypsum.

The Keuper in Britain is extremely unfossiliferous ; but it
passes upwards with perfect conformity into a very remarkable
group of beds, at one time classed with the Lias, and now
known under the names of the Penarth beds (from Penarth, in
Glamorganshire), the Rheetic beds (from the Rhezetic Alps), or
the Avicula contorta beds (from the occurrence in them of
great numbers of this peculiar Bivalve). These singular beds
have been variously regarded as the highest beds of the Trias,
or the lowest beds of the Lias, or as an intermediate group.
The phenomena observed on the Continent, however, render
it best to consider them as Triassic, as they certainly agree
with the so-called Upper St Cassian or Kossen beds which
form the top of the Trias in the Austrian Alps.

The Penarth beds occur in Glamorganshire, Gloucestershire,
Warwickshire, Staffordshire, and the north of Ireland; and
they generally consist of a small thickness of grey marls, white
limestones, and black shales, surmounted conformably by the
lowest beds of the Lias. The most characteristic fossils which
they contain are the three Bivalves Cardium Rheticum, Avicula
contorta, and Fecten Valoniensis ; but they have yielded many |
other fossils, amongst which the most important are the re-
mains of Fishes and small Mammals (J@crolestes).

In the Austrian Alps the Trias terminates upwards in an

-

THE TRIASSIC PERIOD. 205

extraordinary series of fossiliferous beds, replete with marine
fossils. Sir Charles Lyell gives the following table of these
remarkable deposits :—

Strata below the Lias in the Austrian Alps, in descending order.

Grey and black limestone, with calcareous
marls having a thickness of about 50
feet. Among the fossils, Brachiopoda
1. Koessen beds. very ia ea a species com-
mon to the genuine Lias; many pecu-
SO ha oe spent liar. <Avicula contorta, LPecten Valo-
and Merian.) niensis, Cardium Rheticum, <Avicula
neguivaluis, Spirifer Muinstert, Dav.
Strata containing the above fossils al-
ternate with the Dachstein beds, lying
next below.

White or greyish limestone, often in beds
three or four feet thick. Total thick-
ness of the formation above 2000 feet.

; Upper part fossiliferous, with some
3 strata composed of corals (Lithoden-
2. Dachstein beds. dron.) ier portion ar fossils.
Among the characteristic shells are He-
micardium Wulfent, Megalodon triqueter,
and other large bivalves.

Red, pink, or white marbles, from 800 to
1000 feet in thickness, containing more
than 800 species of marine fossils, for
3. Hallstadt beds the most part mollusca. Many species
(or St Cassian). of Orthoceras. True Ammonites, besides
Ceratites and Gonzatites, Belemnites (rare),
Porcellia, Pleurotomaria, Trochus, Mono-
tis salinarta, &c.

A. Black and grey lime-

4. A. Guttenstein beds. stone 150 feet thick, al- | Among the fossils

B. Werfen beds, base of ternating with the un- are Ceratites

Upper Trias 2 derlyme Wierfed beds, \) ee 7

Lower Trias of some} B. Red and green shale sis, Naticella
geologists. and sandstone, with costata, &c.

salt and gypsum.

In the United States, rocks of Triassic age occur in several
areas between the Appalachians and the Atlantic seaboard ;
but they show no such triple division as in Germany, and their
exact place in the system is uncertain. The rocks of these
areas consist of red sandstones, sometimes shaly or conglomer-
atic, occasionally with beds of impure limestone. Other more
extensive areas where Triassic rocks appear at the surface, are
found west of the Mississippi, on the slopes of the Rocky Moun-
tains, where the beds consist of sandstones and gypsiferous

15

206 HISTORICAL PALAZON TOLOGY.

marls. The American Trias is chiefly remarkable for having
yielded the remains of a small Marsupial (Dromatherium), and —
numerous footprints, which have generally been referred to
Birds (Brontozoum), along with the tracks of undoubted Rep-
tiles (Ofozoum, Anisopus, &c.)

The subjoined section (fig. 139) expresses, in a diagram-
matic manner, the general sequence of the Triassic rocks when
fully developed, as, for example, in the Bavarian Alps :—

GENERALISED SECTION OF THE TRIASSIC ROCKS OF
CENTRAL EUROPE.

des Keuper (Késsen or
Rheetic beds, and Dach-
( stein beds).

Middle Keuper (Hallstadt
or St Cassian beds).

UPPER TRIAS,

Lower Keuper (Keuper
Sandstones proper).

---20-- Muschelkalk.

MIDDLE
TRIAS

Bunter Sandstein. (Gutten-
“~~ 4 stein and Werfen beds ?)

LOWER TRIAS.

With regard to the // of the Triassic period, we have to

THE TRIASSIC PERIOD. 207

notice a difference as concerns the different members of the
group similar to that which has been already mentioned in
connection with the Permian formation. The arenaceous
deposits of the series, namely, resemble those of the Permian,
not only in being commonly red or variegated in their colour,
but also in their conspicuous paucity of organic remains.
They for the most part are either wholly unfossiliferous, or
they contain the remains of plants or the bones of reptiles,
such as may easily have been drifted from some neighbouring
shore. ‘The few fossils which may be considered as properly
belonging to these deposits are chiefly Crustaceans (£s¢heria)
or Fishes, which may well have lived in the waters of estuaries
or vast inland seas. We may therefore conclude, with con-
siderable probability, that the barren sandy and marly accumu-
lations of the Bunter Sandstein and Lower Keuper were not
laid down in an open sea, but are probably brackish-water —
deposits, formed in estuaries or land-locked bodies of salt
water. This at any rate would appear to be the case as regards
these members of the series as developed in Britain and in
their typical areas on the continent of Europe; and the origin
of most of the North American Trias would appear to be
much the same. Whether this view be correct or not, it is
certain that the beds in question were laid down in shallow
water, and in the immediate vicinity of /and, as shown by the
numerous drifted plants which they contain and the common
occurrence in them of the footprints of air-breathing animals
(Birds, Reptiles, and Amphibians). On the other hand, the
middle and highest members of the Trias are largely calca-
reous, and are replete with the remains of undoubted marine
animals. There cannot, therefore, be the smallest doubt but
that the Muschelkalk and the Rheetic or Kossen beds were
slowly accumulated in an open sea, of at least a moderate
depth ; and they have preserved for us a very considerable
selection from the marine fauna of the Triassic period.

The plants of the Trias are, on the whole, as distinctively
Mesozoic in their aspect as those of the Permian are Paleo-
zoic. In spite, therefore, of the great difficulty which is ex-
perienced in effecting a satisfactory stratigraphical separation
between the Permian and the Trias, we have in this fact a
proof that the two formations were divided by an interval of
time sufficient to allow of enormous changes in the terrestrial
vegetation of the world. The Lepidodendroids, Asterophyllites,
and Annularie, of the Coal and Permian formations, have now
apparently wholly disappeared ; and the Triassic flora consists
mainly of Ferns, Cycads, and Conifers, of which only the two

208 HISTORICAL PALAEONTOLOGY.

last need special notice. ‘The Cycads (fig. 140) are true exo-
genous plants, which in general form and habit of growth pre-

Fig. 140.—Zamiia spirals, a living Cycad, Australia.

sent considerable resemblance to young Palms, but which in
reality are most nearly related to the Pines and Firs (Cozzfere).
The trunk is unbranched, often much shortened, and bears a
crown of feathery pinnate fronds. The leaves are usually
“‘circinate”— they unroll in expanding, like the fronds of
ferns. The seeds are not protected by a seed-vessel, but are
borne upon the edge of altered leaves, or are carried on the
scales of acone. All the living species of Cycads are natives
of warm countries, such as South America, the West Indies,
Japan, Australia, Southern Asia, and South Africa. The
remains of Cycads, as we have seen, are not known to occur
in the Coal formation, or only to a very limited extent towards
its close ; nor are they known with certainty as occurring in
Permian deposits. In the Triassic period, however, the re-
mains of Cycads belonging to such genera as Prerophyllum
(fig. 141, 6), Zamites, and Podozamites (fig. 141, ¢c), are suffi-
ciently abundant to constitute quite a marked feature in the
vegetation ; and they continue to be abundantly represented
throughout the whole Mesozoic series. The name “ Age of
Cycads,” as applied to the Secondary epoch, is therefore,
from a botanical point of view, an extremely appropriate one.
The Conifers of the Trias are not uncommon, the principal
form being Vo/tzza (fig. 141, a), which possesses some peculiar
characters, but would appear to be most nearly related to the
recent Cypresses.

As regards the /nvertebrate animals of the Trias, our know-
ledge is still principally derived from the calcareous beds
which constitute the centre of the system (the Muschelkalk)

THE TRIASSIC: PERIOD: 209

on the continent of Europe, and from the St Cassian and
Rheetic beds still higher in the series; whilst some of the

Fig. 141.—Triassic Conifers and Cycads. a, Voltzia (Schizoneura) heterophylla, por-
tion of a branch, Europe and America; 4, Part of the frond of Pterophyllum Fegert,
Europe; c, Part of the frond of Podozamites lanceolatus, America.

Tnassic strata of California and Nevada have likewise yielded
numerous remains of marine Invertebrates. The Protozoans
are represented by Foraminifera and Sponges, and the Celen-
terates by a small number of Corals; but these require no
special notice. It may be mentioned, however, that the great
Paleozoic group of the Augose corals has no known repre-
sentative here, its place being taken by corals of Secondary
type (such as Montlvaltia, Synastrea, &c.)

The Lchinoderms are represented principally by Cvinozds,
the remains of which are extremely abundant in some of the
limestones. The best-known species is the famous ‘“ Lily-
Encrinite” (Lucrinus lilitformis, fig. 142), which is character-

Z1O HISTORICAL PALAZONTOLOGY. :

istic of the Muschelkalk. In this beautiful species, the flower-
like head is supported upon a rounded stem, the joints of
which are elaborately articulated with one
another; and the fringed arms are com-
posed each of a double series of alter-
nating calcareous pieces. The Paleozoic
Urchins, with their supernumerary rows of
plates, the Cystideans, and the Pentremites
have finally disappeared; but both Star-
fishes and Brittle-stars continue to be rep-
resented. One of the latter—namely, the
A spidura loricata of Goldfuss (fig. 143)—is

»

BUTes =
: L SS ELE Ae
Si oO Oe ook SAAS

Fig. 143.—Astidura loricata, a Triassic Ophiuroid.
Muschelkalk, Germany.

highly characteristic of the Muschelkalk.
The remains of Articulate Animals are
not very abundant in the Trias, if we except
the bivalved cases of the little Water-fleas
(Ostracoda), which are occasionally very
plentiful. There are also many species
— of the horny, concentrically-striated valves
Fig. 142.—Head and of the Zstheri@ (see fig. 122, 6), which
ape tober Oe eeu might easily be taken for small Bivalve
The lower figure shows Molluscs. The “ Long-tailed” Decapods,
the articulating surface :
of one of the jointsofthe Of the type of the Lobster, are not with-
cglumn._ Muschelkalk, ~~ out examples, but they become much more
numerous in the succeeding Jurassic pe-
riod. Remains of insects have also been discovered.
Amongst the J/od//usca we have to note the disappearance,
amongst the lower groups, of many characteristic Palzeozoic
types. Amongst the VPolyzoans, the characteristic ‘‘ Lace-

corals,’ Fenestella, Retepora,* Synocladia, Polypora, &c., have

* The genus Refefora is really a recent one, represented by living forms ;
and the so-called Retepore of the Paleozoic rocks should properly receive
another name (PAyllofora), as being of a different nature. The name
Ketepora has been here retained for these old forms simply in accordance
with general usage.

THE TRIASSIC PERIOD. 211

become apparently extinct. The same is true of many of the
ancient types of Srachiopods, and conspicuously so of the
great family of the Productide, which played such an important
part in the seas of the Carboniferous and Permian periods.
Bivalves (Lamellibranchiata) and Univalves (Gasteropoda)
are well represented in the marine beds of the Trias, and
some of the former are particularly characteristic either of the
formation as a whole or of minor subdivisions of it. A few of
these characteristic species are figured in the accompanying
illustration (fig. 144). Buivalve shells of the genera Daonella
(fig. 144, 2) and Halobia (Monotis) are very abundant, and are

Fig. 144. Triassic Lamellibranchs. @, Daonella (Halobia) Lommelli; 6, Pecten
Valoniensis; c, Myophoria lineata; d, Cardium Rheticum; e, Avicula contorta :
Jj Avicula socialis.

found in the Triassic strata of almost all regions. These
groups belong to the family of the Pearl-oysters (Aviculide),
and are singular from the striking resemblance borne by some
of their included forms to the Strophomene amongst the Lamp-
shells, though, of course, no real relation exists between the
two. The little Pearl-oyster, Avicula soctalis (fig. 144, f), is
found throughout the greater part of the Triassic series, and is
especially abundant in the Muschelkalk. The genus J/yo-
Pphoria (fig. 144, c), belonging to the Z7zgonzad@, and related
therefore to the Permian Schizodus, is characteristically Trias-
sic, many species of the genus being known in deposits of this
age. Lastly, the so-called “‘ Rhetic” or “ Kossen” beds are

212 HISTORICAL PALZONTOLOGY.

characterised by the occurrence in them of the Scaliop, Pecten
Valoniensts (fig. 144, 6); the small Cockle, Cardium Rheticum
(fig. 144, @); and the curiously-twisted Pearl-oyster, dvzcula
contorta (fig. 144, e)—this last Bivalve being so abundant that
the strata in question are often spoken of as the “ Avicula
contorta beds.” .
Passing over the groups of the Heteropods and Pteropods,
we have to notice the Cephalopoda, which are represented in
the Trias not only by the chambered shells of Zetvrabranchiates,
but also, for the first time, by the internal skeletons of Dzbran-
chiate forms. ‘The Trias, therefore, marks the first recognised
appearance of true Cuttle-fishes. All the known examples of
these belong to the great Mesozoic group of the Belemnitide ;
and as this family is much more largely developed in the suc-
ceeding Jurassic period, the consideration of its characters
will be deferred till that formation is treated of. Amongst the
chambered Cefhalopods we find quite a number of the Pale-
ozoic Orthoceratites, some of them of considerable size, along
with the ancient Cyz¢oceras and Gonzatites ; and these old types,
singularly enough, occur in the higher portion of the Trias
(St Cassian beds), but have, for some unexplained reason, not
yet been recognised in the lower and equally fossiliferous
formation of the Muschelkalk. Along with these we meet for
the first time with true Ammonites, which fill such an extensive
place in the Jurassic
seas, and which will
be spoken of here-
after. The form, how-
ever, which is most
characteristic of the
Trias is Ceratites (fig.
145). In this genus
the shell is curved into
a flat spiral, the volu-
tions of which are in
contact ; and it further
agrees with both Go-
niatites and Ammonites
in the fact that the

Fig. 145.—Ceratites nodosus, viewed from the side ane
and from behind. Muschelkalk. septa or partitions be-

tween the air-cham-
bers are not simple and plain (as in the Vau¢iZus and its allies),
but are folded and bent as they approach the outer wall of the
shell. In the Gondatite these foldings of the septa are of a simply
lobed or angulated nature, and in the Ammonite they are ex-

THE TRIASSIC PERIOD. 213

tremely complex; whilst in the Ceratife there is an inter-
mediate state of things, the special feature of which is, that
those foldings which are turned towards the mouth of the
shell are merely rounded, whereas those which are turned
away from the mouth are characteristically toothed. The
genus Ceratites, though principally Triassic, has recently been
recognised in strata of Carboniferous age in India.

From the foregoing it will be gathered that one of the most
important points in connection with the Triassic A/ollusca is
the remarkable intermixture of Palzeozoic and Mesozoic types
which they exhibit. It is to be remembered, also, that this
intermixture has hitherto been recognised, not in the Middle
Triassic limestones of the Muschelkalk, in which —as the
oldest Triassic beds with marine fossils—we should naturally
expect to find it, but in the St Cassian beds, the age of which
is considerably later than that of the Muschelkalk. The
intermingling of old and new types of Shell-fish in the Upper
Trias is well brought out in the annexed table, given by Sir
Charles Lyell in his ‘Student’s Elements of Geology’ (some
of the less important forms in the table being omitted here) :—

GENERA OF FossIL MOLLUSCA IN THE ST CASSIAN
AND HALLSTADT BEDS.

Characteristic of Triassic

Common to Older Rocks. Common to Newer Rocks.

Rocks.

Orthoceras. Ceratites. Ammonites.
Bactrites. Cochloceras. Chemnitzia.
Macrocheilus. Rhabdoceras. Cerithium.
Loxonema. Aulacoceras. Monodonta.
Holopella. Naticella. Spheera.
Murchisonia. Platystoma. Cardita.
Porcellia. Halobia. Myoconcha.
Athyris. Hornesia. Hinnites.
Retzia. Koninckia. Monotis.
Cyrtina. Scoliostoma. Plicatula.
Euomphalus. Myophoria. Pachyrisma.

(The last two are princi- Thecidium.

pally but not exclus-

ively Triassic. )
Thus, to emphasise the more important points alone, the Trias
has yielded, amongst the Gasteropods, the characteristically
Paleozoic Loxonema, Holopella, Murchisonia, Euomphalus, and
Porcellia, along with typically Triassic forms like Platystoma
and Scoliostoma, and the great modern groups Chemnitzia and
Cerithium. Amongst the Bivalves we find the Paleozoic
Megalodon side by side with the Triassic /zalobia and MMyo-
phoria, these being associated with the Cardite, Hinnites,
Piicatula, and Trigoni@ of later deposits. The Brachiopods

214 HISTORICAL PALAIONTOLOGY.

exhibit the Palzeozoic Athyris, Retzia, and Cyrtina, with the
Triassic Koninckia and the modern Zhectdium. Finally, it is
here that the ancient genera Orthoceras, Cyrtoceras, and Gonia-
tites make their last appearance upon the scene of life, the
place of the last of these being taken by the more complex
and almost exclusively Triassic Ceratites ; whilst the still more
complex genus Ammonites first appears here in force, and is
never again wanting till we reach the close of the Mesozoic
period. The first representatives of the great Secondary
family of the 4elemnites are also recorded from this horizon.
Amongst the Vertebrate Animals of the Trias, the Azshes are
represented by numerous forms belonging to the Ganoids and
the Placoids. The Ganoids of the period are still all provided
with unsymmetrical (‘‘heterocercal”) tails, and belong prin-
cipally to such genera as FPadl@oniscus and Catopterus. The
remains of Placoids are in the form of teeth and spines, the
two principal genera being the two important Secondary
groups Acrodus and Hybodus. Very nearly at the summit
of the Trias in England, in the Rheetic series, is a singular
stratum, which is well known as the “ bone-bed,” from the
number of fish-remains which it contains. More interesting,
however, than the above, are the curious palate-teeth of the
Trias, upon which Agassiz founded the genus Ceratodus. The
teeth of Ceratodus (fig. 146) are singular flattened plates,

Fig. 146.—a, Dental plate of Ceratodus serratus, Keuper ; 4, Dental plate of
Ceratodus altus, Keuper. (After Agassiz.)

composed of spongy bone beneath, covered superficially with
a layer of enamel. Each plate is approximately triangular,
one margin (which we now know to be the outer one) being
prolonged into prongs or conical prominences, whilst the
surface is more or less regularly undulated. Until recently,
though the master-mind of Agassiz recognised that these
singular bodies were undoubtedly the teeth of fishes, we were
entirely ignorant as to their precise relation to the animal, or
as to the exact affinities of the fish thus armed. Lately, how-
ever, there has been discovered in the rivers of Queensland
(Australia) a living species of Ceratodus (C. Fosteri, fig. 147),

DEE) TREASSIC (PERIOD: 215

with teeth precisely similar to those of its Triassic predecessor ;
and we thus have become acquainted with the use of these

Fig. 147.—Ceratodus Fosteri, the Australian Mud-fish, reduced in size.

structures and the manner in which they were implanted in
the mouth. The palate carries two of these plates, with their
longer straight sides turned towards each other, their sharply-
sinuated sides turned outwards, and their short straight sides
or bases directed backwards. Two similar plates in the lower
jaw correspond to the upper, their undulated surfaces fitting
exactly to those of the opposite teeth. There are also two
sharp-edged front teeth, which are placed in the front of the
mouth in the upper jaw; but these have not been recognised
in the fossil specimens. ‘The living Ceratodus feeds on vege-
table matters, which are taken up or torn off from plants by
the sharp front teeth, and then partially crushed between the
undulated surfaces of the back’ teeth (Gunther); and there
need be little doubt but that the Triassic Ceratod: followed
a similar mode of existence. From the study of the. living
Ceratodus, it is certain that the genus belongs to the same
group as the existing Mud-fishes (Dzfuoz); and we therefore
learn that this, the highest, group of the entire class of Fishes
existed in Triassic times under forms little or not at all differ-
ent from species now alive; whilst it has become probable
that the order can be traced back into the Devonian period.
The Amphibians of the Trias all belong to the old order of
the Labyrinthodonts, and some of them are remarkable for
their gigantic dimensions. ‘They were first known by their
footprints, which were found to occur plentifully in the Tn-
assic sandstones of Britain and the continent of Europe, and
which consisted of a double series of alternately-placed pairs
of hand-shaped impressions, the hinder print of each pair being
much larger than the one in front (fig. 148). So like were these
impressions to the shape-of the human hand, that the at that
time unknown animal which produced them was at once chris-
tened Cheirotherium, or *‘ Hand-beast.” Further discoveries,
however, soon showed that the footprints of Chetrotherium
were really produced by species of Amphibians which, like the
existing Frogs, possessed hind-feet of a much larger size than

216 HISTORICAL PALZONTOLOGY.

‘
the fore-feet, and to which the
name of Labyrinthodonts was ap-
plied in consequence of the
complex microscopic structure of
the teeth (fig. 149). In the essen-
tial details of their structure, the
Triassic Labyrinthodonts did not
differ materially from their pre-
decessors in the Coal-measures
and Permian rocks. ‘They pos-
sessed the same frog-lke skulls
(fig. 150), with a lizard-like body,
a long tail, and comparatively
feeble limbs. ‘The hind - limbs
were stronger and longer than
the fore-limbs, and the lower

ye —— rx}
———

SH

—<——

Zz

Fig. 148.—Footprints of a Labyrinthodont (Cheivotherium), from the Triassic Sand-
stones of Hessberg, near Hildburghausen, Germany, reduced one-eighth. The lower
figure shows a slab, with several prints, and traversed by reticulated sun-cracks: the
upper figure shows the impression of one of the hind-feet, one-half of the natural size,
(After Sickler.)

THE TRIASSIC PERIOD. 217

surface of the body was protected by an armour of bony plates.
Some of the Triassic Labyrinthodonts must have attained
dimensions utterly unapproached amongst existing Amphibians,
the skull of Zadbyrinthodon Jegeri (fig. 150) being upwards of

Fig. 150.—a, Skull of Za-
byrinthodon Fageri, much
reduced in size; 6, Tooth
of the same. ‘Trias, Wiirt-
temberg.

Fig. 149.—Section of the tooth of Labyrinthodon
Mastodonsaurus) Fegeri, showing the microscopic
structure. Greatly enlarged. ‘Trias.

three feet in length and two feet in breadth. Restorations of
some of these extraordinary creatures have been attempted in
the guise of colossal Frogs; but they must in reality have more
closely resembled huge Newts.

Remains of Reptiles are very abundant in Triassic deposits,
and belong to very varied types. ‘The most marked feature,
in fact, connected with the Vertebrate fauna of the Trias, and
of the Secondary rocks in general, is the great abundance of
Reptilian life. Hence the Secondary period is often spoken
of as the “Age of Reptiles.” Many of the Triassic reptiles
depart widely in their structure from any with which we are
acquainted as existing on the earth at the present day, and it is
only possible here to briefly note some of the more important
of these ancient forms. Amongst the group of the Lizards
(Lacertilia), represented by Protorosaurus in the older Permian
strata, three types more or less certainly referable to this order
may be mentioned. One of these is a small reptile which
was found many years ago in sandstones near Elgin, in Scot.
land, and which excited special interest at the time in conse-
quence of the fact that the strata in question were believed to
belong to the Old Red Sandstone formation. It is, however,

218 HISTORICAL PALZONTOLOGY.

now certain that the Elgin sandstones which contain Z¢lerpeton
Elginense, as this reptile is termed, are really to be regarded as
of Triassic age. By Professor Huxley, Z/erpeton is regarded
as a Lizard, which cannot be considered as “in any sense
a less perfectly - organised creature than the Gecko, whose
swift and noiseless run over walls and ceilings surprises the
traveller in climates warmer than our own.” The “Elgin Sand-
stones” have also yielded another Lizard, which was originally
described by Professor Huxley under the name of Wyferoda-
pedon, the remains of the same genus having been subsequently
discovered in Triassic strata in India and South Africa. The
Lizards of this group must therefore have at one time enjoyed
a very wide distribution over the globe ; and the living Spheno-
don of New Zealand is believed by Professor Huxley to be the
nearest living ally of this family. The Wyperodapedon of the
Elgin Sandstones was about six feet in length, with limbs
adapted for terrestrial progression, but with the bodies of the
vertebre slightly biconcave, and having two rows of palatal -
teeth, which become worn down to the bone in old age.
Lastly, the curious RAynchosaurus of the Trias is also referred,
by the eminent comparative anatomist above mentioned, to the
order of the Lizards. In this singular reptile (fig. 151) the skull
is somewhat bird-like, and the
jaws appear to have been desti-
tute of teeth, and to have been
encased in a horny sheath like
the beak of a Turtle or a Bird.
It is possible, however, that the
ao CE as palate was furnished with teeth.
Riese asl (Ate Owen) The group of the Crocodiles
and Alligators (Crocodilia), dis-

tinguished by the fact that the teeth are implanted in dis-
tinct sockets and the skin more or less extensively provided
with bony plates, is represented in the Triassic rocks by the
Stagonolepis of the Elgin Sandstones. The so-called “ Theco-
dont” reptiles (such as Belodon, Thecodontosaurus, and Faleo-
saurus, fig. 152, ¢, d, e).are also nearly related to the Croco-
diles, though it is doubtful if they should be absolutely referred
to this group. In these reptiles, the teeth are implanted in
distinct sockets in the jaws, their crowns being more or less
compressed and pointed, “with trenchant and finely serrate
margins” (Owen). The bodies of the vertebre are hollowed
out at both ends, but the limbs appear to be adapted for pro-
gression on the land. The genus Beélodon (fig. 152, c) is
known to occur in the Keuper of Germany and in America;

THE TRIASSIC PERIOD. 219

and Palgosaurus (fig. 153, €) has also been found in the Trias
of the same region. ‘Teeth of the latter, however, are found,
along with remains of Zhecodontosaurus (fig. 153, @), in a
singular magnesian conglomerate near Bristol, which was
originally believed to be of Permian age, but which appears
to be undoubtedly Triassic.

ze
eS SNNAAN A

Fig. 152.—Triassic Reptiles. a, Skull of Mothosaurus mirabilis, reduced in size—Mus-
chelkalk, Germany ; 4, Tooth of Simosaurus Gatllardot?, of the natural size—Muschel-
kalk, Germany ; G Tooth of Belodon Carolinensis—Tri rias, America; @, Tooth of Theco-
dontosaurus an tiguus, slightly enlarged—Britain ; e, Tooth of Paleosaurus platyodon, of ©
the natural size—Britain.

The Trias has also yielded the remains of the great marine
reptiles which are often spoken of collectively as the ‘ Enalio-
saurians” or “ Sea-lizards,” and which will be more particularly
spoken of in treating of the Jurassic period, of which they are
more especially characteristic. In all these reptiles the limbs
are flattened out, the digits being enclosed in a continuous
skin, thus forming powerful swimming-paddles, resembling the
“flippers” of the Whales and Dolphins both in their general
structure and in function. The tail is also long, and adapted
to act as a swimming-organ ; and there can be no doubt but
that these extraordinary and often colossal reptiles frequented
the sea, and only occasionally came to the land. The Triassic
Enaliosaurs belong to a group of which the later genus
Plestosaurus is the type (the Sauropterygia). One of the best
known of the Triassic genera is /Vothosaurus (fig. 152, a), 1 in
which the neck was long and bird-like, the jaws being im-
mensely elongated, and carrying numerous powerful conical
teeth implanted in distinct sockets. The teeth in Szmosaurus
(2 152, 6) are of a similar nature ; but the orbits are of enormous
size, indicating eyes of corresponding dimensions, and perhaps
pointing to the nocturnal habits of the animal. In the singular

220 HISTORICAL PALZONTOLOGY.

Placodus, again, the teeth are in distinct sockets, but resemble
those of many fishes in being rounded and obtuse (fig. 153),
forming broad crushing plates
adapted for the comminu-
tion of shell-fish. There is a
row of these teeth all round
the upper jaw proper, and a
double series on the palate,
but the lower jaw has only a
single row of teeth. Placodus
is found in the Muschelkalk,
and the characters of its den-
tal apparatus indicate that
it was much more peaceful
sei de2a_Under puree of te wore in its habits than its eae
chelkalk, Germany. ciates the Nothosaur and Si-
mosaur.

The Triassic rocks of South Africa and India have yielded
the remains of some extraordinary Reptiles, which have been
placed by Professor Owen in a separate order under the name
of Anomodontia. ‘The two principal genera of this group are
Dicynodon and Oudenodon, both of which appear to have been
large Reptiles, with well-developed limbs, organised for pro-
gression upon the dry land. In Oxdenodon (fig. 154, B) the
jaws seem to have been wholly destitute of teeth, and must
have been encased in a horny sheath, similar to that with
which we are familiar in the beak of a Turtle. In Ducynodon
(fig. 154, A), on the other hand, the front of the upper jaw
and the whole of the lower jaw were destitute of teeth, and
the front of the mouth must have constituted a kind of beak; |
but the upper jaw possessed on each side a single huge conical
tusk, which is directed downwards, and must have continued
to grow during the life of the animal.

It may be mentioned that the above-mentioned Triassic
sandstones of South Africa have recently yielded to the re-
searches of Professor Owen a new and unexpected type of
Reptile, which exhibits some of the structural peculiarities
which we have been accustomed to regard as characteristic
of the Carnivorous quadrupeds. ‘The Reptile in question has
been named Cyzodraco, and it is looked upon by its distin-
guished discoverer as the type of a new order, to which he has
given the name of Zheriodontia. The teeth of this singular
form agree with those of the Carnivorous quadrupeds in con-
sisting of three distinct groups—namely, front teeth or zuczsors,
eye teeth or canines, and back teeth or molars. ‘The canines

THE TREASSIC PERIOD. 22%

also are long and pointed, very much compressed, and having
their lateral margins finely serrated, thus presenting a singular

Fig. 154.—Triassic Anomodont Reptiles. A, Skull of Dzcynodon lacerticeps, showing
one of the great maxillary tusks; B, Skull of Oudenodon Bainiz, showing the toothless,
beak-like jaws. From the Trias of South Africa. (After Owen.)

resemblance to the teeth of the extinct “ Sabre-toothed Tiger”
(Machairodus). The bone of the upper arm (humerus) further
shows some remarkable resemblances to the same bone in the
Carnivorous Mammals. As has been previously noticed, Pro-
fessor Owen is of opinion that some of the Reptilian remains
of the Permian deposits will also be found to belong to this
group of the ‘‘ Theriodonts.”

Lastly, we find in the Triassic rocks the remains of Reptiles
belonging to the great Mesozoic order of the Deznosaurta.
This order attains its maximum at a later period, and will be
spoken of when the Jurassic and Cretaceous deposits come to
be considered. The chief interest of the Triassic Reptiles of
this group arises from the fact that they are known by their
footprints as well as by their bones; and a question has arisen
whether the supposed footprints of ézrds which occur in the
Tnas have not really been produced by Deinosaurs. This
leads us, therefore, to speak at the same time as to the evi-
dence which we have of the existence of the class of Birds

during the Triassic period. No actual bones of any bird have
16

222 HISTORICAL PALZONTOLOGY.

as yet been detected in any Triassic deposit; but we have
tolerably clear evidence of their existence at this time in the
form of footprints. ‘The impressions in question are found in
considerable numbers in certain red sandstones of the age of
the Trias in the valley of the Connecticut River, in the United
States. They vary much in size, and have evidently been
produced by many different animals walking over long
stretches of estuarine mud and sand exposed at low water.
The footprints now under consideration form a double series
of simgde prints, and therefore, beyond all question, are the
tracks of a dzfed—that is, of an animal which walked upon
two legs. No living animals, save Man and the Birds, walk
habitually on two legs; and there is,.therefore, a prima facie
presumption that the authors of these prints were Birds.
Moreover, each impression consists of the marks of three toes
turned forwards (fig. 155), and therefore are precisely such as

Fig. 155.—Supposed footprint of a 'Bird, from the Triassic Sandstones of the Con-
necticut River. The slab shows also numerous “ rain-prints.”

might be produced by Wading or Cursorial Birds. Further,
the impressions of the toes show exactly the same numerical
progression in the number of the joints as is observable in
living Birds—that is to say, the innermost of the three toes
consists of three joints, the middle one of four, and the outer
one of five joints. Taking this evidence collectively, it would
have seemed, until lately, quite certain that these tracks could
only have been formed by Birds. It has, however, been
shown that the Deinosaurian Reptiles possess, in some cases
at any rate, some singularly bird-like characters, amongst

THE TRIASSIC PERIOD. 223

which is the fact that the animal possessed the power of
walking, temporarily at least, on its hind-legs, which were
much longer and stronger than the fore-limbs, and which
were sometimes furnished with no more than three toes.
As the bones and teeth of Deinosaurs have been found in
the Triassic deposits of North America, it may be regarded as
certain that some of the bipedal tracks originally ascribed to
Birds must have really been produced by these Reptiles. It
seems at the saine time almost a certainty that others of the
three-toed impressions of the Connecticut sandstones were in
truth produced by Birds, since it is doubtful if the bipedal
mode of progression was more than an occasional thing
amongst the Deinosaurs, and the greater number of the
many known tracks exhibit no impressions of fore - feet.
Upon the whole, therefore, we may, with much probability,
conclude that the great class of Birds (Aves) was in existence
in the Triassic period. If this be so, not only must there
have been quite a number of different forms, but some of
them must have been of very large size. Thus the largest
footprints hitherto discovered in the Connecticut sandstones
are 22 inches long and 12 inches wide, with a proportionate
length of stride. These measurements indicate a foot four
times as large as that of the African Ostrich ; and the animal
which produced them—whether a Bird or a Deinosaur—must
have been of colossal dimensions.

Finally, the Trias completes the tale of the great classes of
the Vertebrate sub-kingdom by presenting us with remains of
the first known of the true Quadrupeds or J/ammalia. These
are at present only known by their teeth, or, in one instance,

. by one of the halves of the lower jaw ; and these indicate
minute Quadrupeds, which present greater affinities with the
little Banded Ant-eater (IZyrmecobius fasciatus, fig. 158) of
Australia than with any other living form. If this conjecture

Fig. 157.—a@, Molar tooth of

Microlestes antiquus, magni-

: fied; 4, Crown of the same,

Fig. 156.—Lower jaw of Dromatherium sylvestre. magnified still further. Trias,
Trias, North Carolina. (After Emmons.) Germany.

be correct, these ancient Mammals belonged to the order of
the Marsupials or Pouched Quadrupeds (AZarsupialia), which

224 HISTORICAL PALASONTOLOGY.

are now exclusively confined to the Australian province, South
America, and the southern portion of North America. In

= =
Fig. 158.—The Banded Ant-eater (IZyrmecobius fasctatus) of Australia. ,

the Old World, the only known Triassic Mammals belong to
the genus JZicrolestes, and to the probably identical Wypsez-
prymnopsts of Professor Boyd Dawkins. The teeth of AZzcro-
lestes (fig. 157) were originally discovered by Pheninger in
1847 in the ‘“ bone-bed” which is characteristic of the sum-
mit of the Rhetic series both in Britain and on the continent
of Europe ; and the known remains indicate two species. In
Britain, teeth of JZzcrolestes have been discovered by Mr
Charles Moore in deposits of Upper Triassic age, filling a
fissure in the Carboniferous limestone near Frome, in Somer-
setshire ; and a molar tooth of Aypszprymnopsis was found by
Professor Boyd Dawkins in Rheetic marls below the “ bone-
bed” at Watchet, also in Somersetshire. In North America,
lastly, there has been found in strata of Triassic age one of
the branches of the lower jaw of a small Mammal, which has
been described under the name of Dvromatherium sylvestre
(fig. 156). The fossil exhibits ten small molars placed side
by side, one canine, and three incisors, separated by small
intervals, and it indicates a small insectivorous animal, pro-
bably most nearly related to the existing AZyrmecobiits.

LITERATURE.

The following list comprises a few of the more important sources of
information as to the Triassic strata and their fossil contents :—

(1) ‘ Geology of Oxford and the Valley of the Thames.’ Phillips.

(2) ‘Memoirs of the Geological Survey of Great Britain and Ireland.’

(3) ‘Report on the Geology of Londonderry,’ &c. Portlock.

(4)

(37)
(38)

PEE RASS ey PERIOD: 225

‘On the Zone of Avicula contorta,” &c.—‘Quart. Journ. Geol.
Soc.,’ vol. xvi., 1860. Dr Thomas Wright.

**On the Zones of the Lower Lias and the Avicula contorta Zone”’
—‘ Quart. Journ. Geol. Soc.,’ vol. xvil., 1861. Charles Moore.

‘*Qn Abnormal Conditions of Secondary Deposits,” &c.—‘ Quart.
Journ. Geol. Soc.,’ vol. xxiiis, 1876-77. Charles Moore.

‘Geognostische Beschreibung des_ Bayerischen Alpengebirges.’
Giimbel.

‘Lethzea Rossica.’ Pander.

‘ Letheea Geognostica.’ Bronn.

‘ Petrefacta Germaniz.’ Goldfuss.

‘ Petrefaktenkunde.’ Quenstedt.

‘Monograph of the Fossil Estherize’ (Palzeontographical Society).
Rupert Jones.

“ Fossil Remains of Three Distinct Saurian Animals, recently dis-

- covered in the Magnesian Conglomerate near Bristol ”—‘ Trans.
Geol. Soc.,’ ser. 2, vol. v., 1840. Riley and Stutchbury.

‘Die Saurier des Muschekalkes.’ Von Meyer.

‘Beitrage zur Palezontologie Wiirttembergs.’ Von Meyer and
Plieninger.

‘Manual of Paleontology.’ Owen.

‘Qdontography.’ Owen.

‘Report on Fossil Reptiles’ (British Association, 1841). Owen.

**On Dicynodon ”—‘ Trans. Geol. Soc.,’ vol. iii., 1845. Owen.

‘ Descriptive Catalogue of Fossil Reptilia and Fishes in the Museum
of the Royal College of Surgeons, England.’ Owen.

**On Species of Labyrinthodon from Warwickshire ”—‘ Trans. Geol.
Soc.,’ ser. 2, vol. vi. Owen.

**On a Carnivorous Reptile” (Cynodraco major), &c.——‘ Quart.
Journ. Geol. Soc.,’ vol. xxxil., 1876. Owen.

**On Evidences of Theriodonts in Permian Deposits,” &c.—‘ Quart.
Journ. Geol. Soc.,’ vol. xxxil., 1876. Owen.

**On the Stagonolepis Robertsoni,” &c.—‘ Quart. Journ. Geol.
SOG, VOl-exv.. 1959, | Hluxley:

‘Qn a New Specimen of Telerpeton Elginense ’’—‘ Quart. Journ.
Geol. Soc.,’ vol. xxiii., 1866. Huxley.
‘On Hyperodapedon ’”’—‘ Quart. Journ. Geol. Soc.,’ vol. xxv.,

1869. Huxley.

*“On the Affinities between the Deinosaurian Reptiles and Birds”
—‘Quart. Journ. Geol. Soc.,’ vol. xxvi., 1870. Huxley.

**On the Classification of the Deinosauria,” &c.—‘ Quart. Journ.
Geol. Soc.,’ vol. xxvi., 1870. Huxley.

“ Palzeontologica Indica ’’—‘ Memoirs of the Geol. Survey of India.’

** On the Geological Position and Geographical Distribution of the
Dolomitic Conglomerate of the Bristol Area”—‘ Quart. Journ.
Geol. Soc.,’ vol. xxvi., 1870. KR. Etheridge, sen.

** Remains of Labyrinthodonta from the Keuper Sandstone of War-
wick ”—‘ Quart. Journ. Geol. Soc.,’ vol. xxx., 1874. Miall.

‘Manual of Geology.’ Dana.

‘Synopsis of Extinct Batrachia and Reptilia of North America.’
Cope.

‘Fossil Footmarks.’ Hitchcock.

‘Ichnology of New England.’ Hitchcock.

‘Traité de Paléontologie Végétale.’ Schimper.

‘Histoire des Végétaux Fossiles.’ Brongniart.

‘ Monographie der Fossilen Coniferen.’ Goeppert.

226 HISTORICAL PALZONTOLOGY.

CHA PTE Recvir
THE FORASSTOC PERIOM:

Resting upon the Trias, with perfect conformity, and with
an almost undeterminable junction, we have the great series of
deposits which are known as the Oolitic Rocks, from the com-
mon occurrence in them of oolitic limestones, or as the /uras-
sic Rocks, from their being largely developed in the mountain-
range of the Jura, on the western borders of Switzerland.
Sediments of this series occupy extensive areas in Great Britain,
on the continent of Europe, and in India. In North America,
limestones and marls of this age have been detected in “the
Black Hills, the Laramie range, and other eastern ridges of the
Rocky Mountains ; also over the Pacific slope, in the Uintah,
Wahsatch, and Humboldt Mountains, and in the Sierra Ne-
vada” (Dana); but in these regions their extent is still un-
known, and their precise subdivisions have not been deter-
mined. Strata belonging to the Jurassic period are also known
to occur in South America, in Australia, and in the Arctic
zone. When fully developed, the Jurassic series is capable of
subdivision into a number of minor groups, of which some are
clearly distinguished by their mineral characters, whilst others
are separated with equal certainty by the differences of the
fossils that they contain. It will be sufficient for our present
purpose, without entering into the more minute subdivisions
of the series, to give here a very brief and general account
of the main sub-groups of the Jurassic rocks, as developed in
Britain—the arrangement of the Jura-formation of the continent
of Europe agreeing in the main with that of England.

I, THE Lias.—The base of the Jurassic series of Britain
is formed by the great calcareo-argillaceous deposit of the
‘“‘Tjias,” which usually rests conformably and almost inseparably
upon the Rhetic beds (the so-called “ White Lias”), and
passes up, generally conformably, into the calcareous sand-
stones of the Inferior Oolite. The Lias is divisible into the
three principal groups of the Lower, Middle, and Upper Lias,
as under, and these in turn contain many well-marked ‘“zones;”
so that the Lias has some claims to be considered as an inde-
pendent formation, equivalent to all the remaining Oolitic
rocks. The Lower Lias (Terrain Sinemurien of T’Orbigny)
sometimes attains a thickness of as much as 600 feet, and con-
sists of a great series of bluish or greyish laminated clays,

THE JURASSIC PERIOD. 227

alternating with thin bands of blue or grey limestone—the
whole, when seen in quarries or cliffs from a little distance,
assuming a characteristically striped and banded appearance.
By means of particular species of Ammonites, taken along with
other fossils which are confined to particular zones, the Lower
Lias may be subdivided into several well-marked horizons.
The Middle Lias, or Martstone Series (Terrain Liasien of
D’Orbigny), may reach a thickness of 200 feet, and consists of _
sands, arenaceous marls, and argillaceous limestones, sometimes
with ferruginous beds. The Upfer Lias (Terrain Toarcien of
D’Orbigny) attains a thickness of 300 feet, and consists princi-
pally of shales below, passing upwards into arenaceous strata.

II. THe Lower Oo.ites.—Above the Lias comes a com-
plex series of partly arenaceous and argillaceous, but prin-
cipally calcareous strata, of which the following are the more
important groups: a, The Jnfertor Oolite (Terrain Bajocien
of D’Orbigny), consisting of more than 200 feet of oolitic
limestones, sometimes more or less sandy; 4, The Fuller's
Earth, a series of shales, clays, and marls, about 120 feet in
thickness ; c, The Great Oolite or Bath Oolite (Terrain Bath-
onien of D’Orbigny), consisting principally of oolitic lme-
stones, and attaining a thickness of about 130 feet. The well-
known “ Stonesfield Slates” belong to this horizon ; and the
locally developed ‘‘ Bradford Clay,” ‘“ Cornbrash,” and “ For-
est-marble” may be regarded as constituting the summit of
this group.

III. THE MrippLe Ootites.——The central portion of the
Jurassic series of Britain is formed by a great argillaceous de-
posit, capped by calcareous strata, as follows : a, The Oxford
Clay (Terrain Callovien and Terrain Oxfordien of D’Orbigny),
consisting of dark-coloured laminated clays, sometimes reach-
ing a thickness of 700 feet, and in places having its lower por-
tion developed into a hard calcareous sandstone (“ Kelloway
Rock”); 6, The Coral-Rag (Terrain Corallien of D’Orbigny,
“Nerinean Limestone” of the Jura, “‘ Diceras Limestone” of
the Alps), consisting, when typically developed, of a central
mass of oolitic limestone, underlaid and surmounted by cal-
careous grits.

IV. THe Upper Oo.ites.—a, The base of the Upper
Oolites of Britain is constituted by a great thickness (600 feet
or more) of laminated, sometimes carbonaceous or bituminous
clays, which are known as the Aimmeridge Clay (Terrain Kim-
méridgien of D’Orbigny); 4, The Portland Beds (Terrain Port-
landien of D’Orbigny) succeed the Kimmeridge clay, and con-
sist inferiorly of sandy beds surmounted by oolitic limestones

228 HISTORICAL PALALAONTOLOGY.

(“ Portland Stone”), the whole series attaining a thickness of
150 feet or more, and containing marine fossils; ¢, The Pur-
beck Beds are apparently peculiar to Great Britain, where they
form the summit of the entire Oolitic series, attaining a total
thickness of from 150 to 200 feet. The Purbeck beds consist
of arenaceous, argillaceous, and calcareous strata, which can
be shown by their fossils to consist of a most remarkable alter-
nation of fresh-water, brackish-water, and purely marine sedi-
ments, together with old land-surfaces, or vegetable soils, which
contain the upright stems of trees, and are locally known as
“* Dirt-beds.”

One of the most important of the Jurassic deposits of the
continent of Europe, which is believed to be on the horizon
of the Coral-rag or of the lower part of the Upper Oolites, is
the ‘‘ Solenhofen Slate” of Bavaria, an exceedingly fine-grained
limestone, which is largely used in lithography, and is cele-
brated for the number and beauty of its organic remains, and
especially for those of Vertebrate animals.

The subjoined sketch-section (fig. 159) exhibits in a dia-
grammatic form the general succession of the Jurassic rocks of
Britain.

Regarded as a whole, the Jurassic formation is essentially
marine ; and though remains of drifted plants, and of insects
and other air-breathing animals, are not uncommon, the fossils
of the formation are in the main marine. In the Purbeck
‘series of Britain, anticipatory of the great river-deposit of the
Wealden, there are fresh-water, brackish-water, and even terres-
trial strata, indicating that the floor of the Oolitic ocean was
undergoing upheaval, and that the marine conditions which
had formerly prevailed were nearly at an end. In places
also, as in Yorkshire and Sutherlandshire, are found actual
beds of coal: but the great bulk of the formation is an indu-
bitable sea-deposit ; and its limestones, oolitic as they com-
monly are, nevertheless are composed largely of the commin-
uted skeletons of marine animals. Owing to the enormous
number and variety of the organic remains which have been
yielded by the richly fossiliferous strata of the Oolitic series,
it will not be possible here to do more than to give an outline-
sketch of the principal forms of life which characterise the
Jurassic period as a whole. It is to be remembered, however,
that every minor group of the Jurassic formation has its own
peculiar fossils, and that by the labours of such eminent ob-
servers as Quenstedt, Oppel, D’Orbigny, Wright, De la Beche,
Tate, and others, the entire series of Jurassic sediments admits
of a more complete and more elaborate subdivision into zones

THE: JURASSIC PERIOD. 229

characterised by special life-forms than has as yet been found
practicable in the case of any other rock-series.

GENERALISED SECTION OF THE JURASSIC Rocks
OF ENGLAND.

Fig. 159.

a SLAG peel Beds.
g pa Portland Beds.
5
©
Es
SN ———————————————— Kimmeridge Clay.
2)
go eee oT TTT TT --------- Coral-Rag.
ct
=
S)
‘o)
<2) —S—SaSSSZ_
. = ...--------Oxford Clay.
A
=
“PO Ee ay CD ed cape ea Cornbrash and Forest-marble.
ea)
: pease Great Oolite.
je) ——
aa Ge Pe Fuller’s Earth.
fc} 5)
z saawencenr -Inferior Oolite.
=

Aan Upper Lias.

2) | Sacer a param WAC Middle Lias (Marlstone
3 series).

CPi toma Lower Lias.

Rhetic Marls (‘* White
eias,7);

-cos messes

The lants of the Jurassic period consist principally of
Ferns, Cycads, and Conifers—agreeing in this respect, there-

230 HISTORICAL PALAEONTOLOGY.

fore, with those of the preceding Triassic formation. The
ferns are very abundant, and belong partly to old and partly
to new genera. The Cycads are also very abundant, and, on
the whole, constitute the most marked feature of the Jurassic
vegetation, many genera of this group being known (/¢ero-
phyllum, Otozamites, Zamites, Crossozamia, Wilhiamsonia, Buck-
landia, &c.) The so-called “ dirt-bed” of the Purbeck series
consists of an ancien soil, in which stand erect the trunks of
Conifers and the silicified stools of Cycads of the genus M/antel-
fia (fig. 160). The Conzfere of the Jurassic are represented by

Fig. 160.—MWantellia (Cycadcoidea) megalophylla, a Cycad from the Purbeck
‘“dirt-bed.” Upper Oolites, England.

various forms more or less nearly allied to the existing Avau-
carié; and these are known not only by their stems or
branches, but also in some cases by their cones. We meet,
also, with the remains of undoubted Endogenous plants, the
most important of which are the fruits of forms allied to the
existing Screw-pines (Pandanee), such as Podocarya and Kaida-
carpum. So far, however, no remains of Palms have been
found ; nor are we acquainted with any Jurassic plants which
could be certainly referred to the great “ Angiospermous ”
group of the Exogens, including the majority of our ordinary
plants and trees.

Amongst animals, the Pyvotozoans are well represented in
the Jurassic deposits by numerous Foraminifers and Sponges ;
as are the Celenterates by numerous Corals. Remains
of these last-mentioned organisms are extremely abundant
in some of the limestones of the formation, such as the
“Coral-rag” and the Great Oolite ; and the former of these
may fairly be considered as an ancient “reef.” The Augose
Corals have not hitherto been detected in the Jurassic rocks ;
and the “‘ Zabulate Corals,” so-called, are represented only by
examples of the modern genus M///epora. With this excep-

THE JURASSIC PERIOD. 231

tion, all the Jurassic Corals belong to the great group which
predominates in recent seas (Zoantharia sclerodermata); and
the majority belong to the important reef-building family of
the ‘“‘Star-corals” (Astreide). The form here figured (Zzhecos-
milia annularis, fig. 161) is one of the characteristic species
of the Coral-rag. |

Fig. 161.—Thecosmilia annularis. Coral-rag, England.

The L£chinoderms are very numerous and abundant fossils
in the Jurassic series, and are represented by Sea-lilies, Sea-
urchins, Star-fishes, and Brittle-stars. The Cvrzvozds are still
common, and some of the limestones of the series are largely |
composed of the déébris of these organisms. Most of the
Jurassic forms resemble those with which we are already
familiar, in having the body permanently attached to some
foreign object by means of a longer or shorter jointed stalk
or “column.” One of the most characteristic Jurassic genera
of these “‘ stalked ” Crinoids (though not exclusively confined
to this period) is Pentacrinus (fig. 162). In this genus, the
column is five-sided, with whorls of “‘side-arms ;” and the arms
are long, slender, and branched. The genus is represented
at the present day by the beautiful ‘‘ Medusa-head Pentacrin-
ite” (Pentacrinus caput-meduse). Another characteristic Oolitic
genus 1s Afiocrinus, comprising the so-called “‘ Pear Encrinites.”
In this group the column is long and rounded, with a dilated
base, and having its uppermost joints expanded so as to form,
with the cup itself, a pear-shaped mass, from the summit of
which spring the comparatively short arms. Besides the

232

HISTORICAL PALAEONTOLOGY.

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Fig. 162.
joints of the column
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isting

These forms resemble the ex

Saccosoma.

THE JURASSIC PERIOD. 233

foreign body by means of a jointed stem, from which they
detach themselves when fully grown to lead an independent
existence. In this later stage of their life, therefore, they
closely resemble the Brittle-stars in appearance. ‘True Star-
fishes (Asterotds) and Brittle-stars (Ophzwroids) are abundant
in the Jurassic rocks, and the Sea-urchins (Zchznoids) are so
numerous and so well preserved as to constitute quite a marked
feature of some beds of the series. All the Oolitic urchins
agree with the modern Zchznozds in having the shell composed
of no more than twenty rows of plates. Many different genera
are known, and a characteristic species of the Middle Oolites
(Hemicidaris creniularis, fig. 163) is here figured.

Fig. 163.—Hemicidaris crenularis, showing the great tubercles on which the
spines were supported. Middle Oolites.

Passing over the Aznelides, which, though not uncommon,
are of little special interest, we come to the Articulates, which
also require little notice. Amongst the Crustaceans, whilst the
little Water-fleas (Ostracoda) are still abundant, the most mark-
ed feature is the predominance which is now assumed by the
Decapods—the highest of the known groups of the class. ‘True
Crabs (Brachyura) are by no means unknown; but the prin-
cipal Oohtic Decapods belonged to the ‘“ Long-tailed” group
(Macrura), of which the existing Lobsters, Prawns, and
Shrimps are members. The fine-grained lithographic slates of
Solenhofen are especially famous as a depot for the remains
of these Crustaceans, and a characteristic species from this
locality (Eryon arctiformis, fig. 164) is here represented.
Amongst the air-breathing Articulates, we meet in the Oolitic
rocks with the remains of Spiders (Arachnida), Centipedes
(Myriapoda), and numerous true Insects (/msecta). In con-
nection with the last-mentioned of these groups, it is of interest
to note the occurrence of the oldest known fossil Butterfly
—the Palgontina Oolitica of the Stonesfield slate—the rela-

234 HISTORICAL PALAZONTOLOGY.

tionships of which appear to be with some of the living
Butterflies of Tropical America.
Coming to the JZollusca, the Polyzoans, numerous and

eet

Fig. 164.—Eryon arctiformis, a “ Long-tailed Decapod,” from the Middle
Oolites (Solenhofen Slate).

beautiful as they are, must be at once dismissed; but the
Brachiopods deserve a moment’s attention. The Jurassic
Lamp-shells (fig. 165) do not fill by any means such a pre-
dominant place in the marine fauna of the period, as in many
Palzeozoic deposits, but they are still individually numerous.
The two ancient genera Leptena (fig. 165, a) and Sperifera (fig.
165, 4), dating the one from the Lower and the other from the
Upper Silurian, appear here for the last time upon the scene,
but they have not hitherto been recognised in deposits later
than the Lias. The great majority of the Jurassic Brachiopods,
however, belong to’ the genera Zerebratula (fig. 165, ¢ @ f)
and ARhyachonella (fig. 165, 2), both of which are represented
by living forms at the present day. The Zerebratule, in par-
ticular, are very abundant, and the species are often confined
to special horizons in the series.

Remains of Szvalves (Lamellibranchiata) are very numerous

THE JURASSIC PERIOD. 235

in the Jurassic deposits, and in many cases highly character-
istic. In the marine beds of the Oolites, which constitute by

Fig. 165.—Jurassic Brachiopods. a, Leptena Liassica, enlarged, the small cross below
the figure indicating the true size of the shell—Lias; 4, Spzvifera rostrata, Lias; c,
Terebratula quadrifida, Lias ; d, ad’, Rhynchonella varians, Fuller’s Earth and Kello-
way Rock; e, Tevebratula spheroidalis, Inferior Oolite ; 4, Terebratula digona, Brad-
ford Clay, Forest-marble, and Great Oolite. (After Davidson).

far the greater portion of the whole formation, the Bivalves
are of course marine, and belong to such genera as 77zgonza,
Lima, Pholadomya, Cardinia, Avicula, Hippopodium, &c.; but
in the Purbeck beds, at the summit of the series, we find
bands of Oysters alternating with strata containing fresh-water
or brackish-water Bivalves, such as Cyrene and Corbule. ‘The
predominant Bivalves of the Jurassic, however, are the Oysters,
which occur under many forms, and often in vast numbers,
particular species being commonly restricted to particular
horizons. Thus of the true Oysters, Ostrea distorta is char-
acteristic of the Purbeck series, where it forms a bed twelve
feet in thickness, known locally as the ‘‘ Cinder-bed ;” Ostrea
expansa abounds in the Portland beds; Ostrea deltoidea is
characteristic of the Kimmeridge clay; Ostrea gregaria pre-
dominates in the Coral-rag ; Ostrea acuminata characterises the
small group of the Fuller’s Earth; whilst the plaited Ostrea
Marshi (fig. 166) is a common shell in the Lower and Middle
Oolites. Besides the more typical Oysters, the Oolitic rocks
abound in examples of the singularly unsymmetrical forms

236 HISTORICAL PALZONTOLOGY.

belonging to the genera Exogyra and Gryphea (fig. 167). In
the former of these are included Oysters with the beaks

Fig. 166.—-Ostrea Marshiz. Middle
and Lower Oolites. Fig. 167.—Gryphea incurva. Lias.

‘reversed ”—that is to say, turned towards the hinder part of
the shell; whilst in the latter are Oysters in which the lower
valve of the shell is much the largest, and has a large incurved
beak, whilst the upper valve is small and concave. One of
the most characteristic Lxogyr@ is the Z. virgula of the Oxford
Clay, and of the same horizon on the Continent; and the
Gryphea incurva (fig. 167).1s equally abundant in, and char-
acteristic of, the formation of the Lias. Lastly, we may
notice the extraordinary shells belonging to the genus Diceras
(fig. 168), which are exclusively confined to the Middle
Oolites. In this formation in
the Alps they occur in such
abundance as to give rise to
the name of “Calcaire a Di-
cerates,” applied to beds of
the same age as the Coral-
rag of Britain. The genus Dz-
ceras belongs to the same fam-
ily as the “ Thorny Clams”
(Chama) of the present day—
the shell being composed of
pense Oey, a nearly equally-sized valves, the
oS erg CGA ae Middle peaks of which are extremely
prominent and twisted into a
spiral. The shell was attached to some foreign body by the
beak of one of its valves. :
Amongst the Jurassic Univalves (Gasteropoda) there are
many examples of the ancient and long-lived Pleurotomaria ;
but on the whole the Univalves begin to have a modern
aspect. The round-mouthed (‘holostomatous”), vegetable-

THE JURASSIC PERIOD. 237

eating Sea-snails, such as the Limpets (fave//ide), the Nerites
(Nerita), the Turritelle, Chemnitzia, &c., still hold a predomi-
nant place. The two most noticeable genera of this group
are Cerithium and Verinea —the former of these attaining
great importance in the Tertiary and Recent seas, whilst the
latter (fig. 169) is highly characteristic of the Jurassic series,
though not exclusively confined to
it. One of the limestones of the
Jura, believed to be of the age of
the Coral-rag (Middle Oolite) of Bri-
tain, abounds to such an extent in
the turreted shells of (Verinea as to
have gained the name of “ Calcaire
a Nérinées.” In addition to forms
such as the preceding, we now for
the first time meet, in any force,
with the Carnivorous Univalves, in
which the mouth of the shell is
notched or produced into a canal,
giving rise to the technical name
of “siphonostomatous,” applied to [hand feure shows the appear-
the shell. Some of the carnivorous ance presented by the shell when
forms belong to extinct types, such eae pd Ce eee
as the Purpuroidea of the Great Oo-
lite; but others are referable to well-known existing genera.
Thus we meet here with species of the familiar groups of the
Whelks (Lucconum), the Spindle-shells (Fusus), the Spider-
shells (Preroceras), Murex, Rostellaria, and others which are
not at present known to occur in any earlier formation.
Amongst the Wing-shells (Preropfoda), it is sufficient to mark
the final appearance in the Lias of the ancient genus Conwdaria.
Lastly, the order of the Cephalopoda, in both its Tetrabran-
chiate and Dibranchiate sections, undergoes a vast devel-
opment in the Jurassic period. The old and comparatively
simple genus /Vauizlus is still well represented, one species
being very similar to the living Pearly Nautilus (4V. pompzlzus);
but the Orthocerata and Gonzatites of the Trias have finally
disappeared ; and the great majority of the Tetrabranchiate
forms are referable to the comprehensive genus Ammonites,
with its many sub-genera and its hundreds of recorded species.
The shell in Ammonites is in the form of a flat spiral, all the
coils of which are in contact (figs. 170 and 171). ‘The inner-
most whorls of the shell are more or less concealed ; and the
body-chamber is elongated and narrow, rather than expanded
towards the pone The tube or siphuncle which runs through
1

238 HISTORICAL PALZONTOLOGY.

the air-chambers is placed on the dorsal or convex side of the
shell; but the principal character which distinguishes Ammon-

Fig. 170.—A mmonites Humphresianus. Inferior Oolite.

ates from Gonzatites and Ceratites is the wonderfully complex
manner in which the seffa, or partitions between the air-cham-
bers, are folded and undulated. ‘To such an extent does this
take place, that the edges of the septa, when exposed by the

SSS EY yyy wane

Sh SSS

Fig. 171.—Asmmonites bifrons. Lias.

removal of the shell-substance, present in an exaggerated man-
ner the appearance exhibited by an elaborately-dressed shirt-
frill when viewed edgewise. The species of Ammonites range
from the Carboniferous to the Chalk ; but they have not been

THE JURASSIC PERIOD. 239

found in deposits older than the Secondary, in any region
except India; and they are therefore to be regarded as essen-
tially Mesozoic fossils. Within these limits, each formation
is characterised by particular species, the number of individ-
uals being often very great, and the size which is sometimes
attained being nothing short of gigantic. In the Lias, par-
ticular species of Ammonites may succeed one another regu-
larly, each having a more or less definite horizon, which it does
not transgress. It is thus possible to distinguish a certain
number of zones, each characterised by a particular Ammonite,
together with other associated fossils. Some of these zones
are very persistent and extend over very wide areas, thus afford-
ing valuable aid to the geologist in his determination of
rocks. It is to be remembered, however, that there are other
species which are not thus restricted in their vertical range,
even in the same formations in which definite zones occur.
The Cuttle-fishes or Dibranchiate Cephalopods constitute a
feature in the life of the Jurassic period little less conspicuous
and striking than that afforded by the multitudinous and varied
chambered shells of the Ammonitide. ‘The remains by which
these animals are recognised are necessarily less perfect, as a
rule, than those of the latter, as no external shell is present
(except in rare and more modern groups), and the internal
skeleton is not necessarily calcareous. Nevertheless, we have
an ample record of the Cuttle-fishes of the Jurassic period, in
the shape of the fossilised jaws or beak, the ink-bag, and, most
commonly of all, the horny or calcareous structure which is
embedded in the soft tissues, and is variously known as the
“pen” or “bone.” The beaks of Cuttle-fishes, though not
abundant, are sufficiently plentiful to have earned for them-
selves the general title of ‘‘ Rhyncholites ;” and in their form
and function they resemble the horny, parrot-like beak of the
existing Cephalopods. ‘The ink-bag or leathery sac in which
the Cuttle-fishes store up the black pigment with which they
obscure the water when attacked, owes its preservation to the
fact that the colouring-matter which it contains is finely-divid-
ed carbon, and therefore nearly indestructible except by heat.
Many of these ink-bags have been found in the Lias; and the
colouring-matter is sometimes so well preserved that it has
been, as an experiment, employed in painting as a fossil
“sepia.” The “pens” of the Cuttle-fishes are not commonly
preserved, owing to their horny consistence, but they are not
unknown. The form here figured (Leloteuthis subcostata, fig.
172) belonged to an old type essentially similar to our modern
Calamaries, the skeleton of which consists of a horny shaft

240 HISTORICAL PALAONTOLOGY.

and two lateral wings, somewhat like a feather in general
shape. When, on the other hand, the internal skeleton is
calcareous, then it is very easily preserved
in a fossil condition; and the abundance
of remains of this nature in the Secondary
rocks, combined with their apparent total
absence in Paleozoic strata, is a strong pre-
sumption in favour of the view that the order
of the Cuttle-fishes did not come into exis-
tence till the commencement of the Meso-
zoic period. The great majority of the skele-
tons of this kind which are found in the Jur-
assic rocks belong to the great extinct family
of the “‘ Belemnites” (Belemnitide), which, so
far as known, is entirely confined to rocks
of Secondary age. From its pointed, gener-
ally cylindro-conical form, the skeleton of
the Belemnite is popularly known as a “thun-
ees derbolt ” (fig. 173, C). In its perfect condition
Pease —1in which it is, however, rarely obtainable—
the skeleton consists of a chambered conical
shell (the ‘“phragmacone ”’), the partitions between the chambers
of which are pierced by a marginal tube or “siphuncle.” This
conical shell—curiously similar in its structure to the external
shell of the Nautilus—is extended forwards into a horny
“pen,” and is sunk in a corresponding conical pit (fig. 173, B),
excavated in the substance of a nearly cylindrical fibrous
body or ‘‘guard,” which projects backwards for a longer or
shorter distance, and is the part most usually found in a fossil
condition. Many different kinds of Belemnites are known, and
their guards literally swarm in many parts of the Jurassic series,
whilst some specimens attain very considerable dimensions.
Not only is the internal skeleton known, but specimens of
Belemnites and the nearly allied Belemnoteuthts have been found
in some of the fine-grained sediments of the Jurassic formation,
from which much has been learnt even as to the anatomy of
the soft parts of the animal. Thus we know that the Belem-
nites were in many respects comparable with the existing
Calamaries or Squids, the body being furnished with lateral
fins, and the head carrying a circle of ten “arms,” two of
which were longer than the others (fig. 173, A). The suckers
on the arms were provided, further, with horny hooks; there
was a large ink-sac; and the mouth was armed with horny
mandibles resembling in shape the beak of a parrot.
Coming next to the Vertebrates, we find that the Jurassic

THE JURASSIC PERIOD. 241

Fishes are still represented by Ganoids and Placoids. The
Ganoids, however, unlike the old forms, now for the most

Fig. 173.—A, Restoration of the animal of the Belemnite ; B, Diagram showing the
complete skeleton of a Belemnite, consisting of the chambered phragmacone (a), the

guard (4), and the horny pen (c); C, Specimen of Belemnites canaliculatus, from the
Inferior Oolite. (After Phillips.)

part possess nearly or quite symmetrical (‘‘ homocercal”) tails.
A characteristic genus is Zeragonolepis (fig. 174), with its

WS

Fig. 174.—Tetragonolepis (restored), and scales of the same. Lias.

deep, compressed body, its rhomboidal, closely-fitting scales,
and its single long dorsal fin. Amongst the Placoids the teeth

242 HISTORICAL PALEZONTOLOGY.

of true Sharks (JVotedanus) occur for the first time ; but by far
the greater number of remains referable to this group are still
the fin-spines and teeth of ‘ Cestracionts,’ resembling the
living Port-Jackson Shark. Some of these teeth are pointed
(Hybodus) ; but others are rounded, and are adapted for crush-
ing shell-fish. Of these latter, the commonest are the teeth of
Acrodus (fig. 175), of which the hinder ones are of an elon-
gated form, with a rounded
surface, covered with fine
transverse striz proceed-
ing from a central longi-
tudinal line. From their

ee: general form and striation,
Fig. 175.—Tooth of Acrodus nobilis. Lias. and their dark colour, these
teeth are commonly called

“fossil leeches” by the quarrymen.

The Amphibian group of the Zabyrinthodonts, which was so
extensively developed in the Trias, appears to have become
extinct, no representative of the order having hitherto been
detected in rocks of Jurassic age.

Much more important than the Fishes of the Jurassic series
are the Aeftiles, which are both very numerous, and belong to
a great variety of types, some of these being very extraordinary
in their anatomical structure. The predominant group is that
of the ‘‘ Enaliosaurs” or ‘ Sea-lizards,” divided into two great
orders, represented respectively by the /cithyosaurus and the
Plestosaurus.

The J/chthyosauri or “ Fish-Lizards” are exclusively Meso-
zoic in their distribution, ranging from the Lias to the Chalk,
but abounding especially in the former. They were huge
Reptiles, of a fish-like form, with a hardly conspicuous neck
(fig. 176), and probably possessing a simply smooth or

Fig. 176.—Ilckthyosaurus communis. Lias.

wrinkled skin, since no traces of scales or bony integumentary,
plates have ever been discovered. The tail was long, and
was probably furnished at its extremity with a powerful ex-
pansion of the skin, constituting a tail-fin similar to that pos-
sessed by the Whales. The limbs are also like those of Whales

THE JURASSIC PERIOD. 243

in the essentials of their structure, and in their being adapted
to act as swimming-paddles. Unlike the Whales, however,
the Ichthyosaurs possessed the hind-limbs as well as the fore-
limbs, both pairs having the bones flattened out and the fin-
gers completely enclosed in the skin, the arm and leg being at
the same time greatly shortened. The limbs are thus con-
verted into efficient ‘ flippers,” adapting the animal for an
active existence in the sea. The different joints of the back-
bone (vertebree) also show the same adaptation to an aquatic
mode of life, being hollowed out at both ends, like the bicon-
cave vertebrz of Fishes. The spinal column in this way was
endowed with the flexibility necessary for an animal intended
to pass the greater part of its time in water. ‘Though the /cA-
thyosaurs are undoubtedly marine animals, there is, however,
reason to believe that they occasionally came on shore, as they
possess a strong bony arch, supporting the fore-limbs, such as
would permit of partial, if laborious, terrestrial progression.
The head is of enormous size, with greatly prolonged jaws,
holding numerous powerful conical teeth lodged in a common
groove. The nature of the dental apparatus is such as to
leave no doubt as to the rapacious and predatory habits of the
Ichthyosaurs—an inference which is further borne out by the
examination of their petrified droppings, which are known to
geologists as “coprolites,” and which contain numerous frag-
ments of the bones and scales of the Ganoid fishes which
inhabited the same seas. The orbits are of huge size; and as
the eyeball was protected, like that of birds, by a ring of bony
plates in its outer coat, we even know that the pupils of the
eyes were of correspondingly large dimensions. As these bony
plates have the function of protecting the eye from injury
under sudden changes of pressure in the surrounding medium,
it has been inferred, with great probability, that the Ichthy-
esaurs were in the habit of diving to considerable depths in
the sea. Some of the larger specimens of /chthyosaurus which
have been discovered in the Lias indicate an animal of from
20 to nearly 4o feet in length ; and many species are known to
have existed, whilst fragmentary remains of their skeletons are
very abundant in some localities. We may therefore safely
conclude that these colossal Reptiles were amongst the most
formidable of the many tyrants of the Jurassic seas.

The Plestosaurus (fig. 177) is another famous Oolitic
Reptile, and, like the preceding, must have lived mainly or
exclusively in the sea. It agrees with the Ichthyosaur in some
important features of its organisation, especially in the fact
that both pairs of limbs are converted into “flippers” or

244 HISTORICAL PALASONTOLOGY.

swimming-paddles, whilst the skin seems to have been equally
destitute of any scaly or bony investiture. Unlike the /cAthy-

ae MUU

> AASRRRAELE

Fig. 177.—Plestosaurus dolichodeirus, restored. Lias.

osaur, however, the Plestosaur had the paddles placed far back,
the tail being extremely short, and the neck greatly lengthened
out, and composed of from twenty to forty vertebre. The
bodies of the vertebrze, also, are not deeply biconcave, but are
flat, or only slightly cupped. The head is of relatively small
size, with smaller orbits than those of the /cAthyosaur, and with
a snout less elongated. The jaws, however, were armed with
numerous conical teeth, inserted in distinct sockets. As re-
gards the habits of the /Vestosaur, Dr Conybeare arrives at the
following conclusions: ‘“ That it was aquatic is evident from
the form of its paddles ; that it was marine is almost equally
so from the remains with which it is universally associated ;
that it may have occasionally visited the shore, the resem-
blance of its extremities to those of the Turtles may lead us to
conjecture: its movements, however, must have been very
awkward on land; and its long neck must have impeded its
progress through the water, presenting a strong contrast to the
organisation which so admirably fits the /chthyosaurus to cut
through the waves.” As its respiratory organs were such that
it must of necessity have required to obtain air frequently, we
may conclude “that it swam upon or near the surface, arching
back its long neck like a swan, and occasionally darting it
down at the fish which happened to float within its reach. It
may perhaps have lurked in shoal water along the coast, con-
cealed amongst the sea- weed ; and raising its nostrils to a

THE JURASSIC PERIOD. 245

level with the surface from a considerable depth, may have
found a secure retreat from the assaults of powerful enemies ;
while the length and flexibility of its neck may have compen-
sated for the want of strength in its jaws, and its incapacity
for swift motion through the water.”

About twenty species of Fleszosaurus are known, ranging
from the Lias to the Chalk, and specimens have been found
indicating a length of from eighteen to twenty feet. The
nearly related ‘‘ Plziosaurs,” however, with their huge heads
and short necks, must have occasionally reached a length of at
least forty feet—the skullin some species being eight, and the
paddles six or seven feet long, whilst the teeth are a foot in
length.

Another extraordinary group of Jurassic Reptiles is that of
the “ Winged Lizards” or Prerosauria. ‘These are often spoken
of collectively as ‘‘ Pterodactyles,” from Prerodactylus, the
type-genus of the group. As now restricted, however, the
genus Pterodactylus is more Cretaceous than Jurassic, and it is
associated in the Oolitic rocks with the closely allied genera
Dimorphodon and Rhamphorhynchus. In all three of these
genera we have the same general structural organisation, in-
' volving a marvellous combination of characters, which we are in
the habit of regarding as peculiar to Birds on the one hand, to
Reptiles on another hand, and to the Flying Mammals or
Bats in a third direction. The “ Pterosaurs” are ‘“ Flying”
Reptiles, in the true sense of the term, since they were indu-
bitably possessed of the power of active locomotion in the air,
after the manner of Birds. ‘The so-called “ Flying” Reptiles
of the present day, such as the little Draco volans of the East
Indies and Indian Archipelago, possess, on the other hand, no
power of genuine flight, being merely able to sustain themselves,
in the air through the extensive leaps which they take from tree
to tree, the wing-like expansions of the skin simply exercising
the mechanical function of a parachute. The apparatus of flight
in the ‘‘ Pterosaurs” is of the most remarkable character, and
most resembles the “wing” of a Bat, though very different in
some important particulars. The “wing” of the Pterosaurs is
like that of Bats, namely, in consisting of a thin leathery expan-
sion of the skin which is attached to the sides of the body, and
stretches between the fore and hind limbs, being mainly sup-
ported by an enormous elongation of certain of the digits of
the hand. In the Bats, it is the four outer fingers which are-
thus lengthened out ; but in the Pterosaurs, the wing-membrane
is borne by a single immensely - extended finger (fig. 178).
No trace of the actual wing-membrane itself has, of course,

246 HISTORICAL PALZZONTOLOGY.

been found fossilised ; but we could determine that the ‘ Ptero-
dactyles”’ possessed the power of flight, quite apart from the ex-

Fig. 178.—Ptrerodactylus crasstrostris. From the Lithographic Slates of Solenhofen
(Middle Oolite). The figure is “‘ restored,” and it seems certain that the restoration is
incorrect in the comparatively unimportant particular, that the hand should consist of no

more than four fingers, three short and one long, instead of five, as represented.

traordinary conformation of the hand. The proofs of this are to
be found partly in the fact that the breast-bone was furnished
with an elevated ridge or keel, serving for the attachment of
the great muscles of flight, and sti!l more in the fact that the
bones were hollow and were filled with air —a peculiarity
wholly confined amongst living animals to Birds only. The
skull of the Pterosaurs is long, light, and singularly bird-like in
appearance—a resemblance which is further increased by the
comparative length of the neck and the size of the vertebrze of
this region (fig. 178). The jaws, however, unlike those of any
existing Bird, were, with one exception to be noticed hereafter,
furnished with conical teeth sunk in distinct sockets; and
there was always a longer or shorter tail composed of distinct
vertebrze ; whereas in all existing Birds the tail is abbreviated,
and the terminal vertebre are amalgamated to form a single
bone, which generally supports the great feathers of the tail.
Modern naturalists have been pretty generally agreed that
the Prerosaurs should be regarded as a peculiar group of the
Reptiles ; though they have been and are still regarded by
high authorities, like Professor Seeley, as being really referable

THE JURASSIC PERIOD. 2am

to the Birds, or as forming a class by themselves. The chief
‘points which separate them from Birds, as a class, are the
character of the apparatus of flight, the entirely different struc-
ture of the fore-limb, the absence of feathers, the composition
of the tail out of distinct vertebree, and the general presence
of conical teeth sunk in distinct sockets in the jaws. The gap
between the Pterosaurs and the Birds has, however, been
greatly lessened of late by the discovery of fossil animals
(Lchthyornis and Hesperornis) with the skeleton proper to Birds
combined with the presence of teeth in the jaws, and by the
still more recent discovery of other fossil animals (/%eranodon)
with a Pterosaurian skeleton, but without teeth ; whilst the un-
doubtedly feathered A7cheopteryx possessed a long tail com-
posed of separate vertebrze. Upon the whole, therefore, the
relationships of the Pterosaurs cannot be regarded as absolutely
settled. It seems certain, however, that they did not possess
feathers—this implying that they were cold-blooded animals ;
and their affinities with Reptiles in this, as in other characters,
are too strong to be overlooked.

The Prerosaurs are wholly Mesozoic, ranging from the Lias
to the Chalk inclusive ; and the fine-grained Lithographic Slate
of Solenhofen has proved to be singularly rich in their remains.
The genus Prerodactylus itself has the jaws toothed to the ex-
tremities with equal-sized conical teeth, and its species range
from the Middle Oolites to the Cretaceous series, in connec-
tion with which they will be again noticed, together with the
toothless genus Pteranodon. ‘The genus Dimorphodon is Li-
assic, and is characterised by having the front teeth long and
pointed, whilst the hinder teeth are small and lancet-shaped.
Lastly, the singular genus Ahamphorhynchus, also from the
Lower Oolites, is distinguished by the fact that there are teeth
present in the hinder portions of both jaws; but the front por-
tions are toothless, and may have constituted a horny beak.
Like most of the other Jurassic Pterosaurs, Rhamphorhynchus
(fig. 179) does not seem to have been much bigger than a
pigeon, in this respect falling far below the giant ‘‘ Dragons”’
of the Cretaceous period. It differed from its relatives, not
only in the armature of the mouth, but also in the fact that
the tail was of considerable length. With regard to its habits
and mode of life, Professor Phillips remarks that, “ gifted with
ample means of flight, able at least to perch on rocks and
scuffle along the shore, perhaps competent to dive, though not
so well as a Palmiped bird, many fishes must have yielded to
the cruel beak and sharp teeth of Rhamphorhynchus. If we
ask to which of the many families of Birds the analogy of

248 HISTORICAL PALZONTOLOGY.

structure and probable way of life would lead us to assimilate
Rhamphorhynchus, the answer must point to the swimming

Fig. 179.—Rhamphorhynchus Buckland, restored. Bath Oolite, England.
(After the late Professor Phillips.)

races with long wings, clawed feet, hooked beak, and habits of
violence and voracity ; and for preference, the shortness of the
legs, and other circumstances, may be held to claim for the
Stonesfield fossil a more than fanciful similitude to the groups
of Cormorants, and other marine divers, which constitute an
effective part of the picturesque army of robbers of the sea.”
Another extraordinary and interesting group of the Mesozoic
Reptiles is constituted by the Deznosauria, comprising a series
of mostly gigantic forms, which range from the Trias to the
Chalk. All the ‘‘ Deinosaurs” are possessed of the two pairs
of limbs proper to Vertebrate animals, and these organs are in
the main adapted for walking on the dry land. Thus, whilst
the Mesozoic seas swarmed with the huge Ichthyosaurs and
Plesiosaurs, and whilst the air was tenanted by the Dragon-like
Pterosaurs, the land-surfaces of the Secondary period were
peopled by numerous forms of Deinosaurs, some of them of
even more gigantic dimensions than their marine brethren.
The limbs of the Dezzosaurs are, as just said, adapted for pro-
gression on the land; but in some cases, at any rate, the
hind-limbs were much longer and stronger than the fore-limbs ;
and there seems to be no reason to doubt that many of these
forms possessed the power of walking, temporarily or perman-
ently, on their hind-legs, thus presenting a singular resemblance
to Birds. Some very curious and striking points connected
with the structure of the skeleton have also been shown to
connect these strange Reptiles with the true Birds; and such
high authorities as Professors Huxley and Cope are of opinion
that the Deinosaurs are distinctly related to this class, being in
some respects intermediate between the proper Reptiles and
the great wingless Birds, like the Ostrich and Cassowary. On
the other hand, Professor Owen has shown that the Deinosaurs

THE JURASSIC PERIOD. 249

possess some weighty points of relationship with the so-called
“‘ Pachydermatous” Quadrupeds, such as the Rhinoceros and
Hippopotamus. The most important Jurassic genera of
Deinosauria are Megalosaurus and Cetiosaurus, both of which
extend their range into the Cretaceous period, in which
flourished, as we shall see, some other well-known members
of this order.

Megalosaurus attained gigantic dimensions, its thigh and
shank bones measuring each about three feet in length, and its
total length, including the tail, being estimated at from forty
to fifty feet. As the head of the thigh-bone is set on nearly
at right angles with the shaft, whilst all the long bones of the
skeleton are hollowed out internally for the reception of the
marrow, there can be no doubt as to the terrestrial habits of
the animal. ‘The skull (fig. 180) was of large size, four or five

Fig. 180.—Skull of Megalosaurus, on a scale one-tenth of nature. Restored.
(After Professor Phillips.)

feet in length, and the jaws were armed with a series of power-
ful pointed teeth. The teeth are conical in shape, but are
strongly compressed towards their summits, their lateral edges
being finely serrated. In their form and their saw-like edges,
they resemble the teeth of the “‘ Sabre-toothed Tiger” (dZachat-
vodus), and they render it certain that the Megalosaur was in
the highest degree destructive and carnivorous in its habits.
So far as is known, the skin was not furnished with any armour
of scales or bony plates; and the fore-limbs are so dispro-"
portionately small as compared with the hind-limbs, that this
huge Reptile—like the equally huge Iguanodon—may be

250 HISTORICAL PALAZONTOLOGY.

conjectured to have commonly supported itself on its hind-
legs only.

The Cetiosaur attained dimensions even greater than those
of the Megalosaur, one of the largest thigh-bones measuring
over five feet in length and a foot in diameter in the middle,
and the total length of the animal being probably not less than
fifty feet. It was originally regarded as a gigantic Crocodile,
but it has been shown to bea true Deinosaur. Having ob-
tained a magnificent series of remains of this reptile, Professor
Phillips has been able to determine many very interesting
points as to the anatomy and habits of this colossal animal,
the total length of which he estimates as being probably not
less than sixty or seventy feet. As to its mode of life, this
accomplished writer remarks :—

“‘ Probably when ‘standing at ease’ not less than ten feet
in height, and of a bulk in proportion, this creature was un-
matched in magnitude and physical strength by any of the
largest inhabitants of the Mesozoic land or sea. Did it live
in the sea, in fresh waters, or on the land? This question
cannot be answered, as in the case of Ichthyosaurus, by appeal
to the accompanying organic remains; for some of the bones
lie in marine deposits, others in situations marked by estuarine
conditions, and, out of the Oxfordshire district, in Sussex, in
fluviatile accumulations. Was it fitted to live exclusively in
water? Such an idea was at one time entertained, in conse-
quence of the biconcave character of the caudal vertebrze, and
it is often suggested by the mere magnitude of the creature,
which would seem to have an easier life while floating in water,
than when painfully lifting its huge bulk, and moving with
slow steps along the ground. But neither of these arguments
is valid. The ancient earth was trodden by larger quadrupeds
than our elephant ; and the biconcave character of vertebre,
which is not uniform along the column in Cetiosaurus, is per=
haps as much a character of a geological period as of a me-
chanical function of life. Good evidence of continual life in
water is ylelded in the case of Ichthyosaurus and other Ena-
liosaurs, by the articulating surfaces of their limb-bones, for
these, all of them, to the last phalanx, have that slight and
indefinite adjustment of the bones, with much intervening
cartilage, which fits the leg to be both a flexible and forcible
instrument of natation, much superior to the ordinary oar-
blade of the boatman. On the contrary, in Cetiosaur, as well
as in Megalosaur and Iguanodon, all the articulations are
definite, and made so as to correspond to determinate move-

ments in particular directions, and these are such as to be

THE JURASSIC PERIOD. 251

suited for walking. In particular, the femur, by its head pro-
jecting freely from the acetabulum, seems to claim a movement
of free stepping more parallel to the line of the body, and
more approaching to the vertical than the sprawling gait of
the crocodile. The large claws concur in this indication of
terrestrial habits. But, on the other hand, these characters
are not contrary to the belief that the animal may have been
amphibious ; and the great vertical height of the anterior part
of the tail seems to support this explanation, but it does not
go further. . . . We have therefore a marsh-loving or
river-side animal, dwelling amidst filicine, cycadaceous, and
coniferous shrubs and trees full of insects and small mamma-
ha. What was its usual diet? If ex ungue leonem, surely ex
dente cibum. We have indeed but one tooth, and that small
and incomplete. It resembles more the tooth of Iguanodon
than that of any other reptile; for this reason it seems pro-
bable that the animal was nourished by similar vegetable food
which abounded in the vicinity, and was not obliged to con-
tend with Megalosaurus for a scanty supply of more stimu-
lating diet.”

All the groups of Jurassic Reptiles which we have hitherto
been considering are wholly unrepresented at the present day,
and do not even pass upwards into the Tertiary period. It
may be mentioned, however, that the Oolitic deposits have
also yielded the remains of Reptiles belonging to three of the
existing orders of the class—namely, the Lizards (Lacertilia),
the Turtles (Che/onza), and the Crocodiles (Crocodilia). ‘The
Lizards occur both in the marine strata of the Middle Oolites
and also in the fresh-water beds of the Purbeck series ; and
they are of such a nature that their affinities with the typical
Lacertilians of the present day cannot be disputed. The.
Chelonians, up to this point only known by the doubtful evi-
dence of footprints in the Permian and Triassic sandstones, are
here represented by unquestionable remains, indicating the ex-
istence of marine Turtles (the Chelone planiceps of the Portland
Stone). No remains of Serpents (Op/zdians) have as yet been
detected in the Jurassic ; but strata of this age have yielded
the remains of numerous Crocodilians, which probably inhab-
ited the sea. The most important member of this group is
Teleosaurus, which attained a length of over thirty feet, and
is in some respects allied to the living Gavials of India.

The great class of the Birds, as we have seen, is represented
in rocks earlier than the Oolites simply by the not absolutely
certain evidence of the three-toed footprints of the Connecti-
cut Trias. In the Lithographic Slate of Solenhofen (Middle

252 HISTORICAL PALAONTOLOGY.,

Oolite), there has been discovered, however, the at present
unique skeleton of a Bird well-known under the name of the
Archaeopteryx macrura (figs. 181, 182).- The only known

Fig. 181.—A rcheopteryx macrura, showing tail and tail-feathers, with detached bones.
Reduced, From the Lithographic Slate of Solenhofen.

specimen—now in the British Museum—unfortunately does
not exhibit the skull; but the fine-grained matrix has pre-

<>

Fig. 182.—Restoration of Archeopteryx macrura. (After Owen.)
s S.

served a number of the other bones of the skeleton, along with
the impressions of the tail and wing feathers. From these
remains we know that Archaeopteryx differed in some remark-

&

THE JURASSIC PERIOD. 253

able peculiarities of its structure from all existing members of
the class of Birds, ‘This extraordinary Bird (fig. 182) appears
to have been about as big as a Rook—the tail being long and
extremely slender, and composed of separate vertebre, each
of which supports a single pair of quill-feathers. In the flying
Birds of the present day, as before mentioned, the terminal
vertebree of the tail are amalgamated to form a single bone
(‘‘ ploughshare-bone ”), which supports a cluster of tail-feathers ;
and the tail itself is short. In the embryos of existing Birds
the tail is long, and is made up of separate vertebrae, and the
same character is observed in many existing Reptiles. The
tail of Archeopteryx, therefore, is to be regarded as the per-
manent retention of an embryonic type of structure, or as an
approximation to the characters of the Reptiles. Another
remarkable point in connection with Avcheopteryx, in which
it differs from ali known Birds, is, that the wing was furnished
with two free claws. From the presence of feathers, Arche-
opteryx may be inferred to have been hot-blooded ; and this
character, taken along with the structure of the skeleton of the
wing, may be held as sufficient to justify its being considered
as belonging to the class of Birds. In the structure of the
tail, however, it is singularly Reptilian ; and there is reason to
believe that its jaws were furnished with teeth sunk in distinct
sockets, as is the case in no existing Bird. This conclusion,
at any rate, is rendered highly probable by the recent discovery
of “ Toothed Birds” (Odontornithes) in the Cretaceous rocks
of North America.

The dZammadls of the Jurassic period are known to us by
a number of small forms which occur in the “ Stonesfield
Slate” (Great Oolite) and in the Purbeck beds (Upper.
Oolite). The remains of these are almost exclusively sepa-
rated halves of the lower jaw, and they indicate the existence
during the Oolitic period in Europe of.a number of small
“ Pouched animals” (J/arsupials). In the horizon of the
Stonesfield Slate four genera of these little Quadrupeds have
been described —viz., Amphilestes, Amphitherium, Phascolo-
thertum, and Stereognathus. In Amphitherium (fig. 183), the
molar teeth are furnished with small pointed eminences or
“cusps ;” and the animal was doubtless insectivorous. By
Professor Owen, the highest living authority on the subject,
Amphitherium is believed to be a small Marsupial, most
nearly allied to the living Banded Ant-eater (AZyrmecobius) of
Australia (fig. 158). Amphilestes and Phascolotherium (fig.
134) are also believed by the same distinguished anatomist
and Nee to have been insect-eating Marsupials, and

254 HISTORICAL PALZONTOLOGY.

the latter is supposed to find its nearest living ally in the
Opossums (Dzdelphys) of America. Lastly, the Stereognathus

Fig. 183.—Lower jaw of Amphitherium (Thylacotherium) Prevostit.
Stonesfield Slate (Great Oolite.)

of the Stonesfield Slate is in a dubious position. It may have
been a Marsupial; but, upon the whole, Professor Owen is
inclined to believe that it must have been a hoofed and her-
bivorous Quadruped belonging to the series of the higher Mam-
mals (flacentalia). In the Middle Purbeck beds, near to the
close of the Oolitic period, we have also evidence of the exist-
ence of a number of small Mammals, all of which are probably
Marsupials. Fourteen species are known, all of small size,
the largest being no bigger than a Polecat or Hedgehog. The
genera to which these little quadrupeds have been referred are’
Plagiaulax, Spatacothertum, Triconodon, and Gatlestes. The
first of these (fig. 184, 4) is believed by Professor Owen to

Fig. 184. Oolitic Mammals.—1, Lower jaw and teeth of Phascolotherium, Stonesfield
Slate ; 2, Lower jaw and teeth of Asmphitherium, Stonesfield Slate; 3, Lower jaw and
teeth of T7zconodon, Purbeck beds; 4, Lower jaw and teeth of Plagzaulaz, Purbeck

beds. All the figures are of the natural size.

have been carnivorous in its habits; but other authorities
maintain that it was most nearly allied to the living Kangaroo-
rats ({Zypsiprymnus) of Australia, and that it was essentially
herbivorous. The remaining three genera appear to have
been certainly insectivorous, and find their nearest living rep-
resentatives in the Australian Phalangers and the American
Opossums.

Finally, it is interesting to notice in how many respects the

THE JURASSIC PERIOD: 255

Jurassic fauna of Western Europe approached to that now
inhabiting Australia. At the present day, Australia is almost
wholly tenanted by Marsupials ; upon its land-surface flourish
Araucarig and Cycadaceous plants, and in its seas swims the
Port-Jackson Shark (Cestracion Philippz) ; whilst the Mollus-
can genus 7Z77gonta is nowadays exclusively confined to the
Australian coasts. In England, at the time of the deposition
of the Jurassic rocks, we must have had a fauna and flora very
closely resembling what we now see in Australia. The small
Marsupials, Amphitherium, Phascolothertum, and others, prove
that the Mammals were the same in order; cones of Arau-
carian pines, with tree-ferns and fronds of Cycads, occur
throughout the Oolitic series; spine-bearing fishes, like the
Port-Jackson Shark, are abundantly represented by genera
such as Acrodus and Strophodus ; and lastly, the genus 7Z7z-
gonia, now exclusively Australian, is represented in the Oolites
by species which differ little from those now existing. More-
over, the discovery during recent years of the singular Mud-fish,
the Ceratodus Fosteri, in the rivers of Queensland, has added
another and a very striking point of resemblance to those
already mentioned; since this genus of Fishes, though pre-
eminently Triassic, nevertheless extended its range into the
Jurassic. Upon the whole, therefore, there is reason to con-
clude that Australia has undergone since the close of the
Jurassic period fewer changes and vicissitudes than any other
known region of the globe; and that this wonderful continent
has therefore succeeded in preserving a greater number of
the characteristic life-features of the Oolites than any other
country with which we are acquainted.

LITERATURE,

The following list comprises some of the more important sources of
information as to the rocks and fossils of the Jurassic series :—
(1) ‘ Geology of Oxford and the Thames Valley.’ Phillips.
(2) ‘ Geology of Yorkshire,’ vol. ii. Phillips.
(3) ‘ Memoirs of the Geological Survey of Great Britain.’
(4) ‘ Geology of Cheltenham.’ Murchison, 2d ed. Buckman.
(5) ‘ Introduction to the Monograph of the Oolitic Asteriadz’ (Paleon-
tographical Society). Wright.
(6) ‘* Zone of Avicula contorta and the Lower Lias of the South of
England ”—‘ Quart. Journ. Geol. Soc.,’ vol. xvi., 1860. Wright.
(7) ‘‘ Oolites of Northamptonshire ”—‘ Quart. Journ. Geol. Soc.,’ vols.
xxvi. and xxix. Sharp.
(3) ‘Manual of Geology.’ Dana.
(9) ‘ Der Jura.’ Quenstedt.
(10) ‘ Das Flotzgebirge Wiirttembergs.’ Quenstedt,
(11) ‘Jura Formation.’ Oppel.

256 HISTORICAL PALASON TOLOGY.

(12) ‘ Paléontologie du Département de la Moselle.” Terquem.

(13) ‘Cours elementaire de Paléontologie.’ D’Orbigny.

(14) * Paléontologie Francaise.’ D’Orbigny.

(15) ‘ Fossil Echinodermata of the Oolitic Formation’ (Palzeontographi-
cal Society). Wright.

(16) ‘ Brachiopoda of the Oolitic Formation’ (Palzeontographical So-
ciety). Davidson.

(17) ‘ Mollusca of the Great Oolite’ (Palzeontographical Society). Mor-
ris and Lycett.

(18) ‘ Monograph of the Fossil Trigoniz’ (Palzontographical Society).
Lycett.

(19) ‘Corals of the Oolitic Formation’ (Palzontographical Society).
Edwards and Haime.

(20) ‘Supplement to the Corals of the Oolitic Formation’ (Palzeonto-
graphical Society). Martin Duncan. .

(21) ‘Monograph of the Belemnitidze’ (Palzeontographical Society).
Phillips.

(22) ‘Structure of the Belemnitidee’ (Mem. Geol. Survey). Huxley.

(23) ‘Sur les Belemnites.’ Blainville.

(24) ‘Cephalopoden.’ Quenstedt.

(25) ‘ Mineral Conchology.’ Sowerby.

(26) ‘Jurassic Cephalopoda’ (Palzeontologica Indica). Waagen.

(27) ‘ Manual of the Mollusca.” Woodward.

) ‘Petrefaktenkunde.’ Schlotheim.

(29) ‘ Bridgewater Treatise.’ Buckland.

(30) ‘ Versteinerungen des Oolithengebirges.” Roemer.

(31) ‘ Catalogue of British Fossils.’ Morris.

(32) ‘ Catalogue of Fossils in the Museum of Practical Geology.’ Ether-
idge.

(33) ‘ Beitrage zur Petrefaktenkunde.’ Miinster.

(34) ‘ Petrefacta Germaniz.’ Goldfuss.

(35) ‘ Lethzea Rossica.’ Eichwald.

(36) ‘ Fossil Fishes’ (Decades of the Geol. Survey). Sir Philip Egerton.

(37) ‘ Manual of Palzeontology.’ Owen.

(38) ‘ British Fossil Mammals and Birds.’ Owen.

(39) ‘Monographs of the Fossil Reptiles of the Oolitic Formation’ (Pale-
ontographical Society). Owen.

(40) ‘ Fossil Mammals of the Mesozoic Formations’ (Palzeontographical
Society). Owen.

(41) ‘Catalogue of Ornithosauria.’ Seeley.

(42) ‘* Classification of the Deinosauria ”—‘ Quart. Journ. Geol. Soc.,’
vol. xxvi., 1870, Huxley.

GHAPTER -XVIFT.
THE: CRETACEOUS: PERIOD.
The next series of rocks in ascending order is the great and

important series of the Cretaceous Rocks, so called from the
general occurrence in the systemvof chalk (Lat. cre¢a, chalk).

THE CRETACEOUS PERIOD. 257

As developed in Britain and Europe generally, the following
leading subdivisions may be recognised im the Cretaceous
series :—

. Wealden,

Lower Greensand or Neocomian,
Gault,

Upper Greensand,

Chalk,

. Maestricht beds,

Lower Cretaceous.

Upper Cretaceous.

Duy Sm

I. Wealden.—The Wealden formation, though of consider-
able importance, is a local group, and is confined to the south-
east of England, France, and some other parts of Europe. Its
name is derived from the Wea/d, a district comprising parts of
Surrey, Sussex, and Kent, where it is largely developed. Its
lower portion, for a thickness of from 500 to 1000 feet, is
arenaceous, and is known as the Hastings Sands. Its Upper
portion, for a thickness of 150 to nearly 300 feet, is chiefly
argillaceous, consisting of clays with sandy layers, and occa-
sionally courses of limestone. The geological importance of
the Wealden formation is very great, as it is undoubtedly the
delta of an ancient river, being composed almost wholly of
fresh-water beds, with a few brackish-water and even marine
strata, intercalated in the lower portion. Its geographical
extent, though uncertain, owing to the enormous denudation
to which it has been subjected, is nevertheless great, since it
extends from Dorsetshire to France, and occurs also in North
Germany. Still, even if it were continuous between all these
points, it would not be larger than the delta of such a modern
river as the Ganges. The river which produced the Wealden
series must have flowed from an ancient continent occupying
what is now the Atlantic Ocean; and the time occupied in
the formation of the Wealden must have been very great,
though we have, of course, no data by which we can accurately
calculate its duration.

The fossils of the Wealden series are, naturally, mostly the
remains of such animals as we know at the present day as in-
habiting rivers. We have, namely, fresh-water Mussels ( Uz),
River-snails (Paludina), and other fresh-water shells, with
numerous little bivalved Crustaceans, and some fishes.

Il. Lower Greensand (Néocomien of D'Orbigny). — The
Wealden beds pass upward, often by insensible gradations,
into the Lower Greensand. The name Lower Greensand is
not an appropriate one, for green sands only occur sparingly
and occasionally, and are found in other formations. For this

258 HISTORICAL PALZONTOLOGY.

reason it has been proposed to substitute for Lower Greensand
the name /Veocomian, derived from the town of Neufchatel—
anciently called Veocomum—in Switzerland. If this name
were adopted, as it ought to be, the Wealden beds would be
called the Lower Neocomian.

The Lower Greensand or Neocomian of Britain has a thick-
ness of about 850 feet, and consists of alternations of sands,
sandstones, and clays, with occasional calcareous bands. ‘The
general colour of the series is dark brown, sometimes red ; and
the sands are occasionally green, from the presence of silicate
of iron.

The fossils of the Lower Greensand are purely marine, and
among the most characteristic are the shells of Cephalopods.

The most remarkable point, however, about the fossils of
the Lower Cretaceous series, is their marked divergence from
the fossils of the Upper Cretaceous rocks. Of 280 species of
fossils in the Lower Cretaceous series, only 51, or about 18
per cent, pass on into the Upper Cretaceous. This break in
the life of the two periods is accompanied by a decided phy-
sical break as well; for the Gault is often, if not always, un-
conformably superimposed on the Lower Greensand. At the
same time, the Lower and Upper Cretaceous groups form a
closely-connected and inseparable series, as shown by a com-
parison of their fossils with those of the underlying Jurassic
rocks and the overlying Tertiary beds. Thus, in Britain no
marine fossil is known to be common to the marine beds of
the Upper Oolites and the Lower Greensand ; and of more
than 500 species of fossils in the Upper Cretaceous rocks,
almost every one died out before the formation of the lowest
Tertiary strata, the only survivors being one Brachiopod and a
few Foraminifera. .

Ill. Gault (Aptien of D’Orbigny).—The lowest member of
the Upper Cretaceous series is a stiff, dark - grey, blue, or
brown clay, often worked for brick-making, and known as the
Gault, from a provincial English term. It occurs chiefly in
the south-east of England, but can be traced through France
to the flanks of the Alps and Bavaria. It never exceeds 100
feet in thickness ; but it contains many fossils, usually in a
state of beautiful preserv ation.

IV. Upper Greensand (Albien of D’Orbigny ; Unterquader
and Lower Plainerkalk of Germany).—The Gault is succeeded
upward by the Upper Greensand, which varies in thickness
from 3 up to roo feet, and which derives its name from the
occasional occurrence in it of green sands. These, however,
are local and sometimes wanting, and the name “ Upper

THE CRETACEOUS PERIOD. 259

Greensand ” is to be regarded as a zame and not a description.
The group consists, in Britain, of sands and clays, sometimes
with bands of calcareous grit or siliceous limestone, and occa-
sionally containing concretions of phosphate of lime, which are
largely worked for agricultural purposes.

V. White Chalk.—TVhe top of the Upper Greensand be-
comes argillaceous, and passes up gradually into the base of
the great formation known as the true Chavk, divided into
the three subdivisions of the chalk-marl, white chalk without
flints, and white chalk with flints. The first of these is sim-
ply argillaceous chalk, and passes up into a great mass of
obscurely-stratified white chalk in which there are no flints
(Zuronien of D’Orbigny ; Alcttelguader of Germany). This, in
turn, passes up into a great mass of white chalk, in which the
stratification is marked by nodules of black flint arranged in
layers (.Sézonzen of D’Orbigny ; Oberguader of Germany). The
thickness of these three subdivisions taken together is some-
times over 1ooo feet, and their geographical extent is very
great. White Chalk, with its characteristic appearance, may
be traced from the north of Ireland to the Crimea, a distance
of about 1140 geographical miles; and, in an opposite direction,
from the south of Sweden to Bordeaux, a distance of about
840 geographical miles.

VI. In Britain there occur no beds containing Chalk fossils,
or in any way referable to the Cretaceous period, above the
true White Chalk with flints. On the banks of the Maes,
however, near Maestricht in Holland, there occurs a series of
yellowish limestones, of about too feet in thickness, and un-
doubtedly superior to the White Chalk. These Maestricht
beds (Danien of D’Orbigny) contain a remarkable series of
fossils, the characters of whieh are partly Cretaceous and
partly Tertiary. Thus, with the characteristic Chalk fossils,
Belemnites, Baculites, Sea-Urchins, &c., are numerous Univalve
Molluscs, such as Cowries and Volutes, which are otherwise
exclusively Tertiary or Recent.

Holding a similar position to the Maestricht beds, and
showing a similar intermixture of Cretaceous forms with later
types, are certain beds which occur in the island of Seeland,
in Denmark, and which are known as the Faxce Limestone.

Of a somewhat later date than the Maestricht beds is the
Pisolitic Limestone of France, which rests unconformably on
the White Chalk, and contains a large number of Tertiary
fossils along with some characteristic Cretaceous types.

The subjoined sketch-section exhibits the general succession
of the Cretaceous deposits in Britain :—

260 HISTORICAL PALEONTOLOGY.

GENERALISED SECTION OF THE CRETACEOUS SERIES
OF BRITAIN.

Fig. 185.
Eocene.

---—--- White Chalk with Flints.

n------ White Chalk without Flints.

UPPER CRETACEOUS.

Par ed ee Upper Greensand.

(2 SS SS SaaS Chalk Marl.

Lower Greensand or Neo-
comian.

SS Weald Clay.

une Wealden Series.

LOWER CRETACEOUS.

Hastings Sands.

In North America, strata of Lower Cretaceous age are well
represented in Missouri, Wyoming, Utah, and in some other
areas-; but the greater portion of the American deposits of
this period are referable to the Upper Cretaceous. The rocks
of this series are mostly sands, clays, and limestones— Chalk
itself being unknown except in Western Arkansas. Amongst
the sandy accumulations, one of the most important is the so-

THE CRETACEOUS PERIOD. 261

called “‘marl” of New Jersey, which is truly a “ Greensand,”
and contains a large proportion of glauconite (silicate of iron
ard potash). It also contains a little phosphate of lime, and is
largely worked for agricultural purposes. ‘The greatest thick-
ness attained by the Cretaceous rocks of North America is
about gooo feet, as in Wyoming, Utah, and Colorado. Ac-
cording to Dana, the Cretaceous rocks of the Rocky Mountain
territories pass upwards “without interruption into a coal-
bearing formation, several thousand feet thick, on which the
following Tertiary strata lie unconformably.” ‘The lower por-
tion of this “ Lignitic formation” appears to be Cretaceous,
and contains one or more beds of Coal; but the upper part of it
perhaps belongs to the Lower Tertiary. In America, therefore,
the lowest Tertiary strata appear to rest conformably upon the
highest Cretaceous ; whereas in Europe, the succession at this
point is invariably an unconformable one. Owing, however, to
the fact that the American “ Lignitic formation” is a shallow-
water formation, it can hardly be expected to yield much
material whereby to bridge over the great palzontological gap
between the White Chalk and Eocene in the Old World.

- Owing to the fact that so large a portion of the Cretaceous
formation has been deposited in the sea, much of it in deep
water, the plants of the period have for the most part been
found special members of the series, such as the Wealden beds,
the Aix-la-Chapelle sands, and the Lignitic beds of North
America. Even the purely marine strata, however, have
yielded plant-remains, and some of these are peculiar and
proper to the deep-sea deposits of the series. Thus the little
calcareous discs termed ‘‘ coccoliths,” which are known to be
of the nature of calcareous sea-weeds (A/g@) have been de-
tected in the White Chalk ; and the flints of the same forma-
tion commonly contain the spore-cases of the microscopic
Desmids (the so-called Xanthidia), along with the siliceous cases
of the equally diminutive Dzazoms.

The plant-remains of the Lower Cretaceous greatly resemble
those of the Jurassic period, consisting mainly of Ferns, Cy-
cads, and Conifers. The Upper Cretaceous rocks, however,
both in Europe and in North America, have yielded an abun-
dant flora which resembles the existing vegetation of the globe -
in consisting mainly of Angiospermous Exogens and of Mono-
cotyledons.* In Europe the plant-remains in question have

* The ‘‘ Flowering plants” are divided into the two great groups of the
Endogens and Exogens. The Zzdogens (such as Grasses, Palms, Lilies,
&c.) have no true bark, nor rings of growth, and the stem is said to be
**endogenous ;” the young plant also possesses but a single seed-leaf or

262 HISTORICAL PALEONTOLOGY.

been found chiefly in certain sands in the neighbourhood of Aix-
la-Chapelle, and they consist of numerous Ferns, Conifers (such
as Cycadopteris), Screw Pines (Pandanus), Oaks (Quercus), Wal-
nut (Juglans), Fig (Ficus), and many Proteacee, some of which are
referred to existing genera (Dryandra, Banksia, Grevillea, &c.)
In North America, the Cretaceous strata of New Jersey,
Alabama, Nebraska, Kansas, &c., have yielded the remains of
numerous plants, many of which belong to existing genera.
Amongst these may be mentioned Tulip-trees (Lzriodendron),
Sassafras (fig. 186), Oaks (Quercus), Beeches (Fagus), Plane-
trees (Platanus), Alders (Alnus), Dog-wood (Cornus), Willows
(Salex), Poplars (Populus), Cypresses (Cupressus), Bald Cy-
presses (Zaxodium), Magnolias, &c. Besides these, however,
there occur other forms which have now entirely disappeared
from North America—as, for example, species of Cimnamomum
and Araucarvia.
It follows from the above, that the Lower and Upper Creta-
ceous rocks are, from a botanical point of view, sharply sepa-
rated from one another. The Palzozoic period, as we have
seen, is characterised by the prevalance of “ Flowerless” plants
(Cryptogams), its higher vegetation consisting almost exclu-
sively of Conifers. The Mesozoic period, as a whole, is charac-
terised by the prevalence of the Cryptogamic group of the
Ferns, and the Gymnospermic groups of the Conifers and the
Cycads. Up to the close of the Lower Cretaceous, no Angio-
spermous Exogens are certainly known to have existed, and
Monocotyledonous plants or Endogens are very poorly repre-
sented. With the Upper Cretaceous, however, a new era of
plant-life, of which our present is but the culmination, com-
menced, with a great and apparently sudden development of new
forms. In place of the Ferns, Cycads, and Conifers of the earlier
Mesozoic deposits, we have now an astonishingly large number
of true Angiospermous Exogens, many of them belonging to
existing types; and along with these are various Monocotyle-
donous plants, including the first examples of the great and 1m-

**cotyledon.” Hence these plants are often simply called ‘‘ M/onocotyledons.”
The £xogens, on the other hand, have a true bark; and the stem increases
by annual additions to the outside, so that rings of growth are produced.
The young plant has two seed-leaves or ‘‘cotyledons,” and these plants
are therefore called ‘‘ Dicotyledons.’’ Amongst the Exogens, the Pines
(Conifers) and the Cycads have seeds which are unprotected by a seed-
vessel, and they are therefore called ‘‘ Gymmnosperms.” All the other
Exogens, including the ordinary trees, shrubs, and flowering plants, have
the seeds enclosed in a seed-vessel, and are therefore called ‘* Angzo-
sperms.” The derivation of these terms will be found in the Glossary at
the end of the volume.

THE CRETACEOUS PERIOD. 263

portant group of the Palms. It is thus a matter of interest to
reflect that plants closely related to those now inhabiting the

Fig. 186 —Cretaceous Angiosperms. a, Sassafras Cretaceum ; b, Liriodendron
Meekii; c, Leguminosites Marcouanus ; da, Salix Meekit. (After Dana.)

earth, were in existence at a time when the ocean was tenanted
by Ammonites and Belemnites, and when land and sea and
air were peopled by the extraordinary extinct Reptiles of the
Mesozoic period.

As regards animal life, the Profozoans of the Cretaceous
period are exceedingly numerous, and are represented by /ora-
minifera and Sponges. As we have already seen, the White
Chalk itself is a deep-sea deposit, almost entirely composed
of the microscopic shells of Foraminzifers, along with Sponge-
spicules, and organic d@ébris of different kinds (see p. 22, fig. 7).
The green grains which are so abundant in several minor sub-
divisions of the Cretaceous, are also in many instances really
casts in glauconite of the chambered shells of these minute
organisms. A great many species of Foraminifera have been
recognised in the Chalk; but the three principal genera are

264 HISTORICAL PALHONTOLOGY.

Globigerina, Rotalia (fig. 187), and Textularia—groups which —

are likewise characteristic of the ‘‘ ooze” of the Atlantic and

Fig. 187.—Rotalia Boueana.

Pacific Oceans at great depths. ‘The flints of the Chalk also
commonly contain the shells of Foraminifera. The Upper
Greensand has yielded in considerable numbers the huge
Foraminifera described by Dr Carpenter under the name of
FParkeria, the spherical shells of which are composed of sand-
grains agglutinated together, and sometimes attain a diameter
of two and a quarter inches. The Cretaceous Sponges are
extremely numerous, and occur under a great number of varie-
ties of shape and structure; but the two most characteristic
genera are Stphonia and Ventriculites, both of which are ex-
clusively confined to strata of this age. The Siphonie (fig.
188) consist of a pear-shaped, sometimes lobed head, supported
by a longer or shorter stem, which breaks up at its base into a
number of root-like processes of attachment. The water gained
access to the interior of the Sponge by a number of minute
openings covering the surface, and ultimately escaped by a
single, large, chimney-shaped aperture at the summit. In some
respects these sponges present a singular resemblance to the
beautiful “ Vitreous Sponges” (o/tenia or Pheronema) of the
deep Atlantic ; and, like these, they were probably denizens
of a deep sea. The Ventriculites of the Chalk (fig. 189) is,
however, a genus still more closely allied to the wonderful
flinty Sponges, which have been shown, by the researches of
the Porcupine, Lightning, and Challenger expeditions, to live
half buried in the calcareous ooze of the abysses of our great
oceans. Many forms of this genus are-known, having ‘ usu-
ally the form of graceful vases, tubes, or funnels, variously
ridged or grooved, or otherwise ornamented on the surface,
frequently expanded above into a cup-like lip, and continued
below into a bundle of fibrous roots. The minute structure of
these bodies shows an extremely delicate tracery of fine tubes,

sometimes empty, sometimes filled with loose calcareous mat-

THE CRETACEOUS PERIOD. 265

ter dyed with peroxide of iron.”—(Sir Wyville Thomson.)
Many of the Chalk sponges, originally calcareous, have been
converted into flint subsequently ; but the Ventriculites are

YY

7 lyf
P,

\\

Fig. 188.—S7phonia ficus. Fig. 189.—Ventriculites simplex.
Upper Greensand, Europe. White Chalk, Britain.

really composed of this substance, and are therefore genuine
“‘Siliceous Sponges,” like the existing Venus’s Flower-Basket
(Zuplectella). Like the latter, the skeleton was doubtless ori-
ginally composed, in the young state, of disconnected six-
rayed spicules, which ultimately become fixed together to
constitute a continuous frame-work. The sea-water, as in the
recent forms, must have been admitted to the interior of the
Sponge by numerous apertures on its exterior, subsequently
escaping by a single large opening at its summit.

Amongst the Cwlenterates, the “‘Hydroid Zoophytes” are
represented by a species of the encrusting genus //ydractinia,
the horny polypary of which is so commonly found at the
present day adhering to the exterior of shells. The occurrence
of this genus is of interest, because it is the first known instance
in the entire geological series of the occurrence of an unques-
tionable Hydroid of a modern type, though many of the exist-
ing forms of these animals possess structures which are per-

266 HISTORICAL PALEONTOLOGY.

fectly fitted for preservation in the fossil condition. The corals
of the Cretaceous series are not very numerous, and for the
most part are referable to types suchas Z7ochocyathus, Stephano-
phyllia, Parasmilia, Synhelia (fig. 190), &c., which belong to
the same great group of corals as the majority of existing

Fig. 190.—Synhelia Sharpeana. Chalk, England.

forms. We have also a few “Tabulate Corals” (Polytre-
macs), hardly, if at all, generically separable from very ancient
forms (/Ze/iolites); and the Lower Greensand has yielded the
remains of the little Holocystis elegans, long believed to be the
last of the great Palzeozoic group of the Rugosa.

As regards the Echinoderms, the group of the Cvinords now
exhibits a marked decrease in the number and variety of its
types. The “stalked” forms are represented by Fentacrinus
and Bourgueticrinus, and the free forms by Feather-stars like
our existing Comatule ; whilst a link between the stalked and
free groups is constituted by the curious ‘‘ Tortoise Encrinite
(Marsupites). By far the most abundant Cretaceous Echino- .
derms, however, are Sea-urchins (Zchznoids); though several
Star-fishes are known as well. The remains of Sea-urchins are
so abundant in various parts of the Cretaceous series, especi-
ally in the White Chalk, and are often so beautifully preserved,
that they constitute one of the most marked features of the
fauna of the period. From the many genera of Sea-urchins
which occur in strata of this age, it is difficult to select char-
acteristic types; but the genera Ga/lerites (fig. 191), Descotdea
(fig. 192), Micraster, Ananchytes, Diadema, Salenia, and Ci-

THE CRETACEOUS. PERIOD: 267

daris, may be mentioned as being all important Cretaceous
groups. :
Coming to the Aznulose Animals of the Cretaceous period,

Fig. 191.—Galerites albogalerus, viewed from below, from the side, and from above.
White Chalk.

there is little special to remark. The Crustaceans belong for
the most part to the highly-organised groups of the Lobsters

Fig. 192.—Dzéscoidea cylindrica ; under, side, and upper aspect.
Upper Greensand.

and the Crabs (the Macrurous and Brachyurous Decapods) ;
but there are also numerous little Ostracodes, especially in the
fresh-water strata of the Wealden. It should further be noted
that there occurs here a great development of the singular
Crustaceous family of the Barnacles (Lepadid@), whilst the allied
family of the equally singular Acorn-shells (Ba/anide) is feebly
represented as well.

Passing on to the A/o//usca, the class of the Sea-mats and
Sea-mosses (/olyzoa) is immensely developed in the Cretaceous
period, nearly two hundred species being known to occur in
the Chalk. Most of the Cretaceous forms belong to the family
of the Escharide, the genera Eschara and Lscharina (fig. 193)
being particularly well represented. Most of the Cretaceous
Polyzoans are of small size, but some attain considerable di-
mensions, and many simulate Corals in their general form and
appearance.

268 HISTORICAL PALAZZONTOLOGY.

The Lamp-shells (Brachiopods) have now reached a further
stage of the progressive decline, which they have been under-
going ever since the close of
the Palzozoic period. Though
individually not rare, especially
in certain minor subdivisions
of the series, the number of
generic types has now be-
come distinctly diminished, the
principal forms belonging to
the genera TZerebratuia, Tere-
bratella (fig. 194), Terebratulina,
Rhynchonella, and Cranza (fig.

193.—A small fragment of Eschariza 195). In the last mentioned
Oceani, of the natural size ; and a portion —
of the same enlarged. Upper Greensand. Of these, the shell issatached

to foreign bodies by the sub-
stance of one of the valves (the ventral), whilst the other or
free valve is more or less limpet-shaped. All the above-men-

Fig. 194.—Terebratella Astieriana. Gault.

tioned genera are in existence at the present day; and one
species—namely, Terebratulina striata—appears to be undis-
tinguishable from one now hving—the Terebratulina caput-
serpentts.

Whilst the Lamp-shells are slowly declining, the Bivalves
(Lamellibranchs) are greatly developed, and are amongst the
most abundant and characteristic fossils of the Cretaceous
period. In the great river-deposit of the Wealden, the Bivalves
are forms proper to fresh water, belonging to the existing
River-mussels (Unio), Cyrena and Cydas; but most of the
Cretaceous Lamellibranchs are marine. Some of the most
abundant and characteristic of these belong to the great family
of the Oysters. (Ostverd@@). Amongst these are the genera
Gryphea and Exogyra, both of which we have seen to occur

THE CRETACEOUS PERIOD. 269

abundantly in the Jurassic ; and there are also numerous true
Oysters ( Ostrea, fig. 196) and Thorny Oysters (Spondylus, fig.

Fig. 195.—Cvranta Ignabergensis. The left-hand figure shows the perfect shell, at-
tached by its ventral valve to a foreign body; the middle figure shows the exterior of the
limpet-shaped dorsal valve ; and the right-hand figure represents the interior of the at-
tached valve. White Chalk.

197). The genus Z7rigonza, so characteristic of the Mesozoic
deposits in general, is hkewise well represented in the Creta-

Fig. 196.—Ostrea Couloni. Lower Greensand.

ceous strata. No single genus of Bivalves is, however, so highly
characteristic of the Cretaceous period as /oceramus, a group
belonging to the family of the Pearl-mussels (Avicudide). The
shells of this genus (fig. 198) have the valves unequal in size,
the larger valve often being much twisted, and both valves
being marked with radiating ribs or concentric furrows. The
hinge-line is long and straight, with numerous pits for the
attachment of the ligament which serves to open the shell.
Some of the /zocerami attain a length of two or three feet, and
fragments of the shell are often found perforated by boring

19

270 HISTORICAL PALAXONTOLOGY.

Sponges. Another extraordinary family of Bivalves, which is
exclusively confined to the Cretaceous rocks, is that of the

Fig. 197.—Sfondylus spinosus. White Chalk.

fTippuritide. All the members of this group (fig. 199) were
attached to foreign objects, and lived associated in beds, like

Fig. 198.—Joceramus sulcatus. Gault.

Oysters. The two valves of the shell are always altogether
unlike in sculpturing, appearance, shape, and size; and the
cast of the interior of the shell is often extremely unlike the
form of the outer surface. The type-genus of the family is
Fiippurites itself (fig. 199), in which the shell is in the shape of
a straight or slightly-twisted horn, sometimes a foot or more in
length, constituted by the attached lower valve, and closed
above by a small lid-like free upper valve. About a hundred
species of the family of the Azppuritide are known, all of these
being Cretaceous, and occurring in Britain (one species only),
in Southern Europe, the West Indies, North America, Algeria,
and Egypt. Species of this family occur in such numbers in
certain compact marbles in the south of Europe, of the age of
the Upper Cretaceous (Lower Chalk), as to have given origin

to the name of “ Hippurite Limestones,” applied to these
Strata.

THE CRETACEOUS PERIOD. 271

The Univalves (Gasteropods) of the Cretaceous period are
not very numerous, nor particularly remarkable. Along with
species of the persistent genus Pleurotomaria and the Meso-

Fig. 199.—Hippurites Toucasiana.
A large individual, with two smaller
ones attached to it. Upper Cretace- Fig. 200.—Voluta elongata.
ous, South of Europe. White Chalk.

zoic /Veringa, we meet with examples of such modern types
as Turritella and JNatita, the Staircase-shells (Solarium), the
Wentle-traps (S¢a/aria), the Carrier-shells (Phorus), &c. To-
wards the close of the Cretaceous period, and especially in
such transitional strata as the Maestricht beds, the FaxGde
Limestone, and the Pisolitic Limestone of France, we meet
with a number of carnivorous (“ siphonostomatous”) Uni-
valves, in which the mouth of the shell is notched or pro-
duced into a canal. Amongst these it is interesting to
recognise examples of such existing genera as the Volutes
(Voluta, fig. 200), the Cowries (Cyfrea), the Mitre-shells
(Mitra), the Wing-shells (Strombus), the Scorpion - shells
(Pteroceras), &c.

272 HISTORICAL PALZONTOLOGY.

Upon the whole, the most characteristic of all the Creta-
ceous Molluscs are the Cephalopods, represented by the remains
of both Zetrabranchiate and Dibranchiate forms. Amongst the
former, the long-lived genus /Vautilus (fig. 201) again reap-

Fig. 201.—Different views of Nautilus Danicus. Faxée Limestone
(Upper Cretaceous), Denmark.

pears, with its involute shell, its capacious body-chamber, its
simple septa between the air-chambers, and its nearly or quite
central siphuncle. The majority of the chambered Cephalo-
pods of the Cretaceous belong, however, to the complex and
beautiful family of the Ammonztide, with their elaborately-
folded and lobed septa and dorsally-placed siphuncle. This
family disappears wholly at the close of the Cretaceous period ;
but its approaching extinction, so far from being signalised by
any slow decrease and diminution in the number of specific
or generic types, seems to have heen attended by the develop-
ment of whole series of new forms. The genus Ammonites
itself, dating from the Carboniferous, has certainly passed its
prime, but it is still represented by many species, and some of
these attained enormous dimensions (two or three feet in
diameter). The genus Axcyloceras (fig. 202), though likewise
of more ancient origin (Jurassic), is nevertheless very charac-
teristic of the Cretaceous. In this genus the first portion of —
the shell is in the form of a flat spiral, the coils of which are
not in contact ; and its last portion is produced at a tangent,
becoming ultimately bent back in the form of a crosier. Be-
sides these pre-existent types, the Cretaceous rocks have
yielded a great number of .entirely new forms of the Ammont-
tide, which are not known in any deposits of earlier or later
date. Amongst the more important of these may be men-
tioned Cvrioceras, Turrilites, Scaphites, Hamites, Ptychoceras,

THE CRETACEOUS PERIOD. 273

and Baculites. Inthe genus Cvioceras (fig. 204, @), the shell
consists of an open spiral, the volutions of which are not in

Fig. 202.—Aneyloceras Matheronianus. Gault.

contact, thus resembling a partially-unrolled Ammonite or the
inner portion of an Azcyloceras. In Turrilites (fig. 203), the
shell is precisely like that of the Ammonite in its structure ;
but instead of forming a flat spiral, it is: coiled into an ele-
vated turreted shell, the whorls of which are in contact with
one another. In the genus Scaphites (fig. 204, ¢), the shell
resembles that of Ancyloceras i in consisting of a series of volu-
tions coiled into a flat spiral, the last being detached from the
others, produced, and ultimately bent back in the form of a
crosier ; but the whorls of the enrolled part of the shell are in
contact, instead of being separate as in the latter. In the
genus HZamites (fig. 204, f), the shell is an extremely elongated
cone, which is bent upon itself more than once, in a hook-like
manner, all the volutions being separate. The genus Ptycho-
ceras (fig. 204, @) is very like Hlamites, except that the shell is
only bent once; and the two portions thus bent are in contact
with one another. Lastly, in the genus Baculites (fig. 204, 0
and c) the shell is simply a straight elongated cone, not bent
in any way, but possessing the folded septa which characterise
the whole Ammonite family. The Aaculite is the simplest of
all the forms of the Ammonzitide; and all the other forms, how-
ever complex, may be regarded as being simply produced by
the bending or folding of such a conical septate shell in differ-
ent ways. The Aaculite, therefore, corresponds, in the series
of the Ammonitide, to the Orthoceras in the series of the Vau-
tilide. All the above-mentioned genera are characteristically,
or exclusively, Cretaceous, and they are accompanied by a
number of other allied forms, which cannot be noticed here.
Not a single one of these genera, further, has hitherto been
detected in any strata higher than the Cretaceous. We may
therefore consider that these wonderful, varied, and elaborate

274 HISTORICAL PALAONTOLOGY.

forms of Ammonitide constitute one of the most conspicuous

features in the life of the Chalk period.

The Dibranchiate Cephalopods are represented partly by the

LELLID

I
=
NS
x 5
YF SS
XX
K 3
xs
t

RS
S

we
Ries
ES

Fig. 203.—Turrilites cate- Fig. 204.—a, Ptychoceras Emericianum, reduced
natus. The lower figure rep- —Lower Greensand; 6, Baculites anceps, reduced
resents the entire shell; the —Chalk; c, Portion of the same, showing the folded
upper figure represents the edges of the septa; d, Crioceras cristatum, reduced
base of the shell seen from —Gault; e, Scaphites egualis, natural size—Chalk 5
below. Gault. J, Hamites rotundus, restored—Gault.

beak-like jaws of unknown species of Cuttle-fishes and partly
by the internal skeletons of Belemnites. Amongst the latter,
the genus Ae/emnites itself holds its place in the lower part of

THE CRETACEOUS PERIOD. 275

the Cretaceous series ; but it disappears in the upper portion
of the series, and its place is taken by the nearly-allied genus
Belemnitella (fig. 205), distinguished by the possession of a
straight fissurein the upper end of the guard. ‘This
also disappears at the close of the Cretaceous
period; and no member of the great Mesozoic
family of the Belemnitide has hitherto been dis-
covered in any Tertiary deposit, or is known to
exist at the present day.

Passing on next to the Vertebrate Animals of the
Cretaceous period, we find the /zshes represented
as before by the Ganoids and the Placoids, to which,
however, we can now add the first known examples
of the great group of the Bony Fishes or Teleosteans,
comprising the great majority of existing forms.
The Ganoid fishes of the Cretaceous (Lefidotus,
Pycnodus, &c.) present no features of special in-
terest. Little, also, need be said about the Placoid
fishes of this period. As in the Jurassic deposits, Bi ae
the remains of these consist partly of the teeth of Becemnitella
genuine Sharks (Zamna, Odontaspis,&c.), and partly (ycregia
of the teeth and defensive spines of Cestracionts,
such as the living Port-Jackson Shark. The pointed and sharp-
edged teeth of true Sharks are very abundant in some beds, such
as the Upper Greensand, and are beautifully preserved. The
teeth of some forms (Carcharias, &c.) attain occasionally a
length of three or four inches, and indicate the existence in the
Cretaceous seas of huge predaceous fishes, probably larger than
any existing Sharks. The remains of Cestracionts consist
partly of the flattened teeth of genera such as Acrodus and
Ftychodus (the latter confined to rocks of this age), and partly
of the pointed teeth of AZybodus, a genus which dates from the
Trias. In this genus the teeth (fig. 206) consist of a principal
central cone, flanked by minor lateral cones; and the fin-

Fig. 206.—Tooth Fig. 207.—Fin-spine of Hybodus. Lower Greensand.
of Hybodus.

spines (fig. 207) are longitudinally grooved, and carry a series
of small spines on their hinder or concave margin, Lastly,

270) HISTORICAL PALEZONTOLOGY.

the great modern order of the Bony Fishes or Zéleosteans
makes its first appearance in the Upper Cretaceous rocks,
where it 1s represented by forms belonging to no less than
three existing groups — namely, the Salmon family (Sa/
monide), the Herring family (Clupecde), and the Perch family
(Percide). All these fishes have thin, horny, overlapping

oy

H

——

Fig. 208.—1, Beryx Lewesiensts, a Percoid fish from the Chalk ; 2, Osszeroides
Manteliz, a Salmonoid fish from the Chalk.

scales, symmetrical (“‘ homocercal”) tails, and bony skeletons.
The genus Zeryx (fig. 208, 1) is one represented by existing
species at the present day, and belongs to the Perch family.
The genus Osmeroides, again (fig. 208, 2), 1s supposed to be
related to the living Smelts (Osmerus), and, therefore, to
belong to the Salmon tribe.

No remains of Amphibians have hitherto been detected in
any part of the Cretaceous series; but Aepie/es are extremely
numerous, and belong to very varied types. As regards the
great extinct groups of Reptiles which characterise the Meso-
zoic period as a whole, the huge “ Enaliosaurs” or ‘ Sea-
Lizards” are still represented by the /chthyosaur and the
Plestosaur. Nearly allied to the latter of these is the 2/as-
mosaurus of the American Cretaceous, which combined the

THE CRETACEOUS PERIOD. 277

long tail of the Ichthyosaur with the long neck of the Plesio-
saur. The length of this monstrous Reptile could not have
been less than fifty feet, the neck consisting of over sixty
vertebree and measuring over twenty feet in length. The
extraordinary Flying Reptiles of the Jurassic are likewise well
represented in the Cretaceous rocks by species of the genus
Pterodactylus itself, and these later forms are much more
gigantic in their dimensions than their predecessors. Thus
some of the Cretaceous P¢tervosaurs seem to have had a spread
of wing of from twenty to twenty-five feet, more than realising
the ‘“ Dragons” of fable in point of size. The most remark-
able, however, of the Cretaceous Prevosaurs are the forms
which have recently been described by Professor Marsh under
the generic title of Preranodon. In these singular forms—so
far only known as American—the animal possessed a skeleton
in all respects similar to that of the typical Pterodactyles,
except that the jaws are completely destitute of teeth. There
is, therefore, the strongest probability that the jaws were
encased in a horny sheath, thus coming to resemble the beak
of a Bird. Some of the recognised species of P¢eranodon are
very small; but the skull of one species (P. /ongiceps) is not
less than a yard in length, and there are portions of the skull
of another species which would indicate a length of four feet
for the cranium. ‘These measurements would point to dimen-
sions larger than those of any other known Pterosaurs.

The great Mesozoic order of the Deznosaurs is largely rep-
resented in the Cretaceous rocks, partly by genera which
previously existed in the Jurassic period, and partly by entirely
new types. The great delta-deposit of the Wealden, in the
Old World, has yielded the remains of various of these huge
terrestrial Reptiles, and very many others have been found in
the Cretaceous deposits of North America. One of the most
celebrated of the Cretaceous Deinosaurs 1s the /ewanodon, so
called from the curious resemblance of its teeth to those of the
existing but comparatively diminutive Zevana. The teeth (fig.
209) are soldered to the inner face of the jaw, instead of being
sunk in distinct sockets; and they have the form of somewhat
flattened prisms, longitudinally ridged on the outer surface,
with an obtusely triangular crown, and having the enamel
crenated on one or both sides. They present the extraordinary
feature that the crowns became worn down flat by mastication,
showing that the /gwanodon employed its teeth in actually
chewing and triturating the vegetable matter on which it fed.
There can therefore be no doubt but that the Zewanodon, in
spite of its immense bulk, was an herbivorous Reptile, and

278 HISTORICAL PALZONTOLOGY.

lived principally on the foliage of the Cretaceous forests
amongst which it dwelt. Its size has been variously estimated

Fig. 209.—Teeth of Iguanodon Mantelliiz. Wealden, Britain.

at from thirty to fifty feet, the thigh-bone in large examples
measuring nearly five feet in length, with a circumference of
twenty-two inches in its smallest part. With the strong and
massive hind-limbs are associated comparatively weak and
small fore-limbs ; and there seems little reason to doubt that
the Zevanodon must have walked temporarily or permanently
upon its hind-limbs, after the manner of a Bird. This conjec-
ture is further supported by the occurrence in the strata which
contain the bones of the Zewanodon of gigantic three-toed foot-
prints, disposed szzg/y in a double track. These prints have
undoubtedly been produced by some animal walking on two
legs; and they can hardly, with any probability, be ascribed to
any other than this enormous Reptile. Closely allied to the
LIguanodon is the Hadrosaurus of the American Cretaceous, the
length of which is estimated at twenty-eight feet. guanodon
does not appear to have possessed any integumentary skeleton;
but the great Wy/eosaurus of the Wealden seems to have been
furnished with a longitudinal crest of large spines running
down the back, similar to that which is found in the compara-
tively small Iguanas of the present day. The A/egalosaurus of
the Oolites continued to exist in the Cretaceous period; and, as
we have previously seen, it was carnivorous in its habits. The
American L@/aps was also carnivorous, and, like the Megalosaur,

THE CRETACEOUS PERIOD. 279

which it very closely resembles, appears to have walked upon
its hind-legs, the fore-limbs being disproportionately small.
Another remarkable group of Reptiles, exclusively confined
to the Cretaceous series, is that of the A/osasauroids, so called
from the type-genus JZosasaurus. ‘The first species of Afosa-
saurus known to science was the JZ. Camferi (fig. 210), the

NS =
ISS
\

Fig. 210.—Skull of Mosasaurus Camperi, greatly reduced. Maestricht Chalk.

skull of which—six feet in length—was discovered in 1780 in
the Maestricht Chalk at Maestricht. As this town stands on
the river Meuse, the name of Mosasaurus (‘ Lizard of the
Meuse”) was applied to this immense Reptile. Of late years
the remains of a large number of Reptiles more or less closely
related to Mosasaurus, or absolutely belonging to it, have been
discovered in the Cretaceous deposits of North America, and
have been described by Professors Cope and Marsh. All
the known forms of this group appear to have been of large
size—one of them, Mosasaurus princeps, attaining the length of
seventy-five or eighty feet, and thus rivalling the largest of ex-
isting Whales in its dimensions. The teeth in the ‘“ Mosa-
sauroids” are long, pointed, and slightly curved; and instead
of being sunk in distinct sockets, they are firmly amalgamated
with the jaws, as in modern Lizards. The palate also carried
teeth, and the lower jaw was so constructed as to allow of the
mouth being opened to an immense width, somewhat as in the
living Serpents. The body was long and snake-like, with a
very long tail, which is laterally compressed, and must have
served as a powerful swimming-apparatus. In addition to this,
both pairs of limbs have the bones connecting them with the

280 HISTORICAL PALAZONTOLOGY.

trunk greatly shortened; whilst the digits were enclosed in the
integuments, and constituted paddles, closely resembling in
structure the “ flippers” of Whales and Dolphins. The neck
is sometimes moderately long, but oftener very short, as the
great size and weight of the head would have led one to anti-
cipate. Bony plates seem in some species to have formed an
at any rate partial covering to the skin; but it is not certain
that these integumentary appendages were present in all. Up-
on the whole, there can be no doubt but that the Mosasauroid
Reptiles—the true ‘“ Sea-serpents ” of the Cretaceous period—
were essentially aquatic in their habits, frequenting the sea,
and only occasionally coming to the land.

The ‘‘ Mosasauroids” have generally been regarded as a
greatly modified group of the Lizards (Lacertitia). Whether
this reference be correct or not—and recent investigations
render it dubious—the Cretaceous rocks have yielded the
remains of small Lizards not widely removed from existing
forms. ‘The recent oni of the Chelonzans 1s also represented
in the Cretaceous rocks,
by forms closely re-
sembling living types.
Thus the fresh - water
deposits of the Wealden
have yielded examples
of the ‘“‘Terrapins” or
“‘Mud-Turtles” (mys);
and the marine Creta-
ceous strata have been
found to contain the
remains of various spe-
cies of Turtles, one of
which is here figured
(fig. 221). + MNepiaTe
Serpents ( Ophidia) have
as yet been detected in
the Cretaceous rocks;
and this order does not
appear to have come
into existence till the
Tertiary period. Last-
ly, true Crocodiles are

Fig. 2r1.—Carapace of Chelone Benstedz. i
Lower Chalk. (After Owen.) known to have existed

in considerable num-
bers in the Cretaceous period. The oldest of these occur
in the fresh-water deposit of the Wealden ; and they differ from

THE CRETACEOUS PERIOD. 281

the existing forms of the group in the fact that the bodies
of the vertebre, like those of the Jurassic Crocodiles, are
bi-concave, or hollowed out at both ends. In the Greensand
of North America, however, occur the remains of Crocodiles
which agree with all the living species in having the bodies of
the vertebrz in the region of the back hollowed out in front
and convex behind.

Zirds have not hitherto been shown, with certainty, to have
existed in Europe during the Cretaceous period, except in a
few instances in which fragmentary remains belonging to this
class have been discovered. The Cretaceous deposits of
North America have, however, been shown by Professor
Marsh to contain a considerable number of the remains of
Birds, often in a state of excellent preservation. Some of
these belong to Swimming or Wading Birds, differing in no
point of special interest from modern birds of similar habits.
Others, however, exhibit such extraordinary peculiarities that
they merit more than a passing notice. One of the forms in
question constitutes the genus /chthyornis of Marsh, the type-
species of which (/. dsfar) was about as large as a Pigeon.
In two remarkable respects, this singular Bird differs from all
known living members of the class. One of these respects
concerns the jaws, both of which exhibit the Reptilian char-
acter of being armed with numerous small pointed éee¢h (fig.
212, a), sunk in distinct sockets. No existing bird possesses
teeth; and this character forcibly recalls the Bird-like Ptero-
saurs, with their toothed jaws. Jchthyornis, however, possessed
fore-limbs constructed strictly on the type of the “ wing” of the
living Birds; and it cannot, therefore, be separated from this
class. Another extraordinary peculiarity of /chthyornis is, that
the bodies of the vertebre (fig. 212, c) were bz-concave, as is the
case with many extinct Reptiles and almost all Fishes, but as
does not occur in any living Bird. ‘There can be little doubt
that /chthyornis was aquatic in its habits, and that it lived prin-
cipally upon fishes; but its powerful wings at the same time
indicate that it was capable of prolonged flight. The tail of
Lchthyornis has, unfortunately, not been discovered ; and it is
at present impossible to say whether this resembled the tail of
existing Birds, or whether it was elongated and composed of
separate vertebree, as in the Jurassic Archaeopteryx.

Still more wonderful than /chthyornis is the marvellous bird
described by Marsh under the name of Hesperornis regalis.
This presents us with a gigantic diving bird, somewhat re-
sembling the existing “ Loons” (Colymbus), but agreeing
with /chthyornis in having the jaws furnished with conical,

282 HISTORICAL PALZONTOLOGY.

recurved, pointed teeth (fig. 212, 4). Hence these forms are
grouped together in a new sub-class, under the name of Odon-
tornithes or “‘'Toothed Birds.” The teeth of Hesperornis (fig.
212, 2) resemble those of /chthyornis in their general form ;

Fig, 2t2.—Toothed Birds (Odontornzthes) of the Cretaceous Rocks of America. a,
Left lower jaw of /chthyornis dispar, slightly enlarged ; 6, Left lower jaw of Hesperornis
vegalis, reduced to nearly one-fourth of the naturalsize; c, Cervical vertebra of /chthyornis
dispar, front view, twice the natural size; c’, Side view of the same ; @, Tooth of Hesper-
ornis regalis, enlarged to twice the natural size. (After Marsh.)

but instead of being sunk in distinct sockets, they are simply
implanted in a deep continuous groove in the bony substance
of the jaw. ‘The front of the upper jaw does not carry teeth,
and was probably encased in a horny beak. ‘The breast-bone
is entirely destitute of a central ridge or keel, and the wings
are minute and quite rudimentary ; so that Hespferornis, unlike
Ichthyornis, must have been wholly deprived of the power of
flight, in this respect approaching the existing Penguins. The
tail consists of about twelve vertebre, of which the last three or
four are amalgamated to form a flat terminal mass, there being
at the same time clear indications that the tail was capable
of up and down movement in a vertical plane, this proba-
bly fitting it to serve as a swimming-paddle or rudder. The
legs were powerfully constructed, and the feet were adapted to
assist the bird in rapid motion through the water. The known
remains of Hlesperornis regalis prove it to have been a swim-
ming and diving bird, of larger dimensions than any of the

~~

THE CRETACEOUS PERIOD. 283

aquatic members of the class of Birds with which we are ac-
quainted at the present day. It appears to have stood between
five and six feet high, and its inability to fly is fully compen-
sated for by the numerous adaptations of its structure to a
watery life. Its teeth prove it to have been carnivorous in its
habits, and it probably lived upon fishes. It is a curious fact
that two Birds agreeing with one another in the wholly abnor-
mal character of possessing teeth, and in other respects so
entirely different, should, like /chthyornis and Hesperornts,
have lived not only in the same geological period, but also in
the same geographical area; and it is equally curious that
the area inhabited by these toothed Birds should at the same
time have been tenanted by winged and bird-like Reptiles
belonging to the toothed genus Prerodactylus and the toothless
genus Preranodon.

_ No remains of Wammals, finally, have as yet been detected
in any sedimentary accumulations of Cretaceous age.

LITERATURE.

The following list comprises some of the more important works and
memoirs which may be consulted with reference to the Cretaceous strata
and their fossil contents :—

(1) ‘Memoirs of the Geological Survey of Great Britain.’

(2) ‘Geology of England and Wales.’ Conybeare and Phillips.

(3) ‘Geology of Yorkshire,’ vol. ii. Phillips.

(4) ‘Geology of Oxford and the Thames Valley.’ Phillips.

(5) *‘ Geological Excursions through the Isle of Wight.’ Mantell.

(6) ‘Geology of Sussex.’ Mantell.

(7) ‘Report on Londonderry,’ &c. Portlock.

(3) ‘Recherches sur le Terrain Crétacé Supérieur de fe sate et de

VIrlande.’ Barrois.

(9) ‘* Geological Survey of Canada””—‘ Report of Progress, 1872-73.’

) ‘Geological Survey of California.’ Whitney.

(11) ‘Geological Survey of Montana, Idaho, Wyoming, and Utah.’
Hayden and Meek.

(12) ‘Report on Geology,’ &c. (British North American Boundary
Commission). G. M. Dawson.

(13) ‘Manual of Geology.’ Dana.

14) ‘Lethza Rossica.’ Eichwald.

(15) ‘ Petrefacta Germaniz.’ Goldfuss.

(16) ‘ Fossils of the South Downs.’ Mantell.

(17) ‘Medals of Creation.’ Mantell.

(18) ‘Mineral Conchology.’ Sowerby.

(19) ‘ Lethzea Geognostica.’ Bronn.

(20) ‘Malacostracous Crustacea of the British Cretaceous Formation’
(Palzontographical Society). Bell.

(21) ‘Brachiopoda of the Cretaceous Formation’ (Palzeontographical
Society). “Davidson,

(22) ‘Corals of the Cretaceous Formation’ (Palzeontographical Society).

Milne-Edwards and Haime.

284 HISTORICAL PALZONTOLOGY.

(23) ‘Supplement to the Fossil Corals’ (Paleeontographical Society).
Martin Duncan.

(24) ‘Echinodermata of the Cretaceous Formation’ (Palzontographical
Society). Wright.

(25) ‘Monograph of the Belemnitide’ (Palzeontographical Society).
Phillips.

(26) ‘Monograph of the Trigoniz’ (Paleontographical Society).
Lycett.

(27) ‘Fossil Cirripedes ’ (Paleeontographical Society). Darwin.

(28) ‘Fossil Mollusca of the Chalk of Britain’ (Paleontographical
Society). Sharpe.

(29) ‘Entomostraca of the Cretaceous Formation’ (Palzeontographical
Society). Rupert Jones.

(30) ‘Monograph of the Fossil Reptiles of the Cretaceous Formation’
(Palzeontographical Society). Owen.

(31) ‘Manual of Paleontology.” Owen.

(32) ‘ Synopsis of Extinct Batrachia and Reptilia.” Cope.

(33) ‘‘Structure of the Skull and Limbs in Mosasauroid Reptiles ”—

‘American Journ. Sci. and Arts, 1872.’ Marsh.

(34) ‘©On Odontornithes””—‘ American Journ. Sci. and Arts, 1875.’
Marsh.

35) ‘Ossemens Fossiles.” Cuvier.

36) ‘Catalogue of Omithosauria.’ Seeley.

37) ‘ Paléontologie Frangaise.’ D’Orbigny.

38) ‘Synopsis des Echinides fossiles.? Desor.

) ‘Cat. Raisonne des Echinides.’ Agassiz and Desor.

(40) ‘‘ Echinoids”—‘ Decades of the Geol. Survey of Britain.’ E, Forbes.

) ‘Paléontologie Francaise.’ Cotteau.

) ‘ Versteinerungen der Bohmischen Kreide-formation.’ Reuss.

(43) ‘‘ Cephalopoda, Gasteropoda, Pelecypoda, Brachiopoda, &c., of the
Cretaceous Rocks of India”—‘ Palzontologica Indica,’ ser. 1.,
ilil., V., Vi., Vili. Stoliczka.

(44) ‘‘ Cretaceous Reptiles of the United States”—‘ Smithsonian Contri-
butions to Knowledge,’ vol. xiv. Leidy.

(45) ‘Invertebrate Cretaceous, and Tertiary Fossils of the Upper Mis-
souri Country.’ 1876. Meek.

CHAPTER Xvi
THE RL OCE NE PERL OD:

Before commencing the study of the subdivisions of the
Kainozoic series, there are some general considerations to be
noted. In the first place, there is in the Old World a com-
plete and entire physical break between the rocks of the
Mesozoic and Kainozoic periods. Inno instance in Europe
are Tertiary strata to be found resting conformably upon any
Secondary rock. The Chalk has invanably suffered much
erosion and denudation before the lowest Tertiary strata were
deposited upon it. This is shown by the fact that the actually

THE EOCENE PERIOD. 285

eroded surface of the Chalk can often be seen ; or, failing this,
that we can point to the presence of the chalk-flints in the
Tertiary strata. This last, of course, affords unquestionable
proof that the Chalk must have been subjected to enormous
denudation prior to the formation of the Tertiary beds, all the
chalk itself having been removed, and nothing left but the
flints, while these are all rolled and rounded. In the continent
of North America, on the other hand, the lowest Tertiary strata
have been shown to graduate downwards conformably with the
highest Cretaceous beds, it being a matter of difficulty to draw
a precise line of demarcation between the two formations.

In the second place, there is a marked break in the /fe of
the Mesozoic and Kainozoic periods. With the exception of
a few Foraminifera, and one Lrachiopod (the latter doubtful),
no Cretaceous sfecies is known to have survived the Creta-
ceous period ; while several characteristic famzlies, such as the
Ammonitide, Belemnitide, and Hippuritide, died out entirely
with the close of the Cretaceous rocks. In the Tertiary rocks,
on the other hand, not only are all the animals and plants
more or less like existing types, but we meet with a constantly-
increasing number of “ving species as we pass from the bottom
of the Kainozoic series to the top. Upon this last fact is
founded the modern classification of the Kainozoic rocks,
propounded by Sir Charles Lyell.

The absence in strata of Tertiary age of the chambered
Cephalopods, the Belemnites, the Azppurites, the Lnoceramt,
and the diversified types of Reptiles which form such con-
spicuous features in the Cretaceous fauna, render the palezon-
tological break between the Chalk and the Eocene one far too
serious to be overlooked. At the same time, it is to be re-
membered that the evidence afforded by the explorations car-
ried out of late years as to the animal life of the deep sea, ren-
ders it certain that the extinction of marine forms of life at the
close of the Cretaceous period was far less extensive than had
been previously assumed. It is tolerably certain, in fact, that
we may look upon some of the inhabitants of the depths of our
existing oceans as the direct, if modified, descendants of ani-
mals which were in existence when the Chalk was deposited.

It follows from the general want of conformity between the
Cretaceous and Tertiary rocks, and still more from the great
difference in life, that the Cretaceous and Tertiary periods are
separated, in the Old World at any rate, by an enormous lapse
of unrepresented time. How long this interval may have been,
we have no means of judging exactly, but it very possibly was
as long as the whole Kainozoic epoch itself. Some day we

20

286 HISTORICAL PALEONTOLOGY.

shall doubtless find, at some part of the earth’s surface, marine
strata which were deposited during this period, and which wil!
contain fossils intermediate in character between the organic
remains which respectively characterise the Secondary and
Tertiary periods. At present, we have only slight traces of
such deposits—as, for instance, the Maestricht beds, the Faxoe
Limestone, and the Pisolitic Limestone of France.

CLASSIFICATION OF THE TERTIARY Rocks.—The classifica-
tion of the Tertiary rocks is a matter of unusual difficulty, in
consequence of their occurring in disconnected basins, form-
ing a series of detached areas, which hold no relations of
superposition to one another. The order, therefore, of the
Tertiaries in point of time, can only be determined by an ap-
peal to fossils; and in such determination Sir Charles Lyell
proposed to take as the basis of classification the proportion of
living or existing species of Mollusca which occurs in each stratum
or group of strata. Acting upon this principle, Sir Charles
Lyell divides the Tertiary series into four groups :— .

I. The Zocene formation (Gr. cos, dawn; Aazzos, new), con-
taining the smallest proportion of existing species, and being,
therefore, the oldest division. In this classification, only the
Mollusca are taken into account; and it was found that of
these about three and a half per cent were identical with ex-
isting species.

II. The AZocene formation (Gr. meion, less; Rainos, new),
with more recent species than the Eocene, but Zess than the suc-
ceeding formation, and less than one-half the total number in the
formation. As before, only the 1/o//usca are taken into account,
and about 17 per cent of these agree with existing species.

Ill. The Pocene formation (Gr. plecon, more ; 2aznos, new),
with generally more than half the species of shells identical with
existing species—the proportion of these varying from 35 to
5° per cent in the lower beds of this division, up to 90 or 95
per cent in its higher portion.

IV. The Post-Tertiary Formations, in which all the shells
belong to existing species. This, in turn, is divided into two
minor groups—the Post-Plocene and Recent Formations. In
the Fost-Pliocene formations, while all the AZo/usca belong to
existing species, most of the JZammails belong to extinct
species. In the Recent period, the quadrupeds, as well as the
shells, belong to living species.

The above, with some modifications, was the original classi-
fication proposed by Sir Charles Lyell for the Tertiary rocks,
and now universally accepted. More recent researches, it is
true, have somewhat altered the proportions of existing species

THE EOCENE PERIOD. 287

to extinct, as stated above. The general principle, however,
of an increase in the number of living species, still holds good ;
and this is as yet the only satisfactory basis upon which it has
been proposed to arrange the Tertiary deposits.

EOCENE FORMATION.

The Eocene rocks are the lowest of the Tertiary series, and
comprise all those Tertiary deposits in which there is only a
small proportion of existing A/o//usca—from three and a half
to five per cent. ‘The Eocene rocks occur in several basins in
Britain, France, the Netherlands, and other parts of Europe,
and in the United States. The subdivisions which have been
established are extremely numerous, and it is often impossible
to parallel those of one basin with those of another. It will
be sufficient, therefore, to accept the division of the Eocene
formation into three great groups— Lower, Middle, and Upper
Eocene—and to consider some of the more important beds
comprised under these heads in Europe and in North America.

I. EocENE OF BRITAIN. (1.) LOwER Eocrnr.—The base
of the Eocene series in Britain is constituted by about go feet
of light-coloured, sometimes argillaceous sands (Zhanet Sands),
which are of marine origin. Above these, or forming the base
of the formation where these are wanting, come mottled clays
and sands with lignite (Woolwich and Reading series), which
are estuarine or fluvio-marine in origin. The highest member
of the Lower Eocene of Britain is the ‘‘ Zondon Clay,” consist-
ing of a great mass of dark-brown or blue clay, sometimes with
sandy beds, or with layers of “‘septaria,” the whole attaining a
thickness of from 200 to as much as 500 feet. ‘The London
Clay is a purely marine deposit, containing many marine fossils,
with the remains of terrestrial animals and plants ; all of which
indicate a high temperature of the sea and tropical or sub-
tropical conditions of the land.

(2.) MippLe Eocene.—The inferior portion of the Middle
Eocene of Britain consists of marine beds, chiefly consisting
of sand, clays, and gravels, and attaining a very considerable
thickness (Bagshot and Bracklesham beds). 'Yhe superior por-
tion of the Middle Eocene of Britain, on the other hand, con-
sists of deposits which are almost exclusively fresh-water or
brackish-water in origin (/feadon and Osborne series).

The chief Continental formations of Middle Eocene age are
the “‘Calcaire grossier” of the Paris basin, and the ‘‘ Num-
mulitic Limestone” of the Alps.

(3.) Upper Eocense.—If the Headon and Osborne beds of

288 HISTORICAL PALZONTOLOGY.

the Isle of Wight be placed in the Middle Eocene, the only
British representatives of the Upper Eocene are the Bembridge
beds. These strata consist of limestones, clays, and marls,
which have for the most part been deposited in fresh or brack-
ish water.

II. EocENE BEDS OF THE Paris Basin. — The Eocene
strata are very well developed in the neighbourhood of Paris,
where they occupy a large area or basin scooped out of the
Chalk. The beds of this area are partly marine, partly fresh-
water in origin; and the following table (after Sir Charles
Lyell) shows their subdivisions and their parallelism with the
English series :—

GENERAL TABLE OF FRENCH EOCENE STRATA.

UPPER EOCENE. :
French Subdivisions. English Equivalents.

A. 1. Gypseous series of Mont- 1. Bembridge series.
martre.
A. 2. Calcaire silicieux, or Tra- 2. Osborne and Headon series.

vertin Inférieur.

A. 3. Gres de Beauchamp, or White sand and clay of Barton

G2

Sables Moyens. Cliff, Hants.
MIDDLE EOCENE.
B. 1. Calcaire Grossier. 1. Bagshot and Bracklesham beds.
B. 2. Soissonnais Sands, or Lits 2. Wanting.
Coguilliers.

LOWER EOCENE.

C. 1. Argile de Londres at base of I. London clay.
Hill of Cassel, near Dun-

kirk.

C. 2. Argile plastique and lignite. 2. Plastic clay and sand with lig- ,
nite (Woolwich and Reading
series).

C. 3. Sables de Bracheux. 3. Thanet sands.

III, EKocENE STRATA OF THE UNITED StTates.—The low-
est member of the Eocene deposits of North America is the
so-called ‘‘ Lignitic Formation,’ which is largely developed in
Mississippi, Tennessee, Arkansas, Wyoming, Utah, Colorado,
and California, and sometimes attains a thickness of several
thousand feet. Stratigraphically, this formation exhibits the
interesting point that it graduates downwards insensibly and
conformably into the Cretaceous, whilst it is succeeded mscon-
Jormably by strata of Middle Eocene age. Lithologically, the
series consists principally of sands and clays, with beds of lig-
nite and coal, and its organic remains show that it is principally
of fresh-water origin “with a partial intermixture of marine beds,

THE EOCENE PERIOD. 289

These marine strata of the ‘‘ Lignitic formation ” are of special
interest, as showing such a commingling of Cretaceous and
Tertiary types of life, that it is impossible to draw any rigid
line in this region between the Mesozoic and Kainozoic sys-
tems. Thus the marine beds of the Lignitic series contain
such characteristic Cretaceous forms as /roceramus and Am-
monites, along with a great number of Univalves of a distinctly
Tertiary type (Cones, Cowries, &c.) Upon the whole, there-
fore, we must regard this series of deposits as affording a kind
of transition between the Cretaceous and the Eocene, holding
in some respects a position which may be compared with that
held by the Purbeck beds in Britain as regards the Jurassic
and Cretaceous.

The Middle Eocene of the United States is represented
by the Clacborne and Jackson beds. The Claiborne series is
extensively developed at Claiborne, Alabama, and consists of
sands, clays, lignites, marls, and impure limestones, containing
marine fossils along with numerous plant-remains. The /ack-
son series is represented by lignitic clays and marls which occur
at Jackson, Mississippi. Amongst the more remarkable fossils
of this series are the teeth and bones of Cetaceans of the
genus Zeuglodon.

Strata of Upper Eocene age occur in North America at
Vicksburg, Mississippi, and are known as the Vicksburg series.
They consist of lignites, clays, marls, and limestones. Fresh-
water deposits of Eocene age are also largely developed in
parts of the Rocky Mountain region. The. most remarkable
fossils of these beds are Mammals, of which a large number of
species have been already determined.

LIFE OF THE EOCENE PERIOD.

The fossils of the Eocene deposits are so numerous that
nothing more can be attempted here than to give a brief and
general sketch of the life of the period, special attention being
directed to some of the more prominent and interesting types,
amongst which—as throughout the Tertiary series—the Mam-
mals hold the first place. It is not uncommon, indeed, to
speak of the Tertiary period as a whole under the name of the
“‘ Age of Mammals,” a title at least as well deserved as that of
“ Age of Reptiles” applied to the Mesozoic, or “‘ Age of Mol-
luscs” applied to the Paleozoic epoch.

As regards the plants of the Eocene, the chief point to be
noticed is, that the conditions which had already set in with
the commencement of the Upper Cretaceous, are here con-

290 HISTORICAL PALZONTOLOGY.

tinued, and stillfurther enforced. The Cycads of the Secondary
period, if they have not totally disappeared, are exceedingly
rare; and the Conzfers, losing the predominance which they
enjoyed in the Mesozoic, are now relegated to a subordinate
though well-defined place in the terrestrial vegetation. The
great majority of the Eocene plants are referable to the groups
of the Angiospermous Exogens and the Monocotyledons ; and
the vegetation of the period, upon the whole, approximates
closely to that now existing upon the earth. ‘The plants of the
European Eocene are, however, in the main most closely allied
to forms which are now characteristic of tropical or sub-tropical .
regions. ‘Thus, in the London Clay are found numerous fruits
of Palms (Vifadites, fig. 213), along with various other plants,
most of which indicate a warm chmate
as prevailing in the south of England
at the commencement of the Eocene
period. In the Eocene strata of North
America occur numerous plants belong-
ing to existing types—such as Palms,
Conifers, the Magnolia, Cinnamon, Fig,
Dog-wood, Maple, Hickory, Poplar,
Plane, &c. Taken as sa whole, the
Eocene flora of North America is nearly
related to that of the Miocene strata of
Europe, as well as to that now existing
ee ees (ee im the American area: We mayjeum
zs, the fruit of a fossil Palm.
London Clay, Isle of Sheppey. Clude, therefore, that ‘‘the forests of
the American Eocene resembled those
of the European Miocene, and even of modern America”
(Dana).

As regards the azzmads of the Eocene period, the Protozoans
are represented by numerous Foraminifera, which reach here
their maximum of development, both as regards the size of
individuals and the number of generic types. Many of the
Eocene Foraminifers are of small size; but eyen these not
uncommonly form whole rock-masses. Thus, the so-called
“Miliolite Limestone” of the Paris basin, largely used as a
building-stone, is almost wholly composed of the shells of a.
small species of Wz/iola. ‘The most remarkable, however, of
the many members of this group of animals which flourished in
Eocene times, are the “ Nummulites ” (Vammulina), so called
from their resemblance in shape to coins (Lat. zummus, a coin).
The Nummulites are amongst the largest of all known Fora-
minifera, sometimes attaining a size of three inches in circum-
ference ; and their internal structure is very complex (fig. 214).

THE EOCENE PERIOD. 29f

Many species are known, and they are particularly character-
istic of the Middle and Upper of these periods—their place

Fig. 214.—Nummulina levigata. Middle Eocene.

being sometimes taken by Ordztoides, a form very similar to the
Nummulite in external appearance, but differing in its internal
details. In the Middle Eocene, the remains of Nummulites
are found in vast numbers in a very widely-spread and easily-
recognised formation known as the “‘ Nummulitic Limestone”
(fig. t0). According to Sir Charles Lyell, “the Nummulitic
Limestone of the Swiss Alps rises to more than 10,000 feet
above the level of the sea, and attains here and in other moun-
tain-chains a thickness of several thousand feet. It may be
said to play a far more conspicuous part than any other Tertiary
group in the solid framework of the earth’s crust, whether in
Europe, Asia, or Africa. It occurs in Algeria and Morocco,
and has been traced from Egypt, where it was largely quarried
of old for the building of the Pyramids, into Asia Minor, and
across Persia by Bagdad to the mouths of the Indus. It has
been observed not only in Cutch, but in the mountain-ranges
which separate Scinde from Persia, and which form the passes
leading to Cabul; and it has been followed still further east-
ward into India, as far as Eastern Bengal and the frontiers of
China.” The shells of Nummulites have been found at an
elevation of 16,500 feet above the level of the sea in Western
Thibet ; and the distinguished and philosophical geologist just
quoted, further remarks, that ‘‘when we have once arrived at
the conviction that the Nummulitic formation occupies a mid-
dle and upper place in the Eocene series, we are struck with
the comparatively modern date to which some of the greatest
revolutions in the physical geography of Europe, Asia, and
Northern Africa must be referred. All the mountain-chains—
such as the Alps, Pyrenees, Carpathians, and Himalayas—into
the composition of whose central and loftiest parts the Num-
mulitic strata enter bodily, could have had no existence till

292 HISTORICAL PALAZONTOLOGY.

after the Middle Eocene period. During that period, the sea
prevailed where these chains now rise; for Nummulites and
their accompanying Testacea were unquestionably inhabitants
of salt water.”

The Calenterates of the Eocene are represented principally
by Corals, mostly of types identical with or nearly allied to
those now in existence. Perhaps the most characteristic group
of these is that of the .Zurbinolide, comprismg a number of
simple “ cup-corals,” which probably lived in moderately deep
water. One of the forms belonging to this family is here
figured (fig. 215). Besides true Corals, the Eocene deposits
have yielded the remains of the “Sea-
pens” (fennatulide) and the branched
skeletons of the “‘Sea-shrubs” ( Gorgonde).

The L£chinoderms are represented prin-
cipally by Sea-urchins, and demand nothing
more than mention. Itis to be observed,
however, that the great group of the Sea-
lilies (Crznozds) is now verging on extinc-
tion, and is but very feebly represented.

Amongst the AZo//usca, the Folyzoans and
Brachiopods also require no special men-
tion, beyond the fact that the latter are
greatly reduced in numbers, and belong
principally to the existing genera TZere-
bratula and Rhynchonella. The Bivalves
(Lamellibranchs) and the Univalves (Gas-
teropods) are exceedingly numerous, and
almost all the principal existing genera are
now represented ; though less than five
per cent of the Eocene species are identical
with those now living. It is difficult to
make any selection from the many Bivalves
which are known in deposits of this age ;.
but species of Cardita, Crassatella, Leda,

Cyrena, Mactra, Cardium, Psammobia, &c.,

Fig. 215.—Turbinolia may be mentioned as very characteristic.
ee es The Cardita planicosta here figured (fig.
Eocene. 216) is not only very abundant in the
Middle Eocene, but.is very widely distri-

buted, ranging from Europe to the Pacific coast of North
America. The Univalves of the Eocene are extremely nu-
merous, and generally beautifully preserved. The majority
of them belong to that great section of the Gasteropods in
which the mouth of the shell is notched or produced into

THE EOCENE PERIOD. 293

a canal (when the shell is said to be “ siphonostomatous ”)—
this section including the carnivorous and most highly-or-

Fig. 216.—Cardita planicosta. Middle Eocene.

ganised groups of the class. Not only is this the case, but
a large number of the Eocene Univalves belong to types
which now attain their maximum of development in the
warmer regions of the globe. Thus we find numerous species
of Cones (Conus), Volutes (Voluta), Cowries (Cyprea, fig. 218),

Fig. 217.—Typhis_ tubifer, a ‘‘siphonosto- Fig. 218. — Cyprea
matous”” Univalve. Eocene. elegans. Eocene.

Olives and Rice-shells (Ova), Mitre-shells (A/i¢ra), Trumpet-
shells (Z7zton), Auger-shells (Zerebra), and Fig-shells (Pyru/a).
Along with these are many forms of Pleurotoma, Rostellaria,
Spindle-shells (Fzsus), Dog-whelks (lVassa), Murices, and many
round-mouthed (‘‘ holostomatous ”) species, belonging to such
genera as Zurritella, Nerita, Natica, Scalaria, &c. ‘The genus
Cerithium (fig. 219), most of the living forms of which are
found in warm regions, inhabiting fresh or brackish waters,
undergoes a vast development in the Eocene period, where it

294 HISTORICAL PALHONTOLOGY.

is represented by an immense number of specific forms, some
of which attain very large dimensions. In the Eocene strata
of the Paris basin alone, nearly one hundred
and fifty species of this genus have been
detected. The more strictly fresh - water
deposits of the Eocene period have also
yielded numerous remains of Univalves such
as are now proper to rivers and lakes, to-
gether with the shells of true Land-snails.
Amongst these may be mentioned numerous
species of Limnea (fig. 220), Physa (fig. 221),
Melania, Paludina, Planorbis, Helix, Bult-
mus, and Cyclostoma (fig. 222).

With regard to the Cephalopods, the chief
point to be noticed is, that all the beautiful
and complex forms which peculiarly char-

Fig. 219. —Cerithi- acterised the Cretaceous period have here
i as Sik Eo disappeared. We no longer meet with a

x single example of the Turrilite, the Baculite,
the Hamite, the Scaphite, or the Ammonite. The only ex-
ception to this statement is the occurrence of one species

Fig. 220.—Limnuea Fig. 221.—Physa Fig. 222.—Cyclostoma
pyramidalis. Eocene. columnaris. Eocene. Arnoudiz. Eocene.

of Ammonite in the so-called “ Lignitic Formation” of North
America ; but the beds containing this may possibly be rather
referable to the Cretaceous—and this exception does not
affect the fact that the Ammonitide, as a family, had be-
come extinct before the Eocene strata were deposited. The
ancient genus /Vaufilus still survives, the sole representative of
the once mighty order of the Tetrabranchiate Cephalopods.
In the order of the Dibranchiates, we have a like phenomenon
to observe in the total extinction of the great family of the
“ Belemnites.”” No form referable to this group has hitherto

THE EOCENE PERIOD. 295
been found in any Tertiary stratum; but the internal skeletons
of Cuttle-fishes (such as Belosepia) are not unknown.

Remains of fishes are very abundant in strata of Eocene
age, especially in certain localities. ‘The most famous depot
for the fossil fishes of this period is the lhmestone of Monte
Bolea, near Verona, which is interstratified with beds of vol-
canic ashes, the whole being referable to the Middle Eocene.
The fishes here seem to have been suddenly destroyed by a
volcanic eruption, and are found in vast numbers. Agassiz
has described over one hundred and thirty species of Fishes
from this locality, belonging to seventy-seven genera. All
the sfeczes are extinct; but about one-half of the genera are
represented by living forms. The great majority of the

Fig. 223.—Rhombus minimus, a small fossil Turbot from the Eocene Tertiary,
Monte Bolca.

Eocene Fishes belong to the order of the “ Bony Fishes”
( Zéleosteans), so that in the main the forms of Fishes charac-
terising the Eocene are similar to those which predominate
in existing seas. In addition to the above, a few Ganoids and
a large number of Placoids are known to occur in the Eocene
rocks. Amongst the latter are found numerous teeth of true
Sharks, such as Ofodus (fig. 224) and Carcharodon. The
pointed and serrated teeth of the latter sometimes attain a
length of over half a foot, indicating that these predaceous
fishes attained gigantic dimensions; and it is interesting to
note that teeth, in external appearance very similar to those
of the early Tertiary genus Carcharodon, have been dredged
from great depths during the recent expedition of the Chal-
lenger. There also occur not uncommonly the flattened

206 ' HISTORICAL PALZONTOLOGY.

teeth of Rays (fig. 225), consisting of flat bony pieces placed
close together, and forming “a kind of mosaic pavement on
both the upper and lower jaws” (Owen).

In the class of the epizles, the disappearance of -the char-

SSSSSe

Fig. 224.—Tooth of Fig. 225.—Flattened dental plates of a Ray
ede obliguus. (Myliobatis Edwardsiz). Eocene.
ocene.

acteristic Mesozoic types is as marked a phenomenon as the
introduction of new forms. The Ichthyosaurs, the Plesio-
saurs, the Pterosaurs, and the Mosasaurs of the Mesozoic,
find no representatives in the Eocene Tertiary ; and the same
is true of the Deinosaurs, if we except a few remains from the
doubtfully-situated ‘“ Lignitic formation” of the United States.
On the other hand, all the modern orders of Reptiles are
known to have existed during the Eocene -period. The
Chelonians are represented by true marine Turtles, by “ Ter-
rapins” (Hmydide), and by “Soft Tortoises” (Z7conycide).
The order of the Snakes and Serpents (Of/zdia) makes its
appearance here for the first time under several forms—all of
which, however, are referable to the non-venomous group of
the “ Constricting Serpents” (Bode). The oldest of these
is the Paleophis toliapicus of the London Clay of Sheppey,
first made known to science by the researches of Professor
Owen. The nearly-allied Paleophis typheus of the Eocene
beds of Bracklesham appears to have been a Boa-constrictor-
like Snake of about twenty feet in length. Similar Python-
like Snakes (Paleophis, Dinophis, &c.) have been described
from the Eocene deposits of the United States. True Lizards
(Lacertilians) are found in some abundance in the Eocene
deposits,—some being small terrestrial forms, like the common
European lizards of the present day ; whilst others equal or
exceed the living Monitors in size. Lastly, the modern order
of the Crocodilia is largely represented in Eocene times, by
species belonging to all the existing genera, together with
others referable to extinct types. As pointed out by Owen,
it is an interesting fact that in the Eocene rocks of the south-

THE EOCENE PERIOD. 297

west of England, there occur fossil remains of all the three
living types of Crocodilians—namely, the Gavials, the true
Crocodiles, and the Alligators (fig. 226)—though at the

Fig. 226.—Upper jaw of Alligator. Eocene Tertiary, Isle of Wight.

present day these forms are all geographically restricted in
their range, and are never associated together.

Almost all the existing orders of Azrds, if not all, are
represented in the Eocene deposits by remains often very
closely allied to existing types. Thus, amongst the Swimming
Birds ((Vatatores) we find examples of forms allied to the
living Pelicans and Mergansers; amongst the Waders (Grad-
Jatores) we have birds resembling the Ibis (the Vwmenztus
gypsorum of the Paris basin); amongst the Running Birds
(Cursores) we meet with the great Gastornis Paristensis, which
equalled the African Ostrich in height, and the still more
gigantic Dasornis Londinensis; remains of a Partridge rep-
resent the Scratching Birds (2asores) ; the American Eocene
has yielded the bones of one of the Climbing Birds (Scan-
sores), apparently referable to the Woodpeckers ; the Protornis
Glarisiensis of the Eocene Schists of Glaris is the oldest
known example of the Perching Birds (/msessores); and the
Birds of Prey (faptores) are represented by Vultures, Owls,
and Hawks. The toothed Birds of the Upper Cretaceous
are no longer known to exist; but Professor Owen has
recently described from the London Clay the skull of a very
remarkable Bird, in which there is, at any rate, an approxi-
mation to the structure of /chthyornis and Hlesperornis. The
bird in question has been named the Odontopteryx toliapicus,
its generic title being derived from the very remarkable char-
acters of its jaws. In this singular form (fig. 227) the margins

298 HISTORICAL PALHZONTOLOGY.

of both jaws are furnished with tooth like denticulations, which
differ from true teeth in being actually portions of the bony

Fig. 227.—Skull of Odontopteryx toliapicus, restored. (After Owen.)

substance of the jaw itself, with which they are continuous,
and which were probably encased: by extensions of the horny
sheath of the bill. These tooth-like processes are of two
sizes, the larger ones being comparable to canines; and they .
are all directed forwards, and have a triangular or compressed
conical form. From a careful consideration of all the dis-
covered remains of this bird, Professor Owen concludes that
““ Odontopteryx was a warm-blooded feathered biped, with
wings; and further, that it was web-footed and a fish-eater,
and that in the catching of its slippery prey it was assisted by
this Pterosauroid armature of its jaws.” Upon the whole,
Odontopteryx would appear to be most nearly related to the
family of the Geese (Azserine) or Ducks (Anatide); but the
extension of the bony substance of the jaws into tooth-like
processes is an entirely unique character, in which it stands
quite alone.

The known AZammadls of the Mesozoic period, as we have
seen, are all of small size; and with one not unequivocal
exception, they appear to be referable to the order of the
Pouched Quadrupeds (J/arsupials), almost the lowest group
of the whole class of the J/ammafia. In the Eocene rocks,
on the other hand, numerous remains of Quadrupeds have
been brought to light, representing most of the great Mam-
malian orders now in existence upon the earth, and in many
cases indicating animals of very considerable dimensions. We
are, in fact, in a position to assert that the majority of the
great groups of Quadrupeds with which we are familiar at the
present day were already in existence in the Eocene period,
and that their ancient root-stocks were even in this early time
separated by most of the fundamental differences of structure

THE EOCENE PERIOD. 299

which distinguish their living representatives. At the same
time, there are some amongst the Eocene quadrupeds which
havea “ generalised” character, and which may be regarded
as structural types standing midway between groups now
sharply separated from one another.

The order of the A/arsupials—including the existing Kan-
garoos, Wombats, Opossums, Phalangers, &c.— is poorly
represented i in deposits of Eocene age. The most celebrated
example of this group is the Dzdelphys gypsorum of the
Gypseous beds of Montmartre, near Paris, an Opossum very
nearly allied to the living Opossums of North and South
America.

No member of the Hentates (Sloths, Ant-eaters, and Arma-
dillos) has hitherto been detected in any Eocene deposit.
The aquatic order of the Szvenzans (Dugongs and Manatees),
with their fish-like bodies and tails, paddle- shaped fore-
limbs, and wholly deficient hind-limbs, are represented in
strata of this age by remains of the ancient ‘‘ Sea-Cows,” to
which the name of Haltherium has been applied. Nearly
allied to the preceding is the likewise aquatic order of the
Whales and Dolphins (Cefaceans), in which the body is also
fish-like, the hind-limbs are wanting, the fore-limbs are con-
verted into powerful “flippers” or swimming-paddles, and
the terminal extremity of the body is furnished with a
horizontal tail-fin. Many existing Cetaceans (such as the
Whalebone Whales) have no true teeth; but others (Dol-
phins, Porpoises, Sperm Whales) possess simple conical teeth.

Fig. 228.—Zeuglodon cetoides. A, Molar tooth of the natural size; B, Vertebra,
reduced in size. From the Middle Eocene of the United States. (After Lyell.)

In strata of Eocene age, however, we find a singular group
of Whales, constituting the genus Zeuglodon (fig. 228), in

300 HISTORICAL PALASONTOLOGY.

which the teeth differed from those of all existing forms in
being of two kinds,—the front ones being conical incisors,
whilst the back teeth or molars have serrated triangular
crowns, and are inserted in the jaw by two roots. Each
molar (fig. 228, A) looks as if it were composed of two
separate teeth united on one side by their crowns; and it is
this peculiarity which is expressed by the generic name (Gr.
seugle, a yoke; odous, tooth). The best-known species of
the genus is the Zeuglodon cetoides of Owen, which attained
a length of seventy feet. Remains of these gigantic Whales
are very common in the ‘‘ Jackson Beds” of the Southern
United States. So common are they that, according to Dana,
“the large vertebrze, some of them a foot and a half long and
a foot in diameter, were formerly so abundant over the
country, in Alabama, that they were used for making walls, or
were burned to rid the fields of them.”

The great and important order of the Hoofed Quadrupeds
(Ungulata) is represented in the Eocene by examples of both
ot its two principal sections—namely, those with an uneven
number of toes (one or three) on the foot (Perzssodactyle Ungu-
ates), and those with an even number of toes (two or four) to
each foot (Artiodactyle Ungulates). Amongst the Odd-toed
Ungulates, the living family of the Tapirs (Zapzrzd@) is repre-
sented by the genus Coryphodon of Owen. Nearly related to
the preceding are the species of Palgotherium, which have
a historical interest as being amongst the first of the Tertiary
Mammals investigated by the illustrious Cuvier. Several
species of Paleothere are known, varying greatly in size, the
smallest being little bigger than a hare, whilst the largest must
have equalled a good-sized horse in its dimensions. The
species of Faleotherium appear to have agreed with the
existing Tapirs in possessing a lengthened and flexible nose,
which formed a short proboscis or trunk (fig. 229), suitable as
an instrument for stripping off the foliage of trees—the char-
acters of the molar teeth showing them to have been strictly
herbivorous in their habits. They differ, however, from the
Tapirs, amongst other characters, in the fact that both the
fore and the hind feet possessed three toes each; whereas in
the latter there are four toes on each fore-foot, and the hind-
feet alone are three-toed. The remains of FPalgotheria have
been found in such abundance in certain localities as to show
that these animals roamed in great herds over the fertile plains
of France and the south of England during the later portion
of the Eocene period. The accompanying illustration (fig.
229) represents the notion which the great Cuvier was induced

THE EOCENE PERIOD. 301

by his researches to form as to the outward appearance of
Paleotherium magnum. Recent discoveries, however, have

Fig. 229.—Outline of Palzotherium magnum, restored. Upper Eocene, Europe.
(After Cuvier.)

rendered it probable that this restoration is in some important
respects inaccurate. Instead of being bulky, massive, and
more or less resembling the living Tapirs in form, it would rather
appear that Paleothertum magnum was in reality a slender,
graceful, and long-necked animal, more closely resembling in
general figure a Llama, or certain ‘of the Antelopes.

The singular genus Anchitherium forms a kind of transition
between the Palgotheria and the true Horses (Lguid@). The
Horse (fig. 230, D) possesses but one fully-developed toe to
each foot, this being terminated by a single broad hoof, and
representing the mzddle toe—the third of the typical five-
fingered or five-toed limb of Quadrupeds in general. In
addition, however, to this fully-developed toe, each foot in
the horse carries two rudimentary toes which are concealed
beneath the skin, and are known as the “splint-bones.”
These are respectively the second and fourth toes, in an
aborted condition; and the frst and f/th toes are wholly
wanting. In Aipparion (fig. 230, C), the foot is essentially
like that of the modern Horses, except that the second and
fourth toes no longer are mere ‘“‘ splint-bones,” hidden be-
neath the skin; but have now little hoofs, and hang freely,
but uselessly, by the side of the great middle toe, not being
sufficiently developed to reach the ground. In Anchitherium,
again (fig. 230, B), the foot is three-toed, like that of Hzpparion;
but the two lateral toes (the second and fourth) are so far

21

302 HISTORICAL PALZONTOLOGY.

developed that they now reach the ground. The js? digit
(thumb or great toe) is still wanting ; as also is the 7th digit

Fig. 230.—Skeleton of the foot in various forms belonging to the family of the Eguzde.
A, Foot of Ovohifpus, Eocene ; B, Foot of Axchitherium, Upper Eocene and Lower
Miocene ; C, Foot of Hipparion, Upper Miocene and Pliocene ; D, Foot of Horse
(Eguzs), Pliocene and Recent. The figures indicate the numbers of the digits in the
typical five-fingered hand of Mammals. (After Marsh.)

(little finger or little toe). Lastly, the Eocene rocks have
yielded in North America the remains of a small Equine
quadruped, to which Marsh has given the name of Ovohippus.
In this singular form—which was not larger than a fox—the
foot (fig. 230, A) carries fowr toes, all of which are hoofed and
touch the ground, but of which the ¢z7d toe is still the largest.
The frst toe (thumb or great toe) is still wanting ; but in this
ancient representative of the Horses, the 7th or “little” toe
appears for the first time. As all the above-mentioned forms
succeed one another in point of time, it may be regarded as
probable that we shall yet be able to point, with some cer-
tainty, to some still older example of the Zguzd@, in which
the first digit is developed, and the foot assumes its typical
five- fingered condition.

Passing on to the Even-toed or Artiodactyle Ungulates, no
representative of the Azppotamus seems yet to have existed,
but there are several forms (Cheropotamus, Hyopotamus, &c. )
more or less closely allied to the Pigs (Swzda); and the
singular group of the Anoplotheride may be regarded as form-
ing a kind of transition between the Swine and the Ruminants.
The Axnoplotheria (fig. 231) were slender in form, the largest
not exceeding a donkey in size, with long tails, and having the
feet terminated by two hoofed toes each, sometimes with a
pair of small accessory hoofs as well. The teeth exhibit the

THE EOCENE PERIOD. « 303

peculiarity that they are arranged in a continuous series, with-
out any gap or interval between the molars and the canines; and

Fig. 231.—Anoplotherium commune. Eocene Tertiary, France. (After Cuvier.)

the back teeth, like those of all the Ungulates, are adapted for
grinding vegetable food, their crowns resembling in form those
of the true Ruminants. The genera Dechobune and Xiphodon,
of the Middle and Upper Eocene, are closely related to
Anoplotherium, but are more slender and deer-like in form.
No example of the great Ruminant group of the Ungulate
Quadrupeds has as yet been detected in deposits of Eocene
age.

Whilst true Ruminants appear to be unknown, the Eocene
strata of North America have yielded to the researches of
Professor Marsh examples of an extraordinary group (D2zno-
cerata), which may be considered as in some respects inter-
mediate between the Ungulates and the Proboscideans. In
Dinoceras itself (fig. 232) we have a large animal, equal in
dimensions to the living Elephants, which it further resembles
in the structure of the massive limbs, except that there are
only four toes to each foot. The upper jaw was devoid of
front teeth, but there were two very large canine teeth, in the
form of tusks directed perpendicularly downwards ; and there
was also a series of six small molars on each. Each upper
jaw-bone carried a bony projection, which was probably of the
nature of a ‘“‘horn-core,” and was originally sheathed in horn.
Two similar, but smaller, horn-cores are carried on the nasal
bones ; and two much larger projections, also probably of the
nature of horn-cores, were carried upon the forehead. We
may thus infer that Dinoceras possessed three pairs of horns,
all of which resembled the horns of the Sheep and Oxen in
consisting of a central bony ‘‘core,” surrounded by a horny

304 HISTORICAL PALAZONTOLOGY.

sheath. The nose was not prolonged into a proboscis or
“trunk,” as in the existing Elephants ; and the tail was short

Fig. 232.—Skull of Dinxoceras mirabilis, greatly reduced. Eocene, North America.
(After Marsh.)

and slender. Many forms of the Dznocerata are known ; but all
these singular and gigantic quadrupeds appear to have been
confined to the North American continent, and to be restricted
to the Eocene period.

The important order of the Elephants (Prodoscidea) is also
not known to have come into existence during the Eocene
period. On the other hand, the great order of the Beasts of
Prey (Carnivora) is represented in Eocene strata by several
forms belonging to different types. Thus the Arctocyon pre-
sents us with an Eocene Carnivore more or less closely allied
to the existing Racoons ; the Paldeonyctis appears to be related
to the recent Civet-cats; the genus Ayenodon is in some
respects comparable to the living Hyznas; and the Canzs
Paristensis of the gypsum-bearing beds of Montmartre may
perhaps be allied to the Foxes.

The order of the Bats (Chezroptera) is represented in Eocene
strata of the Paris basin (Gypseous series of Montmartre) by
the Vespertilio Parisiensis (fig. 233), an insect-eating Bat very
similar to some of the existing European forms. Lastly, the
Eocene deposits have yielded more or less satisfactory evi-

THE MIOCENE PERIOD. 305

dence of the existence in Europe at this period of examples of
the orders of the Gnawing Mammals (Aodentia), the Insect-

Fig. 233.—Portion of the skeleton of Vesfertilio Parisiensis. Eocene Tertiary, France.

eating Mammals (/zsectevora), and the Monkeys (Quwadru-
mana).*

@ORPASP aro iRn XOX
THE MIOCENE PERIOD:

The Miocene rocks comprise those Tertiary deposits which
contain less than about 35 per cent of existing species of shells
(Mollusca), and more than § per cent—or those deposits in
which the proportion of living shells is less than of extinct
species. They are divisible into a Lower Muocene ( Oligocene)
and an Upper Miocene series.

In Gritain, the Miocene rocks are very poorly developed,
one of their leading developments being at Bovey Tracy in
Devonshire, where there occur sands, clays, and beds of lignite

* A short list of the more important works relating to the Eocene
rocks and fossils will be given after all the Tertiary deposits have been
treated of,

306 HISTORICAL PALEZONTOLOGY.

or imperfect coal. These strata contain numerous plants,
amongst which are Vines, Figs, the Cinnamon-tree, Palms,
and many Conifers, especially those belonging to the genus
Seguota (the ‘‘Red-woods’’). These Bovey Tracy lignites are
of Lower Miocene age, and they are lacustrine in origin. Also
of Lower Miocene age are the so-called ‘‘ Hempstead Beds”
of Yarmouth in the Isle of Wight. These attain a thickness of
less than 200 feet, and are shown by their numerous fossils to
be principally a true marine formation. Lastly, the Duke of
Argyll, in 1851, showed that there existed at Ardtun, in the
island of Mull, certain Tertiary strata containing numerous
remains of plants ; and these also are now regarded as belong-
ing to the Lower Miocene.

In France, the Lower Miocene is represented in Auvergne,
Cantal, and Velay, by a great thickness of nearly horizontal
strata of sands, sandstone, clays, marls, and limestones, the
whole of fresh-water origin. The principal fossils of these
lacustrine deposits are WZammalia, of which the remains occur
in great abundance. In -the valley of the Loire occur the
typical European deposits of Upper Miocene age. ‘These are
known as the “ Faluns,” from a provincial term applied to
shelly sands, employed to spread upon soils which are deficient
in ime; and the Upper Miocene is hence sometimes spoken
of as the “‘ Falunian” formation. The Faluns occur in scat-
tered patches, which are rarely more than 50 feet in thickness,
and consist of sands and marls. ‘The fossils are chiefly marine;
but there occur also land and fresh-water shells, together with
the remains of numerous Mammals. About 25 per cent of the
shells of the Faluns are identical with existing species. The
sands, limestones, and marls of the Department of Gers, near
the base of the Pyrenees, rendered famous by the number of
Mammalian remains exhumed from them by M. Lartet, also
belong to the age of the Faluns.

In Switzerland, between the Alps and the Jura, there occurs
a great series of Miocene deposits, known collectively as the
“ Molasse,” from the soft nature of a greenish sandstone,
which constitutes one of its chief members. It attains a thick-
ness of many thousands of feet, and rises into lofty mountains,
some of which—as the Rigi—are more than 6000 feet in
height. The middle portion of the Molasse is of marine
origin, and is shown by its fossils to be of the age of the
Faluns; but the lower and upper portions of the formation
are mainly or entirely of fresh-water origin. The Lower
Molasse (of Lower Miocene age) has yielded about 500 species
of plants, mostly of tropical or sub-tropical forms, The Upper

THE MIOCENE PERIOD. 307

Molasse has yielded about the same number of plants, with
about goo species of Insects, such ‘as wood-eating Beetles
Water-beetles, White Ants, Dragon-flies, &c.

In Belgium, strata-of both Lower and Upper Miocene age
are known,—the former (Aupelian Clays) containing numerous
marine fossils; whilst the latter (Aolderberg Sands) have
yielded numerous shells corresponding with those of the
Faluns.

In Austria, Miocene strata are largely developed, marine
beds belonging to both the Lower and Upper division of the
formation occurring extensively in the Vienna basin. The
well-known Brown Coals of Radaboj, in Croatia, with numer-
ous plants and insects, are also of Lower Miocene age.

In Germany, deposits belonging to both the Lower and
Upper division of the Miocene formation are extensively de-
veloped. To the former belong the marine strata of the May-
ence basin, and the marine Aupelian Clay near Berlin ;. whilst
a celebrated group of strata belonging to the Upper Miocene
occurs near Epplesheim, in Hesse-Darmstadt, and is well
known for the number of its Mammalian remains.

In Greece, at Pikermé, near Athens, there occurs a celebrated
deposit of Upper Miocene age, well known to paleontologists
through the researches of M.M. Wagner, Roth, and Gaudry
upcn the numerous Mammalia which it contains. In /faly,
also, strata of both Lower and Upper Miocene age are well
developed in the neighbourhood of Turin.

In the S7walik Hills, in India, at the southern foot of the
Himalayas, occurs a series of Upper Miocene strata, which
have become widely celebrated through the researches of Dr
Falconer and Sir Proby Cautley upon the numerous remains
of Mammals and Reptiles which they contain. Beds of corre-
sponding age, with similar fossils, are known to occur in the
island of Perim in the Gulf of Cambay.

Lastly, Miocene deposits are found in (Vorth America, in
New Jersey, Maryland, Virginia, Missouri, California, Oregon,
&c., attaining a thickness of 1500 feet or more. They consist
principally of clays, sands, and sandstones, sometimes of
marine and sometimes of fresh-water origin. Near Richmond,
in Virginia, there occurs a remarkable stratum, wrongly called
“Tnfusorial Earth,” which is occasionally 30 feet in thickness,
and consists almost wholly of the siliceous envelopes of cer-
tain low forms of plants (Diatoms), along with the spicules of
Sponges and other siliceous organisms (see fig. 16). The
White River Group of Hayden occurs in the Upper Missouri
region, and is largely exposed over the barren and desolate

308 HISTORICAL PALZONTOLOGY.

district known as the “ Mauvaises Terres.” They have a
thickness of 1000 feet or more, and contain numerous remains
of Mammals. They are of lacustrine origin, and are believed
to be of the age of the Lower Miocene. Upon the whole,
about from 15 to 30 per cent of the A/o//usca of the American
Miocene are identical with existing species.

In addition to the regions previously enumerated, Miocene
strata are known to be developed in Greenland, Iceland, Spitz-
bergen, and in other areas of less importance.

The “/e of the Miocene period is extremely abundant, and,
from the nature of the deposits of this age, also extremely
varied in its character. The marine beds of the formation
have yielded numerous remains of both Vertebrate and Inver-
tebrate sea-animals; whilst the fresh-water deposits contain
the skeletons of such shells, fishes, &c., as now inhabit rivers
or lakes. Both the marine and the lacustrine beds have been
shown to contain an enormous number of plants, the latter
more particularly ; whilst the Brown Coals of the formation
are made up of vegetable matter little altered from its original
condition. The remains of air-breathing animals, such as
Insects, Reptiles, Birds, and Mammals, are also abundantly
found, more especially in the fresh-water beds.

The flants of the Miocene period are extraordinarily num-
erous, and only some of the general features of the vegetation of
this epoch can be indicated here. Our chief sources of informa-
tion as to the Miocene plants are the Brown Coals of Germany
and Austria, the Lower and Upper Molasse of Switzerland,
and the Miocene strata of the Arctic regions. The lignites of
Austria have yielded very numerous plants, chiefly of a tropical
character—one of the most noticeable forms being a Palm of
the genus Sabal (fig. 234, B), now found in America. The
plants of the Lower Miocene of Switzerland are also mostly
of a tropical character, but include several forms now found
in North America, such as a Tulip-tree (Zzriodendron) and a
Cypress (Zaxodium). Amongst the more remarkable forms
from these beds may be mentioned Fan-Palms (Chamerops,
fig 234, A), numerous tropical ferns, and two species of Cin-
namon. The plant-remains of the Upper Molasse of Switzer-
land indicate an extraordinarily rank and luxuriant vegetation,
composed mainly of plants which now live in warm countries.
Among the commoner plants of this formation may be enume-
rated many species of Maple (Acer), Plane-trees (Platanus
fig. 235), Cinnamon-trees (fig. 236), and other members of the
Lauracee, many species of Proteacee (Banksia, Grevillea, &c.),
several species of Sarsaparilla (Svzz/ax), Palms, Cypresses, &c.

THE MIOCENE PERIOD. 309

In Britain, the Lower Miocene strata of Bovey Tracy have
yielded remains of Ferns, Vines, Fig, Cinnamon, Proteaceae,

y
WZ

==>

Fig. 234.—Miocene Palms. A, Chamerops Helvetica; B, Sabal major.
Lower Miocene of Switzerland and France.

&c., along with numerous Conifers. The most abundant of
these last is a gigantic pine—the Seguota Couttsie—which is

Fig. 235.—P/atanus aceroides, an Fig. 236. — Cznnanto-

Upper Miocene Plane-tree. a, Leaf; mune polymorphum. a,
6, The core of a bundle of fruits; c, Leaf; 4, Flower. Upper
A single fruit. Miocene.

very nearly allied to the huge Seguoza (Wellingtonia) gigantea
of California. A nearly-allied form (Seguoza Langsdorfi) has
been detected in the leaf-bed of Ardtun, in the Hebrides.

In Greenland, as well as in other parts of the Arctic regions,
Miocene strata have been discovered which have yielded a
great number of plants, many of which are identical with
species found in the European Miocene, Amongst these

310 HISTORICAL PALZONTOLOGY.

plants are found many trees, such as Conifers, Beeches, Oaks,
Maples, Plane-trees, Walnuts, Magnolias, &c., with numerous
shrubs, ferns, and other smaller plants. With regard to the
Miocene flora of the Arctic regions, Sir Charles Lyell remarks
that ‘‘more than thirty species of Coniferz have been found,
including several Sequoias (allied to the gigantic Wellingtonia
of California), with species of Zhujopsis and Salishuria, now
peculiar to Japan. There are also beeches, oaks, planes,
poplars, maples, walnuts, limes, and even a magnolia, two
cones of which have recently been obtained, proving that
this splendid evergreen not only lived but ripened its fruit
within the Arctic circle. Many of the limes, planes, and
oaks were large-leaved species; and both flowers and fruits,
besides immense quantities of leaves, are in many cases pre-
served. Among the shrubs are many evergreens, as Andro-
meda, and two extinct genera, Daphnogene and M‘Cliniockia,
with fine leathery leaves, together with hazel, blackthorn,
holly, logwood, and hawthorn. A species of Zamia (Zamites)
grew in the swamps, with VPotamogeton, Sparganium, and
Menyanthes; while ivy and vines twined around the forest-
trees, and broad-leaved ferns grew beneath their shade. Even
in Spitzbergen, as far north as lat. 78° 56’, no less than ninety-
five species of fossil plants have been obtained, including
Taxodium of two species, hazel, poplar, alder, beech, plane-
tree, and lime. Such a vigorous growth of trees within 12° of
the pole, where now a dwarf willow and a few herbaceous
plants form the only vegetation, and where the ground is
covered with almost perpetual snow and ice, 1s truly remark-
ables

Taking the Miocene flora as a whole, Dr Heer concludes
from his study of about 3000 plants contained in the Euro-
pean Miocene alone, that the Miocene plants indicate tropical
or sub-tropical conditions, but that there is a striking inter-
mixture of forms which are at present found in countries
widely removed from one another. It is impossible to state
with certainty how many of the Miocene plants belong to
existing species, but it appears that the larger number are
extinct. According to Heer, the American types of plants
are most largely represented in the Miocene flora, next those
of Europe and Asia, next those of Africa, and lastly those of
Australia. Upon the whole, however, the Miocene flora of
Europe is mostly nearly allied to the plants which we now
find inhabiting the warmer parts of the United States; and
this has led to the suggestion that in Miocene times the
Atlantic Ocean was dry land, and that a migration of Ameri-

THE MIOCENE PERIOD. | 311

can plants to Europe was thus permitted. This view is borne
out by the fact that the Miocene plants of Europe are most
nearly allied to the living plants of the eastern or Atlantic
seaboard of the United States, and also by the occurrence of
a rich Miocene flora in Greenland. As regards Greenland,
Dr Heer has determined that the Miocene plants indicate a
temperate climate in that country, with a mean annual tem-
perature at least 30° warmer than it is at present.

_ The present limit of trees is the isothermal which gives the
mean temperature of 50° Fahr. in July, or about the parallel
of 67° N. latitude. In Miocene times, however, the Limes,
Cypresses, and Plane-trees reach the 79th degree of latitude,
and the Pines and Poplars must have ranged even further
north than this.

The Lnvertebrate Animals of the Miocene period are very
numerous, but they belong for the most part to existing types,
and they can only receive scanty consideration here. The
little shells of Foramznzfera are extremely abundant in some
beds, the genera being in many cases such as now flourish
abundantly in our seas. ‘The principal forms belong to the
genera TZextularia (fig. 237), Robulina, Glandulina, Poly-
stomella, Amphistegina, &c.
Corals are very abundant,
in many instances forming
regular “reefs ;” but all the
more important groups are
in existence at the present
day. The Red Coral (Cor-
allium), so largely sought
after as an ornamental ma-
terial, appears for the first
time in deposits ofthis age. Ge ON Cena? Ser
Amongst the Lchinoderms,
we meet with Heart-Urchins (Spatangus), Cake - Urchins
(Scutella, fig. 238), and various other forms, the majority of
which are closely allied to forms now in existence.

Numerous Crabs and Lobsters represent the Crustacea; but
the most important of the Miocene Articulate Animals are the
Insects. Of these, more than thirteen hundred species have
been determined by Dr Heer from the Miocene strata of
Switzerland alone. They include almost all the existing
orders of insects, such as numerous and varied forms of
Beetles (Coleoptera), Forest-bugs (Hemiptera), Ants (Hymen-
optera), Flies (Diptera), Termites and Dragon -flies (JVewrop-
tera), Grasshoppers (Orthoptera), and Butterflies (Lepidoptera).

312 HISTORICAL PALZONTOLOGY.

One of the latter, the well-known Vanessa Pluto of the Brown
Coals of Croatia, even exhibits the pattern of the wing, and to

Fig. 238.—Different views of Scutella subrotunda, a Miocene ‘‘ Cake-Urchin”
from the south of France.

some extent its original coloration ; whilst the more durably-
constructed insects are often in a state of exquisite preser-
vation.

The Mollusca of the Miocene period are very numerous,
but call for little special comment. Upon the whole, they are
generically very similar to the Shell-fish of the present day;
whilst, as before stated, from fifteen to thirty per cent of the
species are identical with those now in existence. So far as the
European area is concerned, the Molluscs indicate a decidedly
hotter climate than the present one, though they have not such
a distinctly tropical character as is the case with the Eocene
shells. Thus we meet with many Cones, Volutes, Cowries,
Olive-shells, Fig-shells, and the lke, which are decidedly
indicative of a high temperature of the sea. Folyzoans are
abundant, and often attain considerable dimensions; whilst
Brachiopods, on the other hand, are few in number. Szvalves
and Univalves are extremely plentiful ; and we meet here with
the shells of Winged-Snails (P¢eropods), belonging to such
existing genera as Hyalea (fig. 239) and Cleodora. Lastly,
the Cephalopods are represent-
ed both by the chambered
shells of WVautidi and by the
internal skeletons of Cuttle-
fishes (.Spzrzzlirostra.)

Fig. 239.—Different views of eke shell The fishes of the Miocene
J le. big. / i i .
freee OomsIana, a Muocen®. period. are’ very abundanaaeae

of little special importance.
Besides the remains of Bony Fishes, we meet in the marine
deposits of this age with numerous pointed teeth belonging
to different kinds of Sharks. Some of the genera of these—
such as Carcharodon (fig. 241), Oxyrhina (fig. 240), Lamna,
and Galeocerdo—are very widely distributed, ranging through

THE MIOCENE PERIOD. 313

both the Old and New Worlds ; and some of the species attain
gigantic dimensions.

Amongst the Amphibians v we meet with distinctly modern
types, such as Frogs (Rana)
and Newts or Salamanders.
The most celebrated of the
latter is the famous Andras
Scheuchzert (fig. 242), dis-
covered in the year 1725
in the fresh-water Miocene
deposits of Qéningen, in
Switzerland. The skeleton
indicates an animal nearly
five feet in length; and it es ee OIE ee Pee Mea
mas eucinally described by Sz’ Micceue’ < guchn Maccee”
Scheuchzer, a Swiss physi-
cian, in a dissertation published in 1731, as the remains of one
of the human beings who were in existence at the time of the
Noachian Deluge. Hence he applied to it the name of Homo
diluvii testis. In reality, however, as shown by Cuvier, we
have here the skeleton of a huge Newt, very closely allied to
the Giant Salamander (AZenofoma maxima) of Java.

The remains of feftles are far from uncommon in the
Miocene rocks, consisting principally of Chelonians and Cro-
codilians. The Land-tortoises ( Zestudimide) make their first
appearance during this period. The most remarkable form
of this group is the huge Colossochelys Atlas of the Upper
Miocene deposits of the Siwalik Hills in India, described by
Dr Falconer and Sir Proby Cautley. Far exceeding any
living Tortoise in its dimensions, this enormous animal ‘is
estimated as having had a length of about twenty feet, measured
from the tip of the snout to the extremity of the tail, and to
have stood upwards of seven feet high. All the details of its
organisation, however, prove that it must have been “ strictly
a land animal, with herbivorous habits, and probably of the
most inoffensive nature.” ‘The accomplished paleontologist
just quoted, shows further that some of the traditions of the
Hindoos would render it not improbable that this colossal
Tortoise had survived into the earlier portion of the human
period.

Of the zrds of the Miocene period it is sufficient to re-
mark that though specifically distinct, they belong, so far as
known, wholly to existing groups, and therefore present no
points of special palzeontolgical interest.

The Mammals of the Miocene are very numerous, and only

314. HISTORICAL PALZONTOLOGY.

i
) i :

Fig. 242.—Front portion of the skeleton of Andrias Scheuchzeri, a Giant Salamander
from the Miocene Tertiary of CEningen, in Switzerland. Reduced in size.

THE MIOCENE PERIOD. iG

the more important forms can be here alluded to. Amongst
the Marsupials, the Old World still continued to possess
species of Opossum (Dzdephys), allied to the existing American
forms. The Adentates (Sloths, Armadillos, and Ant-eaters), at
the present day mainly South American, are represented by
two large European forms. One of these is the large Jacro-
therium giganteum of the Upper Miocene of Gers in Southern
France, which appears to have been in many respects allied to
the existing Scaly Ant-eaters or Pangolins, at the same time
that the disproportionately long fore-limbs would indicate that
it possessed the climbing habits of the Sloths. The other is
the still more gigantic Avncylothertum Pentelict of the Upper
Miocene of Pikermé, which seems to have been as large as, or
larger than, the Rhinoceros, and which must have been terres-
trial in its habits. This conclusion is further borne out by the
comparative equality of length which subsists between the fore
and hind limbs, and is not affected by the curvature and |
crookedness of the claws, this latter feature being well marked
in such existing terrestrial Edentates as the Great Ant-eater.

The aquatic Sirenians and Cetaceans are represented in
Miocene times by various forms of no special importance.
Amongst the former, the previously existing genus Halithertum
continued to survive, and amongst the latter we meet with
remains of Dolphins and of Whales of the ‘‘Zeuglodont”
family. We may also note here the first appearance of true
““Whalebone Whales,” two species of which, resembling the
living “ Right Whale” of Arctic seas, and belonging to the
same genus (La/ena), have been detected in the Miocene
beds of North America.

The great order of the Ungulates or Hoofed Quadrupeds is
very largely developed in strata of Miocene age, various new
types of this group making their appearance here for the first
time, whilst some of the characteristic genera of the preceding
period are still represented under new shapes. Amongst the
Odd-toed or “‘ Perissodactyle’’ Ungulates, we meet for the first
time with representatives of the family R/znoceride compris-
ing only the existing Rhinoceroses. In India in the Upper
Miocene beds of the Siwalik Hills, and in North America,
several species of Rhinoceros have been detected, agreeing with
the existing forms in possessing three toes to each foot, and in
having one or two solid fibrous ‘‘ horns” carried upon the front
of the head. On the other hand, the forms of this group which
distinguish the Miocene deposits of Europe appear to have
been for the most part hornless, and to have resembled the
Tapirs in having three-toed hind-feet, but four-toed fore-feet.

316 HISTORICAL PALAZONTOLOGY.

The family of the Tapirs is represented, both in the Old
and New Worlds, by species of the genus Lophiodon, some of
which were quite diminutive in point of size, whilst others
attained the dimensions of a horse. Nearly allied to this
family, also, is the singular group of quadrupeds which Marsh
has described from the Miocene strata of the United States
under the name of Lrontotheride. ‘These extraordinary ani-
mals, typified by Brontotherium (fig. 243) itself, agree with the

Fig. 243.—Skull of Broxtotherium ingens. Miocene Tertiary, United States.
(After Marsh.)

existing Tapirs of South America and the Indian Archipelago
in having the fore-feet four-toed, whilst the hind-feet are three-
toed ; and a further point of resemblance is found in the fact
(as shown by the form of the nasal bones) that the nose was
long and flexible, forming a short movable proboscis or trunk,
by means of which the animal was enabled to browse on
shrubs or trees. They differ, however, from the Tapirs, not
only in the apparent presence of a long tail, but also in the
possession of a pair of very large “horn-cores,” carried upon
the nasal bones, indicating that the animal possessed horns of
a similar structure to those of the ‘‘ Hollow-horned” Rumin-
ants (e.g., Sheep and Oxen). rontotherium gigas is said to be
nearly as large as an Elephant, whilst &. zzgens appears to
have attained dimensions still more gigantic. The well-known
genus Zitanotherium of the American Miocene would also
appear to belong to this group.

The family of the Horses (Zgued@) appears under various
forms in the Miocene, but the most important and best known
of these is Hzpparion. In this genus the general conformation
of the skeleton is extremely similar to that of the existing
Horses, and the external appearance of the animal must have
been very much the same. The foot of Aifpparion, however,

THE MIOCENE PERIOD. 317

as has been previously mentioned, differed from that of the
Horse in the fact that whilst both possess the middle toe greatly
developed and enclosed in a broad hoof, the former, in addition,
possessed two lateral toes, which were sufficiently developed
to carry hoofs, but were so far rudimentary that they hung idly
by the side of the central toe without touching the ground
(see fig. 230). In the Horse, on the other hand, these lateral
toes, though present, are not only functionally useless, but are
concealed beneath the skin. Remains of the Wzpparzon have
been found in various regions in Europe and in India; and
from the immense quantities of their bones found in certain
localities, it may be safely inferred that these Middle Tertiary
ancestors of the Horses lived, like their modern representa-
tives, in great herds, and in open grassy plains or prairies.
Amongst the Even-toed or A7ztiodactyle Ungulates, we for
the first time meet with examples of the Azppopotamus, with its
four-toed feet, its massive body, and huge tusk-like lower
canine teeth, The Miocene deposits of Europe have not
hitherto yielded any remains of Hippopotamus ; but several
species have been detected in the Upper Miocene of the Siwalik
Hills by Dr Falconer and Sir Proby Cautley. These ancient
Indian forms, however, differ from the existing [/ippopotamus
amphibius of ‘Africa in the fact that they possessed six incisor
teeth in each jaw (fig. 244), whereas the latter has only four.
Amongst the other Even-toed Ungulates, the family of the
Pigs (Suzda) is represented by true Swine (Sus Erymanthius),
Peccaries (LDucotyles antiguus), and by forms which, like the
great L/otherium of the American Miocene, have no represen-
tative at the present day. The Upper Miocene of India has
yielded examples of the Camels. Small Musk-deer (Amphz-
tragulus and Dremotherium) are known to have existed in
France and Greece; and the true Deer (Cervide), with their
solid bony antlers, appear for the first time here in the person of
species allied to the living Stags (Cervus), accompanied by the
extinct genus Dorcatherium. The Giraffes (Camelopardaiide),
now confined to Africa, are known to have lived in India and
Greece; and the allied Hel/adotherium, in some repects inter-
mediate between the Giraffes and the Antelopes, ranged over
Southern Europe from Attica to France. The great group of
the ‘‘ Hollow-horned” Ruminants (Cavicornia), lastly, came
into existence in the Miocene period; and though the typical
families of the Sheep and Oxen are apparently wanting, there
are true Antelopes, together with forms which, if systemati-
cally referable to the Antilopidaz, nevertheless are more or less
clearly transitional between this and the family of the Sheep
22

318. HISTORICAL PALZONTOLOGY.

and Goats. Thus the Palgoreas of the Upper Miocene of
Greece may be regarded as a genuine Antelope; but the

Fig. 244.—a, Skull of Hippopotamus Sivalensis, viewed from below, one-eighth of the
natural size; 4, Molar tooth of the same, showing the surface of the crown, one-half of
the natural size; c, Front of the lower jaw of the same, showing the six incisors and the

tusk-like canines, one-eighth of the natural size. Upper Miocene, Siwalik Hills. (After
Falconer and Cautley.) F

Tragoceras of the same deposit is intermediate in its characters
between the typical Antelopes and the Goats. Perhaps the
most remarkable, however, of these Miocene Ruminants is the
Sivatherium giganteum (fig. 245) of the Siwalik Hills, in India.
In this extraordinary animal there were two pairs of horns,
supported by bony “horn-cores,” so that there can be no
hesitation in referring .S7z vatherium to the Cavicorn Rumin-
ants. If all these horns had been simple, there would have
been no difficulty in considering Szvatherium as simply a
gigantic four-horned Antelope, essentially similar to the living
Antilope ( Zetraceros) guadricornis of India. The hinder pair
of horns, however, is not only much larger than the front pair,
but each possesses two branches or snags—a peculiarity not to
be paralleled amongst any existing Antelope, save the abnormal
Prongbuck (Axtilocapra) of North America. Dr Murie, how-
ever, in an admirable memoir on the structure and relationships

THE MIOCENE PERIOD. 319

of Szvatherizum, has drawn attention to the fact that the Prong-
buck sheds the sheath of its horns annually, and has suggested

Fig. 245.—Skull of Stvathertum giganteum, reduced in size. Miocene, India.
(After Murie.)

that this may also have been the case with the extinct form.
This conjecture is rendered probable, amongst other reasons,
by the fact that no traces of a horny sheath surrounding the
horn-cores of the Indian fossil have been as yet detected.
Upon the whole, therefore, we may regard the elephantine
Sivatherium as being most nearly allied to the Prongbuck of
Western America, and thus as belonging to the family of the
Antelopes.

It is to the Miocene period, again, to which we must refer
the first appearance of the important order of the Elephants
and their allies (Fr oboscideans), all of which are characterised by
their elongated trunk-hke noses, the possession of five toes to
the foot, the absence of canine teeth, the development of two
or more of the incisor teeth into long tusks, and the adaptation
of the molar teeth to a vegetable diet. Only three generic
groups of this order are known—namely, the extinct Dezno-
therium, the equally extinct AZastodons, and the Elephants; and
all these three types are known to have been in existence as

320 HISTORICAL PALZONTOLOGY.

early as the Miocene period, the first of them being exclusively
confined to deposits of this age. Of the three, the genus
Deinothertum 1s much the most abnormal in its characters ;
so much so, that good authorities regard it as really being one
of the Sea-cows (.Szvenza)—though this view has been rendered
untenable by the discovery of limb-bones which can hardly
belong to any other animal, and which are distinctly Probosci-
dean in type. The most celebrated skull of the Deinothere
(fig. 246) is one which was exhumed from the Upper Miocene
deposits of Epplesheim, in Hesse-
Darmstadt, in the year 1836.
This skull was four and a half
feet in length, and indicated an
animal larger than any existing
species of Elephant. The upper
jaw is destitute of incisor or
canine teeth, but is furnished on
each side with five molars, which
‘are opposed to a corresponding
series of grinding teeth in the
lower jaw. No canines are pre-
sent in the lower jaw; but the
front portion of the jaw is ab-
Fig. 246.—Skull of Deinotherium ruptly bent downwards, and car-
giganteum, greatly reduced. From . : ar ae
the Upper Miocene of Germany. ries two huge tusk-like incisor
teeth, which are curved down-
wards and backwards, and the use of which is rather proble-
matical. Not only does the Deinothere occur in Europe, but
remains belonging to this genus have also been detected in the
Siwalik Hills, in India.

The true Elephants (Z/efias) do not appear to have ex-
isted during the Miocene period in Europe, but several species
have been detected in the Upper Miocene deposits of the
Siwalik Hills, in India. The fossil forms, though in all cases
specifically, and in some cases even sub-generically, distinct,
agree with those now in existence in the general conformation
of their skeleton, and in the principal characters of their den-
tition. In all, the canine teeth are wanting in both jaws; and
there are no incisor teeth in the lower jaw, whilst there are
two incisors in the front of the upper jaw, which are de-
veloped into two huge “tusks.” There are six molar teeth
on each side of both the upper and lower jaw, but only
one, or at most a part of two, is in actual use at any given
time; and as this becomes worn away, it is pushed forward
and replaced by its successor behind it. The molars are of

THE MIOCENE PERIOD. 321

very large size, and are each composed of a number of trans-
verse plates of enamel united together by ivory; and by the

Fig. 247.—A, Molar tooth of Elephas planifrons, one-third of the natural size, show-
ing the grinding surface—from the Upper Miocene of India; B, Profile view of the
last upper molar of Mastodon Sivalensis, one-third of the natural size—from the Upper
Miocene of India. (After Falconer.)

process of mastication, the teeth become worn down to a flat
surface, crossed by the enamel-ridges in varying patterns.
These patterns are different in the different species of Ele-
phants, though constant for each ; and they constitute one of
the most readily available means of separating the fossil
forms from one another. Of the seven Miocene Elephants
of India, as judged by the characters of the molar teeth,
two are allied to the existing Indian Elephant, one is related
to the living African Elephant, and the remaining four are in
some respects intermediate between the true Elephants and
the Mastodons.

The Mastodons, lastly, though quite elephantine in their

322 HISTORICAL PALEONTOLOGY.

general characters, possess molar teeth which have their crowns
furnished with conical eminences or tubercles placed in pairs
(fig. 247, B), instead of having the approximately flat surface
characteristic of the grinders of the Elephants. As in the
latter, there are two upper incisor teeth, which grow perma-
nently during the life of the animal, and which constitute great
tusks ; but the Mastodons, in addition, often possess two lower
incisors, which in some cases likewise grow into small tusks.
Three species of Mastodon are known to occur in the Upper
Miocene of the Siwalik Hills of India; and the Miocene de-
posits of the European area have yielded the remains of four
species, of which the best known are the JZ. /ongirostris and the
M. angustidens.

Whilst herbivorous Quadrupeds, as we have seen, were
extremely abundant during Miocene times, and often attained
gigantic dimensions, Beasts of Prey (Carnivora) were by no
means wanting, most of the principal existing families of the
order being represented in deposits of this age. Thus, we find
aquatic Carnivores belonging to both the living groups of the
Seals and Walruses ; true Bears are wanting, but their place
is filled by the closely-allied genus Amphicyon, of which various
species are known; Weasels and Otters were not unknown,
and the Ayenictts and JSctitherium of the Upper Miocene of
Greece are apparently intermediate between the Civet-cats and
the Hyzenas ; whilst the great Cats of subsequent periods are
more than adequately represented by the huge “‘Sabre-toothed
Tiger ” (AZachairodus), with its immense trenchant and serrated
canine teeth.

Amongst the Rodent Mammals, the Miocene rocks have
yielded remains of. Rabbits, Porcupines (such as the A/ystrex
primigenius of Greece), Beavers, Mice, Jerboas, Squirrels, and
Marmots. All the principal living groups of this order were
therefore differentiated in Middle Tertiary times.

The Cheiroptera are represented by small insect-eating Bats;
and the order of the Insectivorous Mammals is represented by
Moles, Shrew-mice, and Hedgehogs.

Lastly, the Monkeys (Quadrumana) appear to have existed
during the Miocene period under a variety of forms, remains
of these animals having been found both in Europe and in
India ; but no member of this order has as yet been detected
in the Miocene Tertiary of the North American continent.
Amongst the Old World Monkeys of the Miocene, the two
most interesting are the P/opithecus and Dryopithecus of France.
The former of these (fig. 248) is supposed to have been most
nearly related to the living Semmnofitheci of Southern Asia, in

THE PLIOCENE PERIOD: 323

which case it must have possessed a long tail. The JZesopi-
thecus of the Upper Miocene of Greece is also one of the lower

Fig. 248.—Lower jaw of Pliopithecus antiqguus. Upper Miocene, France.

Monkeys, as it is most closely allied to the existing Macaques.
On the other hand, the Dryopithecus of the French Upper
Miocene is referable to the group of the ‘‘Anthropoid Apes,”
and is most nearly related to the Gibbons of the present day,
in which the tail is rudimentary and there are no cheek-
pouches. Dryopithecus was, also, of large size, equalling Man
in stature, and apparently living amongst the trees and feed-
ing upon fruits.

CIREAVP eERe + XX
THE PLIOCENE PERIOD.

The highest division of the Tertiary deposits is termed the
Pliocene formation, in accordance with the classification pro-
posed by Sir Charles Lyell. The Pliocene formations contain
from 40 to 95 per cent of existing species of JZo//usca, the re-
maindes belonging to extinct species. They are divided by Sir
Charles Lyell into two divisions, the Older Pliocene and Newer
Pliocene.

The Pliocene deposits of Britain occur in Suffolk, and are
known by the name of ‘ Crags,” this being a local term used
for certain shelly sands, which are employed in agriculture.
Two of these Crags are referable to the Older Pliocene, viz.,

aon HISTORICAL PALZZONTOLOGY.

-the White and Red Crags,—and one belongs to the Newer
Pliocene, viz., the Norwich Crag.

The White or Coralline Crag of Suffolk is the oldest of the
Pliocene deposits of Britain, and is an exceedingly local for-
mation, occurring in but a single small area, and having a
maximum thickness of not more than 50 feet. It consists of
soft sands, with occasional intercalations of flaggy limestone.
Though of small extent and thickness, the Coralline Crag is of
importance from the number of fossils which it contains. The
name ‘Coralline” is a misnomer; since there are few true
Corals, and the so-called ‘“‘ Corals” of the formation are really
Folyzoa, often of very singular forms. The shells of the Coral-
line Crag are mostly such as inhabit the seas of temperate
regions; but there occur some forms usually looked upon as
indicating a warm climate.

The Upper or Red Crag of Suffolk—like the Coralline Crag
—has a limited geographical extent and a small thickness,
rarely exceeding 40 feet. It consists of quartzose sands, usu-
ally deep red or brown in colour, and charged with numerous
fossils.

Altogether more than 200 species of shells are known from
the Red Crag, of which 60 per cent are referable to existing
species. The shells indicate, upon the whole, a temperate or
even cold climate, decidedly less warm than that indicated by
the organic remains of the Coralline Crag. It appears, there-
fore, that a gradual refrigeration was going. on during the
Pliocene period, commencing in the Coralline Crag, becoming
intensified in the Red Crag, being still more severe in the
Norwich Crag, and finally culminating in the Arctic cold of the
Glacial period.

Besides the J/o//usca, the Red Crag contains the ear-bones
of Whales, the teeth of Sharks and Rays, and remains of the
Mastodon, Rhinoceros, and Tapir.

The (ewer Pliocene deposits are represented in Britain by
the Worwich Crag, a local formation occurring near Norwich.
It consists of incoherent sands, loams, and gravels, resting in
detached patches, from 2 to 20 feet in thickness, upon an
eroded surface of Chalk. The Norwich Crag contains a mix-
ture of marine, land, and fresh-water shells, with remains of
fishes and bones of mammals; so that it must have been de-
posited as a local sea-deposit near the mouth of an ancient
river. It contains altogether more than roo marine shells,
of which 89 per cent belong to existing species. Of the
Mammals, the two most important are an Elephant (£Z/ephas
meridionalis), and the characteristic Pliocene Mastodon (JZ.

THE PLIOCENE PERIOD. 325

Arvernensts), which is hitherto the only Mastodon found in
Britain. :

According to the most recent views of high authorities,
certain deposits—such as the so-called ‘“ Bridlington Crag ” of
Yorkshire, and the ‘‘ Chillesford beds” of Suffolk—are to be
also included in the Newer Plocene, upon the ground that
they contain a small proportion of extinct shells. Our know-
ledge, however, of the existing Molluscan fauna, is still so far
incomplete, that it may reasonably be doubted if these sup-
posed extinct forms have actually made their final disappear-
ance, whilst the strata in question have a strong natural con-
nection with the “ Glacial deposits,” as shown by the number
of Arctic Mollusca which they contain. Here, therefore, these
beds will be included in the Post-Phocene series, in spite of
the fact that some of their species of shells are not known to
exist at the present day.

The following are the more important Phocene deposits
which have been hitherto recognised out of Britain :—

1. In the neighbourhood of Antwerp occur certain “ crags,”
which are the equivalent of the White and Red Crag in part.
The lowest of these contains less than 50 per cent, and the
highest 60 per cent, of existing species of shells, the remainder
being extinct.

2. Bordering the chain of the Apennines, in Italy, on both
sides is a series of low hills made up of Tertiary strata, which
are known as the Sub-Apennine beds. Part of these is of
Miocene age, part is Older Pliocene, and a portion is Newer
Pliocene. ‘The Older Pliocene portion of the Sub-Apennines
consists of blue or brown marls, which sometimes attain a
thickness of 2000 feet.

3. In the valley of the Arno, above Florence, are both
Older and Newer Pliocene strata. The former consist of blue
clays and lignites, with an abundance of plants. The latter
consist of sands and conglomerates, with remains of large Car-
nivorous Mammals, Mastodon, Elephant, Rhinoceros, Hippo-
potamus, &c.

4. In Sicily, Newer Pliocene strata are probably more largely
developed than anywhere else in the world, rising sometimes
to a height of 3000 feet above the sea. ‘The series consists
of clays, marls, sands, and conglomerates, capped by a com-
pact limestone, which attains a thickness of from 700 to 800
feet. The fossils of these beds belong almost entirely to living
species, one of the commonest being the Great Scallop of the
Mediterranean (Pecten Jacobus).

5. Occupying an extensive area round the Caspian, Aral,

326 HISTORICAL PALZONTOLOGY.

-and Azof Seas, are Pliocene deposits known as the “ Aralo-
Caspian”’ beds. The fossils in these beds are partly fresh-
water, partly marine, and partly intermediate in character, and
they are in great part identical with species now inhabiting
the Caspian. The entire formation appears to indicate the
former existence of a great sheet of brackish water, forming an
inland sea, like the Caspian, but as large as, or larger than, the
Mediterranean.

6. In the United States, strata of Pliocene age are found in
North and South Carolina. They consist of sands and clays,
with numerous fossils, chiefly Molluscs and Echinoderms.
From 40 to 60 per cent of the fossils belong to existing
species. On the Loup Fork of the river Platte, in the Upper
Missouri region, are strata which are also believed to be refer-
able to the Pliocene period, and probably to its upper division.
They are from 300 to 400 feet thick, and contain land-shells,
with the bones of nurnerous Mammals, such as Camels, Rhino-
ceroses, Mastodons, Elephants, the Horse, Stag, &c.

As regards the /zfe of the Pliocene period, there are only
two classes of organisms to which our attention need be
directed—namely, the Shell-fish and the Mammals. So far as
the former are concerned, we have to note in the first place
that the introduction of new species of animals upon the globe
went on rapidly during this period. In the Older Pliocene
deposits, the number of shells of existing species is only from
40 to 60 per cent; but in the Newer Pliocene the pro-
portion of living forms mses to as much as from 80 to
95 per cent. Whilst the Molluscs thus become rapidly mo-
dernised, the Mammals still all belong to extinct species,
though modern generic types gradually supersede the more
antiquated forms of the Miocene. In the second place, there
is good evidence to show that the Pliocene period was one in
which the climate of the northern hemisphere underwent a
gradual refrigeration. In the Miocene period, there is evi-.
dence to show that Europe possessed a climate very similar
to that now enjoyed by the Southern United States, and cer-
tainly very much warmer than it is at present. The presence
of Palm-trees upon the land, and of numerous large Cowries,
Cones, and other shells of warm regions in the sea, sufficiently
proves this. In the Older Pliocene deposits, on the other
hand, northern forms predominate amongst the Shells, though
some of the types of hotter regions still survive. In the Newer
Pliocene, again, the Molluscs are such as almost exclusively
inhabit the seas of temperate or even cold regions; whilst if
we regard deposits like the “ Bridlington Crag” and “ Chilles-

THE PLIOCENE PERIOD. 327

ford beds” as truly referable to this period, we meet at the
close of this period with shells such as nowadays are distinct-
ively characteristic of high latitudes. It might be thought
that the occurrence of Quadrupeds such as the Elephant,
Rhinoceros, and Hippopotamus, would militate against this
generalisation, and would rather support the view that the
climate of Europe and the United States must have been a
hot one during the later portion of the Plocene period. We
have, however, reason to believe that many of these extinct
Mammals were more abundantly furnished with hair, and more
adapted to withstand a cool temperature, than any of their
living congeners. We have also to recollect that many of
these large herbivorous quadrupeds may have been, and
indeed probably were, more or less migratory in their habits ;
and that whilst the winters of the later portion of the Pliocene
period were cold, the summers might have been very hot.
This would allow of a northward migration of such terrestrial
animals during the summer-time, when there would be an
ample supply of food and a suitably high temperature, and a
southward recession towards the approach of winter.

The chief palzontological interests of the Phocene deposits,
as of the succeeding Post-Pliocene, centre round the Mammals
of the period ; and amongst the many forms of these we may
restrict our attention to the orders of the Hoofed Quadrupeds
(Ungulates), the Proboscideans, the Carnivora, and the Quad-
rumana. Almost all the other Mammalian orders are more
or less fully represented in Pliocene times, but none of them
attains any special interest till we enter upon the Post-Pliocene.

Amongst the Odd-toed Ungulates, in addition to the remains
of true Tapirs (Zapirws Arvernensis), we meet with the bones
of several species of Rhinoceros, of which the RAznoceros Etrus-
cus and FR. megarhinus (fig. 249) are the most important. The
former of these (fig. 249, A) derives its specific name from its
abundance in the Pliocene deposits of the Val d’Arno, near
Florence, and though principally Pliocene in its distribution,
it survived into the earlier portion of the Post-Pliocene period.
Rhinoceros Etruscus agreed with the existing African forms in
having two horns placed one behind the other, the front one
being the longest ; but it was comparatively slight and slender
in its build, whilst the nostrils were separated by an incom-
plete bony partition. In the Rhinoceros megarhinus (fig. 249,
B), on the other hand, no such partition exists between the
nostrils, and the nasal bones are greatly developed in size. It
was a two-horned form, and is found associated with Elephas
meridionalis and £. antiquus in the Pliocene deposits of the

328 HISTORICAL PALHZONTOLOGY.

Val d’Arno, near Florence. Like the preceding, it survived,
in diminished numbers, into the earlier portion of the 258
Pliocene period.

The Horses (Zguid@) are represented, both in Avrope and

Fig. 249.—A, Under surface of the skull of Rhinoceros Etruscus, one-seventh of the
natural size—Pliocene, Italy; B, Crowns of the three true molars of the upper jaw, left
side, of Rhinoceros ntegarhinus (R. leptorhinus, Falconer), one-half of the natural size
—Pliocene, France. (After Falconer.)

America, by the three-toed Hipparions, which survive from the
Miocene, but are now verging upon extinction. For the first
time, also, we meet with genuine Horses (Zgwus), in which
each foot is provided with a single complete toe only, encased
in a single broad hoof. One of the American species of this
period (the Zgwus excelsus) quite equalled the modern Horse
in stature ; and it is interesting to note the occurrence of indi-
genous horses in America at such a comparatively late geo-
logical epoch, seeing that this continent certainly possessed
none of these animals when first discovered by the Spaniards.

Amongst the Even-toed Ungulates, we may note the occur-

THE PLIOCENE PERIOD. 329

rence of Swine (Swzzda), of forms allied to the Camels (Camel-
ide), and of various kinds of Deer (Cervide@) ; but the most
interesting Pliocene Mammal belonging to this section is the
great Azppopotamus major of Britain and Europe. ‘This well-
known species 1s very closely allied to the living Azppopotamus
amphibius of Africa, from which it is separated only by its
larger dimensions, and by certain points connected with the
conformation of the skeleton. It is found very abundantly in
the Pliocene deposits of Italy and France, associated with the
remains of the Elephant, Mastodon, and Rhinoceros, and it
survived into the earlier portion of the Post-Phocene period.
During this last-mentioned period, it extended its range north-
wards, and is found associated with the Reindeer, the Bison,
and other northern animals. From this fact it has been infer-
red, with great probability, that the Azppopotamus major was
furnished with a long coat of hair and fur, thus differing from
its nearly hairless.modern representative, and resembling its
associates, the Mammoth and the Woolly Rhinoceros.
Passing on to the Pliocene Proboscideans, we find that the
great Deinotheria of the Miocene have now wholly disappeared,
and the sole representatives of the order are Mastodons and
Elephants. ‘The most important member of the former group
is the Mastodon Arvernensis (fig. 250), which ranged widely

Fig. 250.—Third milk-molar of the left side of the upper jaw of Mastodon
Arvernensis, showing the grinding surface. Pliocene.

over Southern Europe and England, being generally associated
with remains of the Hlephas meridionalis, EL. antiquus, Rhino-
ceros megarhinus, and Hippopotamus major. ‘The lower jaw
seems to have been destitute of incisor teeth; but the upper
incisors are developed into great tusks, which sometimes reach

330 HISTORICAL PALZONTOLOGY.

a length of nine feet, and which have the simple curvature of
the tusks of the existing Elephants. Amongst the Pliocene
Elephants the two most important are the Zvephas mertdionalts
and the vephas antiguus. Of these, the Hlephas meridionalis
(fig. 251) 1s found abundantly in the Phocene deposits of

Fig. 251.—Molar tooth of Elephas meridionalis, one-third of the natural size.
Pliocene and Post-Pliocene.

Southern Europe and England, and also survived into the
earlier portion of the Post-Pliocene period. Its molar teeth
are of the type of those of the existing African Elephant, the
spaces enclosed by the transverse enamel-plates being more
or less lozenge-shaped, whilst the curvature of the tusks is
simple. The Ziephas antiquus (fig. 252) is very generally

Fig. 252.—Molar tooth of Elephas antiguus, one-third of the natural size.
Pliocéne and Post-Pliocene.

associated with the preceding, and it survived to an even
later stage of the Post-Pliocene period. ‘The molar teeth are
of the type of the existing Indian Elephant, with compara-
tively thin enamel-ridges, placed closer together than in the
African type ; whilst the tusks were nearly straight. |

Amongst the Phlocene Carnzvores, we meet with true Bears
(Ursus Arvernensis), Hyznas (such as Hyena Hipparionum),
and genuine Lions (such as the Fes angustus of North
America); but the most remarkable of the beasts of prey of

THE PLIOCENE PERIOD. 331

this period is the great “ Sabre-toothed Tiger ” (AZachairodus),
species of which existed in the earlier Miocene, and survived
to the later Post-Pliocene. In this remarkable form we are
presented with perhaps the most highly carnivorous type of
all known beasts of prey. Not only are the jaws shorter in
proportion even than those of the great Cats of the present
day, but the canine teeth (fig. 253) are of enormous size,

Fig. 253.—A, Skull of MWachairodus cultridens, without the lower jaw, reduced in
size ; B, Canine tooth of the same, one-half the natural size. Pliocene, France.

greatly flattened so as to assume the form of a poignard, and
having their margins finely serrated. Apart from the charac-
ters of the skull, the remainder of the skeleton, so far as known,
exhibits proofs that the Sabre-toothed Tiger was extraordi-
narily muscular and powerful, and in the highest degree adapt-
ed for a life of rapine. Species of Machatrodus must have
been as large as the existing Lion; and the genus is not only
European, but is represented both in South America and in
India, so that the geographical range of these predaceous
beasts must have been very extensive.

Lastly, we may note that the Pliocene deposits of Europe
have yielded the remains of Monkeys (Quadrumana), allied to
the existing Semnopitheci and Macaques.

332 HISTORICAL PALEONTOLOGY.

LITERATURE.

The following list comprises a small selection of some of the more im-
portant and readily accessible works and memoirs relating to the Tertiary
rocks and their fossils. With few exceptions, foreign works relating to
the Tertiary strata of the continent of Europe or their organic remains
have been omitted :—

(1) ‘Elements of Geology.’ Lyell.

2) ‘Students’ Elements of Geology.’ Lyell.

(3) ‘Manual of Paleontology.’ Owen.

(4) ‘British Fossil Mammals and Birds.’ Owen.

(5) ‘ Traité de Paléontologie.’ Pictet.

(6) ‘Cours Elémentaire de Palé€ontologie.’ D’Orbigny.

(7) ‘‘ Probable Age of the London Clay,” &c.—‘ Quart. Journ. Geol.

Soc.,’ vol. iii. Prestwich. :
(8) ‘Structure and Probable Age of the Bagshot Sands ’—Ibid., vol. iii.
Prestwich.

(9) ‘Tertiary Formations of the Isle of Wight’—Ibid., vol. ii. Prest-

wich.

(10) ‘Structure of the Strata between the London Clay and the Chalk,’

&c.—Ibid., vols. vi., vill., and x. Prestwich.
(11) ‘Correlation of the Eocene Tertiaries of England, France, and
Belgium ’—Ibid., vol. xxvii. Prestwich.

(12) ‘On the Fluvio-marine Formations of the Isle of Wight ’—Ibid.,

vol. ix. Edward Forbes.
(13) ‘Newer Tertiary Deposits of the Sussex Coast ’—Ibid., vol. xiii.
Godwin- Austen.

(14) ‘Kainozoic Formations of Belgium ’—Ibid., vol. xxii. Godwin-
Austen.

(15) ‘Tertiary Strata of Belgium and French Flanders ’—Ibid., vol. viii.
Lyell.

(16) ‘On Tertiary Leaf-beds in the Isle of Mull’—Ibid., vol. vii. The
Duke of Argyll.

(17) ‘Newer Tertiaries of Suffolk and their Fauna ’—Ibid., vol. xxvi.
Ray Lankester.

(18) ‘Lower London Tertiaries of Kent’—Ibid., vol. xxii. Whitaker.

(19) ‘‘Guide to the Geology of London” — ‘Mem. Geol. Survey.’
Whitaker.

(20) ‘ Memoirs of the Geological Survey of Great Britain.’

(21) ‘Introductory Outline of the Geology of the Crag District’ (Sup-
plement to Crag Mollusca, Palzeontographical Society). S. V.
Wood, jun., and F. W. Harmer.

(22) ‘Tertiary Fluvio-marine Deposits of the Isle of Wight.” Edward
Forbes. Edited by Godwin-Austen; with Descriptions of the
Fossils by Morris, Salter, and Rupert Jones—‘ Memoirs of the
Geological Survey.’

) * Geological Excursions round the Isle of Wight.’ Mantell.

) ‘Catalogue of British Fossils.’ Morris.

) ‘Catalogue of Fossils in the Museum of Practical Geology.’ Ethe-
ridge.

(26) ‘Monograph of the Crag Polyzoa’ (Palzeontographical Society). Busk.

(27) ‘Monograph of the Tertiary Brachiopoda’ (Ibid.) Davidson.

(28) ‘Monograph of the Tertiary Malacostracous Crustacea’ (Ibid.)

Bell.

THE PLIOCENE PERIOD. 333

(29) ‘Monograph of the Tertiary Corals’ (Ibid.) Milne-Edwards and
aime.

(30) ‘Supplement to the Tertiary Corals’ (Ibid.) Martin Duncan.

(31) ‘ Monograph of the Eocene Mollusca’ (Ibid.) Fred. E. Edwards.

(32) ‘ Monograph of the Eocene Mollusca’ (Ibid.) Searles V. Wood,

(33) ‘ Monograph of the Crag Mollusca’ (Ibid.) Searles V. Wood.

(34) ‘Monograph of the Tertiary Entomostraca’ (Ibid.) Rupert Jones.

(35) ‘Monograph of the Foraminifera of the Crag’ (Ibid.) Rupert Jones,
Parker, and H. B. Brady.

(36) ‘Monograph of the Radiaria of the London Clay’ (Ibid.) Edward
Forbes.

(37) ‘Monograph of the Cetacea of the Red Crag’ (Ibid.) Owen.

(38) ‘Monograph of the Fossil Reptiles of the London Clay’ (Tbid.)
Owen and Bell.

(39) ‘On the Skull of a Dentigerous Bird from the London Clay of
Sheppey ”—‘ Quart. Journ. Geol. Soc.,’ vol. xxix. Owen.

(40) ‘Ossemens Fossiles.’ Cuvier.

(41) ‘Fauna Antiqua Sivalensis.’ Falconer and Sir Proby Cautley.

(42) ‘ Paleontological Memoirs.’ Falconer.

(43) ‘ Animaux Fossiles et Géologie de l’Attique.’ Gaudry.

(44) ‘‘ Principal Characters of the Dinocerata”—‘ American Journ. of
Science and Arts,’ vol. xi. Marsh.

(45) ‘ Principal Characters of the Brontotheride’ (Ibid.) Marsh.

(46) ‘ Principal Characters of the Tillodontia’ (Ibid.) Marsh.

(47) ‘‘ Extinct Vertebrata of the Eocene of Wyoming ’”’—‘ Geological
Survey of Montana,’ &c., 1872. Cope.

(48) ‘‘ Ancient Fauna of Nebraska’”—‘ Smithsonian Contributions to
Knowledge,’ vol. vi. Leidy.

(49) ‘Manual of Geology.’ Dana.

(50) ‘* Paleontology and Evolution” (Presidential Address to the
Geological Society of London, 1870)— ‘Quart. Journ. Geol.
Soc.,’ vol. xxvi.. Huxley. ;

(51) ‘Mineral Conchology.’ Sowerby.

(52) ‘ Description des Coquilles Fossiles,’ &c. Deshayes.

(53) ‘ Description des Coquilles Tertiaires de Belgique.’ Nyst.

(54) ‘ Fossilen Polypen des Wiener Tertiar-beckens.’ Reuss.

(55) ‘Palzontologische Studien iiber die alteren Tertiar-schichten der
Alpen.’ Reuss.

(56) ‘Land und Siiss-wasser Conchylien der Vorwelt.’ Sandberger.

(57) ‘Flora Tertiaria Helvetica.’ Heer.

(58) ‘Flora Fossilis Arctica.’ Heer.

(59) ‘ Recherches sur le Climat et la Végétation du Pays Tertiaire.’ Heer.

(60) ‘Fossil Flora of Great Britain.’ Lindley and Hutton.

(61) ‘ Fossil Fruits and Seeds of the London Clay.’ Bowerbank.

(62) ‘Tertiary Leaf-beds of the Isle of Mull” —‘ Quart. Journ. Geol.
Soc.,’ vol. vii. Edward Forbes.

(63) ‘The Geology of England and Wales.’ Horace B. Woodward.*

* This work—published whilst these sheets were going through the press—gives to the
student a detailed view of all the strata of England and Wales, with their various sub-
divisions, from the base of the Paleozoic to the top of the Tertiary.

334 HISTORICAL PALZONTOLOGY.

CHAPTER XX.

THE QUATERNARY, PERIOD |
THE Post-PLIOCENE PERIOD.

Later than any of the Tertiary formations are various de-
tached and more or less superficial accumulations, which are
generally spoken of as the /ost-Tertiary formations, in accord-
ance with the nomenclature of Sir Charles Lyell—or as the
Quaternary formations, in accordance with the general usage
of Continental geologists. In all these formations we meet
with no Mollusca except such as are now alive—with the
partial and very limited exception of some of the oldest de-
posits of this period, in which a few of the shells occasionally
belong to species not known to be in existence at the pre-
sent day. Whilst the Se/7ish of the Quaternary deposits are,
generally speaking, identical with existing forms, the JZammats
are sometimes referable to living, sometimes to extinct species.
In accordance with this, the Quaternary formations are divided
into two groups: (1) The /ost-Piocene, in which the shells are
almost invariably referable to existing species, but some of the
Mammals are extinct; and (2) the Recent, in which the shells
and the Mammals alike belong to existing species. The FPost-
Pliocene deposits are often spoken of as the FVezstocene forma-
tions (Gr. Alezstos, most; ainos, new or recent), in allusion to
the fact that the great majority of the living beings of this
period belong to the species characteristic of the “new” or
Recent period.

The Recent deposits, though of the highest possible interest,
do not properly concern the paleontologist strictly so-called,
but the zoologist, since they contain the remains of none but
existing animals. They are ‘“ Pre-historic,” but they belong
entirely to the existing terrestrial order. The /ost- Phocene
deposits, on the other hand, contain the remains of various
extinct Mammals; and though Man undoubtedly existed in,
at any rate, the later portion of this period, if not through-
out the whole of it, they properly form part of the domain of
the palzontologist.

The Post-Pliocene deposits are extremely varied, and very
widely distributed ; and owing to the mode of their occurrence,
the ordinary geological tests of age are in their case but very
partially available. The subject of the classification of these

THE QUATERNARY PERIOD. 335

deposits is therefore an extremely complicated one ; and as
regards the age of even some of the most important of them,
there still exists considerable difference of opinion. For our
present purpose, it will be convenient to adopt a classifica-
tion of the Post-Pliocene deposits founded on the relations
which they bear in time to the great “ Ice-age”’ or “ Glacial
period ;” though it is not pretended that our present know-
ledge is sufficient to render such a classification more than a
provisional one. 7

In the early Tertiary period, as we have seen, the climate of
the northern hemisphere, as shown by the Eocene animals and
plants, was very much hotter than it is at present—partaking,
indeed, of a sub-tropical character. In the Middle Tertiary or
Miocene period, the temperature, though not so high, was still
much warmer than that now enjoyed by the northern hemi-
sphere ; and we know that the plants of temperate regions at
this time flourished within the Arctic circle. In the later
Tertiary or Pliocene period, again, there is evidence that the
northern hemisphere underwent a further progressive diminu-
tion of temperature ; though the climate of Europe generally
seems at the close of the Tertiary period to have been if any-
thing warmer, or at any rate not colder, than it is at the present
day. With the commencement of the Quaternary period,
however, this diminution of temperature became more de-
cided ; and beginning with a temperate climate, we find the
greater portion of the northern hemisphere to become gradu-
ally subjected to all the rigours of intense Arctic cold. All
the mountainous regions of Northern and Central Europe, of
Britain, and of North America, became the nurseries of huge
ice-streams, and large areas of the land appear to have been
covered with a continuous ice-sheet. The Arctic conditions of
this, the well-known “ Glacial period,” relaxed more than once,
and were more than once re-established with lesser intensity.
Finally, a gradual but steadily progressive amelioration of tem-
perature took place; the ice slowly gave way, and ultimately
disappeared altogether; and the climate once more became
temperate, except in high northern latitudes.

The changes of temperature sketched out above took place
slowly and gradually, and occupied the whole of the Post-
Pliocene period. In each of the three periods marked out by
these changes—in the early temperate, the central cold, and
the later temperate period—certain deposits were laid down
over the surface of the northern hemisphere ; and these de-
posits collectively constitute the Post-Pliocene formations.
Hence we may conveniently classify all the accumulations of

336. HISTORICAL PALEZONTOLOGY.

this age under the heads of (1) Pre-Glacial deposits, (2) Glacial
deposits, and (3) Fost-Glacial deposits, according as they were
formed before, during, or after the “ Glacial period.” It can-
not by any means be asserted that we can definitely fix the
precise relations in time of all the Post-Pliocene deposits to the
Glacial period. On the contrary, there are some which hold a
very disputed position as regards this point; and there are
others which do not admit of definite allocation in this manner
at all, in consequence of their occurrence in regions where no
‘Glacial Period” is known to have been established. For
our present purpose, however, dealing as we shall have to do
principally with the northern hemisphere, the above classifi-
cation, with all its defects, has greater adv ANE than any
other that has been yet proposed.

I, Pre-GuiaciaL Deposits.—The chief pre-glacial deposit of
Britain is found on the Norfolk coast, reposing upon the Newer
Pliocene (Norwich Crag), and consists of an ancient land-sur-
face which is known as the ‘‘ Cromer Forest-bed.”

This consists of an ancient soil, having embedded in it the
stumps of many trees, still in an erect position, with remains
of living plants, and the bones of recent and extinct quadru-
peds. It is overlaid by fresh-water and marine beds, all the
shells of which belong to existing species, and it is finally sur-
mounted by true “glacial drift.” While all the shells and
plants of the Cromer Forest-bed and its associated strata belong
to existing species, the Mammals are partly living, partly ex-
tinct. Thus we find the existing Wolf (Canzs lupus), Red
Deer (Cervus elaphus), Roebuck (Cervus capreolus), Mole
(Zalpa Europea), and Beaver (Castor fiber), living in western
England side by side with the Azppopotamus major, Elephas
antiquus, Elephas meridionalis, Rhinoceros Etruscus, and R.
megarhinus of the Pliocene period, which are not only extinct,
but imply an at any rate moderately warm climate. Besides
the above, the Forest-bed has yielded the remains of several
extinct species of Deer, of the great extinct Beavér (Zvogon-
therium Cuvteri), of the Caledonian Bull or “ Urus” (Bos
primigenius), and of a Horse (Zguus fossilis), little if at all
distinguishable from the existing form.

The so-called ‘ Bridlington Crag” of Yorkshire, and the
“‘Chillesford Beds” of Suffolk, are probably to be regarded as
also belonging to this period; though many of the shells which -
they contain are of an Arctic character, and would indicate
that they were deposited in the commencement of the Glacial
period itself. Owing, however, to the fact that a few of the
shells of these deposits are not known to occur in a living con-

THE QUATERNARY PERIOD. 337

dition, these, and some other similar accumulations, are some-
times considered as referable to the Pliocene period.

IJ. Gracia Deposirs.— Under this head is included a
great series of deposits which are widely spread over both
Europe and America, and which were formed at a time when
the climate of these countries was very much colder than it is
at present, and approached more or less closely to what we see
at the present day in the Arctic regions. These deposits are
known by the general name of the Glacial deposits, or by the
more specialised names of the Drift, the Northern Drift, the
Boulder-clay, the Till, &c.

These glacial deposits are found in Britain as far south as
the Thames, over the whole of Northern Europe, in all the
more elevated portions-:of Southern and Central Europe, and
over the whole of North America, as far south as the 39th
parallel. They generally occur as sands, clays, and gravels,
spread in widely-extended sheets over all the geological forma-
tions alike, except the most recent, and are commonly spoken
of under the general term of “‘ Glacial drift.” They vary much
in their exact nature in different districts, but they universally
consist of one, or all, of the following members :—

1. Unstratified clays, or loams, containing numerous angular
or sub-angular blocks of stone, which have often been trans-
ported for a greater or less distance from their parent rock,
and which often exhibit polished, grooved, or striated surfaces.
These beds are what is called Bowlder-clay, or Till.

2. Sands, gravels, and clays, often more or less regularly
stratified, but containing erratic blocks, often of large size, and
with their edges unworn, derived from considerable distances
from the place where they are now found. In these beds it is
not at all uncommon to find fossil shells; and these, though of
existing species, are generally of an Arctic character, compris-
ing a greater or Jess number of forms which are now exclusively
found in the icy waters of the Arctic seas. ‘These beds are
often spoken of as “ Stratified Drift.”

3. Stratified sands and gravels, in which the pebbles are
worn and rounded, and which have been produced by a re-
arrangement of ordinary glacial beds by the sea. These beds
are commonly known as “ Drift-gravels,” or “ Regenerated
Drift.”

Some of the last-mentioned of these are doubtless post-
glacial ; but, in the absence of fossils, it is often impossible to
arrive at a positive opinion as to the precise age of superficial
accumulations of this nature. It is also the opinion of high
authorities that a considerable number of the so-called ‘‘ cave-

338 HISTORICAL PALZONTOLOGY.

deposits,” with the bones of extinct Mammals, truly belong to
the Glacial period, being formed during warm intervals when
the severity of the Arctic cold had become relaxed. It is
further believed that some, at any rate, of the so-called “ high-
level” river-gravels and “ brick-earths” have likewise been
deposited during mild or warm intervals in the great age of
ice ; and in two or three instances this has apparently been
demonstrated—deposits of this nature, with the bones of ex-
tinct animals and the implements of man, having been shown
to be overlaid by true Boulder-clay.

The fossils of the undoubted Glacial deposits are principally
shells, which are found in great numbers in certain localities,
sometimes with Foramznifera, the bivalved cases of Ostracode
Crustaceans, &c. Whilst some of the shells of the “ Drift”.
are such as now live in the seas of temperate regions, others,
as previously remarked, are such as are now only known to
live in the seas of high latitudes ; and these therefore afford
unquestionable evidence of cold conditions. Amongst these
Arctic forms of shells which characterise the Glacial beds
may be mentioned Pecten Lslandicus (fig. 254), Pecten Gren-

LZ 4; 7

Fig. 254.—Left valve of Pecten Islandicus. Glacial and Recent.

Zandicus, Scalaria Grenlandica, Leda truncata, Astarte borealzts,
Tellina proxima, Natica clausa, &c.

III. Post-Gractat Deposits.—As the intense cold of the
Glacial period became gradually mitigated, and temperate

THE QUATERNARY PERIOD. 339

conditions of climate were once more re-established, various
deposits were formed in the northern hemisphere, which are
found to contain the remains of extinct Mammals, and which,
therefore, are clearly of Post-Plhocene age. To these deposits
the general name of /ost-Glactal formations is given; but it is
obvious that, from the nature of the case, and with our present
limited knowledge, we cannot draw a rigid line of demarcation
between the deposits formed towards the close of the Glacial
period, or during warm “interglacial” periods, and those laid
down after the ice had fairly disappeared. Indeed it is ex-
tremely improbable that any such rigid line of demarcation
should ever have existed ; and it is far more lkely that the
Glacial and Post-Glacial periods, and their corresponding de-
posits, shade into one another by an imperceptible gradation.
Accepting this reservation, we may group together, under the
general head of ‘“ Post-Glacial Deposits,” most of the so-called
“ Valley - gravels,” ‘‘ Brick - earths,” and ‘‘ Cave - deposits,” to-
gether with some ‘“‘raised beaches” and yarious deposits of
peat. Though not strictly within the compass of this work,
a few words may be said here as to the origin and. mode
of formation of the Brick-earths, Valley-gravels, and Cave-
deposits, as the subject will thus be rendered more clearly
intelligible.

Every river produces at the present day beds of fine mud
and loam, and accumulations of gravel, which it deposits at
various parts of its course—the gravel generally occupying the
lowest position, and the finer sands and mud coming above.
Numerous deposits of a similar nature are found in most
countries in various localities, and at various heights above
the present channels of our rivers. Many of these fluviatile
(Lat. 7uvzus, a river) deposits consist of fine loam, worked for
brick-making, and known as “ Brick-earths ;” and they have
yielded the remains of numerous extinct Mammals, of which
the Mammoth (Ziephas primigenius) is the most abundant.
In the valley of the Rhine these fluviatile loams (known as
“ Loess”) attain a thickness of several hundred feet, and con-
tain land and fresh-water shells of existing species. With
these occur the remains of Mammals, such as the Mammoth
and Woolly Rhinoceros. Many of these Brick-earths are
undoubtedly Post-Glacial, but others seem to be clearly ‘‘inter-
glacial ;” and instances have recently been brought forward in
which deposits of Brick-earth containing bones and shells of
fresh-water Molluscs have been found to be overlaid by regu-
lar unstratified boulder-clay.

The so-called “ Valley-gravels,” like the Brick-earths, are

340 HISTORICAL PALZZONTOLOGY.

fluviatile deposits, but are of a coarser nature, consisting of
sands and gravels. Every river gives origin to deposits of
this kind at different points along the course of its valley ;
and it is not uncommon to find that there exist in the valley
of a single river two or more sets of these gravel-beds, formed
by the river itself, but tormed at times when the river ran
at different levels, and therefore formed at different periods.
These different accumulations are known as the “ high-level”
and ‘‘ low-level” gravels; and a reference to the accompany-
ing diagram will explain the origin and nature of these de-
posits (fig. 255). When a river begins to occupy a particular

Fig. 255.—Recent and Post-Pliocene Alluvial Deposits. 1, Peat of the recent period ;
2, Gravel of the modern river; 2’, Loam of the modern river; 3, Lower-level valley-
gravel with bones of extinct Mammals (Post-Pliocene) ; 3’, Loam of the same age as 33
4, Higher-level valley-gravel (Post-Pliocene); 4’, Loam of the same age as 4; 5. Upland
gravels of various kinds (often glacial drift); 6, Older rocks. (After Sir Charles Lyell.)

line of drainage, and to form its own channel, it will deposit
fluviatile sands and gravels along its sides. As it goes on
deepening the bed or valley through which it flows, it will
deposit other fluviatile strata at a lower level beside its new
bed. In this way have arisen the terms “high-level” and
“low-level” gravels. We find, for instance, a modern river
flowing through a valley which it has to a great extent or
entirely formed itself; by the side of its immediate channel
we may find gravels, sand, and loam (fig. 255, 2 2’) deposited
by the river flowing in its present bed. These are recent
fluviatile or alluvial deposits. At some distance from the
present bed of the river, and at a higher level, we may find
other sands and gravels, quite like the recent ones in charac-
ter and origin, but formed at a time when the stream flowed
at a higher level, and before it had excavated its valley to its
present depth. These (fig. 255, 3 3’) are the so-called “‘ low-
level gravels” of a river. At a still higher level, and still
farther removed from the present bed of the river, we may
find another terrace, composed of just the same materials as
the lower one, but formed at a still earlier period, when the

THE QUATERNARY PERIOD. 341

excavation of the valley had proceeded to a much less extent.
These (fig. 255, 4 4’) are the so-called “‘ Aizgh-level gravels”
of a river, and there may be one or more terraces of these.

The important fact to remember about these fluviatile de-
posits is this—that here the ordinary geological rule is reversed.
The high-level gravels are, of course, the highest, so far as
their actual elevation above the sea is concerned ; but geo-
logically the lowest, since they are obviously much older than
the low-level gravels, as these are than the recent gravels.
How much older the high-level gravels may be than the low-
level ones, it is impossible to say. They occur at heights
varying from 10 to 100 feet above the present river-chan
nels, and they are therefore older than the recent gravels
by the time required by the river to dig out its own bed to
this depth. How long this period may be, our data do not
enable us to determine accurately ; but if we are to calculate
from the observed rate of erosion of the actually existing
rivers, the period between the different valley-grayels must
be a very long one.

The lowest or recent fluviatile deposits which occur beside
the bed of the present river, are referable to the Recent period,
as they contain the remains of none but living Mammals.. The
two other sets of gravels are Post-Pliocene, as they contain
the bones of extinct Mammals, mixed with land and fresh-
water shells of existing species. Among the more important
extinct Mammals of the low-level and high-level valley-gravels
may be mentioned the Lvephas antiquus, the Mammoth (£&-
phas primigenius), the Woolly Rhinoceros (RX. ¢ichorhinus), the
Hippopotamus, the Cave-lion, and the Cave-bear. Along
with these are found unquestionable traces of the existence
of Man, in the form of rude flint implements of undoubted
human workmanship.

The so-called ‘“ Cave - deposits,” again, though exhibiting
peculiarities due to the fact of their occurrence in caverns or
fissures in the rocks, are in many respects essentially similar
to the older valley-gravels. Caves, in the great majority of
instances, occur in limestone. When this is not the case, it
will generally be found that they occur along lines of sea-coast,
or along lines which can be shown to have anciently formed
the coast-line. There are many caves, however, in the making
of which it can be shown that the sea has had no hand; and
these are most of the caves of limestone districts. These owe
their origin to the solvent action upon lime of water holding
carbonic acid in solution. The rain which falls upon a lime-
stone district absorbs a certain amount of carbonic acid from

t

342 HISTORICAL PALAZZONTOLOGY.

the air, or from the soil. It then percolates through the rock,
generally along the lines of jointing so characteristic of lime-
stones, and in its progress it dissolves and carries off a certain
quantity of carbonate of lime. In this way, the natural joints
and fissures in the rock are widened, as can be seen at the
present day in any or all limestone districts. By a continu-
ance of this action for a sufficient length of time, caves may
ultimately be produced. Nothing, also, is commoner in a
limestone district than for the natural drainage to take the
line of some fissure, dissolving the rock in its course. In this
way we constantly meet in limestone districts with springs
issuing from the limestone rock—sometimes as large rivers—
the waters of which are charged with carbonate of lime, ob-
tained by the solution of the sides of the fissure through which
the waters have flowed. By these and similar actions, every
district in which limestones are extensively developed will be
found to exhibit a number of natural caves, rents, or fissures.
The first element, therefore, in the production of cave-deposits,
is the existence of a period in which limestone rocks were
largely dissolved, and caves were formed in consequence of
the then existing drainage taking the line of some fissure.
Secondly, there must have been a period in which various
deposits were accumulated in the caves thus formed. ‘These
cavern-deposits are of very various nature, consisting of mud,
loam, gravel, or breccias of different kinds. In all cases, these
materials have been introduced into the cave at some period
subsequent to, or contemporaneous with, the formation of the
cave. Sometimes the cave communicates with the surface by
a fissure through which sand, gravel, &c., may be washed by
rains or by floods from some neighbouring river. Sometimes
the cave has been the bed of an ancient stream, and the de-
posits have been formed as are fluviatile deposits at the surface.
Or, again, the river has formerly flowed at a greater elevation
than it does at present, and the cave has been filled with
fluviatile deposits by the river at a time prior to the excava-
tion of its bed to the present depth (fig. 256). In this last
case, the cave-deposits obviously bear exactly the same rela-
tion in point of antiquity to recent deposits, as do the low-
level and high-level valley-gravels to recent river-gravels. In
any case, it is necessary for the physical geography of the dis-
trict to change to some extent, in order that the cave-deposits
should be preserved. If the materials have been introduced
by a fissure, the cave will probably become ultimately filled
to the roof, and the aperture of admission thus blocked up.
If a river has flowed through the cave, the surface configura-

THE QUATERNARY PERIOD. 343

tion of the district must be altered so far as to divert the river
into a new channel. And if the cave is placed ‘in the side of
a river-valley, as in fig. 256, the river must have excavated

Fig. 256.—Diagrammatic section across a river-valley and cave. aa, Recent valley-
gravels near the channel (4) of the existing river; c, Cavern, partly filled with cave-
earth; dd, High-level gravels, filling fissures in the limestone, which perhaps communi-
cate in some instances with the cave, and form a channel by which materials of various
kinds were introduced into it; e e, Inclined beds of limestone.

its channel to such a depth that it can no longer wash out the
contents of the cave even in high floods.

If the cave be entirely filled, the included deposits generally
get more or less completely cemented together by the percola-
tion through them of water holding carbonate of lime in solu-
tion. If the cave is only partially filled, the dropping of water
from the roof holding lime in solution, and its subsequent
evaporation, would lead to the formation over the deposits
below of a layer of stalagmite, perhaps several inches, or even
feet, in thickness. In this way cave-deposits, with their con-
tained remains, may be hermetically sealed up and preserved
without injury for an altogether indefinite period of time.

In all caves in limestone in which deposits containing bones
are found, we have then evidence of three principal sets of
changes. (1.) A period during which the cave was slowly
hollowed out by the percolation of acidulated water; (2.) A
period in which the cave became the channel of an engulfed
river, or otherwise came to form part of the general drainage-
system of the district; (3.) A period in which the cave was
inhabited by various animals.

As a typical example of a cave with fossiliferous Post-
Pliocene deposits, we may take Kent’s Cavern, near Torquay,
in which a systematic and careful examination has revealed the
following sequence of accumulations in descending order :—

(2) Large blocks of limestone, which lie on the floor of the
cave, having fallen from the roof, and which are sometimes
cemented together by stalagmite.

(4) A layer of black mould, from three to twelve inches
thick, with human bones, fragments of pottery, stone and

344 HISTORICAL PALZONTOLOGY.

bronze implements, and the bones of animals now living in
Britain. This, therefore, is a recent deposit.

(c) A layer of stalagmite, from sixteen to twenty inches
thick, but sometimes as much as five feet, containing the bones
of Man, together with those of extinct Post-Pliocene Mammals.

(7) A bed of red cave-earth, sometimes four feet in thick-
ness, with numerous bones of extinct Mammals (Mammoth,
Cave-bear, &c.), together with human implements of flint and
horn. 7

(ec) A second bed of stalagmite, in places twelve feet in
thickness, with bones of the Cave-bear.

(7) A red-loam and cave-breccia, with remains of the Cave-
bear and human implements.

The most important Mammals which are found in cave-
deposits in Europe generally, are the Cave-bear, the Cave-lion,
the Cave-hyzena, the Reindeer, the Musk-ox, the Glutton, and
the Lemming—of which the first three are probably identical
with existing forms, and the remainder are certainly so—to-
gether with the Mammoth and the Woolly Rhinoceros, which
are undoubtedly extinct. Along with these are found the
implements, and in some cases the bones, of Man himself, in
such a manner as to render it absolutely certain that an early
race of men was truly contemporaneous in Western Europe
with the animals above mentioned.

IV. UnciassiFIED Post-PLIOCENE DEposits.—Apart from
any of the afore-mentioned deposits, there occur other accumu-
lations—sometimes superficial, sometimes in caves—which are
found in regions where a “ Glacial period” has not been fully
demonstrated, or where such did not take place; and which,
therefore, are not amenable to the above classification. The
most important of these are known to occur in South America
and Australia; and though their numerous extinct Mammalia
place their reference to the Post-Pliocene period beyond
doubt, their relations to the glacial period and its deposits in
the northern hemisphere have not been precisely determined.

CEBA PALER xen:
THE POST-PLIOCENE PERIOD—Continued.

As regards the /zfe of the Post-Pliocene period, we have, in
the first place, to notice the effect produced throughout the

FAUNA OF THE POST-PLIOCENE. 345

northern hemisphere by the gradual supervention of the Glacial ©
period. Previous to this the climate must have been temper-
ate or warm-temperate ; but as the cold gradually came on,
two results were produced as regards the living beings of the
area thus affected. In the first place, all those Mammals
which, like the Mammoth, the Woolly Rhinoceros, the Lion,
the Hyzena, and the Hippopotamus, require, at any rate, mode-
rately warm conditions, would be forced to migrate southwards
to regions not affected by the new state of things. In the
second place, Mammals previously inhabiting higher latitudes,
such as the Reindeer, the Musk-ox, and the Lemming, would
be enabled by the increasing cold to migrate southwards, and
to invade provinces previously occupied by the Elephant and
the Rhinoceros. A precisely similar, but more slowly-executed
process, must have taken place in the sea, the northern Mollus-
ca moving southwards as the arctic conditions of the Glacial
period became established, whilst the forms proper to temperate
seas receded. As regards the readily locomotive Mammals,
also, it is probable that this process was, carried on repeatedly
in a partial manner, the southern and northern forms alternately
fluctuating backwards and forwards over the same area, in ac-
cordance with the fluctuations of temperature which have been
shown by Mr James Geikie to have characterised the Glacial
period as a whole. We can thus readily account for the inter-
mixture which is sometimes found of northern and southern types
of Mammalia in the same deposits, or in deposits apparently
synchronous, and within a single district. Lastly, at the final
close of the arctic cold of the Glacial period, and the re-estab-
lishment of temperate conditions over the northern hemisphere,
a reversal of the original process took place—the northern
Mammals retiring within their ancient limits, and the southern
forms pressing northwards and reoccupying their original
domains.

The /xver/ebrate animals of the Post-Pliocene deposits re-
quire no further mention—all the known forms, except a few
of the shells in the lowest beds of the formation, being iden-
tical with species now in existence upon the globe. The only
point of importance in this connection has been previously
noticed—namely, that in the true Glacial deposits themselves
a considerable number of the shells belong to northern or
Arctic types.

As regards the Vertebrate animals of the period, no extinct
forms of Fishes, Amphibians, or Reptiles are known to occur,
but we meet with both extinct Birds and extinct Mammals.
The remains of the former are of great interest, as indicating

346 HISTORICAL PALZONTOLOGY. }
the existence during Post- Pliocene times, at widely remote
points of the southern hemisphere, of various wingless, and for
the most part gigantic, Birds. All the great wingless Birds of
the order Cursores which are known as existing at the pres-
ent day upon the globe, are restricted to regions which are
either wholly or in great part south of the equator. ‘Thus the
true Ostriches are African; the Rheas are South American ;
the Emeus are Australian ; the Cassowaries are confined to
Northern Australia, Papua, and the Indian Archipelago; the
species of Apferyx are natives of New Zealand; and the
Dodo and Solitaire (wingless, though probably not true Cur-
sores), both of which have been exterminated within histori-
cal times, were inhabitants of the islands of Mauritius and
Rodriguez, in the Indian Ocean. In view of these facts, it
is noteworthy that, so far as known, all the Cursorial Birds
of the Post-Pliocene period should have been confined to the
~same hemisphere as that inhabited by the living representatives
of the order. It is still further interesting to notice that the
extinct forms in question are only found in geographical prov-
inces which are now, or have been within historical times, inhab-
ited by similar types. The greater number of the remains of
these have been discovered in New Zealand, where there now
live several species of the curious wingless genus Apferyx ; and
they have been referred by Professor Owen to several generic
groups, of which Dzzornis is the most important (fig. 257).
Fourteen species of Dzzornis have been described by the dis-
tinguished paleeontologist just mentioned, all of them being
large wingless birds of the type of the existing Ostrich, having
enormously powerful hind-limbs adapted for running, but with
the wings wholly rudimentary, and the breast-bone devoid of
the keel or ridge which characterises this bone in all birds
which fly. The largest species is the Dznornis giganteus, one
of the most gigantic of living or fossil birds, the shank (tibia)
measuring a yard in length, and the total height being at least
ten feet. Another species, the Dinornis elephantopus (fig. 257),
though not standing more than about six feet in height, was
of an even more ponderous construction—‘“‘the framework
of the skeleton being the most massive of any in the whole
class of Birds,” whilst “‘ the toe-bones almost rival those of the
Elephant” (Owen). The feet in Dzxornis were furnished with
three toes, and are of interest as presenting us with an un-
doubted Bird big enough to produce the largest of the foot-
prints of the Triassic Sandstones of Connecticut. New Zea-
land has now been so far explored, that it seems questionable
if it can retain in its recesses any living example of Dinornis ;

FAUNA OF THE POST-PLIOCENE. 347

but it is certain that species of this genus were alive during the
human period, and survived up to quite a recent date. Not
only are the bones very numerous in certain localities, but

/ | | Nh
a
CoD

|

|

\

i}
‘

Fig. 257.—Skeleton of Dinornis elephantopus, greatly reduced. Post-Pliocene,
New Zealand. (After Owen.)

they are found in the most recent and superficial deposits, and
they still contain a considerable proportion of animal matter ;
whilst in some instances bones have been found with the
feathers attached, or with the horny skin of the legs still ad-
hering to them. Charred bones have been found in connec-
tior with native “‘ovens;” and the traditions of the Maories
contain circumstantial accounts of gigantic wingless Birds, the
“ Moas,” which were hunted both for their flesh and their
plumage. Upon the whole, therefore, there can be no doubt.

348 HISTORICAL PALZONTOLOGY.

but that the Moas of New Zealand have been exterminated at
quite a recent period—perhaps » within the last century—by the
unrelenting pursuit of Man,—a pursuit which their wingless
condition rendered them unable to evade.

In Madagascar, bones have been discovered of another huge
wingless Bird, which must have been as large as, or larger
than, the Divornis giganteus, and which has been described
under the name of porns maximus. With the bones have
been found eggs measuring from thirteen to fourteen inches in
diameter, and computed to have the capacity of three Ostrich
eggs. Atleast two other smaller species of -£pzornis have been
described by Grandidier and Milne-Edwards as occurring in
Madagascar; and they consider the genus to be so closely allied
to the Dinornzs of New Zealand, as to prove that these regions,
now so remote, were at one time united by land. Unlike New
Zealand, where there 1s the Apteryx, Madagascar is not known
to possess any living wingless Birds ; but in the neighbouring
island of Mauritius the wingless Dodo (Didus ineptus) has been
exterminated less than three hundred years ago ; and the little
island of Rodriguez, in the same geographical province, has in
a similar period lost the equally wingless Solitaire (Pezophaps),
both of these, however, being generally referred to the Rasores.

The JZammatls of the Post-Pliocene period are so numerous,
that in spite of the many points of interest which they present,
only a few of the more important forms can be noticed here,
and that but briefly. The first order that claims our attention
is that of the Marsupials, the headquarters of which at the
present day is the Australian province. In Oolitic times
Europe possessed its small Marsupials, and similar forms
existed in the same area in the Eocene and Miocene periods ;
but if size be any criterion, the culminating point in the history
of the order was attained during the Post-Pliocene period in
Australia. From deposits of
this age there has been disen-
tombed a whole series of re-
mains of extinct, and for the
most part gigantic, examples
of this group of Quadrupeds.
Not to speak of Wombats and
Phalangers, two forms stand
out prominently as represen-

Fig. 258. _ Skullof Diprotedon Australis, ae :
greatly reduced. Post-Pliocene, Australia. tatives of the Post-Plocene

animals of Australia. One of
these is Disrotodon (fig. 258), representing, with many differ-
ences, the well-known modern group of the Kangaroos. In

FAUNA OF THE POST-PLIOCENE. 349

its teeth, Dzfrotodon shows itself to be closely allied to the
living, grass-eating Kangaroos; but the hind-limbs were not
Je) disproportionately long. In size, also, Dzprotodon must
' have many times exceeded the dimensions of the largest of
its living successors, since the skull measures no less than
three feet in length. The other form in question is Zhylacolco
(fig. 259), which is believed by Professor Owen to belong to
the same group as the existing ‘‘ Native Devil” (Dasyurus) of
Van Diemen’s Land, and therefore to have been flesh-eating
and rapacious in its habits, though this view is not accepted
by others. The principal feature in the skull of Thylacoleo is

== NN
S88 W

= ill | ane
Sp ef

y ws

iN
{ << am \\

Fig. 259.—Skull of Tiylacoleo. Post-Pliocene, Australia. Greatly reduced.
(After Flower.)

the presence, on each side of each jaw, of a single huge tooth,
which is greatly compressed, and has a cutting edge. ‘This
tooth is regarded by Owen as corresponding to the great cut-
ting tooth of the jaw of the typical Carnivores, but Professor
Flower considers that 7hy/acoleo is rather related to the Kan-
garoo-rats. The size of the crown of the tooth in question is
not less than two inches and a quarter ; and whether carnivo-
rous or not, it indicates an animal of a size exceeding that of
the largest of existing Lions.

The order of the Zdentates, comprising the existing Sloths,
Ant-eaters, and Armadillos, and entirely restricted at the present
day to South America, Southern Asia, and Africa, is one alike

24.

350 HISTORICAL PALZONTOLOGY.

singular for the limited geographical range of its members,
their curious habits of life, and the well-marked peculiarities
of their anatomical structure. South America is the metropo-
lis of the existing forms ; and it is an interesting fact that there
flourished within Post-Pliocene times in this continent, and to
some extent in North America also, a marvellous group of ex-
tinct Edentates, representing the living Sloths and Armadillos,
but of gigantic size. The most celebrated of these is the huge
Megatherium Cuvieri (fig. 260) of the South American Pampas.

Fig. 260.—Megatherium Cuviert. Post-Pliocene, South America.

The Megathere was a colossal Sloth-like animal which attained
a length of from twelve to eighteen feet, with bones more mas-
sive than those of the Elephant. Thus the thigh-bone is
nearly thrice the thickness of the same bone in the largest
of existing Elephants, its circumference at its narrowest point
nearly equalling its total length; the massive bones of the
shank (tibia and fibula) are amalgamated at their extremities ;
the heel-bone (calcaneum) is nearly half a yard in length; the
haunch-bones (ilia) are from four to five feet across at their
crests ; and the bodies of the vertebre at the root of the tail
are from five to seven inches in diameter, from which it has
been computed that the circumference of the tail at this part
might have been from five to six feet. The length of the fore-
foot is about a yard, and the toes are armed with powerful
curved claws. It is known now that the Megathere, in spite
of its enormous weight and ponderous construction, walked,
like the existing Ant-eaters and Sloths, upon the outside edge
of the fore-feet, with the claws more or less bent inwards

FAUNA OF THE POST-PLIOCENE. 351

towards the palm of the hand. As in the great majority of
the Edentate order, incisor and canine teeth are entirely
wanting, the front of the jaws being toothless. The jaws,
however, are furnished with five upper and four lower molar
teeth on each side. These grinding teeth are from seven to
eight inches in length, in the form of four-sided prisms, the
crowns of which are provided with well-marked transverse
ridges ; and they continue to grow during the whole life of
the animal. There are indications that the snout was pro-
longed, and more or less flexible; and the tongue was proba-
bly prehensile. From the characters of the molar teeth it
is certain that the Megathere was purely herbivorous in its
habits ; and from the enormous size and weight of the body,
it is equally certain that it could not have imitated its modern
allies, the Sloths, in the feat of climbing, back downwards,
amongst the trees. It is clear, therefore, that the Megathere
sought its sustenance upon the ground; and it was originally
supposed to have lived upon roots. By a masterly piece of
deductive reasoning, however, Professor Owen showed that
this great “ Ground-Sloth” must have truly lived upon the
foliage of trees, like the existing Sloths—but with this differ-
ence, that instead of climbing amongst the branches, it actually
uprooted the tree bodily. In this four de force, the animal
sat upon its huge haunches and mighty tail, as on a. tripod,
and then grasping the trunk with its powerful arms, either
wrenched it up by the roots or broke it short off above the
ground. Marvellous as this may seem, it can be shown that
every detail in the skeleton of the Megathere accords with the
supposition that it obtained its food in this way. Similar
habits were followed by the allied AZylodon (fig. 261), another
of the great “‘ Ground-Sloths,” which inhabited South America
during the Post-Pliocene period. In most respects, the AZyl-
don is very like the Megathere; but the crowns of, the molar
teeth- are flat instead of being ridged. The nearly-related
genus MZega/onyx, unlike the Megathere, but like the Mylodon,
extended its range northwards as far as the United States.
Just as the Sloths of the present day were formerly repre-
sented in the same geographical area by the gigantic Megathe-
roids, so the little banded and cuirassed Armadillos of South
America were formerly represented by gigantic species, con-
stituting the genus Glyptodon. The Glyptodons (fig. 262)
differed from the living Armadillos in having no bands in
their armour, so that they must have been unable to roll
themselves up. It is rare at the present day to meet with any
Armadillo over two or three feet in length; but the length of

352 HISTORICAL PALZONTOLOGY.

the Glyptodon clavipes, from the tip of the snout to the end of
the tail, was more than nine feet.
There are no canine or incisor teeth in the G/yftodon, but

Fig. 261.—Skeleton of IZylodox robustus. Post-Pliocene, South America.

there are eight molars on each side of each jaw, and the crowns
of these are fluted and almost trilobed. The head is covered

Fig. 262.—Skeleton of Glyptodon clavifes. Post-Pliocere, South America.

by a helmet of bony plates, and the trunk was defended by an
armour of almost hexagonal bony pieces united by sutures, and

FAUNA OF THE POST-PLIOCENE, 353

exhibiting special patterns of sculpturing in each species. The
tail was also defended by a similar armour, and the vertebree
were mostly fused together so as to form a cylindrical bony
rod. In addition to the above-mentioned forms, a number
of other Edentate animals have been discovered by the re-
searches of M. Lund in the Post-Pliocene deposits of the
Brazilian bone-caves. Amongst these are true Ant-eaters,
Armadillos, and Sloths, many of them of gigantic size, and all
specifically or generically distinct from existing forms.

Passing over the aquatic orders of the Szrenzans and Ce-
taceans, we come next to the great group of the Hoofed Quad-
rupeds, the remains of which are very abundant in Post-
Pliocene deposits both in Europe and North America.
Amongst the Odd-toed Ungulates the most important are
the Rhinoceroses, of which three species are known to have
existed in Europe during the Post-Pliocene period. Two
of these are the well-known Pliocene forms, the AR/Aznoceros
Ltruscus and the R. megarhinus, still surviving in diminished
numbers ; but the most famous is the Rhinoceros tichorhinus
(fig. 263), or so-called ‘‘ Woolly Rhinoceros.” This species

Fig. 263.—Skull of the Tichorhine Rhinoceros, the horns being wanting. One-tenth

of the natural size. Post-Pliocene deposits of Europe and Asia.

is known not only by innumerable bones, but also by a car-
cass, at the time of its discovery complete, which was found
embedded in the frozen soil of Siberia towards the close of
last century, and which was partly saved from destruction by
the exertions of the naturalist Pallas. From this, we know
that the Tichorhine Rhinoceros, like its associate the Mam-
moth, was provided with a coating of hair, and therefore was
enabled to endure a more severe climate than any existing

354 HISTORICAL PALZONTOLOGY.

species. The skin was not thrown into the folds which char-
acterise most of the existing forms; and the technical name
of the species refers to the fact that the nostrils were com-
pletely separated by a bony partition. The head carried two
horns, placed one behind the other, the front one being un-
usually large. As regards its geographical range, the Woolly
Rhinoceros is found in Europe in vast numbers north of the
Alps and Pyrenees, and it also abounded in Siberia; so that
it would appear to be a distinctly northern form, and to have
been adapted for a temperate climate. It is not known to
occur in Phocene deposits, but it makes its first appearance
in the Pre-Glacial deposits, surviving the Glacial period, and
being found in abundance in Post-Glacial accumulations. It
was undoubtedly a contemporary of the earlier races of men
in Western Europe ; and it may perhaps be regarded as being
the actual substantial kernel of some of the “ Dragons” of
fable.

The only other Odd-toed Ungulate which needs notice is
the so-called Lguwus fossilis of the Post-Pliocene of Europe.
This made its appearance before the Glacial period, and ap-
pears to be in reality identical with the existing Horse (Zguus
caballus) True Horses also occur in the Post-Pliocene of
North America; but, from some cause or another, they must
have been exterminated before historic times.

Amongst the Even-toed Ungulates, the great /Yippopotamus
major of the Pliocene still continued to exist in Post-Pliocene
times in Western Europe; and the existing Wild Boar (Sus
scrofa), the parent of our domestic breeds of Pigs, appeared
for the first time. The Old World possessed extinct repre-
sentatives of its existing Camels, and lost types of the living
Llamas inhabited South America. Amongst the Deer, the
Post-Pliocene accumulations have yielded the remains of
various living species, such as the Red Deer (Cervus elaphus),
the Reindeer (Cervus tarandus), the Moose or Elk (Alces
malchis), and the Roebuck (Cervus capreolus), together with
a number of extinct forms. Among the latter, the great
“Trish Elk” (Cervus megaceros) is justly celebrated both for
its size and for the number and excellent preservation of its
discovered remains. This extinct species (fig. 264) has been
found principally in peat- mosses and Post-Pliocene lake-
deposits, and is remarkable for the enormous size of the
spreading antlers, which are widened out towards their ex-
tremities, and attain an expanse of over ten feet from tip to
tip. It is not a genuine Elk, but is intermediate between
the Reindeer and the Fallow-deer. Among the existing Deer

FAUNA OF THE POST-PLIOCENE. 355

of the Post-Pliocene, the most noticeable is the Reindeer,
an essentially northern type, existing at the present day in

Fig. 264.—Skeleton of the “‘ Irish Elk” (Cervus megaceros).
Post-Pliocene, Britain.

Northern Europe, and also (under the name of the ‘ Caribou”)
in North America. When the cold of the Glacial period be-
came established, this boreal species was enabled to invade
Central and Western Europe in great herds, and its remains
are found abundantly in cave-earths and other Post-Pliocene
deposits as far south as the Pyrenees.

In addition to the above, the Post-Pliocene deposits of
Europe and North America have yielded the remains of vari-
ous Sheep and Oxen. One of the most interesting of the

350 HISTORICAL PALAZAONTOLOGY.

latter is the “ Urus” or Wild Bull (Gos primigenius, fig. 265),
which, though much larger than any of the existing forms, is

Fig. 265.—Skull of the Urus (Bos primigenius). Post-Pliocene and Recent.
ter Owen.)

believed to be specifically undistinguishable from the domes-
tic Ox (Bos taurus), and to be possibly the ancestor of some
of the larger European varieties of oxen. In the earlier part
of its existence the Urus ranged over Europe and Britain in
company with the Woolly Rhinoceros and the Mammoth; but
it long survived these, and does not appear to have been
finally exterminated till about the twelfth century. Another
- remarkable member of the Post-Pliocene Cattle, also to be-
gin with an associate of the Mammoth and Rhinoceros, is
the European Bison or ‘ Aurochs” (zson priscus). This
‘““maned” ox formerly abounded in Europe in Post-Glacial
times, and was not rare even in the later periods of the
Roman empire, though ‘nuch diminished in numbers, and
driven back into the wilder and more inaccessible parts of the
country. At present this fine species has been so nearly
exterminated that it no longer exists in Europe save in
Lithuania, where its preservation has been secured by ngid
protective laws. Lastly, the Post- Pliocene deposits have
yielded the remains of the singular living animal which is
known as the Musk-ox or Musk-sheep (Ovzbos moschatus).
At the present day, the Musk-ox is an inhabitant of the
“ barren grounds” of Arctic America, and it is remarkable for
the great length of its hair. It is, like the Reindeer, a dis-

FAUNA OF THE POST-PLIOCENE. 357

tinctively northern animal ; but it enjoyed during the Glacial
period a much wider range than it has at the present day, the
conditions suitable for its existence being then extended over
a considerable portion of the northern hemisphere. Thus
remains of the Musk-Ox are found in greater or less abun-
dance in Post-Pliocene deposits over a great part of Europe,
extending even to the south of France; and closely - related
forms are found in similar deposits in the United States.
Coming to the Proboscideans, we find that the Aastodons
seem to have disappeared. in Europe at the close of the
Pliocene period, or at the very commencement of the Post-
Pliocene. In the New World, on the other hand, a species of
Mastodon (JZ, Americanus or M. Ofioticus) is found abun-
dantly in deposits of Post-Pliocene age, from Canada to
Texas. Very perfect skeletons of this species have been
exhumed from morasses and swamps, and large individuals
attained a length (exclusive of the tusks) of seventeen feet and
a height of eleven feet, the tusks being twelve feet in length.
Remains of £/efhants are also abundant in the Post-Phocene
deposits of both the Old and the New World. Amongst these,
we find in Europe the two familiar Pliocene species Z. meri-
dionalis and £. antiguus still surviving, but in diminished
numbers. With these are found in vast abundance the re-
mains of the characteristic Elephant of the Post-Pliocene, the
well-known “ Mammoth” (Ziephas primigentus), which is ac-
companied in North America by the nearly-allied, but more
southern species, the Llephas Amertcanus. The Mammoth (fig.
266) is considerably larger than the largest of the living Ele-
phants, the skeleton being over sixteen feet in length, exclusive
of the tusks, and over nine feet in height. The tusks are bent
almost into a circle, and are sometimes twelve feet in length,
measured along their curvature. In the frozen soil of Siberia
several carcasses of the Mammoth have been discovered with
the flesh and skin still attached to the bones, the most cele-
brated of these being a Mammoth which was discovered at the
beginning of this century at the mouth of the Lena, on the borders
of the Frozen Sea, and the skeleton of which is now preserved
at St Petersburg (fig. 266). From the occurrence of the remains
of the Mammoth in vast numbers in Siberia, it might have been
safely inferred that this ancient Elephant was able to endure a far
more rigorous climate than its existing congeners. This infer-
ence has, however, been rendered a certainty by the specimens
just referred to, which show that the Mammoth was protected
against the cold by a thick coat of reddish-brown wool, some
nine or ten inches long, interspersed with strong, coarse black

358 HISTORICAL PALAZONTOLOGY.

hair more than a foot in length. The teeth of the Mammoth
(fig. 267) are of the type of those of the existing Indian Ele-
phant, and are found in immense numbers in certain localities.

ions of the integument still adhere
Post-Pliocene.

2S).

minus), Port
s still attached to the feet.

7M

(Elephas prim

to the head, and the thick skin of the soles i

Fig. 266.—Skeleton of the Mammoth

The Mammoth was essentially northern in its distribution,
never passing south of a line drawn through the Pyrenees, the
Alps, the northern shores of the Caspian, Lake Baikal, Kam-

FAUNA OF THE POST-PLIOCENE. 359

schatka, and the Stanovi Mountains (Dawkins). It occurs in
the Pre-Glacial forest-bed of Cromer in Norfolk, survived the

Fig. 267.—Molar tooth of the Mammoth (Zleshas primigenius), upper jaw, right side;
one-third of the natural size. a, Grinding surface; 4, Side view. Post-Pliocene.

Glacial period, and is found abundantly in Post-Glacial de-
posits in France, Germany, Britain, Russia in Europe, Asia,
and North America, being often associated with the Reindeer,
Lemming, and Musk-ox. That it survived into the earlier
portion of the human period is unquestionable, its remains
having been found in a great number of instances associated
with implements of human manufacture ; whilst in one instance
a recognisable portrait of it has been discovered, carved on
bone.

Amongst other Elephants which occur in Post-Pliocene de-
posits may be mentioned, as of special interest, the pigmy
Elephants of Malta. One of these—the Elephas Melitensis, or
so-called ‘‘ Donkey-Elephant””—was not more than four and
a half feet in height. The other—the Livphas Falconert, of
Busk—was still smaller, its average height at the withers not
exceeding two and a half to three feet.

Whilst herbivorous animals abounded during the Post-
Pliocene, we have ample evidence of the coexistence with
them of a number of Carnivorous forms, both in the New and
the Old World. The Bears are represented in Europe by at
least three species, two of which—namely, the great Grizzly
Bear (Ursus ferox) and the smaller Brown Bear (Ursus arctos)
—are in existence at the present day. ‘The third speciesis the

360 HISTORICAL PALEONTOLOGY.

celebrated Cave-bear (Ursus speleus, fig. 268), which is now
extinct. The Cave-bear exceeded in its dimensions the largest

of modern Bears; and its remains, as its name implies, have
been found mainly in cavern-deposits. Enormous numbers of
this large and ferocious species must have lived in Europe in
Post-Glacial times; and that they survived into the human
period, is clearly shown by the common association of their
bones with the implements of man. They are occasionally
accompanied by the remains of a Glutton (the Gulo speleus),
which does not appear to be really separable from the existing
Wolverine or Glutton of northern regions (the Guo luscus).
In addition, we meet with the bones of the Wolf, Fox, Weasel,
Otter, Badger, Wild Cat, Panther, Hyzna, and Lion, &c.,
together with the extinct J/achairodus or ‘‘ Sabre - toothed
Tiger.” The only two of these that deserve further mention
are the Hyzna and the Lion. The Cave-hyzena (Hyena
spelea, fig. 269) is regarded by high authorities as nothing
more than a variety of the living Spotted Hyzena (& crocuta)
of South Africa. This well-known species inhabited Britain
and a considerable portion of Europe during a large part of
the Post-Pliocene period ; and its remains often occur in great
abundance. Indeed, some caves, such as the Kirkdale Cavern
in Yorkshire, were dens inhabited during long periods by these
animals, and thus contain the remains of numerous individuals
and of successive generations of Hyznas, together with in-
numerable gnawed and bitten bones of their prey. That the
Cave-hyzena was a contemporary with Man in Western Europe
during Post-Glacial times is shown beyond a doubt by the
common association of its bones with human implements.

FAUNA OF THE POST-PLIOCENE. 361

Lastly, the so-called Cave-lion (Féis spelea), long supposed
to be a distinct species, has been shown to be nothing more

Fig. 269.—Skull of Hyena spelea, one-fourth of the natural size.
Post-Phocene, Europe.

than a large variety of the existing Lion (Fes “o). This
animal inhabited Britain and Western Europe in times pos-
terior to the Glacial period, and was a contemporary of the
Cave-hyzena, Cave-bear, Woolly Rhinoceros, and Mammoth.
The Cave-lion also unquestionably survived into the earlier
portion of the human period in Europe.

The Post-Pliocene deposits of Europe have further yielded
the remains of numerous Aodents—such as the Beaver, the
Northern Lemming, Marmots, Mice, Voles, Rabbits, &c.—to-
gether with the gigantic extinct Beaver known as the Z7vogon-
thertum Cuviert (fig. 270). The great Castoroides Ohioensts of
the Post-Pliocene of North
America is also a great ex-
tinct Beaver, which reached
a length of about five feet.
Lastly, the Brazilian bone-
caves have yielded the re-
mains of numerous Rodents
of types now characteristic
of South America, such as
Guintea-pigs, Capybaras, tree- Fig, aro Tomer jaw of, other
inhabiting Porcupines, and Pliocene, Britain.

Coypus.

The deposits just alluded to have further yielded the
remains of various Monkeys, such as Howling Monkeys,
Squirrel Monkeys, and Marmosets, all of which belong to the
group of Quadrumana which is now exclusively confined to

362 HISTORICAL PALHONTOLOGY.

the South American continent — namely, the “ Platyrhine”
Monkeys.

We still have very briefly to consider the occurrence of
Man in Post-Pliocene deposits ; but before doing so, it will be
well to draw attention to the evidence afforded by the Post-
Pliocene Mammals as to the climate of Western Europe at
this period. The chief point which we have to notice is, that
a considerable revolution of opinion has taken place on this
point. It was originally believed that the presence of such
animals as Elephants, Lions, the Rhinoceros, and the Hippo-
potamus afforded an irrefragable proof that the climate of
Hurope must have been a warm one, at any rate during Post-
Glacial times. The existence, also, of numbers of Mammoths
in Siberia, was further supposed to indicate that this high tem-
perature extended itself very far north. Upon the whole, how-
ever, the evidence is against this view. Not only is there great
difficulty in supposing that the Arctic conditions of the Glacial
period were immediately followed by anything warmer than a
cold-temperate climate; but there is nothing in the nature of
the Mammals themselves which would absolutely forbid their
living ina temperate climate. The Wzppopotamus major, though
probably clad in hair, offers some difficulty—since, as pointed
out by Professor Busk, it must have required a climate suffi-
ciently warm to insure that the rivers were not frozen over in the
winter; but it was probably a migratory animal, and its occur-
rence may be accounted for by this. The Woolly Rhinoceros
and the Mammoth are known with certainty to have been pro-
tected with a thick covering of wool and hair; and their ex-
tension northwards need not necessarily have been limited by
anything except the absence of a sufficiently luxuriant vege-
tation to afford them food. The great American Mastodon,
though not certainly known to have possessed a hairy covering,
has been shown to have lived upon the shoots of Spruce and
Firs, trees characteristic of temperate regions—as shown by the
undigested food which has been found with its skeleton, oc-
cupying the place of the stomach. The Lions and-~Hyznas,
again, as shown by Professor Boyd Dawkins, do not indicate
necessarily a warm climate. Wherever a sufficiency of her- |
bivorous animals to supply them with food can live, there they
can live also; and they have therefore no special bearing upon
the question of climate. After a review of the whole evidence,
Professor Dawkins concludes that the nearest approach at the
present day to the Post-Pliocene climate of Western Europe
is to be found.in the climate of the great Siberian plains which
stretch from the Altai Mountains to the Frozen Sea. “Covered

FAUNA OF THE POST-PLIOCENE. 363

by impenetrable forests, for the most part of Birch, Poplar,
Larch, and Pines, and low creeping dwarf Cedars, they present
every gradation in climate from the temperate to that in which
the cold is too severe to admit of the growth of trees, which
decrease in size as the traveller advances northwards, and are
replaced by the grey mosses and lichens that cover the low
marshy ‘tundras.’ The maximum winter cold, registered by
Admiral Von Wrangel at Nishne Kolymsk, on the banks of
the Kolyma, is—65° in January. ‘Then breathing becomes
difficult ; the Reindeer, that citizen of the Polar region, with-
draws to the deepest thicket of the forest, and stands there
motionless as if deprived of life ;? and trees burst asunder with
the cold. Throughout this area roam Elks, Black Bears,
Foxes, Sables, and Wolves, that afford subsistence to the
Jakutian and Tungusian fur-hunters. In the northern part
countless herds of Reindeer, Elks, Foxes, and Wolverines
make up for the poverty of vegetation by the rich abundance
of animal life. ‘Enormous flights of Swans, Geese, and Ducks
arrive in the spring, and seek deserts where they may moult
and build their nests in safety. Ptarmigans run in troops
amongst the bushes; little Snipes are busy along the brooks
and in the morasses ; the social Crows seek the neighbourhood
of new habitations; and when the sun shines in spring, one
may even sometimes hear the cheerful note of the Finch, and
in autumn that of the Thrush.’ Throughout this region of
woods, a hardy, middle-sized breed of horses lives under the
mastership and care of man, and is eminently adapted to bear
the severity of the climate. . . . The only limit to their
northern range is the difficulty of obtaining food. The severity
of the winter through the southern portion of this vast wooded
area is almost compensated for by the summer heat and its
marvellous effect on vegetation.”—(Dawkins, ‘ Monograph of
Pleistocene Mammalia.’)

Finally, a few words must be said as to the occurrence of the
remains of Man in Post-Pliocene deposits. That Man existed
in Western Europe and in Britain during the Post-Pliocene
period, is placed beyond a doubt by the occurrence of his bones
in deposits of this age, along with the much more frequent
occurrence of implements of human manufacture. At what
precise point of time during the Post-Pliocene period he first
made his appearance is still a matter of conjecture. Recent
researches would render it probable that the early inhabitants
of Britain and Western Europe were witnesses of the stupend-
ous phenomena of the Glacial period ; but this cannot be said
to have been demonstrated. That Man existed in these

364 HISTORICAL PALAZONTOLOGY.

regions during the Post-Glacial division of Post-Pliocene time
cannct be doubted fora moment. As to the physical peculi-
arities of the ancient races that lived with the Mammoth and
the Woolly Rhinoceros, little is known compared with what
we may some day hope to know. Such information as we
have, however, based principally on the skulls of the Engis,
Neanderthal, Cro-Magnon, and Bruniquel caverns, would lead
to the conclusion that Post-Plocene Man was in no respect
inferior in his organisation to, or less highly developed than,
many existing races. All the known skulls of this period, with
the single exception of the Neanderthal cranium, are in all
respects average and normal in their characters ; and even the
- Neanderthal skull possessed a cubic capacity at least equal to
that of some existing races. The implements of Post-Pliocene
Man are exclusively of stone or bone; and the former are
invariably of rude shape and wndressed. These “ paleeolithic”
tools (Gr. palaios, ancient ; “thos, stone) point to a very early
condition of the arts; since the men of the earlier portion
of the Recent period, though likewise unacquainted with the
metals, were in the habit of polishing or dressing the stone
implements which they fabricated.

It is impossible here to enter further into this subject; and
it would be useless to do so without entering as well into a
consideration of the human remains of the Recent period—a
period which lies outside the province of the present work. So
far as Post-Pliocene Man is concerned, the chief points which
the palzontological student has to remember have been else-
where summarised by the author as follows :—

1. Man unquestionably existed during the later portion of
what Sir Charles Lyell has termed the “ Post-Pliocene” period.
In other words, Man’s existence dates back to a time when
several remarkable Mammals, previously mentioned, had not
yet become extinct; but he does not date back to a time
anterior to the present J/o//uscan fauna.

2. The antiquity of the so-called Post-Pliocene period is
a matter which must be mainly settled by the evidence of
Geology proper, and need not be discussed here.

3. The extinct Mammals with which man coexisted in
Western Europe are mostly of large size, the most important
being the Mammoth (Zivephas primigenius), the Woolly Rhino-
ceros (RAznoceros tichorhinus), the Cave-lion (Fels spelea), the
Cave-hyzena (Hyena spelea), and the Cave-bear ( Ursus speleus).
We do not know the causes which led to the extinction of
these Mammals; but we know that hardly any Mammalian
species has become extinct during the historical period.

FAUNA OF THE POST-PLIOCENE. 365

4. The extinct Mammals with which man coexisted are re-
ferable in many cases to species which presumably required a
very different climate to that now prevailing in Western Europe.
How long a period, however, has been consumed in the bring-
ing about of the climatic changes thus indicated, we have no
means of calculating with any approach to accuracy.

5. Some of the deposits in which the remains of man have
been found associated with the bones of extinct Mammals, are
such as to show incontestably that great changes in the phy-
sical geography and surface-configuration of Western Europe
have taken place since the period of their accumulation. We
have, however, no means at present of judging of the lapse of
time thus indicated except by analogies and comparisons which
may be disputed.

6. The human implements which are associated with the
remains of extinct Mammals, themselves bear evidence of an
exceedingly barbarous condition of the human species. Post-
Pliocene or “‘ Palzolithic” Man was clearly unacquainted with
the use of any of the metals. Not only so, but the workman-
ship of these ancient races was much inferior to that of the
later tribes, who were also ignorant of the metals, and who
also used nothing but weapons and tools of stone, bone, &c.

7. Lastly, it is only with the human remains of the Post-
Pliocene period that the palzontologist proper has to deal.
When we enter the “‘ Recent” period, in which the remains of
Man are associated with those of exzsting species of Mammals,
we pass out of the region of pure paleontology into the do-
main of the Archeologist and the Ethnologist.

LITERATURE.

The following are some of the principal works and memoirs to which
the student may refer for information as to the Post-Pliocene deposits and
the remains which they contain, as well as to the primitive races of man-
kind :—

(1) ‘Elements of Geology.’ Lyell.

(2) ‘ Antiquity of Man.’ Lyell.

(3) ‘ Palzontological Memoirs.’ Falconer.

(4) ‘ The Great Ice-age.’ James Geikie.

(5) ‘ Manual of Palzontology.’ Owen.

(6) ‘ British Fossil Mammals and Birds.’ Owen.

(7) ‘Cave-Hunting.’ Boyd Dawkins.

(8) ‘ Prehistoric Times.’ Lubbock.

(9) ‘ Ancient Stone Implements.’ Evans.

(10) ‘ Prehistoric Man.’ Daniel Wilson.
(11) ‘Prehistoric Races of the United States.’ Foster,
(12) ‘ Manual of Geology.’ Dana.

25

HISTORICAL PALONTOLOGY.

‘Monograph of Pleistocene Mammalia’ (Paleontographical So-
ciety). Boyd Dawkins and Sanford.

‘Monograph of the Post-Tertiary Entomostraca of Scotland, &c.,
with an Introduction on the Post-Tertiary Deposits of Scotland’
(Ibid.) G. S. Brady, H. W. Crosskey, and D. Robertson.

** Reports on Kent's Cavern” —‘ British Association Reports.’
Pengelly.

** Reports on the Victoria Cavern, Settle’’—‘ British Association
Reports.’ Tiddeman.

‘Ossemens Fossiles.’? Cuvier.

*Religuize Diluvianee.’ Buckland.

‘Fossil Mammalia”—‘ Zoology of the Voyage of the Beagle.’
Owen.

‘Description of the Tooth and Part of the Skeleton of the Giyp-
todon.’ Owen.

** Memoir on the Extinct Sloth Tribe of North America ”—‘ Smith-
sonian Contributions to Knowledge.’ Leidy.

‘** Report on Extinct Mammals of Australia ’’—‘ British Association,’
1844. Owen.

‘ Description of the Skeleton of an Extinct Gigantic Sloth (AZylodon
robustus).’ Owen.

“* Affinities and Probable Habits of Thylacoleo””—‘ Quart. Journ.
Geol. Soc.,’ vol. xxiv. Flower.

‘ Prodromus of the Paleontology of Victoria.’ M ‘Coy.

‘Les Ossemens Fossiles des Cavernes de Liege.’ Schmerling.

‘Die Fauna der Pfahlbauten in der Schweiz.’ Riitimeyer.

‘* Extinct and Existing Bovine Animals of Scandinavia ”—‘ Annals
of Natural History,’ ser. 2, vol. iv., 1849. Nilsson.

‘Man’s Place in Nature.’ Huxley.

‘Les Temps Antéhistoriques en Belgique.’ Dupont.

“Classification of the Pleistocene Strata of Britain and the Conti-
nent ”—‘ Quart. Journ. Geol. Soc.,’ vol. xxviii. Boyd Dawkins.

‘Distribution of the Post- Glacial Mammalia’ (Ibid.), vol. xxv.
Boyd Dawkins. ;

‘On British Fossil Oxen’ (Ibid.), vols. xxii. and xxiii. Boyd
Dawkins.

‘British Prehistoric Mammals’ (Congress of Prehistoric Archz-
ology, 1868). Boyd Dawkins.

*Reliquize Aquitanice.’ Lartet and Christy.

‘Zoologie et Paléontologie Frangaises.’ Gervais.

‘ Notes on the Post-Pliocene Geology of Canada.’ Dawson.

“© On the Connection between the existing Fauna and Flora ot Great
Britain and certain Geological Changes” —‘ Mem. Geol. Survey.’
Edward Forbes.

‘Cavern-Researches.’ M‘Enery. Edited by Vivian.

*‘Quaternary Gravels”—‘ Quart. Journ. Geol. Soc.,’ vol. xxv.
Tylor.

SUCCESSION OF LIFE UPON THE GLOBE. 367

GERAD E Rey XOXETT.
tip SUCCESSION OF LIFE UPON THE GLOBE.

In conclusion, it may not be out of place if we attempt to
summarise, in the briefest possible manner, some of the prin-
cipal results which may be deduced as to the succession of
life upon the earth from the facts which have in the preceding
portion of this work been passed in review. That there was
a time when the earth was void of life is universally admitted,
though it may be that the geological record gives us no direct
evidence of this. That the globe of to-day is peopled with
innumerable forms of life whose term of existence has been,
for the most part, but as it were of yesterday, is likewise an
assertion beyond dispute. Can we in any way connect the
present with the remote past, and can we indicate even im-
perfectly the conditions and laws under which the existing
order was brought about? ‘The long series of fossiliferous
deposits, with their almost countless organic remains, is the
link between what has been and what is; and if any answer
to the above question can be arrived at, it will be by the
careful and conscientious study of the facts of Paleontology.
In the present state of our knowledge, it may be safely said
that anything like a dogmatic or positive opinion as to the
precise sequence of living forms upon the globe, and still
more as to the manner in which this sequence may have been
brought about, is incapable of scientific proof. There are,
however, certain general deductions from the known facts
which may be regarded as certainly established.

In the first place, it is certain that there has been a succession
of life upon the earth, different specific and generic types suc-
_ ceeding one another in successive periods. It follows from
this, that the animals and plants with which we are familiar as
living, were not always upon the earth, but that they have been
preceded by numerous races more or less differing from them.
What is true of the species of animals and plants, is true also
of the higher zoological divisions; and it is, in the second
place, quite certain that there has been a similar succession in
the order of appearance of the primary groups (“ sub-king-
doms,” “classes,” &c.) of animals and vegetables. These
great groups did not all come into existence at once, but they
made their appearance successively. It is true that we can-
not be said to be certainly acquainted with the first absolute

365." HISTORICAL PALZONTOLOGY.

appearance of any great group of animals. No one dare
assert positively that the apparent first appearance of Fishes
in the Upper Silurian is really their first introduction upon the
earth: indeed, there is a strong probability against any such
supposition. To whatever extent, however, future discoveries
may push back the first advent of any or of all of the great
groups of life, there is no likelihood that anything will be found
out which will materially alter the ve/atzve succession of these
groups as at present known to us. It is not likely, for
example, that the future has in store for us any discovery by
which it would be shown that Fishes were in existence before
Molluscs, or that Mammals made their appearance before
Fishes. The sub-kingdoms of Invertebrate animals were all
represented in Cambrian times—and it might therefore be in-
ferred that ¢hese had all come simultaneously into existence;
but it is clear that this inference, though incapable of actual
disproof, is in the last degree improbable. Anterior to the
Cambrian is the great series of the Laurentian, which, owing
to the metamorphism to which it has been subjected, has so
far yielded but the singular Hozoon. We may be certain,
however, that others of the Invertebrate sub-kingdoms besides
the Protozoa were in existence in the Laurentian period ; and
we may infer from known analogies that they appeared suc-
cessively, and not simultaneously.

When we come to smaller divisions than the sub-king-
doms—such as classes, orders, and families—a similar suc-
cession of groups is observable. The different classes of
any given sub-kingdom, or the different orders of any given
class, do not make their appearance together and all at once,
but they are introduced upon the earth in swccesston. More
than this, the different classes of a sub-kingdom, or the differ-
ent orders of a class, zz the main succeed one another in the
relative order of their zoological rank—the lower groups appear-
ing first and the higher groups dast. It is true that in the
Cambrian formation—the earliest series of sediments in which
fossils are abundant—we find numerous groups, some very
low, others very high, in the zoological scale, which appear
to have simultaneously flashed into existence. For reasons
stated above, however, we cannot accept this appearance as
real; and we must believe that many of the Cambrian groups
of animals really came into being long before the commence-
ment of the Cambrian period. At any rate, in the long series
of fossiliferous deposits of later date than the Cambrian the
above-stated rule holds good as a broad generalisation—that
the lower groups, namely, precede the higher in point of time;

SUCCESSION OF LIFE UPON THE GLOBE. 369

and though there are apparent exceptions to the rule, there
are none of such a nature as not to admit of explanation.
Some of the leading facts upon which this generalisation is
founded will be enumerated immediately ; but it will be well,
in the first place, to consider briefly what we precisely mean
when we speak of “‘ higher” and “lower” groups.

It is well known that naturalists are in the habit of “ clas-
sifying” the innumerable animals which now exist upon the
globe ; or, in other words, of systematically arranging them into
groups. ‘The precise arrangement adopted by one naturalist
may differ in minor details from that adopted by another; but
all are agreed as to the fundamental points of classification,
and all, therefore, agree in placing certain groups in a certain
sequence. What, then, is the principle upon which this
sequence is based? Why, for example, are the Sponges placed
below the Corals; these below the Sea-urchins; and these, again,
below the Shell-fish? Without entering into a discussion of
the principles of zoological classification, which would here be
out of place, it must be sufficient to say that the sequence in
question is based upon the relative type of organisation of the
groups of animals classified. The Corals are placed above the
Sponges upon the ground that, regarded as a whole, the Alex
or type of structure of a Corai is more complex than that of a
Sponge. It is not in the slightest degree that the Sponge is in
any respect less highly organised or less perfect, as a Sponge,
than is the Coral as a Coral. Each is equally perfect in its
own way; but the structural pattern of the Coral is the highest,
and therefore it occupies a higher place in the zoological scale.
It is upon this principle, then, that the primary subdivisions
of the animal kingdom (the so-called “sub-kingdoms”) are
arranged in a certain order. Coming, again, to the minor -
subdivisions (classes, orders, &c.) of each sub-kingdom, we
find a different but entirely analogous principle employed as a
means of classification. The numerous animals belonging to
any given sub-kingdom are formed upon the same fundamental
plan of structure; but they nevertheless admit of being ar-
ranged in a regular series of groups. All the Shell-fish, for
example, are built upon a common plan, this plan representing
the ideal Mollusc; but there are at the same time various
groups of the AZo/lusca, and these groups admit of an arrange-
ment in a given sequence. The principle adopted in this case -
is simply of the relative elaboration of the common type. The
Oyster is built upon the same ground-plan as the Cuttle-fish; but
this plan is carried out with much greater elaboration, and with
many more complexities, in the latter than in the former: and

370 HISTORICAL PALAZONTOLOGY.

in accordance with this, the Cephalopoda constitute a higher
group than the Bivalve Shell-fish. As in the case of superiority
of structural type, so in this case also, it is not in the least that
the Oyster is an zmperfect animal. On the contrary, it is just
as perfectly adapted by its organisation to fill its own sphere
and to meet the exigencies of its own existence as is the
Cuttle-fish ; but the latter lives a life which is, physiologically,
higher than the former, and its organisation is correspondingly
increased in complexity.

This being understood, it may be repeated that, in the
main, the succession of life upon the globe in point of “me
has corresponded with the relative order of succession of the
great groups of animals in zoological rank ; and some of the
more striking examples of this may be here alluded to.
Amongst the £chinoderms, for instance, the two orders gen-
erally admitted to be the “lowest” in the zoological scale—
namely, the Crzzozds and the Cystozds—are likewise the oldest,
both appearing in the Cambrian, the former slowly dying out
as we approach the Recent period, and the latter disappearing
wholly before the close of the Paleozoic period. Amongst the
Crustaceans, the ancient groups of the Trilobites, Ostracodes,
Phyllopods, Eurypterids, and Limuloids, some of which exist
at the present day, are all “low” types; whereas the highly-
organised Decapods do not make their appearance till near the
close of the Palzeozoic epoch, and they do not become abun-
dant till we reach Mesozoic times. Amongst the A/o/usca,
those Bivalves which possess breathing-tubes (the ‘“ siphonate
Bivalves) are generally admitted to be higher than those which
are destitute of these organs (the ‘‘asiphonate” Bivalves) ; and
the latter are especially characteristic of the Paleozoic period,
whilst the former abound in Mesozoic and Kainozoic forma-
tions. Similarly, the Univalves with breathing-tubes and a
corresponding notch in the mouth of the shell (‘‘ siphonosto-
matous” Univalves) are regarded as higher in the scale than
the round-mouthed vegetable-eating Sea-snails, in which no
respiratory siphons exist (‘‘holostomatous” Univalves) ; but
the latter abound in the Palzeozoic rocks—whereas the former
do not make their appearance till the Jurassic period, and
their higher groups do not seem to have existed till the close
of the Cretaceous. The Cephalopods, again—the highest of all
the groups of Mollusca—are represented in the Palzozoic
rocks exclusively by Tetrabranchiate forms, which constitute
the lowest of the two orders of this class; whereas the more
highly specialised Dibranchiates do not make their appearance
till the commencement of the Mesozoic. The Paleozoic

SUCCESSION OF LIFE UPON THE GLOBE. 371

Tetrabranchiates, also, are of a much simpler type than the
highly complex Ammonitide of the Mesozoic.

Similar facts are observable amongst the Vertebrate animals.
The Fishes are the lowest class of Vertebrates, and they are
the first to appear, their first certain occurrence being in the
Upper Silurian ; whilst, even if the Lower Silurian and Upper
Cambrian ‘“‘ Conodonts” were shown to be the teeth of Fishes,
there would still remain the enormously long periods of the
Laurentian and Lower Cambrian, during which there were In-
vertebrates, but no Vertebrates. The Amphibians, the next
class in zoological order, appears later than the Fishes, and
is not represented till the Carboniferous; whilst its highest
group (that of the Frogs and Toads) does not make its entrance
upon the scene till Tertiary times are reached. The class of
the Reptiles, again, the next in order, does not appear till
the Permian, and therefore not till after Amphibians of very
varied forms had been in existence for a protracted period.
The Birds seem to be undoubtedly later than the Reptiles ;
but, owing to the uncertainty as tc the exact point of their first
appearance, it cannot be positively asserted that they pre-
ceded Mammals, as they should have done. Finally, the
Mesozoic types of J/ammals are mainly, if not exclusively,
referable to the Marsupials, one of the lowest orders of the
class ; whilst the higher orders of the ‘‘ Placental” Quadrupeds
are not with certainty known to have existed prior to the com-
mencement of the Tertiary period.

Facts of a very similar nature are offered by the succession
of Plants upon the globe. ‘Thus the vegetation of the Palzo-
zoic period consisted principally of the lowly-organised groups
of the Cryptogamous or Flowerless plants. The Mesozoic
formations, up to the Chalk, are especially characterised by the
naked-seeded Flowering plants—the Conifers and the Cycads ;
whilst the higher groups of the Angiospermous Exogens and
Monocotyledons characterise the Upper Cretaceous and Ter-
tiary rocks.

Facts of the above nature—and they could be greatly multi-
plied—seem to point clearly to the existence of some law of
progression, though we certainly are not yet in a position to
formulate this law, or to indicate the precise manner in which
it has operated. Two considerations, also, must not be over-
looked. In the first place, there are various groups, some of
them highly organised, which make their appearance at an ex-
tremely ancient date, but which continue throughout geological
time almost unchanged, and certainly unprogressive. Many of
these “ persistent types” are known—such as various of the

372 HISTORICAL PALEONTOLOGY.

Foraminifera, the Lingule, the Mautili, &c.; and they indicate
that under given conditions, at present unknown to us, it is
possible for a life-form to subsist for an almost indefinite period
without any important modification of its structure. In the
second place, whilst the facts above mentioned point to some
general law of progression of the great zoological groups, it
cannot be asserted that the primeval types of any given group
are necessarily ‘“ lower,’ zoologically speaking, than their
modern representatives. Nor does this seem to be at all
necessary for the establishment of the law in question. It
cannot be asserted, for example, that the Ganoid and Placoid
Fishes of the Upper Silurian are in themselves less highly
organised than their existing representatives ; nor can it even
be asserted that the Ganoid and Placoid orders are low groups
of the class Fasces. On the contrary, they are high groups;
but then it must be remembered that these are probably not
really the first Fishes, and that if we meet with Fishes at some
future time in the Lower Silurian or Cambrian, these may
easily prove to be representatives of the lower orders of the
class. ‘This question cannot be further entered into here, as
its discussion could be carried out to an almost unlimited
length; but whilst there are facts pointing both ways, it
appears that at present we are not justified in asserting that the
earlier types of each group—so far as these are known to us,
or really are without predecessors—are necessarily or invariably
more “degraded” or “embryonic” in their structure than
their more modern representatives.

It remains to consider very briefly how far Paleontology
supports the doctrine of “‘ Evolution,” as it is called ; and this,
too, is a question of almost infinite dimensions, which can but
be glanced at here. Does Paleontology teach us that the
almost innumerable kinds of animals and plants which we
know to have successively flourished upon the earth in past
times were produced separately and wholly independently of
each other, at successive periods? or does it point to the
theory that a large number of these supposed distinct forms
have been in reality produced by the slow modification of a
comparatively small number of primitive types? Upon the
whole, it must be unhesitatingly:replied that the evidence of
Paleontology is in favour of the view that the succession of
life-forms upon the globe has been to a large extent regulated
by some orderly and constantly-acting law of modification and
evolution. Upon no other theory can we comprehend how
the fauna of any given formation is more closely related to
that of the formation next below in the series, and to that of

SUCCESSION OF LIFE UPON THE GLOBE. 373

the formation next above, than to that of any other series of
deposits. Upon no other view can we comprehend why the
Post-Tertiary Mammals of South America should consist prin-
cipally of Edentates, Llamas, Tapirs, Peccaries, Platyrhine
Monkeys, and other forms now characterising this continent ;
whilst those of Australia should be wholly referable to the.
order of Marsupials. On no other view can we explain the
common occurrence of “ intermediate” or “ transitional ”
forms of life, filling in the gaps between groups now widely
distinct.

On the other hand, there are facts which point clearly to the
existence of some law other than that of evolution, and pro-
bably of a deeper and more far-reaching character. Upon no
theory of evolution can we find a satisfactory explanation for
the constant introduction throughout geological time of new
forms of life, which do not appear to have been preceded by
pre-existent allied types. The Graptolites and Trilobites have
no known predecessors, and leave no known successors. The
Insects appear suddenly in the Devonian, and the Arachnides
and Myriapods in the Carboniferous, under well-differentiated
and highly-specialised types. The Dibranchiate Cephalopods
appear with equal apparent suddenness in the older Mesozoic
deposits, and no known type of the Palzeozoic period can be
pointed to as a possible ancestor. The Aippuritide of the
Cretaceous burst into a varied life to all appearance almost
immediately after their first introduction into existence. The
wonderful Dicotyledonous flora of the Upper Cretaceous
period similarly surprises us without any prophetic annuncia-
tion from the older Jurassic.

Many other instances could be given; but enough has been
said to show that there is a good deal to.be said on both sides,
and that the problem is one environed with profound difficul-
ties. One point only seems now to be universally conceded,
and that is, that the record of life in past time is not interrupted
by gaps other than those due to the necessary imperfections of
the fossiliferous series, to the fact that many animals are in-
capable of preservation in a fossil condition, or to other causes
of a like nature. All those who are entitled to speak on this
head are agreed that the introduction of new and the destruc-
tion of old species have been slow and gradual processes, in no
sense of the term ‘“catastrophistic.” Most are also willing to
admit that “ Evolution” has taken place in the past, to a
greater or less extent, and that a greater or less number of so-
called species of fossil animals are really the modified descend-
ants of pre-existent forms. How this process of evolution has

374 HISTORICAL PALEZONTOLOGY.

been effected, to what extent it has taken place, under what
conditions and laws it has been carried out, and how far it
may be regarded as merely auxiliary and supplemental to some
deeper law of change and progress, are questions to which, in
spite of the brilliant generalisations of Darwin, no satisfactory
answer can as yet be given. In the successful solution of this
problem—if soluble with the materials available to our hands
—will he the greatest triumph that Paleontology can hope to
attain ; and there is reason to think that, thanks to the guiding-
clue afforded by the genius of the author of the ‘ Origin of
Species,’ we are at least on the road to a sure, though it may
be a far-distant, victory.

Pree N DIX,

TABULAR VIEW OF THE CHIEF DIVISIONS
OF THE ANIMAL KINGDOM.

(Extinct groups are marked with an asterisk. Groups not represented
at all as fossils are marked with two asterisks. )

INVERTEBRATE ANIMALS.

SUB-KINGDOM I.—PROTOZOA.

Animal simple or compound ; body composed of ‘‘sarcode,” not de-
finitely segmented ; no nervous system; and.no digestive apparatus, beyond
occasionally a mouth and gullet.

Cuiass I. GREGARINID.**
CLaAss II. RHIZOPODA.
Order 1. Monera.**
nu 2. Amebea.**
nu 3. Foraminifera.
» 4. Radiolaria (Polycystines, &c.)
nu 5. Spongida (Sponges).
Cuass III. INFusoria.**

SUB-KINGDOM II.—CCELENTERATA.

Animal simple or compound ; body-wall composed of two principal
layers ; digestive canal freely communicating with the general cavity of the
body ; no circulating organs, and no nervous system ora rudimentary one ;
mouth surrounded by tentacles, arranged, like the internal organs, in a
‘‘ radiate’ or star-like manner.

Cuiass I. HYDROZOA.
Sub-class 1. Hydrotda (*‘ Hydroid Zoophytes’’). Zx. Fresh-

water Polypes,** Pipe-corallines (Zubularia), Sea - Firs
(Sertularia).

Sub-class 2. Siphonophora** (** Oceanic Hydrozoa”). LiKe
Portuguese Man-of-war (PAysalia),

376 APPENDIX.

Sub-class 3. Discophora (‘‘Jelly-fishes”). Only known as fossils
by impressions of their stranded carcasses.

Sub-class 4. Lucernarida (‘‘Sea-blubbers”’). Also only known
as fossils by impressions left in fine-grained strata.

Sub-class 5. Graptolitide * (*‘ Graptolites”’).

CLaAss II. ACTINOZOA.

Order 1. Zoantharia. Ex. Sea-anemones** (Actinide), Star-
corals (Astreide).

Order 2. Alcyonaria. Ex. Sea-pens (Pennatula), Organ-pipe

Coral (7uéipora), Red Coral (Corallium).

Order 3. Rugosa (“ Rugose Corals”’).

Ae. Ctenophora.** £x. Venus’s Girdle (Cestum).

SUB-KINGDOM III.—ANNULOIDA.

Animals in which the digestive canal is completely shut off from the
cavity of the body; a distinct nervous system; a system of branched
** water-vessels,” which usually communicate with the exterior. Body of
the adult often ‘‘radiate,” and never composed of a succession of definite
rings.

Cuiass I. ECHINODERMATA.
Order 1. Crinoidea (‘‘Sea-lilies”). Ax. Feather-star Coma-
tula), Stone-lily (Zucrinus*).
Order 2. Blastoidea* (*‘ Pentremites’’).
1 3. Cystoidea* (** Globe-lilies”’).
1 4. Ophiuroidea (“‘ Brittle-stars”). x. Sand-stars (OpAz-
ura), Brittle-stars ( phtoconia). Mt
Order 5. Asteroidea (‘‘Star-fishes”). £x. Cross-fish (Uraster),
Sun-star (So/aster).
Order 6. Echinotidea (‘‘Sea-urchins”). x. Sea-eggs (Echinus),
Heart-urchins (Spatangus).
Order 7. Holothuroidea (‘‘Sea-cucumbers”). . Zx. Trepangs
(Holothuria).
Cass II. ScoLEcrpa ** (Intestinal Worms, Wheel Animalcules, &c.)

SUB-KINGDOM IV.—ANNULOSA.

Animal composed of numerous definite segments placed one behind the
other ; nervous system forming a knotted cord placed along the lower
(ventral) surface of the body.

Division A. Anarthropoda. No jointed limbs.

Ciass I. GEPHYREA ** (‘‘Spoon-worms”).

Cuiass II. ANNELIDA (‘‘ Ringed-worms”). x. Leeches** (Hirudinea),
Earthworms** (Oligocheta), Tube-worms (7Zzéicola), Sea - worms
and Sea-centipedes (Zrrazztia).

Cuiass III. CH2#TOGNATHA ** (‘‘ Arrow-worms”’).

Division B. Arthropoda or Articulata. Limbs jointed to the body.

Cxiass I. CRUSTACEA (‘‘ Crustaceans’). £x. Bamacles and Acorn-
shells (Ctrripedia), Water- fleas (Ostracoda), Brine-shrimps and
Fairy-shrimps (P%y/lofoda), Trilobites* (77zlodita), King - crabs
and Eurypterids* (J/erostomata), Wood-lice and Slaters (/sofoda),
Sand-hoppers (Amphipoda), Lobsters, Shrimps, Hermit-crabs, and
Crabs (Decapoda). .

APPENDIX. | 377

Crass JI. ARACHNIDA. £x. Mites (Acarina), Scorpions (Pedipalpi),
‘Spiders (Araneida).

Cuiass III. Myriapopa. £x. Centipedes (Chilofoda), Millipedes and
Galley-worms (Chzlognatha). :

Cxiass IV. INsEcra (‘Insects’). x. Field-bugs (Hemiptera) ; Crick-
ets, Grasshoppers, &c. (Orthoptera); Dragon-flies and May-flies
(NMeuroptera) ; Gnats and House-flies (Diptera); Butterflies and
Moths (Lepidoptera); Bees, Wasps, and Ants (Avmenoftera) ;
Beetles (Coleoptera).

SUB-KINGDOM V.—MOLLUSCA.

Animal soft-bodied, generally with a hard covering or shell; no dis-
tinct segmentation of the body; nervous system of scattered masses.
Cxiass I. PoLyzoa (‘‘Sea-Mosses”). Ax. Sea-mats (Flustra), Lace-
; corals (Fenestellide*).

Cxiass II. Tunicata** (‘‘ Tunicaries”). x. Sea-squirts (Ascidia).

Cxiass III. BRACHIOPODA (‘‘Lamp-shells”). £2. Goose-bill Lamp-
shell (Zingula).

CxLass IV. LAMELLIBRANCHIATA (‘‘ Bivalves”). Za. Oyster (Ostrea),
Mussel (AZytilus), Scallop (Pecten), Cockle (Cardium).

Ciass V. GASTEROPODA (‘‘ Univalves”’). x. Whelks (Buccinum),
Limpets (Patella), Sea-slugs** (Doris), Land-snails (Ze/ix).

CLass VI. PTEROPODA (“‘ Winged Snails”). Ex. Hyalea, Cleodora.

Ciass VII. CEPHALOPODA (‘‘ Cuttle-fishes”). Ax. Calamary (ZLoligo),
Poulpe (Octopus), Paper Nautilus (Avgonauta), Pearly Nautilus
(Nautilus), Belemnites,* Orthoceratites,* Ammonites. *

VERTEBRATE ANIMALS.

SUB-KINGDOM VI.—VERTEBRATA.

Body composed of definite segments arranged longitudinally one behind
the other; main masses of the nervous system placed dorsally; a back-
bone or ‘‘ vertebral column” in the majority.

Cuiass I. Pisces (‘‘ Fishes”). x. Lancelet** (Amphioxus) ; Lampreys
and Hag-fishes (Marsipobranchii**); Herring, Salmon, Perch, &c.
( Zéleostee or *‘ Bony Fishes”); Gar-pike, Sturgeon, &c. (Ganoidez) ;
Sharks, Dog-fishes, Rays, &c. (EZ/lasmobranchu or ‘‘ Placoids”’).

Crass I]. AmMpuriBia (‘‘ Amphibians’). Ex. Labyrinthodontia,* Cz-
cilians,** Newts and Salamanders (Uvodela), Frogs and Toads
(Anoura).

CiaAss III. Repriia (‘‘ Reptiles”). Ex. Deinosauria,* Pterosauria,*

. Anomodontia,* Plesiosaurs (Sauropterygia*), Ichthyosaurs (/chthy-
opterygia*), Tortoises and Turtles (Chelonia), Snakes (Ophidia),
Lizards (Zacertilia), Crocodiles (Crocodilia).

Cuiass IV. Aves (“Birds”). x. Toothed Birds (Odoztornithes*) ;
Lizard-tailed Birds (Archeopteryx*); Ducks, Geese, Gulls, &c.
(Natatores); Storks, Herons, Snipes, Plovers, &c. (Grallatores) ;
Ostrich, Emeu, Cassowary, Dinornis,* A®piornis,* &c. (Cursores) ;
Fowls, Game Birds, and Doves (Rasores); Cuckoos, Woodpeckers,
Parrots, &c. (Scansores); Crows, Starlings, Finches, Humming-
birds, Swallows, &c. (usessores) ; Owls, Hawks, Eagles, Vultures
(Raptores).

378 APPENDIX.

Ciass V. MAMMALIA (‘‘ Quadrupeds”’). £x. Duck-mole and Spiny
Ant-eater (J/onotremata**); Kangaroos, Phalangers, Opossums,
Tasmanian Devil, &c. (A/arsupialia) ; Sloths, Ant-eaters, Arma-
dillos (Edentata); Manatees and Dugongs (Szvenia); Whales,
Dolphins, Porpoises (Cefacea) ; Rhinoceros, Tapir, Horses, Hip-
popotamus, Pigs, Camels and Llamas, Giraffes, Deer, Antelopes,
Sheep, Goats, Oxen (Ungulata); Hyrax (Hyracoidea**); Ele-
phants, Mastodon,* Deinotherium* (Proboscidea) ; Seals, Walrus,
Bears, Dogs, Wolves, Cats, Lions, Tigers, &c. (Carnivora) ;
Hares, Rabbits, Porcupines, Beavers, Rats, Mice, Lemmings,
Squirrels, Marmots, &c. (Rodentia); Bats (Cheiroptera) ; Moles,
Shrew-mice, Hedgehogs (/nsectivora) ; Lemurs, Spider-monkeys,
Macaques, Baboons, Apes (Quadrumana); Man (4imana).

GlEO'Sis A RY.

ABDOMEN (Lat. abdo, I conceal). The posterior cavity of the body, contain-
ing the intestines and others of the viscera. In many Invertebrates there
is no separation of the body-cavity into thorax and abdomen, and it is only
in the higher Annulosa that a distinct abdomen can be said to exist.

ABERRANT (Lat. aberro, I wander away). Departing from the regular type.

ABNORMAL (Lat. ab, from; norma, a rule). Irregular; deviating from the
ordinary standard.

Acropus (Gr. akros, high ; odous, tooth). A genus of the Cestraciont fishes.
so called from the elevated teeth.

Acrocens (Gr. akros, high; gennao, I produce). Plants which increase in
height by additions made to the summit of the stem by the union of the
bases of the leaves. :

AcROTRETA (Gr. akros, high; trétos, pierced). A genus of Brachiopods, so
called from the presence of a foramen at the summit of the shell.

AcTINocRINUS (Gr. aktin, aray; krinon, a lily). A genus of Crinoids.

Actrnozoa (Gr. aktin, a ray; and zoén, an animal). That division of the
Celenterata of which the Sea-anemones may be taken as the type.

ANGLINA (diglé, a sea-nymph). A genus of Trilobites.

AEPIORNIS (Gr. aipus, huge; ornis, bird). A genus of gigantic Cursorial
birds.

AcnostTus (Gr. a, not; gignosko, 1 know). A genus of Trilobites.

ALCES (Lat. alces, elk). The European Elk or Moose.

ALECTO (the proper name of one of the Furies). A genus of Polyzoa.

ALETHOPTERIS (G7. aléthés, true; pteris, fern). A genus of Ferns,

ALG# (Lat. alga, a marine plant). The order of plants comprising the Sea-
weeds and many fresh-water plants.

ALVEOLUS (Lat. alwus, belly). Applied to the sockets of the teeth.

AMBLYPTERUS (Gr. amblus, blunt ; pteron, fin). An order of Ganoid Fishes.

AMBONYCHIA (Gr. ambén, a boss; onux, claw). A genus of Paleozoic Bi-
valves.

AMBULACRA (Lat. ambulacrum, a place for walking). The perforated spaces
or “‘ avenues” through which are protruded the tube-feet, by means of which
locomotion is effected in the Echinodermata.

AMMONITIDZ. A family of Tetrabranchiate Cephalopods, so called from the
resemblance of the shell of the type-genus, Ammonites, to the horns of the
Egyptian God, Jupiter-Ammon.

AMORPHOZOA (Gr. a, without ; morphe, shape ; zon, animal). A name some-
times used to designate the Sponges.

AMPHIBIA (Gr. amphi, both; bios, life). The Frogs, Newts, and the like,
ahs have gills when young, but can always breathe air directly when

ult,

AmpPpuHicyon (Gr. amphi, both—implying doubt; kudn, dog), An extinct
genus of Carnivora, e

380 GLOSSARY.

oe (Gr. amphi, both; léstés, a thief). A genus of Jurassic Mam-

mals.

AMPHISPONGIA (Gr. amphi, both; spoggos, sponge). A genus of Silurian
sponges.

AMPHISTEGINA (Gr. amphi, both; stegé, roof). A genus of Foraminifera.

ee (Gr. amphi, both; thérion, beast). A genus of Jurassic Mam-
mals.

AMPHITRAGULUS (Gr. amphi, both ; dim. of tragos, goat). An extinct genus
related to the living Musk-deer.

AMPLEXUS (Lat. an embrace). A genus of Rugose Corals.

AmpyYXx (Gr. ampux, a wreath or wheel). A genus of Trilobites.

ANARTHROPODA (Gr. a, without ; arthros, a joint; pous, foot). That division
of Annulose animals in which there are no articulated appendages.

ANCHITHERIUM (Gr. agchi, near ; thérion, beast). An extinct genus of Mammals.

ANCYLOCERAS (Gr. agkulos, crooked ; ceras, horn). A genus of Ammonitide.

ANCYLOTHERIUM (Gr. agkulos, crooked ; thérion, beast). Anextinct genus of
Edentate Mammals.

Sone (Gr. andrias, image of man). An extinct genus of tailed Amphi-

ians.

ANGIOSPERMS (Gr. angeion, a vessel; sperma, seed). Plants which have their
seeds enclosed in a seed-vessel.

ANNELIDA (a Gallicised form of Annulata). The Ringed Worms, which form
one of the divisions of the Anarthropoda.

ANNULARIA (Lat. annulus, a ring). A genus of Paleozoic plants, with leaves
in whorls.

ANNULOSA (Lat. annulus). The sub-kingdom comprising the Anarthropoda
and the Arthropoda or Articulata, in all of which the body is more or less
evidently composed of a succession of rings.

ANOMODONTIA (Gr. @nomos, irregular; odous, tooth). An extinct order of
Reptiles, often called Dicynodontia.

AnomuRa (Gr. anomos, irregular ; owra, tail). A tribe of Decapod Crustacea,
of which the Hermit-crab is the type.

ANOPLOTHERIDE (Gr. anoplos, unarmed ; ther, beast). A family of Tertiary
Ungulates.

AnouRra (Gr. @, without; owra, tail). The order of Amphibia comprising the
Frogs and Toads, in which the adult is destitute of a tail. Often called
Batrachia.

ANTENN& (Lat. antenna, a yard-arm). The jointed horns or feelers possessed
by the majority of the Articulata. :

ANTENNULES (dim. of Antenze). Applied to the smaller pair of antennz in
the Crustacea.

ANTHRACOSAURUS (Gr. anthrax, coal; saura, lizard). A genus of Labyrintho-
dont Amphibians.

ANTHRAPALEMON (Gr. anthrax, coal; palemén, a prawn—originally a proper
name), A genus of long-tailed Crustaceans from the Coal-measures.

ANTLERS. Properly the branches of the horns of the Deer tribe (Cervide), but
generally applied to the entire horns.

APIOCRINIDE (Gr. apion, a pear; krinon, lily). A family of Crinoids—the
‘* Pear-encrinites.”

APTERYX (Gr. a, without; pterva, a wing). A wingless bird of New Zealand,
belonging to the order Cursores.

AQUEOUS (Lat. agua, water). Formed in or by water.

ARACHNIDA (Gr. arachne, a spider). A class of the Articulata, comprising
Spiders, Scorpions, and allied animals.

ARBORESCENT. Branched like a tree.

ARCHZOCIDARIS (Gr. archaios, ancient; Lat. cidaris, a diadem). A Palzo-
zoic genus of Sea-urchins, related to the existing Cidaris.

ARCHEOCYATHUS (Gr. archaios, ancient ; kuathos, cup). A genus of Palzozoic
fossils allied to the Sponges.

ARCHZOPTERYX (Gr. archaios, ancient; pterux,a wing). The singular fossil
bird which alone constitutes the order of the Sauwrure.

GLOSSARY. 381

Arctocyon (Gr. arctos, bear; kwon, dog). An extinct genus of Carnivora.

ARENACEOUS. Sandy, or composed of grains of sand.

ARENICOLITES (Lat. arena, sand ; colo, I inhabit). A genus founded on = bur-
rows supposed_to be formed by worms resembling the living Lobworms
(Arenicola).

ARTICULATA (Lat. articulus, a joint). A division of the animal kingdom, com-
prising Insects, Centipedes, Spiders, and Crustaceans, characterised by the
possession of jointed bodies or jointed limbs. The term Arthropoda is now
more usually employed.

ARTIODACTYLA (Gr. artios, even; daktulos, a finger or toe). A division of the
hoofed quadrupeds (Ungulata) in which each foot has an even number of
toes (two or four).

ASAPHUS (Gr. asaphés, obscure). A genus of Trilobites.

ASCOCERAS (Gr. askos, a leather bottle ; keras, horn). A genus of Tetrabran-
chiate Cephalopods.

ASIPHONATE. Not possessing a respiratory tube or siphon. (Applied to a
division of the Lamellibranchiate Molluscs.)

ASTEROID (Gr. aster, a star; and eidos, form). Star-shaped, or possessing
radiating lobes or rays.like a star-fish.

ASTEROIDEA. An order of Echinodermata, comprising the Star-fishes, charac-
terised by their rayed form.

ASTEROPHYLLITES (Gr. aster, a star; phullon, leaf). A genus of Paleozoic
plants, with leaves in whorls.

ASTR#IDH (Gr. Astrea, a proper name). The family of the Star-corals.

ASTYLOSPONGIA (Gr. @, without; stulos, a column; spoggos, a sponge). <A
genus of Silurian Sponges.

ATHyRIS (Gr. a, without ; thura, door). A genus of Brachiopods.

Atrypa (Gr. 4, without ; trupa, a hole). A genus of Brachiopods.

AVEs (Lat. avis, a bird). The class of the Birds.

AVICULA (Lat. a little bird). The genus of Bivalve Molluscs comprising the
Pearl-oysters.

0 ae (Gr. axon, a pivot; phullon, a leaf). A genus of Rugose

orals.

Azotc (Gr. a, without; z0é, life). Destitute of traces of living beings.

BAcuULITES (Lat. baculum, a staff). A genus of the Ammonitide.

BALZNA (Lat. a whale). The genus of the Whalebone Whales.

BALANID& (Gr. balanos, an acorn). A family of sessile Cirripedes, commonly
called “‘ Acorn-shells.”

BaTRACHIA (Gr. batrachos, a frog). Often loosely applied to any of the Am-
phibia, but sometimes restricted to the Amphibians as a class, or to the
single order of the Anoura.

BELEMNITID (Gr. belemnon, a dart). An extinct group of Dibranchiate Ceph-
alopods, comprising the Belemnites and their allies.

BELEMNOTEUTHIS (Gr. belemnon, a dart ; teuthis, a cuttle-fish). A genus allied
to the Belemnites proper.

BELINURUS (Gr. belos, a dart; owra, tail). A genus of fossil King-crabs.

BELLEROPHON (Gr. proper name). A genus of oceanic Univalves (Heteropoda).

BELOTEUTHIS (Gr. belos, a dart ; teuthis, a cuttle-fish). An extinct genus of
Dibranchiate Cephalopods.

BEYRICHIA (named after Prof. Beyrich). A genus of Ostracode Crustaceans.

BILATERAL. Having two symmetrical sides.

BIMANA (Lat. bis, twice; manus, a hand). The order of Mammalia compris-
ing man alone.

BIPEDAL (Lat. bis, twice; pes, foot). Walking upon two legs.

BIVALVE (Lat. bis, twice ; valve, folding-doors), Composed of two plates or
valves ; applied to the shell of the Lamellibranchiata and Brachiopoda, and
to the carapace of certain Crustacea.

BLASTOIDEA (Gr. blastos, a bud; and eidos, form). An extinct order of Echi-
nodermata, often called Pentremites.

BrRacuHiopopa (Gr. brachion, an arm ; pous, the foot). A class of the Mollus-

26

382 GLOSSARY.

coida, often called ‘‘ Lamp-shells,” characterised by possessing two fleshy
arms continued from the sides of the mouth.

BracHyura (Gr. bruchus, short ; oura, tail). A tribe of the Decapod Crusta-
ceans With short tails (7.e., the Crabs).

BRADYPODID (Gr. bradus, slow; podes, feet). The family of Edentata com-
prising the Sloths.

Brancuia (Gr. bragchia, the gill of a fish). A respiratory organ adapted to
breathe air dissolved in water.

BRANCHIATE. Possessing gills or branchie.

Brontevus (Gr. bronté, thunder—an epithet of Jupiter the Thunderer). A
genus of Trilobites.

BRONTOTHERIUM (Gr. bronté, thunder ; thzrion beast). An extinct genus of
Ungulate Quadrupeds.

Brontozoum (Gr. bronté, thunder ; zodn, animal). A genus founded on the
largest footprints of the Triassic Sandstones of Connecticut.

Buccrinum (Lat. bucctnum, a trumpet). The genus of Univalves comprising
the Whelks.

Catnozoic (See Kainozoic.)

CALAMITES (Lat. calamus, a reed). Extinct plants with reed-like stems, be-
lieved to be gigantic representatives of the Hguisetacee.

CALCAREOUS (Lat. calz, lime). Composed of carbonate of lime.

CaLicE. The little cup in which the polype of a coralligenous Zoophyte (Ac-
tinozoén) is contained.

CALYMENE (Gr. kaluméné, concealed). A genus of Trilobites.

CaLyx (Lat. a cup). Applied to the cup-shaped body of a Crinoid ( Echino-
dermata).

CAMAROPHORIA (Gr. kamara, a chamber ; phero, I carry). A genus of Brachio-
pods.

CAMELOPARDALID# (Lat. camelus, a camel; pardalis, a panther). The family
of the Giraffes.

CANINE (Lat. canis, a dog). The eye-tooth of Mammals, or the tooth which
is placed at or close to the premaxillary suture in the upper jaw, and the
corresponding tooth in the lower jaw.

CARAPACE. A protective shield. Applied to the upper shell of Crabs, Lobsters,
and many other Crustacea. Also the upper half of the immovable case in
which the body of a Chelonian is protected.

CARCHARODON (Gr. karcharos, rough ; odous, tooth). A genus of Sharks.

CARDIOCARPON (Gr. kardia, the heart; karpos, fruit). A genus of fossil fruit
from the Coal-measures.

CaRpDIuM (Gr. kardia, the heart). The genus of Bivalve Molluscs comprising
the Cockles. Cardinia, Cardiola, and Cardita have the same derivation.
CaRNIVORA (Lat. caro, flesh ; voro, I devour). An order of the Mammalia.

The ‘‘ Beasts of Prey.”

CARNIVOROUS (Lat. caro, flesh,; voro, I devour). Feeding upon flesh.

CarRyocaRIs (Gr. karua, a nut; saris, a shrimp). A genus of Phyllopod Crus-
taceans.

CaRYOCRINUS (Gr. karua, a nut; krinon, a lily). A genus of Cystideans.

CAUDAL (Lat. cauda, the tail). Belonging to the tail.

CaVICORNIA (Lat. cavus, hollow; cornu, a horn). The ‘‘hollow-horned”
Ruminants, in which the horn consists of a central bony ‘‘ horn-core”’ sur-
rounded by a horny sheath.

CENTRUM (Gr. kentron, the point round which a circle is described by a pair
of compasses). The central portion or ‘‘ body”’ of a vertebra.

CEPHALASPID® (Gr. kephale, head; aspis, shield). A family of fossil fishes.

CepuHatic (Gr..kephale, head). Belonging to the head.

CEPHALOPODA (Gr. kephale ; and podes, feet). A class of the Mollusca, com-
prising the Cuttle-fishes and their allies, in which there is a series of arms
ranged round the head.

CERATIOCARIS (Gr. keras, a horn; karis, a shrimp). A genus of Phyllopod
Crustaceans.

ae

GLOSSARY. 383

CERATITES (Gr. keras, a horn). A genus of Ammonitide. ;

CERATODUS (Gr. keras, a horn ; odous, tooth). A genus of Dipnoous fishes.

CERVICAL (Lat. cervix, the neck). Connected with or belonging to the region
of the neck.

CERVID (Lat. cervus, a stag). The family of the Deer.

CESTRAPHORI (Gr. kestra, a weapon ; phero, I carry). The group of the ‘‘ Ces-
traciont Fishes,” represented at the present day by the Port-Jackson Shark ;
so called from their defensive spines.

CreTacka (Gr. kétos, a whale). The order of Mammals comprising the Whales
and the Dolphins.

CETIOSAURUS (Gr. étos, whale ; saura, lizard). A genus of Deinosaurian
Reptiles.

CHETIROPTERA (Gr. cheir, hand ; pteron, wing). The Mammalian order of the
Bats.

CHEIROTHERIUM (Gr. cheir, hand ; thérion, beast). The generic name applied
originally to the hand-shaped footprints of Labyrinthodonts.

CHEIRURUS (Gr. cheir, hand ; oura, tail). A genus of Trilobites.

CHELONIA (Gr. cheloné, a tortoise). The Reptilian order of the Tortoises and
Turtles.

CHONETES (Gr. chdné or chéané, a chamber or box). A genus of Brachiopods.

CrpaRIs (Lat. a diadem). A genus of Sea-urchins,

CLapovus (Gr. klados, branch ; odous, tooth). A genus of Fishes.

CLATHROPORA (Lat. clathri, a trellis ; porus, a pore). A genus of Lace-corals
(Polyzoa).

CLISIOPHYLLUM (Gr. Klision, a hut; phullon, leaf). A genus of Rugose Corals.

CLYMENIA (Clumene, a proper name). A genus of Tetrabranchiate Cephalopods.

CoccosteEus (Gr. kokkos, berry ; osteon, bone). A genus of Ganoid Fishes.

CocuLiopus (Gr. kochlion, a snail-shell; odous, tooth). A genus of Cestra-
ciont Fishes.

C@LENTERATA (Gr. Koilos, hollow ; enteron, the bowel). The sub-kingdom
which comprises the Hydrozoa and Actinozoa. Proposed by Frey and
Leuckhart in place of the old term Radiata, which included other animals
as well.

COLEOPTERA (Gr. Koleos, a sheath; pteron, wing). The order of Insects
(Beetles) in which the anterior pair of wings are hardened, and serve as pro-
tective cases for the posterior pair of membranous wings.

COLOSSOCHELYS (Gr. Kolossos, a gigantic statue; chelus, a tortoise). A huge
extinct Land-tortoise.

ComaTULA (Gr. koma, the hair). The Feather-star, so called in allusion to its
tress-like arms.

COoNDYLE (Gr. kondulos, a knuckle). The surface by which one bone articulates
with another. Applied especially to the articular surface or surfaces by
which the skull articulates with the vertebral column.

CONIFER& (Lat. conus, a cone; fero, I carry). The order of the Firs, Pines,
and their allies, in which the fruit is generally a ‘‘ cone” or ‘‘ fir-apple.”

CoNULARIA (Lat. conulus, a little cone). An extinct genus of Pteropods.

Copro.ites (Gr. kopros, dung; lithos, stone). Properly applied to the fossil-
ised excrements of animals ; but often employed to designate phosphatic con-
cretions which are not of this nature.

CoRALLITE. The corallum secreted by an Actinozodn which consists of a single
polype; or the portion of a composite corallum which belongs to, and is
secreted by, an individual polype.

CoRALLUM (from the Latin for Red Coral). The hard structures deposited in,
or by, the tissues of an Actinozoén—commonly called a “ coral.”

CORIACEOUS (Lat. corium. hide). Leathery.

CorYPHODON (Gr. korus, helmet; odous, tooth). An extinct genus of Mam-
mals, allied to the Tapirs.

Cranium (Gr. kranion, the skull). The bony or cartilaginous case in which
the brain is contained,

CRETACEOUS (Lat. creta, chalk). The formation which in Europe contains
white chalk as one of its most conspicuous members.

384 GLOSSARY.

CRINOIDEA (Gr. krinon, a lily ; etdos, form). An order of Echinodermata,
comprising forms which are usually stalked, and sometimes resemble lilies
in shape.

CRIOCERAS (Gr. krios, a ram; keras,a horn). A genus of Ammonitide.

Crocopizia (Gr. krokodeilos, a crocodile). An order of Reptiles.

CROSSOPTERYGIDE (Gr. krossotos, a fringe; pleruz, a fin). A sub-order of
Ganoids in which the paired fins possess a central lobe.

CRUSTACEA (Lat. crusta, a crust). A class of Articulate animals, comprising
Crabs, Lobsters, &c., characterised by the possession of a hard shell or
crust, which they cast periodically.

CrYPTOGAMS (Gr. kruptos, concealed ; gamos, marriage). A division of plants
in which the organs of reproduction are obscure and there are no true
flowers.

CTENACANTHUS (Gr. kteis,a comb; akantha, a thorn). A genus of fossil fishes,
named from its fin-spines.

CTENOID (Gr. kteis, a comb; eidos, form). Applied to those scales of fishes
the hinder margins of which are fringed with spines or comb-like projections.

CURSORES (Lat. curvo, I[run). An order of Aves, comprising birds destitute
of the power of flight, but formed for running vigorously (e.g., the Ostrich
and Emeu).

CUSPIDATE. Furnished with small pointed eminences or ‘‘ cusps.”

CYATHOCRINUS (Gr. kuathos, a cup; krinon, a lily). A genus of Crinoids.

ee enna (Gr. kuathos, a cup; phullon, a leaf). A genus of Rugose

orals.

CycLo1p (Gr. kukios, a circle ; eidos, form). Applied to those scales of fishes
which have a regularly circular or elliptical outline with an even margin.

CYCLOPHTHALMUS (Gr. kuklos, a circle ; ophthalmos, eye). A genus of fossil
Scorpions.

CycLostomi (Gr. kuklos, and stoma, month). Sometimes used to designate the
Hag-fishes and Lampreys, forming the order Marsipobranchit.

CYPRHA (a name of Venus). The genus of Univalve Molluscs comprising the
Cowries.

CYRTOCERAS (Gr. kurtos, crooked; keras, horn). A genus of Tetrabranchiate
Cephalopods.

CYSTIPHYLLUM (Gr. kustis, a bladder ; phullon, a leaf). A genus of Rugose
Corals.

CystTompEA (Gr. kustis, a bladder ; eidos, form). The ‘‘ Globe-crinoids,” an
extinct order of Echinodermata.

DaDOXYLon (Gr. dadion, a torch; zulon, wood). An extinct genus of Con-
iferous trees. ;

Decapopa (Gr. deka, ten ; podes, feet). The division of Crustacea which have
ten feet; also the family of Cuttle-fishes, in which there are ten arms or
cephalic processes.

Decipuovs (Lat. decido, I fall off). Applied to parts which fall off or are shed
during the life of the animal.

DEINOSAURIA (Gr. deinos, terrible ; saura, lizard). An extinct order of Rep-
tiles.

DEINOTHERIUM (Gr. deinos, terrible; thérion, beast). An extinct genus of
Proboscidean Mammals.

DENDROGRAPTUS (Gr. dendron, tree ; grapho, I write). A genus of Grapto-
lites.

DeEsMIDIz. Minute fresh-water plants, of a green colour, without a siliceous
epidermis.

DIATOMACE (Gr. diatemno, I sever). An order of minute plants which are
provided with siliceous envelopes.

DIBRANCHIATA (Gr. dis, twice ; bragchia, gill). The order of Cephalopoda
(comprising the Cuttle-fishes, &c.) in which only two gills are present.

Dicreras (Gr. dis, twice; keras, horn). An extinct genus of Bivalve Molluscs.

eee (Gr. diktuon, a net; nema, thread). An extinct genus of Poly-
wou (*).

GLOSSARY, . 385

SeenON ELA (Gr. dis, twice; kuon, dog; odous, tooth). An extinct order of

eptiles.

pecan (Gr. didumos, twin ; grapho, I write). A genus of Graptolites.

DrmMoRPHODON (Gr. dis, twice; morphé, shape; odous, tooth). <A genus of
Pterosaurian Reptiles.

DINICHTHYS (Gr. deinos, terrible ; tchthus, fish). An extinct genus of Fishes.

DrnocerRas (Gr. deinos, terrible ; keras, horn). An extinct genus of Mammals.

DrinopuHis (Gr. deinos, terrible ; ophis, snake), An extinct genus of Snakes.

Drnornis (Gr. deinos, terrible; ornis, bird). An extinct genus of Birds.

DIPLOGRAPTUS (Gr. diplos, double ; grapho, I write). A genus of Graptolites.

Drenor (Gr. dis, twice; pnoé, breath). An order of Fishes, comprising the
Mud-tishes, so called in allusion to their double mode of respiration.

DIPROTODON (Gr. dis, twice ; protos, first; odous, tooth). A genus of extinct
Marsupials.

Dretera (Gr. dis, twice; pteron, wing). An order of Insects characterised
by the possession of two wings.

Disco (Gr. diskos, a quoit; eidos, form). Shaped like a round plate or

noit.

Dorowrre (named after M. Dolomieu). Magnesian limestone.

Dorsal (Lat. dorsum, the back). Connected with or placed upon the back.

DROMATHERIUM (Gr. dromazos, nimble ; thérion, beast). A genus of Triassic
Mammals.

DryopiTHEcus (Gr. drus, an oak; pithekos, an ape). An extinct genus of
Monkeys.

ECHINODERMATA (Gr. echinos; and derma, skin). A class of animals com-
prising tke Sea-urchins, Star-fishes, and others, most of which have spiny
skins.

EcHINOIDEA (Gr. echinos ; and ezdos, form). An order of Echinodermata, com-
prising the Sea-urchins.

EDENTATA (Lat. é, without ; dens, tooth). An order of Mammailia often called
Bruta.

EpDENTULOUs. Toothless, without any dental apparatus. Applied to the
mouth of any animal, or to the hinge of the Bivalve Molluscs.

ELASMOBRANCHII (Gr. elasma, a plate; bragchia, gill). An order of Fishes,
including the Sharks and Rays.

ENALIOSAURIA (Gr. enalios, marine ; saura, lizard). Sometimes employed as
a common term to designate the extinct Reptilian orders of the [chthyosauria
and Plesiosauria.

Eocene (Gr. eos, dawn; kainos, new or recent). The lowest division of the
Tertiary rocks, in which species of existing shells are to a small extent
represented.

EopHyTon (Gr. eos, dawn; phuton, a plant). A genus of Cambrian fossils,
supposed to be of a vegetable nature.

E0zoon (Gr. eos, dawn; zodm, animal). A genus of chambered calcareous or-
ganisms found in the Laurentian and Huronian formations.

EQUILATERAL (Lat. equus, equal; Jatus, side). Having its sides equal. Usu-
ally applied to the shells of the Brachiopoda. When applied to the spiral
shells of the Foraminifera, it means that all the convolutions of the shell lie
in the same plane.

EQUISETACEH (Lat. equus, horse ; seta, bristle). A group of Cryptogamous
plants, commonly known as ‘‘ Horse-tails.”

EQUIVALVE (Lat. equus, equal ; valve, folding-doors). Applied to shells which
are composed of two equal pieces or valves.

ERRANTIA (Lat. erro, I wander). An order of Annelida, often called Nereidea,
distinguished by their great locomotive powers.

EUOMPHALUS (Gr. ev, well; omphalos, navel). An extinct genus of Univalve
Molluscs.

EURYPTERIDA (Gr. ewrus, broad; pteron, wing). An extinct sub-order of Crus-

- tacen.

ExoeyRa (Gr. exo, outside ; guros, circle). An extinct genus of Oysters.

386 GLOSSARY.

Fauna (Lat. Fauni, the rural deities of the Romans). The general assemblage
of the animals of any region or district.

FavosItEs (Lat. favus, a honeycomb). <A genus of Tabulate Corals.

FENESTELLID# (Lat. jfenestella, a little window). The ‘‘ Lace-corals,” a group
of Paleozoic Polyzoans.

Finicks (Lat. flix, a fern). The order of Cryptogamic plants comprising the
Ferns.

FinirorM (Lat. flum, a thread ; forma, shape). Thread-shaped.

Fora (Lat. Flora, the goddess of flowers). The general assemblage of the
plants of any region or district.

FORAMINIFERA (Lat. foramen, an aperture ; fero, I carry). An order of Pro-
tozoa, usually characterised by the possession of a shell perforated by numer-
ous pseudopodial apertures.

FRUGIVOROUS (Lat. frux, fruit ; voro, I devour). Living upon fruits.

Fucorps (Lat. fucus, sea-weed; Gr. eidos, likeness). Fossils, often of an
obscure nature, believed to be the remains of sea-weeds.

FUSULINA (Lat. fusus, a spindle). An extinct genus of Foraminifera.

GANOID (Gr. ganos, splendour, brightness). Applied to those scales or plates
which are composed of an inferior layer of true bone covered by a superior
layer of polished enamel.

GANOIDEI. An order of Fishes.

GASTEROPODA (Gr. gaster, stomach ; pous, foot). The class of the Mollusca
comprising the ordinary Univalves, in which locomotion is usually effected by
a muscular expansion of the under surface of the body (the ‘‘foot”’).

GLOBIGERINA (Lat. globus, a globe; gero, I carry). A genus of Foraminifera.

GLYPTODON (Gr. glupho, I engrave ; odovs, tooth). An extinct genus of Arma-
dillos, so named in allusion to the fluted teeth.

GONIATITES (Gr. génia, angle). A genus of Tetrabranchiate Cephalopods.

GRALLATORES (Lat. gralle, stilts). The order of the long-legged Wading Birds.

GRAPTOLITIDA (Gr. grapho, I write; lithos, stone). An extinct sub-class of
the Hydrozoa.

GYMNOSPERMS (Gr. gumnos, naked ; sperma, seed). The Conifers and Cycads,
in which the seed is not protected within a seed-vessel.

HALITHERIUM (Gr. als, sea; thérion, beast). An extinct genus of Sea-cows
(Sirenia).

HAmMITES (Lat. hamus, a hook). <A genus of the Ammonitide.

HELIOPHYLLUM (Gr. /élios, the sun; phullon, leaf). A genus of Rugose
Corals.

HELLADOTHERIUM (Gr. Hellas, Greece ; thérion, beast). An extinct genus of
Ungulate Mammals.

HEMIPTERA (Gr. hemi ; and pteron, wing). An order of Insects in which the
anterior wings are sometimes ‘‘ hemelytra.”’

HESPERORNIS (Gr. Hesperos, the evening star; ornis, bird). An extinct genus
of Birds.

HETEROCERCAL (Gr. heteros, diverse ; kerkos, tail). Applied to the tail of
Fishes when it is unsymmetrical, or composed of two unequal lobes.

HeTeropopa (Gr. heteros, diverse; podes, feet). An aberrant group of the
Gasteropods, in which the foot is modified so as to form a swimming organ.

HIPPARION (Gr. Aipparidn, a little horse). An extinct genus of Hquide.

HIPPopoTaMus (Gr. Aippos, horse ; potamos, river). A genus of Hoofed Quad-
rupeds—the ‘‘ River-horses.”

HIPPURITIDE (Gr. hippos, horse; oura, tail). An extinct family of Bivalve
Molluscs.

Houoprycuius (Gr. holos, whole; ptuché, wrinkle). An extinct genus of
Ganoid Fishes.

Ho.ostoMata (Gr. iolos, whole ; stoma, mouth). A division of Gasteropodous
Molluscs, in which the aperture of the shell is rounded, or ‘‘ entire.”

HOLOTHUROIDEA (Gr. holothowrion ; and eidos, form). An order of Echinoder-.
mata comprising the Trepangs.

GLOSSARY. 387

Homocercat (Gr. homos, same; kerkos, tail). Applied to the tail of Fishes
when it is symmetrical, or composed of two equal lobes.

Hysoponts (Gr. hubos, curved ; odous, tooth). A group of Fishes of which
Hybodus is the type-genus.

Hyproima (Gr. hudra; and eidos, form). The sub-class of the Hydrozoa,
which comprises the animals most nearly allied to the Hydra.

Hyprozoa (Gr. hudra ; and zoén, animal). The class of the Celenterata which
comprises animals constructed after the type of the Hydra.

HYMENOPTERA (Gr. humen, a membrane; pteron, a wing). An order of In-
sects (comprising Bees, Ants, &c.) characterised by the possession of four
membranous wings.

ICHTHYODORULITE (Gr. ichthus, fish ; dorus, spear; lithos, stone). The fossil
fin-spine of Fishes.

ICHTHYOPTERYGIA (Gr. ichthus ; pterux, wing). An extinct order of Reptiles.

IcCHTHYORNIS (Gr. zchthus, fish; ornis, bird). An extinct genus of Birds.

ICHTHYOSAURIA (Gr. ichthus; saura, lizard). Synonymous with Jchthyop-
terygua.

ig conen (Iguana, a living lizard ; Gr. odous, tooth). A genus of Deinosau-
rian Reptiles.

Inctsor (Lat. zncido, I cut). The cutting teeth fixed in the intermaxillary
bones of the Mammalia, and the corresponding teeth in the lower jaw.

INEQUILATERAL. Having the two sides unequal, as in the case of the shells of
the ordinary bivalves (Lamellibranchiata). When applied to the shells of
the Foraminifera, it implies that the convolutions of the shell do not lie in
the same plane, but are obliquely wound rcund an axis.

INEQUIVALVE. Composed of two unequal pieces or valves.

INOCERAMUS (Gr. 7s, a fibre ; keramos, an earthen vessel). An extinct genus of
Bivalve Molluscs.

Insecta (Lat. ixseco, I cut into). The class of articulate animals commonly
known as Insects.

INSECTIVORA (Lat. insectum, an insect ; voro, I devour). An order of Mammals.

INsEcTIvorous. Living upon Insects.

INSESSORES (Lat. zxsedeo, I sit upon). The order of the Perching Birds, often
called Passeres.

INTERAMBULACRA. The rows of plates in an Echinoid which are not per-
forated for the emission of the ‘‘ tube-feet.”

INTERMAXILLA or PREMAXILLH. The two bones which are situated between
the two superior maxille in Vertebrata. In man, and some monkeys, the
premaxille anchylose with the maxille, so as to be irrecognisable in the
adult.

INVERTEBRATA (Lat. in, without; vertebra, a bone of the back). Animals
without a spinal column or backbone.

IsopoDA (Gr. isos, equal; podes, feet). An order of Crustacea in which the
feet are like one another and equal.

Katnozoic (Gr. kainos, recent ; zoe, life). The Tertiary period in Geology
comprising those formations in which the organic remains approximate
more or less closely to the existing fauna and flora.

LABYRINTHODONTIA (Gr. laburinthos, a labyrinth ; odows, tooth). An extinct
vet of Amphibia, so called from the complex microscopic structure of the
teeth.

LACERT?LIA (Lat. lacerta, alizard). An order of Reptilia comprising the Liz-
ards and Slow-worms.

LAMELLIBRANCHIATA (Lat. lamella, a plate; Gr. bragchia, gill). The class of
Mollusca comprising the ordinary bivalves, characterised by the possession
of lamellar gills.

LEPIDODENDRON (Gr. lepis, ascale ; dendron, atree). A genus of extinct plants,
5 named from the scale-like scars upon the stem left by the falling off of the
eaves.

388 GLOSSARY.

LEpmpopTERA (Gr. lepis, a scale; pteron, a wing). An order of Insects, com-
prising Butterflies and Moths, characterised by possessing four wings which
are usually covered with minute scales.

LEPIDOSIREN (Gr. lepis, a scale ; seirén, a siren—the generic name of the Mud-
oe Stren lacertina). A genus of Dipnoous fishes, comprising the ‘‘ Mud-
fishes.”

LEPIDOSTROBUS (Gr. lepis,a scale ; strobilos, a fir-cone). A genus founded on
the cones of Lepidodendron.

Leprana (Gr. leptos, slender). A genus of Brachiopods.

LincuLa (Lat. lingula, a little tongue). A genus of Brachiopods.

LYCOPODIACE# (Gr. lupos, a wolf; pous, foot). The group of Cryptogamic
plants generally known as ‘‘ Club-mosses.”

MACHAZRACANTHUS (Gr. machaira, a sabre; ccantha, thorn or spine). An ex-
tinct genus of Fishes.

MACHAIRODUS (Gr. machaira, a sabre ; odous, tooth). An extinct genus of
Carnivora.

MACROTHERIUM (Gr. makros, long; thérion. beast). An extinct genus cf
Edentata.

Macroura (Gr. makros, long; oura, tail). A tribe of Decapod Crustaceans with
long tails (e.g., the Lobster, Shrimp, &c.)

MAMMALIA (Lat. mamma, the breast). The class of Vertebrate animals which
suckle their young.

MANDIBLE (Lat. mandibulum, a jaw). The upper pair of jaws in Insects; also
applied to one of the pairs of jaws in Crustacea and Spiders, to the beak of
Cephalopods, the lower jaw of Vertebrates, &c. :

MANTLE. The external integument of most of the Mollusca, which is largely
developed, and forms a cloak in which the viscera are protected. Techni-
cally called the ‘‘ pallium.”

Manus (Lat. the hand), The hand of the higher Vertebrates.

MARSIPOBRANCHIT (Gr. marsipos, a pouch; bragchia, gill). The order of
Fishes comprising the Hag-fishes and Lampreys, with pouch-like gills.

MARSUPIALIA (Lat. marsupium, a pouch). An order of Mammals in which the
females mostly have an abdominal pouch in which the young are carried.

MAastTopDON (Gr. mastos, nipple ; odows, tooth). An extinct genus of Elephant-
ine Mammals.

MrGALONYX (Gr. megas, great; onux, nail). An extinct genus of Edentate
Mammals.

MEGALOSAURUS (Gr. megas, great; saura, lizard). A genus of Deinosaurian
Reptiles. !

MEGATHERIUM (Gr. megas, great; thérion, beast). An extinct genus of
Edentata.

Mesozoic (Gr. mesos, middle ; and zoe, life). The Secondary period in Geology.

MICROLESTES (Gr. mikros, little ; /éstes, thief). An extinct genus of-Triassic
Mammals.

MILLEpora (Lat. mille, one thousand ; porvs, a pore). A genus of ‘‘ Tabulate
Corals.”

MIOCENE (Gr. meion, less; kainos, new). The Middle Tertiary period.

Motars (Lat. mola, a mill). The ‘‘ grinders” in man, or the teeth in diphyo-
dont Mammals which are not preceded by milk-teeth.

Motzvsca (Lat. mollis, soft). The sub-kingdom which includes the Shell-fish
proper, the Polyzoa, the Tunicata, and the Lamp-shells ; so called from the
generally soft nature of their bodies.

Mottuscorpa (Mollusca ; Gr. eidos, form). The lower division of the Mol-
lusca, comprising the Polyzoa, Tunicata, and Brachiopoda.

MonocraPptus (Gr. monos, single ; grapho, I write). A genus of Graptolites.

MYLoDoN (Gr. mulos, a mill; odouws, tooth). An extinct genus of Edentate ~

Mammals.

MyrIapopDa or MYyRIOPODA (Gr. murios, ten thousand ; podes, feet). A class
of Arthropoda comprising the Centipedes and their allies, characterised by
their numerous feet.

GLOSSARY. 389

NATATORES (Lat. nave, to swim). The order of the Swimming Birds.

Natatory (Lat. nare, to swim). Formed for swimming.

NavtiLom. Resembling the shell of the Nautilus in shape.

NERVURES (Lat. nervus, a sinew). The ribs which support the membranous
wings of insects.

NEUROPTERA (Gr. newron, a nerve ; pteron, a wing). An order of Insects char-
acterised by four membranous wings with numerous reticulated nervures
(e.g., Dragon-tflies).

NEUROPTERIS (Gr. neuron, a nerve; pteris, a fern). An extinct genus of
Ferns.

nuns (Gr. nothos, spurious ; saura, lizard). A genusof Plesiosaurian
Reptiles.

NoTOCHORD (Gr. notos, back ; chorde, string). A cellular rod which is devel-
oped in the embryo of Vertebrates immediately beneath the spinal cord, and
which is usually replaced in the adult by the vertebral column. Often it is
spoken of as the “ chorda dorsalis.”

NUDIBRANCHIATA (Lat. nudus, naked; and Gr. bragchia, gill). An order of
the Gasteropoda in which the gills are naked.

NUMMULINA (Lat. nwmmus, acoin). A genus of Foraminifera, comprising the
coin-shaped ‘‘ Nummulites.”

OBOLELLA (Lat. dim. of obolus, a small coin). An extinct genus of Brachio-

ods.

oe Connected with the occiput, or the back part of the head.

Oceanic. Applied to animals which inhabit the open ocean (= pelagic).

ODONTOPTERYX (Gr. odous, tooth; pterux, wing). An extinct genus of
Birds.

ODONTORNITHES (Gr. odows, tooth; ornis, bird). The extinct order of Birds,
comprising forms with distinct teeth in sockets.

OLIGOCENE (Gr. oligos, few ; kainos, new). A name used by many Continental
geologists as synonymous with the Lower Miocene.

Opuntia (Gr. ophis, a serpent). The order of Reptiles comprising the Snakes.

OPHIUROIDEA (Gr. ophis, snake 3 owra, tail ; eidos, form), An order of Echino-
dermata, comprising the Brittle-stars and Sand-stars.

ORNITHOSCELIDA (Gr. ornis, bird; skelos, leg). Applied by Huxley to the
Deinosaurian Reptiles, together with the genus Compsognathus, on account
of the bird-like character of their hind-limbs.

OrTHIS (Gr. orthos, straight). A genus of Brachiopods, named in allusion to the
straight hinge-line.

ORTHOCERATIDA (Gr. orthos, straight; keras, horn). A family of the Nau-
tilide, in which the shell is straight, or nearly so.

ORTHOPTERA (Gr. orthos, straight ; pteron, wing). An order of Insects.

OSTEOLEPIS (Gr. osteon, bone; lepis, scale). An extinct genus of Ganoid
Fishes.

OstracopDa (Gr. ostrakon, a shell). An order of small Crustaceans which are
enclosed in bivalve shells.

Otopus (Gr. ofa, ears; odous, tooth). An extinct genus of Sharks,

OUDENODON (Gr. ouden, none; odous, tooth). A genus of Dicynodont Rep-
tiles.

OviBos (Lat. ovis, sheep ; bos, ox). The genus comprising the Musk-ox.

PACHYDERMATA (Gr. pachus, thick; derma, skin). An old Mammalian order
constituted by Cuvier for the reception of the Rhinoceros, Hippopotamus,
Elephant, &c.

ee (Gr. palaios, ancient; aster, star). An extinct genus of Star-
fishes.

PALH#OCARIS (Gr. palaios, ancient ; karis, shrimp), An extinct genus of Deca-
pod Crustaceans.

PALAOLITHIC (Gr. palaios, ancient; lithos, stone). Applied to the rude stone
implements of the earliest known races of men, to the men who made these
implements, or to the period at which they were made.

390 GLOSSARY.

PALZONTOLOGY (Gr. palaios, ancient ; and dogos, discourse). The science of
fossil remains or of extinct organised beings.

pete (Gr. palaios, ancient ; ophis, serpent). An extinct genus of
Snakes.

PALZOSAURUS (Gr. palaios, ancient ; saura, lizard). A genus of Thecodont
Reptiles.

PALHOTHERIDA (Gr. palaios, ancient; ther, beast). A group of Tertiary
Ungulates.

PaLzZ0Zolc (Gr. palaios, ancient ; and zoe, life). Applied to the oldest of the
great geological epochs.

PARADOXIDES (Lat. paradoxus, marvellous). A genus of Trilobites.

PaTAGIUM (Lat. the border of a dress). Applied to the expansion of the in-
tegument by which Bats, Flying Squirrels, and other animals support them-
selves in the air.

PECOPTERIS (Gr. peko, | comb; pteris,afern). An extinct genus of Ferns.

aa (Lat. a comb). The genus of Bivalve Molluscs comprising the

callops.

PECTORAL (Lat. pectus, chest). Connected with, or placed upon, the chest.
PENTACRINUS (Gr. penta, five; krinon, lily). A genus of Crinoids in which
the column is five-sided. :
PENTAMERUS (Gr. penta, five; meros, part). An extinct genus of Brachiopods.
PENTREMITES (Gr. penta, five; trema, aperture). A genus of Blastoidea, so
named in allusion to the apertures at the summit of the calyx. :
PERENNIBRANCHIATA (Lat. perennis, perpetual ; Gr. bragchia, gill). Applied
to those Amphibia in which the gills are permanently retained throughout

life.

PERISSODACTYLA (Gr. gerissos, uneven ; daktulos, finger). Applied to those
Hoofed Quadrupeds (Ungulata) in which the feet have an uneven number of
toes.

PreTaLormD. Shaped like the petal of a flower.

Puacops (Gr. phaké, a lentil; ops, the eye). A genus of Trilobites.

PHALANGES (Gr. phalanx, arow). The small bones composing the digits of
the higher Vertebrata. Normally each digit has three phalanges.

PHANEROGAMS (Gr. phaneros, visible ; gamos, marriage). Plants which have
the organs of reproduction conspicuous, and which bear true flowers.

PHARYNGOBRANCHII (Gr. pharugz, pharynx; bragchia, gill). The order of
Fishes comprising only the Lancelet.

PHASCOLOTHERIUM (Gr. phaskolos, a pouch; thérion, a beast). A genus of
Oolitic Mammals.

PHRAGMACONE (Gr. phragma, a partition ; and konos,a cone). The chambered
portion of the internal shell of a Belemnite.

PHYLLOPODA (Gr. phullon, leaf; and pous, foot). An order of Crustacea.

PINNATE (Lat. pinna, a feather). Feather-shaped; or possessing lateral pro-
cesses.

PINNIGRADA (Lat. pinna, a feather ; gradior, I walk). The group of Carniv-
ora, comprising the Seals and Walruses, adapted for an aquatic life. Often
called Pinnipedia.

PINNULZ (Lat. dim. of pinna). The lateral processes of the arms of Crinoids.

Pisces (Lat. piscis, a fish’. The class of Vertebrates comprising the Fishes.

PLACOID (Gr. plaz, a plate; eidos, form). Applied to the irregular bony
plates, grains, or spines which are found in the skin of various fishes
(Elasmobranchii).

PLAGIOSTOMI (Gr. plagios, transverse ; stoma, mouth). The Sharks and Rays,
in which the mouth is transverse, and is placed on the under surface of the
head.

PLATYCERAS (Gr. platus, broad; keras, horn). A genus of Univalve Molluscs.

PLATYCRINUS (Gr. platus, broad; krinon, lily). A genus of Crinoidea.

PLATYRHINA (Gr. platus, broad ; rhines, nostrils). A group of the Quadrumana.

PLaATYSOMUS (Gr. platus, wide ; soma, body). A genus of Ganoid Fishes. ~

PLEISTOCENE (Gr. pleistos, most; kainos, new). Often used as synonymous
with “ Post-Pliocene.”

GLOSSARY. 391

PLEUROTOMARIA (Gr. pleura, the side; tomé, notch). A genus of Univalve
shells.

PLIOCENE (Gr. pleion, more ; kainos, new). The later Tertiary period.

PLIOPITHECUS (Gr. pleion, more ; pithekos, ape). An extinct genus of Monkeys.

PLIosauRUS (Gr. pletion, more; saura, lizard), A genus of Plesiosaurian
Reptiles.

PotycystTiIna (Gr. polus, many ; and kustis, a cyst). An order of Protozoa
with foraminated siliceous shells.

PotypaRy. The hard chitinous covering secreted by many of the Hydrozoa.

POLYPE (Gr. polus, many ; pous, foot). Restricted to the single individual of
a simple Actinozoén, such as a Sea-anemone, or to the separate zooids of a
compound Actinozoén. Often applied indiscriminately to any of the Celen-
terata, or even to the Polyzoa.

Potypora (Gr. polus, many; poros, a passage). A genus of Lace-corals
(Fenestellide).

POLYTHALAMOUS (Gr. polus ; and thalamos, chamber). Having many chambers ;
applied to the shells of Foraminifera and Cephalopoda.

PoLyzoa (Gr. polus; and zoén, animal). A division of the Molluscoida com-
prising compound animals, such as the Sea-mat—sometimes called Bryozoa.

PORIFERA (Lat. porus,a pore ; and fero, I carry). Sometimes used to desig-
nate the Foraminifera, or the Sponges.

' PREMOLARS (Lat. pre, before; molares, the grinders). The molar teeth of
Mammals which succeed the molars of the milk-set of teeth. In man, the
bicuspid teeth.

PROBOSCIDEA (Lat. proboscis, the snout). The order of Mammals comprising
the Elephants.

Proce ous (Gr. pro, before ; koilos, hollow). Applied to vertebre the bodies
of which are hollow of concave in front.

Propucta (Lat. productus, drawn out or extended). An extinct genus of
Brachiopods, in which the shell is ‘‘ eared,” or has its lateral angles drawn
out.

PROTICHNITES (Gr. protos, first; ichnos, footprint). Applied to certain im-
pressions in the Potsdam sandstone of North America, believed to have
been produced by large Crustaceans.

PROTOPHYTA (Gr. protos ; and phuton, plant). The lowest division of plants.

PROTOPLASM (Gr, protos ; and plasso, | mould). The elementary basis of or-
ganised tissues. Sometimes used synonymously for the ‘‘sarcode” of the
Protozoa.

PROTOROSAURUS Or PROTEROSAURUS (Gr. protos, first ; orao, I see or discover;
saura, lizard: or proteros, earlier; sawra, lizard). A genus of Permian
lizards.

Protozoa (Gr. protos; and zoén, animal). The lowest division of the animal
kingdom.

PSAMMODUS (Gr. psammos,.sand ; odous, tooth). An extinct genus of Cestra-
ciont Sharks.

PsEubDopopia (Gr. pseudos, falsity; and pous, foot). The extensions of the
body-substance which are put forth by the Rhizopoda at will, and which
serve for locomotion and prehension.

PsILOPHYTON (Gr. psilos, bare; phuton, plant). An extinct genus of Lyco-
podiaceons plants.

PTERANODON (Gr. pteron, wing ; a, without; odows, tooth). A genus of Ptero-
saurian Reptiles,

PTERASPIS (Gr. pteron, wing; aspis, shield). A genus of Ganoid Fishes.

PTERICHTHYS (Gr. pteron, wing ; ichthus, fish). A genus of Ganoid Fishes.

poe (Gr. pleron, wing ; daktulos, finger). A genus of Pterosaurian

teptiles.

PTEROPODA (Gr. pteron, wing ; and pous, foot). A class of the Mollusca which
swim by means of fins attached near the head.

PTEROSAUBIA (Gr. pteron, wing ; sawra, lizard). An extinct order of Reptiles.

PTILODIcTYA (Gr. ptilon, a feather; diktuon, a net), An extinct genus of
Polyzoa,

392 GLOSSARY.

PrycHocERAS (Gr. ptuché, a fold; keras, ahorn). A genus of Ammonitide.
PULMONATE. Possessing lungs.
PYRIFORM (Lat. pyrus, a pear; and forma, form). Pear-shaped.

QUADRUMANA (Lat. guatuor, four ; manus, hand). The order of Mammals
comprising the Apes, Monkeys, Baboons, Lemurs, &c.

RapD1ata (Lat. radius, a ray). Formerly applied to a large number of animals
which are now placed in separate sub-kingdoms (e.g., the Celenterata, the
Echinodermata, the Infusoria, &c.)

RADIOLARIA (Lat. radius, aray). <A division of Protozoa.

Ramus (Lat. a branch). Applied to each half or branch of the lower jaw, or
mandible, of Vertebrates.

RaPToREs (Lat. vapto, I plunder). The order of the Birds of Prey.

RasorESs (Lat. vado, I scratch). The order of the Scratching Birds (Fowls,
Pigeons, &c.)

RECEPTACULITES (Lat. receptaculum, a storehouse). An extinct genus of
Protozoa.

REPTILIA (Lat. repto, I crawl). The class of the Vertebrata comprising the
Tortoises, Snakes, Lizards, Crocodiles, &c.

RETEPORA (Lat. veté, a net ; porws, a pore). A genus of Lace-corals (Polyzoa).

RHAMPHORHYNCHUS (Gr. rhamphos, beak; rhugchos, nose). A genus of
Pterosaurian Reptiles.

RHINOCEROS (Gr. rhis, the nose; keras, horn). A genus of Hoofed Quadru-
peds.

RHIZOPODA (Gr. rhtza, a root; and pous, foot). The division of Protozoa com-
prising all those which are capable of emitting pseudopodia.

RHYNCHOLITES (Gr. rhugchos, beak; and lithos, stone). Beak-shaped fossils
consisting of the mandibles of Cephalopoda.

RHYNCHONELLA (Gr. riugchos, nose or beak). A genus of Brachiopods.

RODENTIA (Lat. odo, I gnaw). An order of the Mammals; often called Glires
(Lat. glzs, a dormouse).

Rota. (Lat. vota, a wheel). A genus of Foraminifera.

Rueosa (Lat rugosus, wrinkled). An order of Corals.

RUMINANTIA (Lat. ruminor, I chew the cud). The group of Hoofed Quadru-
peds (Ungulata) which ‘‘ ruminate”’ or chew the cud.

SARCODE (Gr. sarz, flesh; eidos, form). The jelly-like substance of which the
bodies of the Protozoa are composed. It is an albuminous body containing

_ oil-granules, and is sometimes called ‘‘ animal protoplasm.”

SAURIA (Gr. saura, a lizard). Any lizard-like Reptile is often spoken of as a
‘‘Saurian ;”’ but the term is sometimes restricted to the Crocodiles alone,
or to the Crocodiles and Lacertilians.

SAUROPTERYGIA (Gr. saura ; pterux, wing). An extinct order of Reptiles,
called by Huxley Plestosauria, from the typical genus Plesiosaurus.

SAURURZ (Gr. saura; oura, tail). The extinct order of Birds comprising
only the Archeopteryz.

SCANSORES (Lat. scando, I climb). The order of the Climbing Birds (Parrots,
Woodpeckers, &c.)

SCAPHITES (Lat. scapha, a boat). A genus of the Ammonitide.

ScoLituus (Gr. skolex, a worm ; lithos, a stone). The vertical burrows of sea-
worms in rocks.

Scuta (Lat. scutwm, a shield). Applied to any shield-like plates ; especially to
those which are developed in the integument of many Reptiles.

SELACHIA or SELAcHTI (Gr. selachos, a cartilaginous fish, probably a shark).
The sub-order of Elasmobranchii comprising the Sharks and Dog-fiskes.

SEPIOSTAIRE. The internal shell of the Sepia, commonly known as the
““cuttle-bone.”’ ;

SEPTA. Partitions.
SERPENTIFORM. Resembling a serpent in shape. -
SERTULARIDA (Lat. sertum, a wreath). An order of Hydrozoa.

ieee

GLOSSARY. 393

SESSILE (Lat. sedo, I sit), Not supported upon a stalk or peduncle; attached
by a base.

Ser (Lat. bristles). Bristles or long stiff hairs.

SIGILLARIOIDS (Lat. szgilla, little images). A group of extinct plants of nine
Sigillaria is the type, so called from the seal-like markings on the bark.

SILICEOUS (Lat. szdex, flint). Composed of flint.

SINISTRAL (Lat. sinistrd, the left hand). Left-handed ; applied to the direc-
tion of the spiral in certain shells, which are said to be ‘‘ reversed.”

SIPHON (Gr. a tube). Applied to the respiratory tubes in the Mollusca ;
also to other tubes of different functions.

SIPHONIA (Gr. siphon, atube). A genus of fossil Sponges.

SIPHONOSTOMATA (Gr. siphon ; and stoma, mouth). The division of Glastero-
podous Molluscs in which the aperture of the shell is not ‘‘ entire,” but
possesses a notch or tube for the emission of the respiratory siphon.

SIPHUNCLE (Lat. siphunculus, a little tube). The tube which connects to-
gether the various chambers of the shell of certain Cephalopoda (e.g., the
Pearly Nautilus).

STRENIA (Gr. seiven, a mermaid). The order of Mammalia comprising the
Dugongs and Manatees.

SIVATHERIUM (Siva, a Hindoo deity ; Gr. thérion, beast). An extinct genus
of Hoofed Quadrupeds.

SOLIDUNGULA (Lat. solidus, solid; wngula, a hoof), The group of Hoofed
Quadrupeds comprising the Horse, Ass, and Zebra, in which each foot has
only a single solid hoof. Often called Solipedia.

SPHENOPTERIS (Gr. sphén, a wedge; pteris, a fern). An extinct genus of
ferns.

SPICULA (Lat. speculum, a point). Pointed needle-shaped bodies.

SPIRIFERA (Lat. spira, a spire or coil; jfero, I carry). An extinct genus of
Brachiopods, with large spiral supports forthe ‘‘arms.’

SPIRORBIS (Lat. spira, a spire ; orbzs, a circle). A genus of tube-inhabiting
Annelides, in which the shelly tube is coiled into a ‘spiral disc.

SPONGIDA (Gr. spoggos, asponge). The division of Protozoa commonly known
as sponges.

StaLactites (Gr. stalasso, I drop). Icicle-like encrustations and deposits of
lime, which hang from the roof of caverns in limestone.

STALAGMITE (Gr. stalagma, a drop). Encrustations of lime formed on the floor
of caverns which are hollowed out of limestone.

STIGMARIA (Gr. stigma, a mark made with a pointed instrument). A genus
founded on the roots of various species of Sigillaria.

STRATUM (Lat. stratus, spread out ; or stratum, a thing spread out). A layer
of rock.

STROMATOPORA (Gr. stroma, a thing spread out ; poros, a passage or pore). A
Paleozoic genus of Protozoa.

'STROPHOMENA (Gr. strophao, I twist; méné, moon).. An extinct genus of
Brachiopods.

SUB-CALCAREOUS. Somewhat calcareous.

SUB-CENTRAL. Nearly central, but not quite. é

SUTURE (Lat. suo, I sew). The line of junction of two parts which are immov-
ably connected together. Applied to the line where the whorls of a univalve
shell join one another ; also to the lines made upon the exterior of the shell
of a chambered C ephalopod. by the margins of the septa.

SYRINGOPORA (Gr. surigz, a pipe ; poros,a pore). A genus of Tabulate Corals.

TABUL& (Lat. tabula, a tablet). Horizontal plates or floors found in some
Corals, extending across the cavity of the ‘‘ theca”’ from side to side.

TEGUMENTARY (Lat. tegumentum, a covering), Connected with the integu-
ment or skin.

TELEOSAURUS (Gr. teleios, perfect ; sawra, lizard). An extinct genus of Cro-
codilian Reptiles.

eae (Gr. teleios, perfect; osteon, bone). The order of the ‘Bony
Fishes,”

304 GLOSSARY.

TeLson (Gr. a limit). The last joint in the abdomen of Crustacea; va-
riously regarded as a segmer without appendages, or as an azygous
appendage.

TENTACULITES (Lat. fentaculuwm, a feeler). A genus of Pteropoda,

'TEREBRATULA (Lat. terebratus, bored or pierced). A genus ot Brachiopoda, so
called in allusion to the perforated beak of the ventral valve.

Test (Lat. testa, shell). The shell of Mollusca, which are for this reason
sometimes called ‘‘ Testacea ;” also, the calcareous case of Echinoderms ;
also, the thick leathery outer tunic in the Tunicata.

TesTacEous. Provided with a shell or hard covering.

TESTUDINID& (Lat. testudo, a tortoise). The family of the Tortoises.

TETRABRANCHIATA (Gr. tetra, four ; bragchia, gill). The order of Cephalopoda
characterised by the possession of four gills.

TEXTULARIA (Lat. textilis, woven). A genus of Foraminifera.

THECA (Gr. théké, asheath). A genus of Pteropods.

THECODONTOSAURUS (Gr. théké, a sheath; odous, tooth; saura, lizard). A
genus of ‘“‘Thecodont ” Reptiles, so named in allusion to the fact that the
teeth are sunk in distinct sockets.

THERIODONT (Gr. thérion, a beast ; odous, tooth). A group of Reptiles so
named by Owen in allusion to the Mammalian character of their teeth.

THORAX (Gr. a breastplate). The region of the chest.

aes (Gr. thulakos, a pouch; leo, alion). An extinct.genus of Mar-
supials.

TRIGONIA (Gr. treis, three ; gonia, angle). A genus of Bivalve Molluscs.

TRIGONOCARPON (Gr. ¢reis, three; gonia. angle; karpos, fruit). A genus
founded on fossil fruits of a three-angled form.

TRILOBITA (Gr. treis, three ; lobos,a lobe). An extinct order of Crustaceans.

TRINUCLEUS (Lat. tris, three ; nucleus, a kernel). A genus of Trilobites.

TROGONTHERIUM (Gr. trogo, | gnaw; thérion, beast). An extinct genus of
Beavers.

TuBicoLa (Lat. tuba, a tube; and colo, I inhabit). The order of Annelida
which construct a tubular case in which they protect themselves.

TuBIcoLous. Inhabiting a tube.

Tunicata (Lat. tunica, a cloak). A class of Molluscoida which are enveloped
in a tough leathery case or ‘‘ test.”

TURBINATED (Lat. turbo, atop). Top-shaped ; conical with a round base.

TURRILITES (Lat, turris, a tower). A genus of the Ammonitide.

Umpo (Lat. the boss of a shield), The beak of a bivalve shell.

UNGUICULATE (Lat. unguis, nail). Furnished with claws.

Uneuxata (Lat. ungula, hoof). The order of Mammals comprising the Hoofed
Quadrupeds.

UnevLaTE. Furnished with expanded nails constituting hoofs.

UNILOCULAR (Lat. wnus, one; and loculus. a little purse). Possessing a single
cavity or chamber. Applied to the shells of Foraminifera and Mollusca.
UNIVALVE (Lat. uwnus, one; valve, folding-doors). A shell composed of a

single piece or valve.
UropeEra (Gr. owra, tail ; delos, visible). The order of the Tailed Amphibians
(Newts, &c.)

ae (Lat. venter, the stomach). Relating to the inferior surface of the

ody.

Ree cures (Lat. ventriculum, a little stomach). A genus of siliceous

_ Sponges.

VERMIFORM (Lat. vermis, worm; and forma, form). Worm-like.

VERTEBRA (Lat. verto, I turn). One of the bony segments of the vertebral
column or backbone.

VERTEBRATA (Lat. vertebra, a bone of the back, from vertere, to turn). The
division of the Animal Kingdom roughly characterised by the possession of
a backbone,

VESICLE (Lat. vesica, a bladder). A little sac or cyst.

GLOSSARY. __ 305

Wauort. The spiral turn of a univalve shell.

XipHosuRA (Gr. xiphos, a sword ; and oura, tail). An order of Crustacea,
comprising the Limuli or King-Crabs, characterised by their long sword-
like tails. ‘

XYLOBIUS (Gr. zulon, wood ; bios, life). An extinct genus of Myriapods,
named in allusion to the fact that the animal lived on decaying wood.

ZAPHRENTIS (proper name). A genus of Rugose Corals.

ZEUGLODONTID& (Gr. zeuglé, a yoke ; odous, a tooth). An extinct family of
Cetaceans, in which the molar teeth are two-fanged, and Jook as if composed
of two parts united by a neck.

ZOOPHYTE (Gr. zoén, animal ; phuton, plant). loosely applied to many plant-
like animals, such as Sponges, Corals, Sea-anemones, Sea-mats, &c.

INDEX.

Acadian Group, 79.
Acer, 308.
Acervularia, 119, 173.
Acidaspis, 123.
Acorn-shells, 267.
Acroculia, 128.
Acrodus, 214, 242, 275;
Acrotreta, 110.
Acroura, 120.
Actinocrinus,
glina, 108.
LEipiornis, 348.
Agnostus, 85-87, 108 ;
Alces malchis, 354.
Alecto, 108.
Alethopteris, 136, 165, 196.
Alge (see Sea-weeds).
Alligators, 218, 297.
Alnus, 262.
Amblypterus, 188;
Ambonychia, 111.
Ammonites, 187, 212-214, 237-239. 272;
Humphresianus, 238 ; bifrons. 223.

Ammonitide, 239, 272, 285, 294.

Amphibia, 189; of the Carboniferous,
189-191; of the Permian, 200; of the
Trias, 215-217 ; of the Jurassic, 242; of
the Miocene, 313.

Amphicyon, 322.

Aimphilestes, 253.

Amphispongia, 118.

Amphistegina, 311.

Amphitherium, 253 255

Amphitragulus, 317.

Amplexus, 173; coratloides, 174.

Ampyx, 108.

Ananchytes, 266.

Anchitherium, 301, 302.

Ancyloceras, 272, 273;
273.

Ancylotherium Pentelici, 315.

Andrias Scheuchzeri, 313, 314.

Angiosperms, 261, 262.

Animal Kingdom, divisions of, 375-378.

Anisopus, 206.

Annelida, of the Cambrian period, 82,
83; of the Lower Silurian, 107; of the
Upper Silurian, 122, 123; of the De-
vonian, 143, 144; of the Carboniferous,
178.

Annularia, 137, 196, 207.

nobilis, 242.
175.

rex, 85.

macropterus, 188.

; Prevostit, 254.

Matheronianus,

Anomodontia, 220.

Anoplotheride, 302.

Anoplotherium, 302, 303 ; commune, 303.

Ant-eaters, 299, 315, 349, 350, 353.

Antelopes, 317.

Anthracosaurus Russelli, 190.

Anthrapalemon gracilis, 180.

Anftilocapra, 318.

Antilope quadricornis, 318.

Antwerp Crag, 325.

Apes, 323.

Apiocrinus, 231.

Apteryxz, 346, 348.

Aqueous rocks, 15.

Arachnida of the Coal-measures, 181.

Aralo-Caspian Beds, 326.

Araucaria, 262.

Araucarioxylon, 170.

Arca, 198; antiqua, 199.

Archeocidaris, 178.

Archeocyathus, 82.

Archeopteryx, 252, 281;
25S:

Archeospherine, 75.

Archimedes, 184; Wortheni, 183.

Archiulus, 182.

Arctic regions, Miocene flora of, 310.

Arctocyon, 304.

Arenaceous rocks, 20.

Arenicolites, 83 ; didymus, 88.

Arenig rocks, 92, 94.

Argillaceous rocks, 20.

Armadillos, 299, 351, 353.

Artiodactyle Ungulates, 300, 317.

Asaphus, 108; tyrannus, 107, 108.

A scoceras, 130.

A spidella, 76.

Aspidura loricata, 210.

Astarte borealis, 338.

Asterophyllites, 137, 196.

A sterosteus, 152.

Astreide, 231.

Astreospongia, 118, 139. ‘*

Astylospongia, 98 ; preemorsa, 9 98.

Athyris, 110, 127, 147, 198 ; subtilita, 185.

Atlantic Ooze, 22, 23.

Atrypa, 127; congesta, 127; hemisphee-
rica, 127 ; reticularis, 147, 148.

Auger-shells, 293.

Aurochs, 356.

Aves (see Birds}

macrura, 252,

INDEX.

Avieula, 235; contorta, 211, 212; socialis,
Ark.

« Avieula contorta Beds,” 204, 212.
Aviculide, 198, 269.
Aviculopecten, 186.

Azxophyllum, 173.

Aymestry Limestone, 116, 117.
Azoic rocks, 67.

Baculites, 273; anceps, 274.

Bagshot and Bracklesham Beds, 287.

Bakewellia, 198.

Baleena, 315.

Bala Group, 93, 94.

Bala Limestone, 93.

Balanide, 267.

Banksia, 262, 308.

Barbadoes Earth, 33.

Barnacles, 267.

Bath Oolite, 227.

Bats, 304, 322.

Bears, 330, 359.

Beaver, 322, 336.

Beetles, 182, 311.

Belemnitella mucronata, 275.

Belemnites, 214, 240, 274; canaliculatus,
241.

Belemnitide, 240, 285.

Belemnoteuthis, 240.

Belinurus, 179.

Bellerophon, 111, 129, 148, 186; Argo, 111.

Belodon, 218; Carolinensis, 219.

Belosepia, 295.

Beloteuthis subcostata, 239, 240.

Bembridge Beds, 288.

Beryx, 276; Lewesiensis, 276.

Beyrichia, 107; complicata, 107.

Bird’s-eye Limestone, 95, 96.

Birds, of the Trias, 222; of the Jurassic,
251-253; of the Cretaceous, 281, 282; of
the Eocene, 297; of the Post-Pliocene,
345-348.

Bison priscus, 356.

Bituminous Schists of Caithness, 36.

Bivalves (see Lamellibranchiata).

Black-lead (see Graphite).

Black-River Limestone, 95, 96.

Blastoidea, 176; of the Devonian, 143;
of the Carboniferous, 176.

Boide, 296.

Bolderberg Beds, 307.

Bone-bed, of the Upper Ludlow, 116; of
the Trias, 224.

Bony Fishes (see Teleostean Fishes).

Bos primigenius, 356; taurus, 356.

Boulder-clay, 337.

Bourgueticrinus, 266.

Bovey-Tracy Beds, 305, 309.

Brachiopoda, 125; of the Cambrian rocks,
87; of the Lower Silurian, 108-110; of
the Upper Silurian, 125-128; of the De-
vonian, 147, 148; of the Carboniferous,
184-186 ; of the Permian, 198; of the
Trias, 211; of the Jurassic, 234; of the
Cretaceous, 268; of the Eocene, ’299,

Brachymetopus, 179.

Brachyurous Crustaceans, 180, 197.

Bradford Clay, 227.

Breaks in the Geological and Palzonto-
logical record, 44-52.

Breccia, 19.

Brick-earths, 339

o7

_ Cambrian period,

397

Bridlington Crag, 325, 326, 336.
Brittle-stars (see Ophiuroidea).
Bronteus, 145.

Brontotheride, 316.
Brontotherium ingens, 316.
Brontozoum, 206.

Buccinum, 237.

Bucklandia, 230.

Bulimus, 294.

Bunter Sandstein, 203, 204, 206.
Butterflies, 233, 311.
Byssoarea, 198.

Cainozoic (see Kainozoic).

Calamaries, 239.

Calamites, 165, 166, 196; canneeformis,
166.

Caleaire Grossier, 287, 288.

Calcareous rocks, 20-32; Tufa, 21.

Calciferous Sand-rock, 95, 96.

Calveria, 178.

Calymene, 108, 123; Blumenbachii, 107.

Camarophoria globulina, 198.

77-90; rocks of, in
Britain, 77, 78; in Bohemia, 79; in
North America, 79; life of, 80- 90.

Camelopardalide, 317.

Camels, 317, 354.

Canis lupus, 336; Parisiensis, 304.

Caradoc rocks, 98, 94, 96.

Carbon, origin of, 36.

Carboniferous Limestone, 157, 158.

Carboniferous period, 157-192; rocks of,
157-160 ; life of, 160-191.

Carboniferous Slates of Ireland, 135, 158,
159.

Carcharias, 275.

Carcharodon, 295, 312; productus, 313.

Cardinia, 235.

Cardiocarpon, Bi:

Cantina, 128; jfibrosa, 128; imterrupta,
128

Cardita, 213, 292; planicosta, 292, 293.
Cardium, 292 : Rheticum, 211, 212.
Caribou, 355.

Carnivora, of the Eocene, 304; of the
Miocene, 322; of the Pliocene, 330, Balk
of the Post- Pliocene, 359-361.

Caryocaris, 107, 108.

Caryocrinus ornatus, 106.

Castor fiber, 336.

Castoroides Ohioensis, 361.

Catastrophism, theory of, 3.

Catopterus, 214.

Cauda-Galli Grit, 135, 137.

Caulopteris, 136, 164.

Cave-bear, 360.

Cave-deposits, 337, 339, 341-344.

Cave-hyena, 360.

Cave-lion, 361.

Caves, formation of, 341 ; deposits in, 342.

Cavicornia, 317.

Cement-stones, 31.

Cephalaspis, 152.

Cephalopoda, of the Cambrian period, 88 ;
of the Lower Silurian, 111-114; of the
Upper Silurian, 130; of the Devonian,
149 ; of the Carboniferous, 186, 187; of
the Permian, 199; of the Trias, 212; of
the Jurassic, 237-240; of the Cretaceous,
272-275; of the Eocene, 294; of the
Miocene, 312.

398

Ceratiocaris, 108.

Ceratites, 212-214; nodosus, 212.

Ceratodus, 214; alius, 214; Fosteri, 214,
215, 255; serratus, 214.

Ceriopora, 145; Hamiltonensis, 146.

Cerithium, 213, 293; hexagonum, 294.

Cervide, of the Miocene period, 317; of
the Pliocene, 329; of the Post-Pliocene,
354, 355.

Cervus, 317 ; capreolus, 336, 354; elaphus,
336, 354; megaceros, 354, 355; taran-
dus, 354.

Cestracion Philippi, 188, 255.

Cestracionts, of the Devonian, 154; of the
Carboniferous, 188; of the Permian,
199; of the Trias, 214; of the Jurassic,
242; of the Cretaceous, 275.

Cetacea, 299; of the Hocene, 299; of the
Miocene, 315.

Cetiosaurus, 249, 25

Cheropotamus, 302.

Cheetetes, 105, 173;

Chain-coral, 119.

Chalk, 259; structure of, 21-23; Foramin-
ifera of, 22, 268; origin of, 28; with
flints, 259; without flints, 259.

Chama, 236.

Chamerops, 308; Helvetica, 309.

Chazy Limestone, 95, 96.

Cheiroptera, of the Eocene, 304, 305; of
the Miocene, 322.

Cheirotherium, 215, 216.

Cheirurus, 108, 123 ; bimucronatus, 124.

Chelichnus Duncani, 202.

Chelone Benstedi, 280; planiceps, 251.

Chelonia, of the Permian, 202; of the
Jurassic, 251; of the Cretaceous, 280 ;
of the Kocene, 296; of the Miocene, 213.

Chemnitzia, 213.

Chemung Group, 135, 136, 137.

Chert, 34.

Chillesford Beds, 325, 326, 336.

Chonetes, 127, 147, 184; Hardrensis, 185.

Chonoph yllum, 173.

Cidaris, 266.

Cincinnati Group, 95, 96.

Cinnamomum polymorphum, 309.

Cinnamon-trees, 262, 290, 306, 308, 309.

Cladodus, 188.

Claiborne Beds, 289.

Clathropora, 145; intertexta, 146.

Clay, 20; Red, origin of, 35

Clay-ironstone, nodules of, 31.

Cleidophorus, 111.

Cleodora, 312.

Climacograptus, 101, 119.

Clinton Formation, 116, 117.

Clisiophyllum, 173.

Clupeide, 276.

Clymenia, 149; Sedgwickii, 149.

Coal, 36; structure of, 163; mode of for-
mation of, 162.

Coal-measures, 159, 160; mineral char-
acters of, 159; mode of formation of,
160, 162; plants of, 162-170.

Coccoliths, 261.

Coccosteus, 151, 152.

Cochliodus, 188; contortus, 189.

Coleoptera, 182, 311.

Colossochelys Atlas, 313.

Columnaria, 105; alveolata, 105.

Comatula, 232, 266.

twmidus, 174.

INDEX.

Conclusions to be drawn from Fossils,

52-56

Concretions, calcareous, 29; phosphatic,
31; of clay-ironstone, 31; of manganese,

31.

Conglomerate, 18.

Coniferce, 262; wood of, 13; of Devonian
period, 138; ’ of the Carboniferous, 170;
of the Permian, 196; of the Trias, 208 ;
of the Jurassic * period, 230.

Coniston Flags and Grits, 116.

Connecticut Sandstones, footprints of,
222, 346.

Conocoryphe Mathewi, 85; Sultzeri, 85.

Conodonts, 114, 131.

Constellaria, 105.

Constricting serpents of the Eocene, 296.

Contemporaneity of strata, 44-46.

Continuity, theory of, 5-7.

Conularia, 111, 129, 148, 186, 199, 237;
ornata, 149.

Conulus, 186.

Conus, 293.

Coomhola Grits, 158, 159.

Coprolites, 31, 243.

Coralline Crag, 324.

Corallines, 25.

Corallium, 311.

Coral-rag, 227, 229, 230.

Coral-reefs, 24-26.

Coral-rock, 26.

Coral-sand, 19, 26.

Corals, 103; of the Lower Silurian, 104,
105 ; of the Upper Silurian, 119 ; of the
Devonian, 140-143; of the Carbonifer-
ous, 172-175; of the Permian, 197; of
the Trias, 209; of the Jurassic, 230, 231;
of the Cretaceous, 266; of the Hocene,

92; of the Miocene, 311.

Cor Bile 235.

Cornbrash, 227, 229.

Corniferous Limestone, 135, 137.

Cornulites, 123.

Cornus, 262.

Coryphodon, 300.

Cowries, 259, 271, 293.

Crabs, 180, 197, 233, 267.

Crag, Red, 324; White, 324; Norwich,
324; Antwerp, 325; Bridlington, 325;
Coralline, 324.

Crania, 110, 127, 198, 269; Ignabergensis,
269.

Crassatella, 292.

Crepidophyllum, 142; Archiaci, 142.

Cretaceous period, 256-283; rocks of, in
Britain, 257-259; in North America,
260, 261; life of, 261-283.

Crinoidal Limestone, 24, 25.

Crinoidea, 120; of the Cambrian, 82; of
the Lower Silurian, 105; of the Upper
Silurian, 120-122; of the Devonian, 143;
of the Carboniferous, 175; of the Per-
mian, 197; of the Trias, 209; of the
Jurassic, 231; of the Cretaceous, 266;
of the Kocene, 292.

Crioceras, 273; ‘cristatum, 274.

Crocodilia, 218; of the Trias, 218; of the
Jurassic, 251; of the Cretaceous, 280;
of the Eocene, 296, 297.

Cromer Forest-bed, 336.

Crossozamites, 230.

Crotalocrinus, 122.

INDEX.

Crustacea, of the Cambrian, 83-87; of the
Lower Silurian, 107, 108; of the Upper
Silurian, 123-125; of the Devonian, 144,
145; of the Carboniferous, 178-181; of
the Permjan, 197; of the Trias, 210; of
the Jurassic, 233; of the Cretaceous,
267.

Cryptogams, 164, 262.

Ctenacanthus, 188.

Ctenodonta, 111.

Cupressus, 262.

Cursores, 297, 346.

Cuttle-fishes (see Dibranchiate Cephalo-
pods).

Cyathocrinus, 175.

Cyathophyllum, 119, 142, 173.

Cycadopteris, 262.

Cycads, 208; of the Carboniferous, 170;
of the Permian, 197; of the Trias, 208;
of the Jurassic, 230; of the Cretaceous,
261.

Cyclas, 268.

Cyclonema, 129.

Cyclophthalmus senior, 181.

Cyclostoma, 294; Arnoudii, 294.

Cynodraco, 220.

Cyprea, 271, 293 ; elegans, 393.

Cypress, 262, 308, 311.

Cypridina, 145.

Cypridina Slates, 145.

Cyrena, 235, 268, 292.

Cyrtina, 213, 214.

Cyrtoceras, 114.

Cystiphyllum, 119, 142, 173; vesiculosum,
14].

Cystoidea, 105-107; of the Cambrian, 82;
of the Lower Silurian, 106; of the
Upper Silurian, 120.

Dachstein Beds, 205, 206.

Dadoxylon, 138, 170.

Daonella, 211; Lommelli, 211.

Dasornis Londinensis, 297.

Decapod Crustaceans, 180.

Deer, 317, 329, 354

Deinosauria, 248; of the Trias, 221; of
the Jurassic, 248-251; of the Cretaceous,
271-279.

Deinotherium, 319, 320; gigantewm, 320.

Denbighshire Flags and Grits, 115.

Dendrocrinus, 82.

Dendrograptus, 100.

Desmids, 138, 261.

Devonian Formation, 133-136; origin of

- hame, 133; relation to Old Red Sand-
stone, 133, 134; of Devonshire, 134;
of North America, 135, 136; life of,
136-156.

Diadema, 266.

Diatoms, 33; of the Devonian, 138; of
the Carboniferous, 164; of flints, 261;
of Richmond Earth, 33, 307.

Dibranchiate Cephalopods, 112; of the
Trias, 212; of the Jurassic, 239-241;
of the Cretaceous, 274, 275; of the
Eocene, 294; of the Miocene, 312.

Diceras, 236; arietina, 236.

Diceras Limestone, 227, 236.

Dichobune, 303.

Dichograptus, 101; octobrachiatus, 101.

Dicotyledonous plants, 262.

Dicotyles antiquus, 317.

Dicranograptus, 101, 119.

399

Dictyonema, 89, 100, 119; sociale, 89.

Dicynodon, 220; lacerticeps, 221.

Didelphys, 254, 315; gypsorum, 299.

Didus ineptus, 348.

Didymograptus, 101; divaricatus, 102.

Dikellocephalus Celticus, 84; Minneso-
tensis, 84.

Dimorphodon, 247.

Dinichthys, 153; Hertzeri, 151.

Dinoceras, 303; mirabilis, 304.

Dinocerata, 303, 304.

Dinophis, 296.

Dinornis, 346, 348;
347; gigantews, 346.

Dinosauria (see Deinosauria).

Dinotherium (see Deinotherium).

Diphyphyllum, 142.

Diplograptus, 101, 119; pristis, 102.

Dipnoi, 153, 187, 215.

Diprotodon, 348, 349; australis, 348.

Diptera, 311.

Discina, 87, 110, 127, 198.

Discoidea, 266 ; cylindrica, 267.

Dithyrocaris, 179; Scouleri, 180.

Dodo, 348.

Dog-whelks, 293.

Dolomite, 27, 28.

Dolomitic Conglomerate of Bristol, 201,
219.

Dolphins, 299, 315.

Dorecatheriwm, 317.

Downton Sandstone, 116.

Draco volans, 245.

Dragon-flies, 311.

Drift, Glacial, 337.

Dremotherium, 317.

Dromatherium sylvestre, 223, 224.

Dryandra, 262.

Dryopithecus, 323.

Dugongs, 299,

elephantopus, 346,

Echinodermata, of the Cambrian, 82; of
the Lower Silurian, 105; of the Upper
Silurian, 120; of the Devonian, 143 ; of
the Carboniferous, 175; of the Permian,
197 ; of the Trias, 209; of the Jurassic,
231; of the Cretaceous, 266; of the
Eocene, 292.

Echinoidea, 177; of the Upper Silurian,
120 ; of the Devonian, 143 ; of the Car-
boniferous, 177 ; of the Permian, 197;
of the Jurassic, 233; of the Cretaceous,
266.

Edentata, 349; of the Hocene, 299 ; of the
Miocene, 315; of the Post-Pliocene,
349-353.

Edriocrinus, 122.

Eifel Limestone, 135.

EHlasmobranchti ‘(see Placoid Fishes).

EHlasmosaurus, 276.

Elephants, 319, 320, 330.

Elephas, 320; Americanus, 357; anti-
quus, 329, 330, 336, 341, 357; Falconeri,
359 ; Melitensis, 359; meridionalis, 329,
330, 336, 357 ; planifrons, 321; primi-
genius, 339, 341, 357, 358.

Elk, 354; Irish, 354, 355.

Ellipsocephalus Hofi, 84.

Elotheriwm, 317.

Emydide, 296.

Emmys, 280.

Enaliosaurians, 219, 242, 276.

Encrinital marble, 24.

400

Encrinurus, 123.

Encrinus liliiformis, 209, 210.

Endogenous plants, 261.

Endophyllum, 173.

Endothyra, 171; Bailyi, 172.

Engis skull, 364.

Entomis, 145.

Entomoconchus Scouleri, 179, 180.

Eocene period, 284; rocks of, in Britain,
287, 288; in France, 288; in North
America, 288, 289 ; life of, 289-305.

Eocidaris, 197.

Eophyton, 80; Linneanum, 81.

Eophyton Sandstone, 79.

Eosaurus Acadianus, 191.

Eozoic rocks, 67.

Eozotn Bavaricum, 76.

Eozotn Canadense, 68, 76; appearance of,
in mass, 69 ; minute structure of, 70, 71;
affinities of, with Foraminifera, 71-74.

Ephemeride@, 145, 183.

Equisetacee, 166.

Equisetites, 196.

Equide, 301, 302, 316, 328.

Equus, 302 ; caballus, 354; excelsus, 328 ;
Fossilis, 336, 354

Eridophyllum, 142.

Eryon arctiformis, 233, 234.

Eschara, 267.

Escharide, 267.

Escharina, 267 ; Oceani, 268.

Estheria, 145, 179, 210; tenella, 180.

Eucalyptocrinus, 122; polydactylus, 122.

Eucladia, 120.

Euomphalus, 128, 148, 186, 199, 212; dis-
cors, 129.

Euplectella, 265.

Euproops, 179.

European Bison, 356.

Eurypterida, 124, 179; of the Upper Silu-
rian, 124; of the Devonian, 144.

Even-toed Ungulates, 300, 317, 354.

Exogenous plants, 266.

Exogyra, 236; virgula, 236.

Extinction of species, 57, 58.

Fagus, 262.

Faluns, 306.

Fan-palms, 308.

Favistella, 105.

Favosites, 119, 142; Gothlandica, 143;
hemispherica, 143.

FaxGe Limestone, 249, 286.

Felis angustus, 330 ; leo, 361 ; spelea, 361.

Fenestella, 108, 125, 145, 184, 198, 210;
cribrosa, 146 ; magnifica, 146 ; retiformis,
198.

Fenestellide, 183.

Ferns, of the Devonian, 136; of the Car-
boniferous, 164; of the Permian, 196;
of the Trias, 207; of the Jurassic, 229;
of the Cretaceous, 261.

Fig-shells, 293.

Fishes, 150; of the Upper Silurian, 130,
131; of the Devonian, 150-155; of the
Carboniferous, 187, 188 ; of the Permian,
199, 200; of the Trias, 214, 215; of the
Jurassic, 240-242 ; of the Cretaceous, 275,
276; of the Eocene, 295, 296; of the
Miocene, 312, 313.

Flint, 33; structure of, 34; origin of, 34;
organisms of, 34, 138, 263; of Chalk, 34,
259, 261.

INDEX.

Human implements associated with bones
of extinct Mammals, 363, 364.

Flora (see Plants).

Footprints of Cheirotherium, 215, 216;
of the Triassic sandstones of Connecti-
cut, 222.

Foraminifera, 22-24, 71-74; of the Cam-
brian, 82; of the Lower Silurian, 98;
of the Carboniferous, 171, 172; of the
Permian, 197; of the Trias, 209; of the
Jurassic, 230; of the Cretaceous, 21,
22, 263; of the Eocene, 290; of the
Miocene, 311; of the Post-Pliocene,
338 ; of Atlantic ooze, 22, 23; as build-
ers of limestone, 24, 25, 28; as forming
green sands, 34.

Forbesiocrinus, 175.

Forest-bed of Cromer, 336.

Forest-bugs, 311.

Forest-marble, 227.

Forman, definition of, 18; succession
of, 42.

Fossiliferous rocks, 14-37; chronological
succession of, 37-44. ;

Fossilisation, processes of, 11-14.

Fossils, definition of, 11; distinctive, of
rock-groups, 38; conclusions to be
drawn from, 52-56; biological relations
of, 57-61.

Foxes, 304.

Fringe-finned Ganoids, 153.

Fucoidal Sandstone, 79, 80.

Fucoids, 80, 97.

Fuller's Earth, 227, 229.

Fusulina, 172; cylindrica, 172.

Fusus, 287, 293.

Galeocerdo, 312.

Galerites, 266; albo-galerus, 267.

Galestes, 254.

Ganoid Fishes, 150; of the Upper Silurian,
130; of the Devonian, 150-153; of the
Carboniferous, 187, 188 ; of the Permian,
199; of the Trias, 214; of the Jurassic,
241; of the Cretaceous, 275; of the
Eocene, 295.

Gaspé Beds, 134.

Gasteropoda, of the Cambrian, 88 ; of the
Lower Silurian, 111; of the Upper Silu-
rian, 128, 129; of the Devonian, 148; of
the Carboniferous, 186; of the Permian,
199; of the Trias, 213; of the Jurassic,
236, 237; of the Cretaceous, 271; of the
Eocene, 292, 293.

Gastornis Parisiensis, 297.

Gault, 257, 258. ;

Gavial, 251, 297.

Genesee Slates, 135.

Geological record, breaks in the, 47-52.

Giraffes, 317.

Glacial period, 335; deposits of, 337, 338.

Glandulina, 211.

Glauconite, 34, 74, 98, 263.

Glauconomeé, 126, 184; pulecherrima, 183.

Globe Crinoids (see Cystoidea).

Globigerina, 22, 23, 264.

Glutton, 360.

Glyptaster, 120.

Glyptocrinus, 122.

Glyptodon, 351, 352; clavipes. 352.

Glyptolemus, 153.

Goats, 318. :

Goniatites, 130, 149, 187, 214; Joss@, 187.

INDEX.

Gorgonide, 292.

Grallatores. 297.

Graphite. 36; mode of occurrence of, 36,
68 ; origin of, 36.

Graptolites, 89, 100; structure of, 100;
of the Lower Silurian, 100-103; “of the
Upper Silurian, 118, 119.

Great Oolite, 227, 229; Upper, 257, 258,
260

Greenland, Miocene plants of, 311.

Greensand, Lower, 257, 260.

Green sands, origin of, 44, 263.

Grevillea, 262, 308.

Grifithides, 179.

Grizzly Bear, 359

Ground Sloths, 551.

Gryphea, 236 ; incurva, 236.

Guelph Limestone, 117.

Gulo luscus, 360 ; speleus, 360.

Guttenstein Beds, 205, 206.

Gymnospermous Exogens, 262.

Gypsum, 32, 193, 204.

Gyracanthus, 188.

Gyroceras, 130.

Hadrosaurus, 278.

Halitheriwm, 299.

Hallstadt Beds, 205, 206.

Halobia, 211.

Halysites, 119 ; agglomerata, 120; caten-
ularia, 120.

Hamilton formation, 135, 137.

Hamites, 273; rotundus, 274.

Haplophlebium Barnesi, 182.

Harlech Grits, 78, 79.

Harpes, 108, 123 ; ungula,124.

Hastings Sands, 257.

Headon and Osborne series, 287, 288.

Heart-urchins, 311.

Heliolites, 105, 119, 266.

Heliophyllum, 142, 172; exiguum, 141.

Helix, 294.

Helladotherium, 317.

Helopora fragilis, 126.

Hemicidaris crenularis, 233.

Hemiptera, 311.

Hemitrochiscus paradoxus, 197.

Hempstead Beds, 306.

Hesperornis, 281, 282; regalis, 282.

Heteropoda, 111; of the Lower Silurian,
111 ; of the Upper Silurian, 129; of the
Devonian, 148; of the Carboniferous,
186.

Hinnites, 213.

Hipparion, 301, 302, 316, 317, 328.

Hippopodium, 235.

Hippopotamus, 302; amphibius, 317, 329;
MAjOT, 329, 336, 354; Sivalensis, 318.

Hippothoa, 108.

Hippurite Marble, 270.

Hippurites, 270; "Poucasiana, Die

Hippuritide, 270, 285.

Histioderma, 82.

Hollow-horned Ruminants, 317.

Holocystis elegans, 266.

Holopea, 129; subeonica, 129.

Holopella, 129, 213; obsoleta, 129.

Holoptychius, 153: "nobilissimus, 154.

Holostomatous Univ alves, 236, 293.

Holothurians, 120.

Holtenia, 264.

Homacanthus, 188.

4O1

Homalonotus, 123, 145; armatus, 144.

Homo diluvii testis, 3138.

Honeycomb Corals, 142

Hoofed Quadrupeds, 300.

Hudson River Group, 95.

Huronian Period, 75, 76; rocks of, 75.

Hyena crocuta, 360; spelea, 360; Hip-
parionum, 330.

Ayenictis, 322.

Hyenodon, 304.

Hyalea D Orbignyana, 312.

Hybodus, 214, 242, 275.

Aydractinia, 265.

~Hydroid Zoophytes, 103, 265.

Hymenocaris vermicauda, 84, 88.
Hymenophyllites, 165.
Hymenoptera, 311.

Hyopotamus, 302.
Hyperodapedon, 218.
Aypsiprymnopsis, 224.

Hystriz primigenius, 322.

Ichthyocrinus levis, 122.

Ichthyornis, 281, 282: dispar, 281, 282.

Ichthyosaurus, 242, 243, 276; communis,
242.

Ictitherium, 322.

Iguana, 277.

Iguanodon, 277, 278; Mantelli, 278.

Ilfracombe Group, 134.

Illeenus, 108, 123 °

Imperfection of the paleontological re-
cord, 50, 51.

Inferior Oolite, 227, 229.

Infusorial Earth, 33.

Inoceramus, 269; sulcatus, 270.

Insectivora, of the Eocene, 395; of the
Miocene, 322.

Insects, of the Devonian, 145; of the
Carboniferous, 182; of the Jurassic,
233 ; of the Miocene, 311, 312.

Trish Elk, 354, 355.

Ischadites, 99, 118.

Isopod Crustaceans, 84.

Jackson Beds, 289

Jurassic period, 226; rocks of, 226-229;
life of, 229-255.

Kaidacarpum, 230.

Kainozoic period, 44, 284-287.

Kangaroo, 348.

Kelloway Rock, 227.

Kent’s Cavern, deposits in, 348.

Keuper, 204, 206.

Kimmeridge Clay, 227, 229.

King-crabs, 84, 124, 125, 179.

Koninckia, 213, 214.

_Kossen Beds, 205, 206.

Labyrinthodon Jegeri, 217.

Labyrinthodontia, 190; of the Carbon-
iferous, 189-191; of the Permian, 2003
of the Trias, 215-217.

Lace-corals, 108, 125, 145, 183, 198, 210.

Lacertilia, 202; of the Permian, 201, 202;
of the Trias, 217, 218; of the Jurassic,
251; of the Cretaceous, 280.

Leelaps, 278.

Lamellibranchiata, of the Cambrian, 88;
of the Lower Silurian, 110; of the
Upper Silurian, 128; of the Devonian,

402

148; of the Carboniferous, 186; of the
Permian, 198; of the Trias, 211; of the
Jurassic, 234-236; of the Cretaceous,
268-270; of the Eocene, 292.

Lamina, 275, 312.

Lamp-shells (see Brachiopoda). ‘

Land-tortoises, 313.

Lauracee, 308.

Laurentian period, 65; rocks of, 65, 66;
Lower Laurentian, 66;
rentian, 66; areas occupied by Lau-
rentian rocks, 66; limestones of, 66,
67; iron-ores of, 68; phosphate of lime
of, 68; graphite of, 68 ; life of, 67-75.

Leaf-beds of the Isle of Mull, 306.

Leda, 292; truncata, 338.

Leguminosites Marcouanus, 263.

Lemming, 344, 343.

Lepadide, 267.

Lepadocrinus Gebhardi, 106.

Leperditia, 108; canadensis, 107.

Lepidaster, 120.

Lepidechinus, 178.

Lepidesthes, 178.

Lepidodendroids, 166, 167, 207.

Lepidodendron, 118, 136, 166, 196; Stern-
bergi, 167.

Lepidoptera, 311.

Lepidosiren, 153.

Lepidosteus, 188.

Lepidostrobus, 166.

Lepidotus, 275

Leptena, 109, 110,
235; sericea, 110.

Leptoceelia, 127 ; plano-convexa, 127.

Lias, 226, 227, 229.

Lichas, 108.

Licrophycus Ottawaensis, 97.

Lignitic Formation of North America,
288, 294.

Lily-encrinite, 209, 210.

Lima, 235.

Lime, phosphate of, 30, 31.

Limestone, 23-27; varieties of, 27-30;
origin of, 21; microscopical structure
of, 26; Crinoidal, 24; Foraminiferal,
24, 26; coralline, 24; magnesian, 27;
metamorphic, 27; oolitic, 28-30; piso-
litic, 29; bituminous, 36; Laurentian,
67.

Limneea, 294; Pandas, 294,

Limulus. 84, 124, 125, 179

Lingula, 87, 88, 110, ‘127, 147, 198 ;
nert, 198.

Lingula Flags, 77, 78, 79, 88.

Lingulella, 87, 88; Davisii, 88; ferruy
ginea, 88.

Lirwdendron, 262, 308; Meeki, 263.

Lithostrotion, 173; irregulare, 174.

Intuites, 130.

Lizards (see Lacertilia).

Llama, 354.

Llanberis Slates, 79.

Llandeilo rocks, 92, 94, 96.

Llandovery rocks, 93; Lower,
iA ey

Lobsters, 180, 210, 233, 267.

Loess, 339.

London Clay, 287, 288.

Longmynd rocks, 77-80, 83.

Lonsdaleia, 173.

Lophiodon, 316.

Lophophyllum, 173.

125, 234; Liassica,

Cred-

93; Upper,

Upper Lau-.

INDEX.

Lower Cambrian, 77-79; Chalk, 259; Cre-
taceous, 257, 258; Devonian, 134;
Eocene, 287, 288; Greensand, 257, 258;
Helderberg, 117, 118; Laurentian rocks,
66; Ludlow rock, 116; Miocene, 305;
Old Red Sandstone, 134; Oolites, 227,
229: Silurian period, 90-114; rocks of,
in Britain, 92-94; in North America,
94-96 ; life of, 97-114.

Loxonema, 186, 199, 213.

Ludlow rocks, 116, 117.

Lycopodiacee, 118, 136, 167.

Lynton Group, 134.

Lyrodesma, 111.

Macaques, 323, 331.

Macheracanthus major, 151, 155.

Machairodus, 221, 249, 322, 331, 360;
cultridens, 331

Maclurea, 111; crenulata, 112.

Macrocheilus, 186, 199, 213.

Macropetalichthys, 152; Sullivanti, 151.

Macrotherivin giganteum, 315.

Macrurous Crustaceans, 180.

Mactra, 292.

Maestricht Chalk, 259, 279, 286.

Magnesian Limestone, 27; nature and
structure of, 28; of the Permian series,
194, 196.

Magnolia, 262, 290, 310.

Mammalia, of the Trias, 223, 224; of the
Jurassic, 253, 254; of the Eocene,
299-305: of the Miocene, 313-323; of
the Pliocene, 327-331; of the Post-
Pliocene, 348-362.

Mammoth, 339, 341, 344, 357-359.

Man, remains of, in Post-Pliocene de-
posits, 341, 344.

Manatee, 299.

Mantellia, 230; megalophylla, 230.

Maple, 290, 308, 310.

Marble, 28; encrinital, 24; statuary, 27.

Marcellus Shales, 135.

Mariacrinus, 122.

Marmots, 322.

Marsupials, 299; of the Trias, 223; of the
Jurassic. 253, 254; of the Eocene, 299;
of the Miocene, 315; of the Post-Plio-
cene, 348, 319.

Marsupiocrinus, 122.

Marsupites, 266. :

Mastodon, 319, 321, 322; Americanus,
angustidens, 322; Arvénensis, 329;
longirostris, 322; Ohioticus, 357; Siva-
lensis, 321.

Medina Sandstone, 116.

Megalichthys, 188.

Megalodon, 148.

Megalomus, 128.

Megalony2, 351.

Megalosaurus, 249, 278.

Megatherium, 350, 351; Cuvieri, 350.

Melania, 294.

Melonites, 178.

Menevian Group, 77-79.

Menobranchus, 189.

Meristelia, 127; cylindrica, 127; inter-
media, 127; ; naviformis, 127.

Mesopithecus, 323.

Mesozoic Period, 44.

Michelinia, 142.

Micraster, 266.

Microlestes, 224; antiquus, 223.

INDEX.

Middle Devonian, 134; Eocene, 287, 288,
289; Oolites, : 297; Silurian, 91.

Miliolite Limestone, 290.

Millepora, 230.

Millstone Grit, 159, 161.

Miocene period, 305; rocks of, in Britain,
305, 306; in France, 306; in Belgium,
307; in Switzerland, 306; in Austria,
307; in Germany, 307; in Italy, 307; in
India, 307; in North America, 307; life
of, 308-323.

Mitre-shells, 271, 293.

Mitra, 271, 293.

_Moas of New Zealand, 346-348.

Modvolopsis, 111; Solvensis, 88.

Molasse, 306.

Mole, 322, 336.

Monkeys, 305, 331.

Monocotyledonous plants, 262.

Monograptus, 100, 119; priodon, 119.

Monotis, 211.

Monte Bolea, fishes of, 295.

Montlivaltia, 209.

Mosasauroids, 279, 280.

Mosasaurus, 279; Camperi, 279; prin-
ceps, 279.

Mountain Limestone, 158, 161.

Mud-fishes, 153, 215.

Mud-turtles, 280.

Mull, Miocene strata of, 306.

Murchisonia, 111, 129, 199, 213; gracilis,

111

Murex, 237, 293.

Muschelkalk, 208, 204, 206.
Musk-deer, 317.

Musk-ox, 344, 345, 356.
Musk-sheep, 356.

Myliobatis Edwardsii, 296.
Mylodon, 351; robustus, 352.
Myophoria, 211; lineata, 211.
Myriapoda of the Coal, 181, 182.

Nassa, 293.

Natatores, 297.

Natica, 271, 293.

Nautilus, 112-114, 130, 149, 186, 199, 237,
272, 294; Danicus, 272 ; pompilius, 237.

Neanderthal skull, 364.

Neocomian series, 257, 260.

Neolimulus, 125.

Nerinea, 237, 271; Goodhallia, 237.

Nerita, 393.

Neuroptera, 311.

Neuropteris, 136, 165, 196.

Newer Pliocene, 323, 324.

New Red Sandstone, 193, 203.

Newts, 189, 200, 217.

Niagara Limestone, 117.

Nipadites, 290; ellipticus, 290.

Neggerathia, 197.

Norwich Crag, 324.

Nothosaurus, 219;

Notidanus, 241.

Numenius gypsorum, 297.

Nummulina, 172, 290;
pristina, 172.

Nummulitic Limestone, 24, 287, 291.

mirabilis, 219.

leevigata, 290 ;

Oak, 262, 310.

Obolella, 87; sagittalis, 88.

Qdd-toed Ungulates, 300, 315, 327, 353.
Odontaspis, 275.

Odontopteris, 165; Schlotheimi, 164.

403

Odontopteryx, 297 ; toliapicus, 297, 298.

Odontornithes, 282.

Ogygia, 108; Buchii, 107.

Older Pliocene, 323, 324.

Oldhamia, 81; antiqua, 82;
Ireland, 79, 80.

Old Red Sandstone, 133 ; origin of name,
133; of Scotland, 134 ; relations of, to
Devonian, 133, 134, 155.

Olenus, 108; macrurus, 88.

Oligocene, 305.

Oligoporus, 178.

Olive-shells, 293.

Omphyma, 119.

Onchus, 130 ; tenwistriatus, 131.

Oneida Conglomerate, 116.

Onychodus, 153; sugmoides, 151.

Oolitic limestone, structure of, 28;
of formation of, 30.

Oolitic rocks (see Jurassic).

Ooze, Atlantic, 22, 33.

Ophidia, 251; of the Eocene, 296.

Ophiuroidea, of the Lower Silurian, 105;
of the Upper Silurian, 120; of the Car-
boniferous, 177; of the Trias, 210; of
the Jurassic, 233.

Opossum, 299, 315.

Orbitoides, 291.

Oriskany Sandstone, 135.

Ormoaylon, 138.

Orohippus, 302.

Orthis, 38, 109, 125, 147, 184, 199; biforata,
109; Davidsoni, 127; elegantula, 127 ;

slates of

mode

flabellulum, 109; Hicksvi, 38; lenticu-
laris, 383 plicatella, 110; resupinata,
testudinaria,

185 ; subquadrata, 109 ;
110

Gane 89, 112, 113, 130, 149, 186;-
DAIRY 2 erebriseptum, 118.

Orthonota, 111.

Orthoptera, 182, 311.

Osmeroides, 276 ; Mantelli, 276.

Osmerus, 276.

Osteolepis, 153.

Ostracode Crustaceans of the Cambrian,
83; of the Lower Silurian, 107; of the
Upper Silurian, 123; of the Devonian,
145; of the Carboniferous, 179; of the
Permian, 197; of the Trias, 210; of the
Jurassic, 233; of the Cretaceous, 267.

Ostrea acuminata, 235; Couloni, 269;
deltoidea, 235; distorta, 235 ; expansa,
‘gregared, 235; Marshti, 235, 236.

Otodus, 295 ; obliquus, 296.

Otozamites, 230.

Otozoum, 206.

Oudenodon, 220; Bainti, 221.

Ovibos moschatus, 356.

Oxford Clay, 227, 229.

Oxyrhinda, 312; xiphodon, 313.

Oysters, 235, 236, 269.

Pachyphyllum, 173.

Paleearea, 111.

Paleaster, 120; Ruthvent, 121.
Palasterina, 120; primeeva, 121.
Paloeechinus, 120, 178 ; ellipticus, 177.
Paleocaris, 180; typus, 180.
Paloocoma, 120; Colvini, 121.
Paleocoryne, 172.

Paleolithic man, remains of, 363-365.
Paleomanon, 118.

Paleoniseus, 188, 200.

404

Paleontina Oolitica, 233.

Paleontological evidence as to Evolution,
60, 372-374.

Paleontological record,
the, 50, 51.

Paleontology, definition of, 10.

Paleonyctis, 304.

Paleeophis, 296 ; toliapicus, 296; typheus,
296.

Paleoreas, 318.

Paleosaurus, 200, 218,
219.

Paleosiren Beinerti, 200.

Paleotherium, 300; magnun, 301.

Paleoxylon, 170.

Paleozoic period, 44.

Palms, 230, 263, 290, 308, 309

Paludina, 257, 294.

Pandanee, 230.

Pandanus, 262.

Paradoxides, 86, 87, 108; Bohemicus, 85.

Parasmilia, 266.

Parkeria, 264.

Pear Encrinite, 231.

Pearly Nautilus, 58, 111, 112, 237.

Peccaries, 317.

Pecopteris, 136, 165, 196.

Pecten Grenlandicus, 338; Islandicus,
338 ; Valoniensis, 211, 212, 204.

Penarth Beds, 204.

Pennatulide, 292.

Pentacrinus, 231;
Fasciculosus, 232.

Pentamerus, 125,
Knight, 128.

Pentremites (see Blastoidea).

Pentremites conoideus, 176; pyriformis,
176.

Perching Birds, 297.

Percide, 276.

Periechocrinus, 122.

Perissodactyle Ungulates, 300, 315, 327.

Permian period, 192-202; rocks of, in
Britain, 194; in North America, 194;
life of, 195-302.

Persistent types of life, 58, 371.

Petalodus, 188.

Petraster, 120.

Petroleum, origin of, 36.

Pezophaps, 348.

Phacops, 108, 123, 145; Downingice, 124;
granulatus, 144; levis, 144; latifrons,
144, 145; longicaudatus, 124; rana, 145.

Phenopora ensiformis, 126.

Phalangers, 348.

Phanerogams, 164.

Phaneropleuron, 153.

Phascolotherium, 258, 254.

Pheronema, 264.

Phillipsastreea, 142.

Phillipsia, 179 ; seminifera, 180.

Pholadomya, 235.

Phormosoma, 178.

Phorus, 271.

Phosphate of lime, concretions of, 30;
disseminated in rocks, 30; origin of, 31.

Phyllograptus, 102; typus, 102.

Phyllopoda, of the Cambrian, 83; of the
Lower Silurian, 108; of the Upper Silu-
rian, 123; of the Devonian, 145; of the
Carboniferous, 179; of the Permian,
197 ; of the Trias, 210.

imperfection of

219 ; platyodon,

caput-meduse, 231;

126; galeatus, 126;

INDEX.

Phyllopora, 210.

Physa, 294 ; columnaris, 294.

Pigs, 302, 317, 329, 354.

Pilton Group, 135.

Pinites, 170.

Pisces (see Fishes).

Pisolite, 29.

Pisolitic Limestone of France, 259, 286.

Placodus, 220; gigas, 220.

Placoid Fishes, 150; of the Upper Silurian,
USO SSH of the Devonian, 153-155; of
the Carboniferous, 188; of the Permian,
199; of the Trias, 214; of the Jurassic,
241; of the Cretaceous, 275; of the
Eocene, 295 ; of the Miocene, 312.

Plagiaulax, 254.

Planolites, 122; vulgaris, 123.

Planorbis, 294.

Plants, of the Cambrian, 80, 81; of the
Lower Silurian, 97, 98; of the Upper
Silurian, 118; of the Devonian, 136-139 ;
of the Carboniferous, 163-170; of the
Permian, 196; of the Trias, 207, 208;
of the Jurassic, 229, 230; of the Cre-
taceous, 261-268; of the Kocene, 289,
290; of the Miocene, 308-311.

Plasmopora, 119.

Platanus, 262, 308 ; aceroides, 309.

Platephemera antiqua, 145.

Platyceras, 128, 148; dumosum, 148;
multisinuatum, 129; ventricosum, 129.

Platycrinus, 122, 175; tricontadactylus,
175.

Platyostoma, 129; Niagarense, 129.

Platyrhine Monkeys, 362.

Platyschisma helicites, 129.

Platysomus, 200; gibbosus, 199.

Platystoma, 213.

Pleistocene period, 334; climate of, 362.

Plesiosaurus, 219, 243-245, 276; dolicho-
deirus, 244.

Pleurocystites squamosus, 106.

Pleurotoma, 293.

Pleurotomaria, 111, 129, 186, 199, 236, 271.

Plicatula, 213.

Pliocene period, 323; rocks of, in Britain,
324; in Belgium, 325; in Italy, 325;
in North America, 326; life of, 326-331.

Pliopithecus, 322; antiquus, 3238.

Pliosaurus, 245.

Podocarya, 230.

Podozamites, 208 ; lites 209.

Polir-schiefer, 33.

Polycystina, 32 ; of Barbadoes-earth, 33.

Polypora, 145, 184; dendroides, 183.

Polypterus, 153, 188.

Polystomella, 311.

Polytremacis, 266.

Polyzoa, of the Cambrian, 81, 89; of the
Lower Silurian, 108; of the Upper

Silurian, 125; of the Devonian, 145,
146; of the Carboniferous, 183, 184;

of the Permian, 198; of the Trias, 210;
of the Cretaceous, 267 ; of the Miocene,
312.

Populus, 262.

Porcellia, 186.

Porcupines, 322.

Portage Group, 135.

Port-Jackson Shark, 154, 188, 242.

Portland beds, 227, 229.

Post-Glacial deposits, 336, 338.

INDEX.

Post-Pliocene period, 334.

Post-Tertiary period, 286.

Poteriocrinus, 175.

Potsdam Sandstone, 79.

Pre-Glacial deposits, 336.

Prestwichia, 179; rotundata, 179.

Primitia, 107; strangulata, 107.

Primordial Trilobites, 85.

Primordial zone, 79.

Proboscidea, of the Miocene, 319, 322; of
the Pliocene, 329, 330; of the Post-
Pliocene, 357-359.

Producta, 147, 184, 198; horrida, 198;
longispinad, 185; semrreticulata, 185.

Productella, 147, 184.

Productide, 147, 211.

Proétus, 123.

Prong-buck, 318.

Protaster, 120; Sedqwickiv, 121.

Proteacee, 262, 308, 309.

Proteus, 189.

Protichnites, 87.

Protocystites, 82.

Protornis Glarisiensis, 297.

Protorosaurus, 201, 202; Speneri, 201.

Protospongia, 81; fenestrata, 88.

Prototaxites, 118, 138; Logani, 139.

Psammobia, 292.

Psammodus, 188.

Psaronius, 136, 164.

Pseudocrinus bifasciatus, 106.

Psilophyton, 118, 137, 138; princeps, 138.

Pteranodon, 247, 277; longiceps, 277.

Pteraspis, 130, 152; Banksii, 1380.

Pteriehthys, 152; cornutus, 153.

Pterinea, 128; subfalcata, 128.

Pteroceras, 237, 271.

Pterodacitylus, 245, 277; crassirostris, 246.

Pterophyllum, 208, 230; Jegeri, 209.

Pteropoda, of the Cambrian, 88; of the
Lower Silurian, 111; of the Upper
Silurian, 129; of the Devonian, 148;
of the Carboniferous, 186; of the Per-
mian, 199; of the Jurassic, 237.

Pterosauria, 245; of the Jurassic, 245-248;
of the Cretaceous, 277.

Pterygotus Anglicus, 124, 125.

Ptilodictya, 108, 125; acuta, 109; falci-
formis, 109; raripora, 126; Schaffert,
109.

Ptychoceras, 273; Emericianum, 274.

Ptychodus, 275.

Pupa vetusta, 186.

Purbeck Beds, 228; Mammals of, 254.

Purpuroidea, 237.

Pycnodus, 275.

Pyrula, 293.

Quadrumana, of the Eocene, 305; of the
Miocene, 322, 323; of the Pliocene, 331;
of the Post-Pliocene, 361.

Quadrupeds (see Mammalia).

Quaternary period, 334.

Quebec Group, 95, 96, 101.

Quercus, 262.

Rabbits, 322.

Rana, 313.

Raptores, 297.
Rasores, 297.

Recent period, 286, 334.
Receptaculites, 99.

405

Red clays, origin of, 35.

Red Coral, 311.

Red Crag, 324.

Red Deer, 336, 354.

Reindeer, 344, 345, 354, 355.

Remopleurides, 188.

Reptiles, 200; cf the Permian, 200-202;
of the Trias, 217-221; of the Jurassic,
242-251; of the Cretaceous, 276-281; of
the Eocene, 296, 297.

Retepora, 108, 125, 145, 184, 198, 210;
Ehrenbergi, 198; Phillipsi, 146.

Retiolites, 119.

Retzia, 127.

Rheetic Beds, 204-206.

Rhamphorhynchus, 247; Bucklandi, 248.

Rhinoceride, 315.

Rhinoceros Etruscus, 327, 328, 336, 353;
leptorhinus, 328; megarhinus, 327-329,
336, 353; tichorhinus, 3538, 354.

Rhinopora verrucosa, 126.

Rhizodus, 188.

Rhombus minimus, 295.

Rhyncholites, 239.

Rhynchonella, 110, 127, 147, 184, 234, 268,
292; cuneata, 127; neglecta, 127; plew-
rodon, 185; varians, 235.

Rhynchosaurus, 218; articeps, 218.

Rice-shells, 293.

Richmond Earth, 33, 307.

Ringed Worms (see Annelida).

River-gravels, high-level and low-level,
340, 341.

Robulina, 311.

Rocks, definition of, 14; divisions of,
14, 15; igneous, 14; aqueous, 15-18;
mechanically-formed, 18-20; chemically-
formed, 20; organically-formed, 20-37;
arenaceous, 20; argillaceous, 20; cal-
careous, 20-32; siliceous, 20, 32-34,

Rodentia, of the Eocene, 305; of the
Miocene, 322; of the Post-Pliocene, 361.

Roebuck, 336, 354.

Rostellarva, 237, 293.

Rotalia, 22, 98, 171, 264; Boweana, 264.

Rugose Corals, 104; of the Lower Silurian,
104, 105; of the Upper Silurian, 119;
of the Devonian, 141; of the Carbon-
iferous, 172-174; of the Permian, 197;
of the Upper Greensand, 266.

Rupelian Clay, 307.

Sabal major, 309.

Sabre-toothed Tiger, 322, 331.
Saccammina, 172.

Saccosoma, 232.

Salamanders, 189, 313.

Salina Group, 117.

Salix, 262; Meeki, 263.

Salmonide, 276.

Sao hirsuta, 85.

Sassafras cretacea, 263.
Sauropterygia, 219.

Scalaria, 271, 293; Grenlandica, 338.
Scaphites, 272, 273; equalis, 274.
Schizodus, 198, 211.

Schoharie Grit, 135, 137.
Scolecoderma, 82.

Scoliostoma, 213.

Scolithus, 82; Canadensis, 83.
Scorpions of the Coal-measures, 181.
Scorpion-shells, 271.

406

Screw-pines, 230.

Scutella, 311; subrotunda, 312.

Sea-cows (see Sirenia).

Sea-lilies (see Crinoidea).

Sea-lizards (see Enaliosaurians).

Seals, 322.

Sea-mats and Sea-mosses (see Polyzoa).

Sea-shrubs (see Gorgonidz).

Sea-urchins (see Echinoidea).

Sea-weeds, 80, 81, 83, 97, 136, 164, 261.

Secondary period, 44

Sedimentary rocks, 15.

Semnopithecus, 322, 331.

Septaria, 31.

Sequoia, 306, 309, 310; Couttsiw, 309;
gigantea, 309; Langsdorfir, 309.

Serolis, 84.

Serpents (see Ophidia).

Serpulites, 123.

Sewalik Hills (see Siwalik Hills).

Sheep, 355.

Shell-sands, 19.

Sigillaria, 168, 169; Greseri, 168.

Sigillarioids, 136, 168, 170, 196.

Silicates, infiltration of the shells of For-
aminifera by, 34, 74.

Siliceous rocks, 20, 32.

Siliceous Sponges, 265.

Silicification, 13, 14.

Silurian period (see Lower Silurian and
Upper Silurian), 90-114, 115-132.

Simosaurus, 219; Gaillardoti, 219.

Siphonia, 264 ; jicus, 265.

Siphonostomatous Univalves, 237, 271, 293.

Siphonotreta, 110.

Sirenia, 299, 320; of the Eocene, 299; of
the Miocene, 315.

Siren lacertina, 200.

Siwatherium, 318; gigantewm, 319.

Siwalik Hills, Miocene strata of, 307.

Skiddaw Slates, 101.

Sloths, 315, 349-351.

Smilax, 308.

Smithia, 173.

Snakes (see Ophidia).

Soft Tortoises, 296.

Solarvum, 271.

Solenhofen Slates, 228.

Solitaire, 346, 348.

Spalacotherium, 254.

Spatangus, 311.

Spherospongia, 139.

Sphagodus, 130.

Sphenodon, 218.

Sphenopteris, 136, 165, 196.

Spiders of the ar 181.

Spider-shells, 23

Spindle- shells, 237.

Spirifera, 125, 147, 184, 198, 934: crispa,
127; disjuncta, 147; hysterica, 126;
mucronata, 147; Niagarensis, 127; ros-
trata, 235 ; seulptilis,147 ; ; trigonalis,185.

Spiriferide, 147.

Spirophyton cauda-Galli, 135, 164.

Sprrorbis, 123, 143, 178 ; Arkonensis, 144 ;
Carbonarvus, 178; laxus, 144; Lewisii,
123; omphalodes, 144 ; spinulifera, 144.

Spirulirostra, 312.

Spondylus, 269; spinosus, 270.

Sponges, of the Cambrian, 81; of the
Lower Silurian, 98; of the Upper Silu-
rian, 119 ; of the Devonian, 139; of the

INDEX.

Carboniferous, 171; of the Permian,
197; of the Trias, 209; of the Jurassic,
230; of the Cretaceous, 264, 265.

Spongilla, 197.

Spongillopsis, 197.

Spongophylium, 1738.

Spore-cases, of Cryptogams in the ibaetTow.
rocks, 118 ; in the Coal, 163.

Squirrels, 322.

Stagonolepis, 218.

Staircase-shells, 271.

Stalactite, 21.

Stalagmite, 21.

Star-corals, 231.

Star-fishes, 105, 120, 210.

St Cassian Beds, 205, 206.

Stephanophyllia, 266.

Stereognathus, 253, 254.

Stigmaria, 169 ; jicovdes, 169.

Stonesfield Slate, 227; Mammals of, 253.

Strata, contemporaneity of, 44.

Stratified rocks, 15-18.

Streptelasma, 105.

Streptorhynchus, 198.

Stromatopora, 98, 99, 118, 139 ; rugosa, 99;
tuberculata, 140.

Strombodes, 119; pentagonus, 104.

Strombus, 271.

Strophalosia, 198.

Strophodus, 255.

Strophomena, 109, 110, 125, 147, 184;
alternata, 110; deltoidea, 109 ; jfilitexta,
110; rhomboidalis, 147, 148; subplana,
127. $

Sub-Apennine Beds, 325.

Sub-Carboniferous rocks, 158, 161.

Succession of life upon the globe, 367-374.

Suida, 302, 317, ae

Sulphate of lime, 2 22.

Sus Erymanthius, 317; scrofa, 354.

Synastrea, 209.

Synhelia Sharpeana, 266.

Synocladia, 198; virgulacea, 198.

Syringopora, 119, 173 ; ramulosa, 174.

Tabulate Corals, 104; of the Lower Silu-
rian, 105; of the Upper Silurian, 119;
of the Devonian, 142; of the Carbon-
iferous, 172; of the Permian, 197.

Talpa Europea, 336.

Tapiride, 300.

Tapirs, 300.

Tapirus Arvernensis, 327.

Taxocrinus tubercuiatus, 122.

Taxodium, 262, 308, 310.

Teleosaurus, 251.

Teleostean Fishes, 150; of the Cretaceous,
276.

Telerpeton Elginense, 218.

Tellina proxvma, 338

Tentaculites, 129, 148; ornatus, 129.

Terebra, 293.

Terebratella, 268 ; Astieriana, 268.

Terebratula, 184, 234; digona, 235; elon-
gata, 168; hastata, 185; quadrijida,
235 ; spheroidalis, 235.

Terebratulina, 268 ; caput-serpentis, 268 ;
striata, 268.

Termites, 311.

Terrapins, 280, 296.

Tertiary period, 44, 284-287.

Tertiary rocks, classification of, 284-287.

INDEX.

Testudinide, 313.

Tetrabranchiate Cephalopods, 112; of the
Cambrian, 89; of the Lower Silurian,
112-114 ; of the Upper Silurian, 130; of
the Devonian, 149; of the Carboniferous,
186, 187; of the Permian, 199; of the
Trias, 212; of the Jurassic, 237-239; of
the Cretaceous, 272-274 ; of the Eocene,
294; of the Miocene, 312.

Teatularia, 22, 264, 311 ; Meyeriana, 311.

Thanet Sands, 287, 288.

Theca, 88, 111, 129.

Theca Davidii, 88.

Thecidium, 213.

Thecodont Reptiles, 218.

Thecodontosaurus, 200, 218; antiquus, 219.

Thecosmila annularis, 231.

Thelodus, 131.

Theriodont Reptiles, 202, 220.

Thylacoleo, 349.

Tile-stones, 116.

Titanotherium, 316.

Toothed Birds, 281-283.

Tortoises, 202, 296.

Tragoceras, 318.

Travertine, 21.

Tree-Ferns, of the Devonian, 136; of the
Coal-measures, 164.

Tremadoc Slates, 77-79.

Trematis, 110.

Trenton Limestone, 95, 96.

Trianthrus Becki, 107.

Triassic period, 203; rocks of, in Britain,
204; in Germany, 204; in the Austrian
Alps, 205; in North America, 205; life
of, 206-224

Triconodon, 254.

Trigonia, 235, 255, 269.

Trigoniade, 198, 211.

Trigonocarpum, 170 ; ovatum, 170.

Trilobites, 84-87; of the Cambrian, 85, 87;
of the Lower Silurian, 107, 108; of the
Upper Silurian, 123, 124; of the De-
vonian, 144, 145; of the Carboniferous,
179.

Trimerellidee, 127.

Trinucleus, 108 ; concentricus, 107.

Trionycide, 296.

Triton, 293

Trochocyathus, 266.

Trochonema, 129.

Trogontherium, 361; Cuvieri, 336, 361.

Trumpet-shells, 293.

Tulip-tree, 262, 308.

Turbinolia sulcata, 292.

Turbinohide, 292.

Turrilites, 272, 273: catenulatus, 274.

Turritella, 271, 293.

Turtles, 202, 251, 280, 296.

Typhis tubifer, 293.

Ulimania selaginoides, 197.
Unconformability of strata, 48.
Under-clay of coal, 162.

Ungulata, of the Hocene, 300-303 ; of the
Miocene, 315-319; of the Pliocene, 327-
329; of the Post-Pliocene, 353-357.

Uniformity, doctrine of, 5-7.

Unio, 250.

407

Univalves (see Gasteropoda).

Upper Cambrian, 77-79; Chalk, 259;
Cretaceous, 257, 260; Devonian, 135;
Eocene, 287, 288; Greensand, 258:
Helderberg, 135 ; Laurentian, 66 ; Llan-
dovery, 115; Ludlow rock, 116; Mio-
cene, 305; Oolites, 227 : Silurian period,
115; rocks of, in Britain, 115, 116; in
North America, 116-118 ; life of, 118-131.

Ursus arctos, 359; Arvernensis, 330 ; fe-
rox, 359 ; speloea, 360.

Urus, 336, 356.

Valley-gravels, high-level and low-level,
339-341.

Vanessa Pluto, 312.

Varamde, 202.

Vegetation (see Plants).

Ventriculites, 264, 265 ; simplea, 265.

Venus’s Flower-basket, 265.

Vermilia, 197.

Vespertilio Parisiensis, 304, 305.

Vicksburg Beds, 289.

Vines, 306, 309, 310.

Vitreous Sponges, 264.

Voltzia, 208; heterophylla, 209.

Voluta, 271, 298 ; elongata, 271.

Volutes, 271, 293, 312.

Walchia, 196, 197; piniformis, 196.

Walrus, 322.

Wealden Beds, 257.

Wellingtonia, 309, 310.

Wenlock Beds, 115, 117; Limestone, 115;
Shale, 115.

Wentle-traps, 271.

Werfen Beds, 205, 206.

Whalebone Whales, 299, 315.

Whales, 299, 315.

Whelks, 237.

White Chalk, 259; structure of, 21, 22;
origin of, 23, 263.

White Crag, 324.

White River Beds, 307.

Wild Boar, 354.

Williamsonia, 230.

Winged Lizards (see Pterosauria).

Winged Snails (see Pteropoda).

Wing-shells, 271.

Wolf, 336, 360.

Wolverine, 360.

Wombats, 348.

Woolhope Limestone, 115.

Woolly Rhinoceros, 339, 341, 344, 353.

Woolwich and Reading Beds, 287.

Worm-burrows, 82, 83, 123.

Xanthidia, 138, 161.
Xenoneura antiquorum, 145.
Xiphodon, 3038.

Xylobius, 182; Sigillarice, 182.

Zamia spiralis, 208.

Zamites, 208, 230, 310.

Zaphrentis, 105, 119, 142, 173; corntcula,
141; Stokesi, 104; vermicularis, 174.

Zeacrinus, 175.

Zechstein, 194.

Zeuglodon, 299, 315; cetoides, 299, 300.

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